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class="user-bio-container"><div class="profile-bio fake-truncate js-profile-about" style="margin: 0px;"><span class="u-fw700">Phone: </span>+16048221697<br /><b>Address: </b>Department of Earth, Ocean and Atmospheric Sciences, University of British Columbia<br />2020-2207 Main Mall, Vancouver, BC, V6T-1Z4, Canada<br /><div class="js-profile-less-about u-linkUnstyled u-tcGrayDarker u-textDecorationUnderline u-displayNone">less</div></div></div><div class="ri-section"><div class="ri-section-header"><span>Interests</span></div><div class="ri-tags-container"><a data-click-track="profile-user-info-expand-research-interests" data-has-card-for-ri-list="62411756" href="https://www.academia.edu/Documents/in/Trace_Elements"><div id="js-react-on-rails-context" style="display:none" 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none;"><span>12</span> Environmental geochemistry</a></li><li role="presentation"><a data-click-track="profile-works-tab" data-section-name="Arc-magmatism:-Cascades" data-toggle="tab" href="#arcmagmatismcascades" role="tab" style="border: none;"><span>6</span> Arc magmatism: Cascades</a></li></ul></li></ul></div><div class="divider ds-divider-16" style="margin: 0px;"></div><div class="documents-container backbone-social-profile-documents" style="width: 100%;"><div class="u-taCenter"></div><div class="profile--tab_content_container js-tab-pane tab-pane active" id="all"><div class="profile--tab_heading_container js-section-heading" data-section="Papers" id="Papers"><h3 class="profile--tab_heading_container">Papers by Dominique Weis</h3></div><div class="js-work-strip profile--work_container" data-work-id="87932538"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/87932538/Petrography_geochemistry_and_Sr_Pb_isotopic_composition_of_basalts_from_the_Western_Indian_Ocean_DSDP_sites_235_236_239_240_"><img alt="Research paper thumbnail of Petrography, geochemistry and Sr-Pb isotopic composition of basalts from the Western Indian Ocean (DSDP - sites 235, 236, 239, 240)" class="work-thumbnail" src="https://attachments.academia-assets.com/92021704/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/87932538/Petrography_geochemistry_and_Sr_Pb_isotopic_composition_of_basalts_from_the_Western_Indian_Ocean_DSDP_sites_235_236_239_240_">Petrography, geochemistry and Sr-Pb isotopic composition of basalts from the Western Indian Ocean (DSDP - sites 235, 236, 239, 240)</a></div><div class="wp-workCard_item"><span>Annales De La Societe Geologique De Belgique</span><span>, Jul 29, 2010</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="9b983adb5940436360ca1fec8e8283df" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":92021704,"asset_id":87932538,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/92021704/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="87932538"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span 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href="https://www.academia.edu/87932523/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area"><img alt="Research paper thumbnail of Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area" class="work-thumbnail" src="https://attachments.academia-assets.com/92021698/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/87932523/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area">Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area</a></div><div class="wp-workCard_item"><span>Proceedings of the Ocean Drilling Program, 153 Scientific Results</span><span>, 1997</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="126a3a368644ddeee3dafde0d94d559e" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":92021698,"asset_id":87932523,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/92021698/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="87932523"><a 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"126a3a368644ddeee3dafde0d94d559e" } } $('.js-work-strip[data-work-id=87932523]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":87932523,"title":"Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area","translated_title":"","metadata":{"publisher":"Ocean Drilling Program","ai_title_tag":"Geochemical and Isotopic Analysis of Gabbros in the MARK Area","grobid_abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gabbroic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troctolitic rocks and gabbros (sensu stricto) can be modeled as comprising a fairly primitive cumulate fraction plus trapped parental intercumulus liquid. Second-order trace-element variations are indicative of fractionation attending adcumulus growth and compaction. The Site 922 troctolitic gabbros (sensu lato) are remarkable because of the high REE abundances and high REE/Sc ratios, characteristics normally associated with evolved compositions. The REE geochemistry of these troctolites cannot be accounted for by mixing between primitive troctolites and diabase liquid as for gabbros from Sites 921 and 923. Instead, these troctolites are modeled as mixtures between barren troctolites and a strongly enriched liquid. Such a liquid is likely to have accompanied the formation of the Fe-Ti oxide gabbros with which these troctolites are associated. Sr-, Nd-, and Pb-isotope ratios for undeformed and deformed and recrystallized gabbros from Sites 921 and 923 have a very restricted range of values: 87 Sr/ 86 Sr = 0.70234-0.70239; 143 Nd/ 144","publication_date":{"day":null,"month":null,"year":1997,"errors":{}},"publication_name":"Proceedings of the Ocean Drilling Program, 153 Scientific Results","grobid_abstract_attachment_id":92021698},"translated_abstract":null,"internal_url":"https://www.academia.edu/87932523/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area","translated_internal_url":"","created_at":"2022-10-05T05:40:00.291-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":92021698,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/92021698/thumbnails/1.jpg","file_name":"sr153_18.pdf","download_url":"https://www.academia.edu/attachments/92021698/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Whole_rock_geochemistry_and_Sr_Nd_and_Pb.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/92021698/sr153_18-libre.pdf?1664975638=\u0026response-content-disposition=attachment%3B+filename%3DWhole_rock_geochemistry_and_Sr_Nd_and_Pb.pdf\u0026Expires=1733034948\u0026Signature=UcdbJYSpV6VRb2aJCKDjWGDqLmMQzbm35~6Q1RCyv8ZHH69je2QqLPYUxb~N5gR472R9nxtChViDalMy1sx0w-e092ZmDNfxwO43s9sl3dIPVi6SuF9D0QL~GAFokyVcOx3aNqM8IBBiqs7JWvfikq4yh0dpBWg0yiZdrZEVIwYMxLSoMD1lIVVnNOj1fObAI5kvBqp602Hc45YdEBIEvXzEZXhq3Sm2d4GqE103babY8UvZzEwlKsVBMBnbRdw8rIudP0kNqSUtU54vUnjq89NIYdHcgHt3xQt928TOMtstpFTPfIXc24X1KWNPc~8i~2AgNvf0Y930KEryASIp6w__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area","translated_slug":"","page_count":12,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":92021698,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/92021698/thumbnails/1.jpg","file_name":"sr153_18.pdf","download_url":"https://www.academia.edu/attachments/92021698/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Whole_rock_geochemistry_and_Sr_Nd_and_Pb.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/92021698/sr153_18-libre.pdf?1664975638=\u0026response-content-disposition=attachment%3B+filename%3DWhole_rock_geochemistry_and_Sr_Nd_and_Pb.pdf\u0026Expires=1733034948\u0026Signature=UcdbJYSpV6VRb2aJCKDjWGDqLmMQzbm35~6Q1RCyv8ZHH69je2QqLPYUxb~N5gR472R9nxtChViDalMy1sx0w-e092ZmDNfxwO43s9sl3dIPVi6SuF9D0QL~GAFokyVcOx3aNqM8IBBiqs7JWvfikq4yh0dpBWg0yiZdrZEVIwYMxLSoMD1lIVVnNOj1fObAI5kvBqp602Hc45YdEBIEvXzEZXhq3Sm2d4GqE103babY8UvZzEwlKsVBMBnbRdw8rIudP0kNqSUtU54vUnjq89NIYdHcgHt3xQt928TOMtstpFTPfIXc24X1KWNPc~8i~2AgNvf0Y930KEryASIp6w__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":65140,"name":"Models","url":"https://www.academia.edu/Documents/in/Models"},{"id":116579,"name":"Lead","url":"https://www.academia.edu/Documents/in/Lead"},{"id":123563,"name":"Drilling","url":"https://www.academia.edu/Documents/in/Drilling"},{"id":126340,"name":"Deformation","url":"https://www.academia.edu/Documents/in/Deformation"},{"id":224577,"name":"Trace Elements","url":"https://www.academia.edu/Documents/in/Trace_Elements"},{"id":258296,"name":"Forage","url":"https://www.academia.edu/Documents/in/Forage"},{"id":521382,"name":"Gabbro","url":"https://www.academia.edu/Documents/in/Gabbro"},{"id":668253,"name":"Lithosphere","url":"https://www.academia.edu/Documents/in/Lithosphere"},{"id":976618,"name":"Igneous Rocks","url":"https://www.academia.edu/Documents/in/Igneous_Rocks"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="87932515"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/87932515/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components"><img alt="Research paper thumbnail of K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/87932515/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components">K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components</a></div><div class="wp-workCard_item"><span>The Journal of Geology</span><span>, 1993</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). According ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="87932515"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="87932515"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 87932515; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=87932515]").text(description); $(".js-view-count[data-work-id=87932515]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 87932515; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='87932515']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 87932515, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=87932515]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":87932515,"title":"K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components","translated_title":"","metadata":{"abstract":"... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). According ...","publisher":"University of Chicago Press","publication_date":{"day":null,"month":null,"year":1993,"errors":{}},"publication_name":"The Journal of Geology"},"translated_abstract":"... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). According ...","internal_url":"https://www.academia.edu/87932515/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components","translated_internal_url":"","created_at":"2022-10-05T05:39:54.305-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":304909,"name":"THE GEOLOGY","url":"https://www.academia.edu/Documents/in/THE_GEOLOGY"}],"urls":[{"id":24489669,"url":"https://www.journals.uchicago.edu/doi/pdf/10.1086/648273"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="87932510"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/87932510/Modelling_of_source_enrichment_and_melting_processes_for_the_calcalkal_ine_shoshonite_lamproite_suite_from_S_E_Spain"><img alt="Research paper thumbnail of Modelling of source enrichment and melting processes for the calcalkal ine-shoshonite-lamproite suite from S.E. Spain" class="work-thumbnail" src="https://attachments.academia-assets.com/92021680/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/87932510/Modelling_of_source_enrichment_and_melting_processes_for_the_calcalkal_ine_shoshonite_lamproite_suite_from_S_E_Spain">Modelling of source enrichment and melting processes for the calcalkal ine-shoshonite-lamproite suite from S.E. Spain</a></div><div class="wp-workCard_item"><span>Chemical Geology</span><span>, 1988</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="ae9d45f9d887d6cbd70bff9eb6d79d7d" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":92021680,"asset_id":87932510,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/92021680/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="87932510"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="87932510"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 87932510; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=87932510]").text(description); $(".js-view-count[data-work-id=87932510]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 87932510; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='87932510']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 87932510, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "ae9d45f9d887d6cbd70bff9eb6d79d7d" } } $('.js-work-strip[data-work-id=87932510]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":87932510,"title":"Modelling of source enrichment and melting processes for the calcalkal ine-shoshonite-lamproite suite from S.E. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="75363095"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/75363095/The_Pelona_Pico_Duarte_basalts_Formation_Central_Hispaniola_an_on_land_section_of_Late_Cretaceous_volcanism_related_to_the_Caribbean_large_igneous_province"><img alt="Research paper thumbnail of The Pelona-Pico Duarte basalts Formation, Central Hispaniola: an on-land section of Late Cretaceous volcanism related to the Caribbean large igneous province" class="work-thumbnail" src="https://attachments.academia-assets.com/83161251/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/75363095/The_Pelona_Pico_Duarte_basalts_Formation_Central_Hispaniola_an_on_land_section_of_Late_Cretaceous_volcanism_related_to_the_Caribbean_large_igneous_province">The Pelona-Pico Duarte basalts Formation, Central Hispaniola: an on-land section of Late Cretaceous volcanism related to the Caribbean large igneous province</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">the Late Cretaceous Caribbean large igneous province magmatism on land. It is composed by a ~2.5k...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">the Late Cretaceous Caribbean large igneous province magmatism on land. It is composed by a ~2.5km-thick pile of massive and monotonous submarine flows of basalts, locally intruded by synvolcanic dikes and sills of dolerite. The Pelona-Pico Duarte basalts Fm. was emplaced onto Turonian-Lower Campanian island-arc volcanic and sedimentary sequences, and is overlain by Maastrichtian platformal carbonates. Two 40Ar/39Ar plateau ages indicate both extrusive and intrusive magmatic activity at least during the 79-68Ma interval (Middle Campanian to Maastrichtian), so the magmas were in part coeval with the late phases of the Caribbean large igneous province. The basalts have a restricted major-and trace-element, and isotopic, compositional variation. For a range of 47.6-50.2wt. % SiO2, the Pelona-Pico Duarte basalts Fm. has relatively high contents in TiO2 (1.5-3.6wt.%) and Fe2O3T (10.7-13.1wt.%). On the basis of MgO contents, samples can be classified into tholeiitic basalts (&lt;8wt.%) an...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2be5bc57a98bc3abe07a2c4fefb7baed" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":83161251,"asset_id":75363095,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/83161251/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="75363095"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="75363095"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 75363095; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=75363095]").text(description); $(".js-view-count[data-work-id=75363095]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 75363095; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='75363095']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 75363095, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2be5bc57a98bc3abe07a2c4fefb7baed" } } $('.js-work-strip[data-work-id=75363095]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":75363095,"title":"The Pelona-Pico Duarte basalts Formation, Central Hispaniola: an on-land section of Late Cretaceous volcanism related to the Caribbean large igneous province","translated_title":"","metadata":{"abstract":"the Late Cretaceous Caribbean large igneous province magmatism on land. 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I...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Introduction: Anthropogenic Pb remains the most important input of Pb in the troposphere today. It is now important to take sources other than automobile emissions (e.g., lead smelters, ferrous and non-ferrous metal manufacturing plants, fossil fuel combustion, waste incinerators, ...) into account in evaluating the lead content of atmospheric aerosols to discriminate the origins of pollution aerosols. The capability of lead isotopes to study the sources and transport of pollution aerosols [1] is demonstrated here above the Straits of Dover. We collected atmospheric aerosols above the Eastern Channel and the Southern Bight of the North Sea between March and November 1995. During the same period, to define more local contributions, we characterized the lead isotopic signatures of the main industrial sources on the French coast, near the Straits of Dover. Urban and automobile-derived aerosols were also collected.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="a38fad56e08e5aecc4ee7fb8609c7c99" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":83161187,"asset_id":75363094,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/83161187/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="75363094"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="75363094"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 75363094; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=75363094]").text(description); $(".js-view-count[data-work-id=75363094]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 75363094; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='75363094']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 75363094, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "a38fad56e08e5aecc4ee7fb8609c7c99" } } $('.js-work-strip[data-work-id=75363094]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":75363094,"title":"Tracing Sources of Channel and North Sea Pollution Aerosols Above the Straits of Dover Using Lead-Isotopic Geochemistry","translated_title":"","metadata":{"abstract":"Introduction: Anthropogenic Pb remains the most important input of Pb in the troposphere today. 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The purpose of our study was to examine the experience of people participating in a specific university-funded interdisciplinary research initiative. As there is a strong emphasis within this program on reporting on the outcomes of the funding that supports interdisciplinary collaboration, our aim was to explore how participation may shape one’s intellectual quality of life (iQoL) and how one’s iQoL could be conceptualized and understood. Using a pragmatic constructivist case study, focus group and individual interviews were undertaken with 30 participants involved with university-funded interdisciplinary research teams. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="75363088"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/75363088/_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_"><img alt="Research paper thumbnail of … analysis of standards and samples using a 207Pb–204Pb double spike and thallium to correct for mass bias with a double-focusing MC–ICP–MS” by Baker et …" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/75363088/_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_">… analysis of standards and samples using a 207Pb–204Pb double spike and thallium to correct for mass bias with a double-focusing MC–ICP–MS” by Baker et …</a></div><div class="wp-workCard_item"><span>Chemical …</span><span>, 2005</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract: Baker et al.(2004) suggest that Pb isotope measurements by MC-ICP-MS using Tl to monito...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract: Baker et al.(2004) suggest that Pb isotope measurements by MC-ICP-MS using Tl to monitor mass fractionation produce results that are erroneous by up to 3300 ppm with respect to &#x27;reference&#x27;double-or triple-spike isotopic measurements by TIMS. 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We will show ...","internal_url":"https://www.academia.edu/75363088/_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_","translated_internal_url":"","created_at":"2022-04-03T19:11:16.377-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":14054,"name":"Chemical","url":"https://www.academia.edu/Documents/in/Chemical"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="75363087"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/75363087/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1"><img alt="Research paper thumbnail of 18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1" class="work-thumbnail" src="https://attachments.academia-assets.com/83161183/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/75363087/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1">18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6dd8337ca954b18ae8dc232f3c3e94a4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":83161183,"asset_id":75363087,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/83161183/download_file?st=MTczMzA5NDM3NSw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="75363087"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="75363087"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 75363087; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=75363087]").text(description); $(".js-view-count[data-work-id=75363087]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 75363087; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='75363087']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 75363087, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "6dd8337ca954b18ae8dc232f3c3e94a4" } } $('.js-work-strip[data-work-id=75363087]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":75363087,"title":"18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1","translated_title":"","metadata":{"abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode..."},"translated_abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="54521429"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/54521429/The_1160_Ma_Hidderskog_meta_charnockite_implications_of_this_A_type_pluton_for_the_Sveconorwegian_belt_in_Vest_Agder_SW_Norway_"><img alt="Research paper thumbnail of The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)" class="work-thumbnail" src="https://attachments.academia-assets.com/70846185/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/54521429/The_1160_Ma_Hidderskog_meta_charnockite_implications_of_this_A_type_pluton_for_the_Sveconorwegian_belt_in_Vest_Agder_SW_Norway_">The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, 1995</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Hidderskog massif is a charnockitic intrusion located in the Rogaland-Vest Agder segment of t...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Hidderskog massif is a charnockitic intrusion located in the Rogaland-Vest Agder segment of the Sveconorwegian province of SW Norway. The U-Pb zircon age (1159 ± 5 Ma) and the Rb-Sr whole-rock isochron age (1153 ± 39 Ma) of this pluton are concordant. This age is interpreted as the magmatic emplacement age. The Hidderskog charnockitic intrusion is deformed and at</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d8b1dd50c5009c1892716f41b57046a2" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":70846185,"asset_id":54521429,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/70846185/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="54521429"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="54521429"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 54521429; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=54521429]").text(description); $(".js-view-count[data-work-id=54521429]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 54521429; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='54521429']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 54521429, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d8b1dd50c5009c1892716f41b57046a2" } } $('.js-work-strip[data-work-id=54521429]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":54521429,"title":"The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)","translated_title":"","metadata":{"abstract":"The Hidderskog massif is a charnockitic intrusion located in the Rogaland-Vest Agder segment of the Sveconorwegian province of SW Norway. 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The Hidderskog charnockitic intrusion is deformed and at","internal_url":"https://www.academia.edu/54521429/The_1160_Ma_Hidderskog_meta_charnockite_implications_of_this_A_type_pluton_for_the_Sveconorwegian_belt_in_Vest_Agder_SW_Norway_","translated_internal_url":"","created_at":"2021-10-01T01:08:04.795-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":70846185,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/70846185/thumbnails/1.jpg","file_name":"0024-4937_2895_2900005-z20211001-10158-1b7o3pi.pdf","download_url":"https://www.academia.edu/attachments/70846185/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"The_1160_Ma_Hidderskog_meta_charnockite.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/70846185/0024-4937_2895_2900005-z20211001-10158-1b7o3pi-libre.pdf?1633088461=\u0026response-content-disposition=attachment%3B+filename%3DThe_1160_Ma_Hidderskog_meta_charnockite.pdf\u0026Expires=1733034949\u0026Signature=LaPZrZn7cEXQL7FBcVvTlQMFKAX2IR-Oe0uU8zhNhWh19Mli4UN94UlYnOCie7xY1lZTCQuC3~NNFgtJ82bh2F4DIVv3lYDVqhYrBlB~133Z1rEsu80aLoO65TWb8ag6aqaylNB5bo4q95gMgC-WG02N63C6pJQ~~ZPZEiegAUSPv5rbk9cE91w61PnbK7Ju2h8dhy9Iz43Hp2dEjE0WRMl7quKz5b6CH7Yq2jamD9syWS29ZtkN70x2luzTM4nJgU29j4RFboKC1ZXaR35EW5TWUYossMTOS3jgekYTv7kMwM1RJY2NR6P96JNCmLDWZGwp7paYe5D-3bErPpnF4A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_1160_Ma_Hidderskog_meta_charnockite_implications_of_this_A_type_pluton_for_the_Sveconorwegian_belt_in_Vest_Agder_SW_Norway_","translated_slug":"","page_count":16,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":70846185,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/70846185/thumbnails/1.jpg","file_name":"0024-4937_2895_2900005-z20211001-10158-1b7o3pi.pdf","download_url":"https://www.academia.edu/attachments/70846185/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"The_1160_Ma_Hidderskog_meta_charnockite.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/70846185/0024-4937_2895_2900005-z20211001-10158-1b7o3pi-libre.pdf?1633088461=\u0026response-content-disposition=attachment%3B+filename%3DThe_1160_Ma_Hidderskog_meta_charnockite.pdf\u0026Expires=1733034949\u0026Signature=LaPZrZn7cEXQL7FBcVvTlQMFKAX2IR-Oe0uU8zhNhWh19Mli4UN94UlYnOCie7xY1lZTCQuC3~NNFgtJ82bh2F4DIVv3lYDVqhYrBlB~133Z1rEsu80aLoO65TWb8ag6aqaylNB5bo4q95gMgC-WG02N63C6pJQ~~ZPZEiegAUSPv5rbk9cE91w61PnbK7Ju2h8dhy9Iz43Hp2dEjE0WRMl7quKz5b6CH7Yq2jamD9syWS29ZtkN70x2luzTM4nJgU29j4RFboKC1ZXaR35EW5TWUYossMTOS3jgekYTv7kMwM1RJY2NR6P96JNCmLDWZGwp7paYe5D-3bErPpnF4A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":758278,"name":"Large Scale","url":"https://www.academia.edu/Documents/in/Large_Scale"}],"urls":[{"id":11890699,"url":"http://dx.doi.org/10.1016/0024-4937(95)00005-Z"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32179559"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32179559/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1"><img alt="Research paper thumbnail of 18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1" class="work-thumbnail" src="https://attachments.academia-assets.com/52414180/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32179559/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1">18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/Hertogen">Jan Hertogen</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2f4c6a1625368ff05425dd5f93946983" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52414180,"asset_id":32179559,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52414180/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32179559"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32179559"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32179559; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32179559]").text(description); $(".js-view-count[data-work-id=32179559]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32179559; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32179559']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32179559, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2f4c6a1625368ff05425dd5f93946983" } } $('.js-work-strip[data-work-id=32179559]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32179559,"title":"18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1","translated_title":"","metadata":{"abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32179577"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32179577/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components"><img alt="Research paper thumbnail of K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32179577/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components">K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/Hertogen">Jan Hertogen</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a></span></div><div class="wp-workCard_item"><span>J Geol</span><span>, 1993</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). According ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32179577"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32179577"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32179577; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32179577]").text(description); $(".js-view-count[data-work-id=32179577]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32179577; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32179577']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32179577, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32179577]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32179577,"title":"K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components","translated_title":"","metadata":{"abstract":"... ably deformed. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="6767132" id="papers"><div class="js-work-strip profile--work_container" data-work-id="87932538"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/87932538/Petrography_geochemistry_and_Sr_Pb_isotopic_composition_of_basalts_from_the_Western_Indian_Ocean_DSDP_sites_235_236_239_240_"><img alt="Research paper thumbnail of Petrography, geochemistry and Sr-Pb isotopic composition of basalts from the Western Indian Ocean (DSDP - sites 235, 236, 239, 240)" class="work-thumbnail" src="https://attachments.academia-assets.com/92021704/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/87932538/Petrography_geochemistry_and_Sr_Pb_isotopic_composition_of_basalts_from_the_Western_Indian_Ocean_DSDP_sites_235_236_239_240_">Petrography, geochemistry and Sr-Pb isotopic composition of basalts from the Western Indian Ocean (DSDP - sites 235, 236, 239, 240)</a></div><div class="wp-workCard_item"><span>Annales De La Societe Geologique De Belgique</span><span>, Jul 29, 2010</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="9b983adb5940436360ca1fec8e8283df" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":92021704,"asset_id":87932538,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/92021704/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="87932538"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="87932538"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 87932538; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="87932523"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/87932523/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area"><img alt="Research paper thumbnail of Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area" class="work-thumbnail" src="https://attachments.academia-assets.com/92021698/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/87932523/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area">Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area</a></div><div class="wp-workCard_item"><span>Proceedings of the Ocean Drilling Program, 153 Scientific Results</span><span>, 1997</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="126a3a368644ddeee3dafde0d94d559e" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":92021698,"asset_id":87932523,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/92021698/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="87932523"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="87932523"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 87932523; 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "126a3a368644ddeee3dafde0d94d559e" } } $('.js-work-strip[data-work-id=87932523]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":87932523,"title":"Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area","translated_title":"","metadata":{"publisher":"Ocean Drilling Program","ai_title_tag":"Geochemical and Isotopic Analysis of Gabbros in the MARK Area","grobid_abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gabbroic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troctolitic rocks and gabbros (sensu stricto) can be modeled as comprising a fairly primitive cumulate fraction plus trapped parental intercumulus liquid. Second-order trace-element variations are indicative of fractionation attending adcumulus growth and compaction. The Site 922 troctolitic gabbros (sensu lato) are remarkable because of the high REE abundances and high REE/Sc ratios, characteristics normally associated with evolved compositions. The REE geochemistry of these troctolites cannot be accounted for by mixing between primitive troctolites and diabase liquid as for gabbros from Sites 921 and 923. Instead, these troctolites are modeled as mixtures between barren troctolites and a strongly enriched liquid. Such a liquid is likely to have accompanied the formation of the Fe-Ti oxide gabbros with which these troctolites are associated. 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Only the central part of the large Feda unit is rather homogeneous and poorly ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). 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According ...","internal_url":"https://www.academia.edu/87932515/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components","translated_internal_url":"","created_at":"2022-10-05T05:39:54.305-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":304909,"name":"THE GEOLOGY","url":"https://www.academia.edu/Documents/in/THE_GEOLOGY"}],"urls":[{"id":24489669,"url":"https://www.journals.uchicago.edu/doi/pdf/10.1086/648273"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="87932510"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/87932510/Modelling_of_source_enrichment_and_melting_processes_for_the_calcalkal_ine_shoshonite_lamproite_suite_from_S_E_Spain"><img alt="Research paper thumbnail of Modelling of source enrichment and melting processes for the calcalkal ine-shoshonite-lamproite suite from S.E. Spain" class="work-thumbnail" src="https://attachments.academia-assets.com/92021680/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/87932510/Modelling_of_source_enrichment_and_melting_processes_for_the_calcalkal_ine_shoshonite_lamproite_suite_from_S_E_Spain">Modelling of source enrichment and melting processes for the calcalkal ine-shoshonite-lamproite suite from S.E. Spain</a></div><div class="wp-workCard_item"><span>Chemical Geology</span><span>, 1988</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="ae9d45f9d887d6cbd70bff9eb6d79d7d" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":92021680,"asset_id":87932510,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/92021680/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="87932510"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="87932510"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 87932510; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=87932510]").text(description); $(".js-view-count[data-work-id=87932510]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 87932510; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='87932510']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 87932510, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "ae9d45f9d887d6cbd70bff9eb6d79d7d" } } $('.js-work-strip[data-work-id=87932510]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":87932510,"title":"Modelling of source enrichment and melting processes for the calcalkal ine-shoshonite-lamproite suite from S.E. 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It is composed by a ~2.5k...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">the Late Cretaceous Caribbean large igneous province magmatism on land. It is composed by a ~2.5km-thick pile of massive and monotonous submarine flows of basalts, locally intruded by synvolcanic dikes and sills of dolerite. The Pelona-Pico Duarte basalts Fm. was emplaced onto Turonian-Lower Campanian island-arc volcanic and sedimentary sequences, and is overlain by Maastrichtian platformal carbonates. Two 40Ar/39Ar plateau ages indicate both extrusive and intrusive magmatic activity at least during the 79-68Ma interval (Middle Campanian to Maastrichtian), so the magmas were in part coeval with the late phases of the Caribbean large igneous province. The basalts have a restricted major-and trace-element, and isotopic, compositional variation. For a range of 47.6-50.2wt. % SiO2, the Pelona-Pico Duarte basalts Fm. has relatively high contents in TiO2 (1.5-3.6wt.%) and Fe2O3T (10.7-13.1wt.%). On the basis of MgO contents, samples can be classified into tholeiitic basalts (&lt;8wt.%) an...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2be5bc57a98bc3abe07a2c4fefb7baed" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":83161251,"asset_id":75363095,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/83161251/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="75363095"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="75363095"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 75363095; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=75363095]").text(description); $(".js-view-count[data-work-id=75363095]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 75363095; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='75363095']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 75363095, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2be5bc57a98bc3abe07a2c4fefb7baed" } } $('.js-work-strip[data-work-id=75363095]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":75363095,"title":"The Pelona-Pico Duarte basalts Formation, Central Hispaniola: an on-land section of Late Cretaceous volcanism related to the Caribbean large igneous province","translated_title":"","metadata":{"abstract":"the Late Cretaceous Caribbean large igneous province magmatism on land. 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I...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Introduction: Anthropogenic Pb remains the most important input of Pb in the troposphere today. It is now important to take sources other than automobile emissions (e.g., lead smelters, ferrous and non-ferrous metal manufacturing plants, fossil fuel combustion, waste incinerators, ...) into account in evaluating the lead content of atmospheric aerosols to discriminate the origins of pollution aerosols. The capability of lead isotopes to study the sources and transport of pollution aerosols [1] is demonstrated here above the Straits of Dover. We collected atmospheric aerosols above the Eastern Channel and the Southern Bight of the North Sea between March and November 1995. During the same period, to define more local contributions, we characterized the lead isotopic signatures of the main industrial sources on the French coast, near the Straits of Dover. Urban and automobile-derived aerosols were also collected.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="a38fad56e08e5aecc4ee7fb8609c7c99" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":83161187,"asset_id":75363094,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/83161187/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="75363094"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="75363094"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 75363094; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=75363094]").text(description); $(".js-view-count[data-work-id=75363094]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 75363094; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='75363094']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 75363094, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "a38fad56e08e5aecc4ee7fb8609c7c99" } } $('.js-work-strip[data-work-id=75363094]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":75363094,"title":"Tracing Sources of Channel and North Sea Pollution Aerosols Above the Straits of Dover Using Lead-Isotopic Geochemistry","translated_title":"","metadata":{"abstract":"Introduction: Anthropogenic Pb remains the most important input of Pb in the troposphere today. 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The purpose of our study was to examine the experience of people participating in a specific university-funded interdisciplinary research initiative. As there is a strong emphasis within this program on reporting on the outcomes of the funding that supports interdisciplinary collaboration, our aim was to explore how participation may shape one’s intellectual quality of life (iQoL) and how one’s iQoL could be conceptualized and understood. Using a pragmatic constructivist case study, focus group and individual interviews were undertaken with 30 participants involved with university-funded interdisciplinary research teams. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="75363088"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/75363088/_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_"><img alt="Research paper thumbnail of … analysis of standards and samples using a 207Pb–204Pb double spike and thallium to correct for mass bias with a double-focusing MC–ICP–MS” by Baker et …" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/75363088/_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_">… analysis of standards and samples using a 207Pb–204Pb double spike and thallium to correct for mass bias with a double-focusing MC–ICP–MS” by Baker et …</a></div><div class="wp-workCard_item"><span>Chemical …</span><span>, 2005</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract: Baker et al.(2004) suggest that Pb isotope measurements by MC-ICP-MS using Tl to monito...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract: Baker et al.(2004) suggest that Pb isotope measurements by MC-ICP-MS using Tl to monitor mass fractionation produce results that are erroneous by up to 3300 ppm with respect to &#x27;reference&#x27;double-or triple-spike isotopic measurements by TIMS. We will show ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="75363088"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="75363088"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 75363088; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=75363088]").text(description); $(".js-view-count[data-work-id=75363088]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 75363088; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='75363088']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 75363088, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=75363088]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":75363088,"title":"… analysis of standards and samples using a 207Pb–204Pb double spike and thallium to correct for mass bias with a double-focusing MC–ICP–MS” by Baker et …","translated_title":"","metadata":{"abstract":"Abstract: Baker et al.(2004) suggest that Pb isotope measurements by MC-ICP-MS using Tl to monitor mass fractionation produce results that are erroneous by up to 3300 ppm with respect to \u0026#x27;reference\u0026#x27;double-or triple-spike isotopic measurements by TIMS. 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We will show ...","internal_url":"https://www.academia.edu/75363088/_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_","translated_internal_url":"","created_at":"2022-04-03T19:11:16.377-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"_analysis_of_standards_and_samples_using_a_207Pb_204Pb_double_spike_and_thallium_to_correct_for_mass_bias_with_a_double_focusing_MC_ICP_MS_by_Baker_et_","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":14054,"name":"Chemical","url":"https://www.academia.edu/Documents/in/Chemical"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="75363087"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/75363087/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1"><img alt="Research paper thumbnail of 18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1" class="work-thumbnail" src="https://attachments.academia-assets.com/83161183/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/75363087/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1">18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6dd8337ca954b18ae8dc232f3c3e94a4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":83161183,"asset_id":75363087,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/83161183/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="75363087"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="75363087"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 75363087; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=75363087]").text(description); $(".js-view-count[data-work-id=75363087]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 75363087; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='75363087']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 75363087, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "6dd8337ca954b18ae8dc232f3c3e94a4" } } $('.js-work-strip[data-work-id=75363087]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":75363087,"title":"18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1","translated_title":"","metadata":{"abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode..."},"translated_abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="54521429"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/54521429/The_1160_Ma_Hidderskog_meta_charnockite_implications_of_this_A_type_pluton_for_the_Sveconorwegian_belt_in_Vest_Agder_SW_Norway_"><img alt="Research paper thumbnail of The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)" class="work-thumbnail" src="https://attachments.academia-assets.com/70846185/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/54521429/The_1160_Ma_Hidderskog_meta_charnockite_implications_of_this_A_type_pluton_for_the_Sveconorwegian_belt_in_Vest_Agder_SW_Norway_">The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, 1995</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Hidderskog massif is a charnockitic intrusion located in the Rogaland-Vest Agder segment of t...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Hidderskog massif is a charnockitic intrusion located in the Rogaland-Vest Agder segment of the Sveconorwegian province of SW Norway. The U-Pb zircon age (1159 ± 5 Ma) and the Rb-Sr whole-rock isochron age (1153 ± 39 Ma) of this pluton are concordant. This age is interpreted as the magmatic emplacement age. The Hidderskog charnockitic intrusion is deformed and at</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d8b1dd50c5009c1892716f41b57046a2" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":70846185,"asset_id":54521429,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/70846185/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="54521429"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="54521429"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 54521429; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=54521429]").text(description); $(".js-view-count[data-work-id=54521429]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 54521429; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='54521429']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 54521429, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d8b1dd50c5009c1892716f41b57046a2" } } $('.js-work-strip[data-work-id=54521429]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":54521429,"title":"The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)","translated_title":"","metadata":{"abstract":"The Hidderskog massif is a charnockitic intrusion located in the Rogaland-Vest Agder segment of the Sveconorwegian province of SW Norway. 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WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1" class="work-thumbnail" src="https://attachments.academia-assets.com/52414180/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32179559/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1">18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/Hertogen">Jan Hertogen</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2f4c6a1625368ff05425dd5f93946983" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52414180,"asset_id":32179559,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52414180/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32179559"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32179559"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32179559; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32179559]").text(description); $(".js-view-count[data-work-id=32179559]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32179559; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32179559']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32179559, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2f4c6a1625368ff05425dd5f93946983" } } $('.js-work-strip[data-work-id=32179559]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32179559,"title":"18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1","translated_title":"","metadata":{"abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode..."},"translated_abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gab- broic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase. Trace-element variations, in particular, reflect the nature of the samples, which varies from troctolite to gabbro (sensu stricto) to Fe-Ti-oxide-rich gabbro. Interpretation of the rare-earth element (REE) and Se characteristics of the gabbros leads to contrasting models for the origin of gabbros from Sites 921 and 923 as compared to those from Site 922. Site 921 and 923 troc- tolitic rocks and gabbros (sensu stricto) can be mode...","internal_url":"https://www.academia.edu/32179559/18_WHOLE_ROCK_GEOCHEMISTRY_AND_Sr_Nd_AND_Pb_ISOTOPIC_CHARACTERISTICS_OF_UNDEFORMED_DEFORMED_AND_RECRYSTALLIZED_GABBROS_FROM_SITES_921_922_AND_923_IN_THE_MARK_AREA1","translated_internal_url":"","created_at":"2017-04-01T01:03:34.560-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62397373,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28298625,"work_id":32179559,"tagging_user_id":62397373,"tagged_user_id":62411756,"co_author_invite_id":6175232,"email":"d***s@eos.ubc.ca","affiliation":"University of British Columbia","display_order":0,"name":"Dominique Weis","title":"18. WHOLE-ROCK GEOCHEMISTRY AND Sr, Nd, AND Pb-ISOTOPIC CHARACTERISTICS OF UNDEFORMED, DEFORMED, AND RECRYSTALLIZED GABBROS FROM SITES 921, 922, AND 923 IN THE MARK AREA1"},{"id":28312824,"work_id":32179559,"tagging_user_id":62397373,"tagged_user_id":null,"co_author_invite_id":6178226,"email":"j***b@earth.ox.ac.uk","display_order":4194304,"name":"Jane Barling","title":"18. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32179577"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32179577/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components"><img alt="Research paper thumbnail of K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32179577/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components">K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/Hertogen">Jan Hertogen</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a></span></div><div class="wp-workCard_item"><span>J Geol</span><span>, 1993</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). According ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32179577"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32179577"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32179577; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32179577]").text(description); $(".js-view-count[data-work-id=32179577]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32179577; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32179577']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32179577, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32179577]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32179577,"title":"K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components","translated_title":"","metadata":{"abstract":"... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). According ...","publication_date":{"day":null,"month":null,"year":1993,"errors":{}},"publication_name":"J Geol"},"translated_abstract":"... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). According ...","internal_url":"https://www.academia.edu/32179577/K_Rich_Calc_Alkaline_Augen_Gneisses_of_Grenvillian_Age_in_SW_Norway_Mingling_of_Mantle_Derived_and_Crustal_Components","translated_internal_url":"","created_at":"2017-04-01T01:03:37.822-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62397373,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28298629,"work_id":32179577,"tagging_user_id":62397373,"tagged_user_id":62411756,"co_author_invite_id":6175232,"email":"d***s@eos.ubc.ca","affiliation":"University of British Columbia","display_order":0,"name":"Dominique Weis","title":"K-Rich Calc-Alkaline Augen Gneisses of Grenvillian Age in SW Norway: Mingling of Mantle-Derived and Crustal Components"},{"id":28312879,"work_id":32179577,"tagging_user_id":62397373,"tagged_user_id":35870725,"co_author_invite_id":null,"email":"b***n@ngu.no","affiliation":"Geological Survey of Norway","display_order":4194304,"name":"B. 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They are difficult to identify in MC-ICP-MS isotopic data because affected analyses exhibit normal mass dependent isotope fractionation. We have therefore investigated a wide range of matrix elements for both stable and radiogenic isotope systems using a Nu Plasma MC-ICP-MS. Matrix elements commonly</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186973"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186973"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186973; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186973]").text(description); $(".js-view-count[data-work-id=32186973]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186973; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186973']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186973, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186973]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186973,"title":"The Influence of Non-spectral Matrix Effects on the Accuracy of Isotope Ratio Measurement by MC-ICP-MS","translated_title":"","metadata":{"abstract":"Non-spectral interferences in ICP-MS are caused by matrix elements effecting the ionisation and transmission of analyte elements. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186959"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32186959/Assessment_of_Instrumental_Mass_Bias_and_Isobaric_Interference_Corrections_for_Hf_Lu_Nd_Isotopic_Geochemistry_on_Zircon_by_MC_ICP_MS"><img alt="Research paper thumbnail of Assessment of Instrumental Mass Bias and Isobaric Interference Corrections for Hf-Lu-Nd Isotopic Geochemistry on Zircon by MC-ICP-MS" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32186959/Assessment_of_Instrumental_Mass_Bias_and_Isobaric_Interference_Corrections_for_Hf_Lu_Nd_Isotopic_Geochemistry_on_Zircon_by_MC_ICP_MS">Assessment of Instrumental Mass Bias and Isobaric Interference Corrections for Hf-Lu-Nd Isotopic Geochemistry on Zircon by MC-ICP-MS</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186959"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186959"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186959; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186924"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186924/Comprehensive_and_systematic_MC_ICP_MS_TIMS_isotopic_characterization_of_USGS_Standards"><img alt="Research paper thumbnail of Comprehensive and systematic MC-ICP-MS/TIMS isotopic characterization of USGS Standards" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186924/Comprehensive_and_systematic_MC_ICP_MS_TIMS_isotopic_characterization_of_USGS_Standards">Comprehensive and systematic MC-ICP-MS/TIMS isotopic characterization of USGS Standards</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT The Pacific Centre for Isotopic and Geochemical Research (PCIGR) at the University of Br...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT The Pacific Centre for Isotopic and Geochemical Research (PCIGR) at the University of British Columbia has undertaken a systematic analysis of isotopic (Nd, Sr, Hf, Pb) composition and concentration of a broad compositional range of United States Geological Survey standards, including basalt (BCR-1, 2; BHVO-1, 2; BIR-1), dunite (DNC-1), andesite (AGV-1, 2), rhyolite (RGM-1, 2), syenite (STM-1, 2) and granite (G-2). USGS rock standards are geochemically well-characterized, but there is no systematic methodology nor database for radiogenic isotopic analyses, even for the widely used BCR-I. This investigation represents the first comprehensive, systematic analysis of the isotopic concentration and composition of USGS standards, and will provide an important database for the isotopic community. The wide range of equipment at PCIGR, including a Nu MC-ICPMS, a Triton TIMS, and an ElementII HR-ICPMS, permits a rigorous assessment and comparison of precision and accuracy in isotopic analyses. Our separation technique involves an HF/HNO3 dissolution in Teflon bombs, standard cation exchange elutriation for Sr and REE separation, and HDEHP Teflon columns for Nd separation. Samples are unspiked, and elemental concentration is determined by HR-ICPMS. Isotopic composition is determined by both thermal ionization mass spectrometry (Sr, Nd) and by multi-collector inductively coupled plasma mass spectrometry (Nd, Hf, Pb). Replicate runs of La Jolla Nd standard demonstrate excellent agreement between MC-ICPMS (143Nd/144Nd=0.511846+/-14 [n=100]) and TIMS (0.511850+/-16 [n=67]). Replicate analyses of strontium standard NBS987 yield 86Sr/87Sr values of 0.710256+/-15 [n=130]. Neodymium isotopic analyses (143Nd/144Nd values and Sm/Nd ratios) of previously characterized standards, such as BCR-1 (143Nd/144Nd=0.512623+/-2 [Nu; n=2]; 0.512627+/-8 [Triton; n=8]; Sm/Nd=0.1389) and BHVO-1 (0.512972+/-5 [Nu; n=2]; 0.512973+/-6 [Triton; n=14]; 0.1522-0.1532) are within error of published values. Replicate analyses of previously uncharacterized standards, such as AGV-1 (0.512776+/-4 [Nu; n=4]; 0.512781+/-7 [Triton; n=7]) and RGM-1 (0.512799+/-2 [Triton; n=2]), and second generation standards, such as BCR-2 (0.512639+/-6 [Triton; n=3]), BHVO-2 (0.512984+/-3 [Triton; n=3]), and AGV-2 (0.512792+/-1 [Triton; n=2]), provide the first reproducible data for these standards. Strontium analyses of BCR-1 (87Sr/86Sr= 0.705027+/-8 [Triton; n=4]) and BHVO-1 (0.703482+/-13 [Triton; n=6]) yield 86Sr/87Sr values that replicate known values. Replicate analyses of other standards, such as BCR-2 (0.705024+/-5 [Triton; n=3]), BHVO-2 (0.703487+/-9 [Triton; n=4]) and AGV-1 (0.703997+/-8 [Triton; n=7]) provide the first data for these standards. Hafnium and lead isotopic analyses on the same suite of samples are underway.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186924"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186924"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186924; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186924]").text(description); $(".js-view-count[data-work-id=32186924]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186924; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186924']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186924, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186924]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186924,"title":"Comprehensive and systematic MC-ICP-MS/TIMS isotopic characterization of USGS Standards","translated_title":"","metadata":{"abstract":"ABSTRACT The Pacific Centre for Isotopic and Geochemical Research (PCIGR) at the University of British Columbia has undertaken a systematic analysis of isotopic (Nd, Sr, Hf, Pb) composition and concentration of a broad compositional range of United States Geological Survey standards, including basalt (BCR-1, 2; BHVO-1, 2; BIR-1), dunite (DNC-1), andesite (AGV-1, 2), rhyolite (RGM-1, 2), syenite (STM-1, 2) and granite (G-2). USGS rock standards are geochemically well-characterized, but there is no systematic methodology nor database for radiogenic isotopic analyses, even for the widely used BCR-I. This investigation represents the first comprehensive, systematic analysis of the isotopic concentration and composition of USGS standards, and will provide an important database for the isotopic community. The wide range of equipment at PCIGR, including a Nu MC-ICPMS, a Triton TIMS, and an ElementII HR-ICPMS, permits a rigorous assessment and comparison of precision and accuracy in isotopic analyses. Our separation technique involves an HF/HNO3 dissolution in Teflon bombs, standard cation exchange elutriation for Sr and REE separation, and HDEHP Teflon columns for Nd separation. Samples are unspiked, and elemental concentration is determined by HR-ICPMS. Isotopic composition is determined by both thermal ionization mass spectrometry (Sr, Nd) and by multi-collector inductively coupled plasma mass spectrometry (Nd, Hf, Pb). Replicate runs of La Jolla Nd standard demonstrate excellent agreement between MC-ICPMS (143Nd/144Nd=0.511846+/-14 [n=100]) and TIMS (0.511850+/-16 [n=67]). Replicate analyses of strontium standard NBS987 yield 86Sr/87Sr values of 0.710256+/-15 [n=130]. Neodymium isotopic analyses (143Nd/144Nd values and Sm/Nd ratios) of previously characterized standards, such as BCR-1 (143Nd/144Nd=0.512623+/-2 [Nu; n=2]; 0.512627+/-8 [Triton; n=8]; Sm/Nd=0.1389) and BHVO-1 (0.512972+/-5 [Nu; n=2]; 0.512973+/-6 [Triton; n=14]; 0.1522-0.1532) are within error of published values. Replicate analyses of previously uncharacterized standards, such as AGV-1 (0.512776+/-4 [Nu; n=4]; 0.512781+/-7 [Triton; n=7]) and RGM-1 (0.512799+/-2 [Triton; n=2]), and second generation standards, such as BCR-2 (0.512639+/-6 [Triton; n=3]), BHVO-2 (0.512984+/-3 [Triton; n=3]), and AGV-2 (0.512792+/-1 [Triton; n=2]), provide the first reproducible data for these standards. Strontium analyses of BCR-1 (87Sr/86Sr= 0.705027+/-8 [Triton; n=4]) and BHVO-1 (0.703482+/-13 [Triton; n=6]) yield 86Sr/87Sr values that replicate known values. Replicate analyses of other standards, such as BCR-2 (0.705024+/-5 [Triton; n=3]), BHVO-2 (0.703487+/-9 [Triton; n=4]) and AGV-1 (0.703997+/-8 [Triton; n=7]) provide the first data for these standards. 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The wide range of equipment at PCIGR, including a Nu MC-ICPMS, a Triton TIMS, and an ElementII HR-ICPMS, permits a rigorous assessment and comparison of precision and accuracy in isotopic analyses. Our separation technique involves an HF/HNO3 dissolution in Teflon bombs, standard cation exchange elutriation for Sr and REE separation, and HDEHP Teflon columns for Nd separation. Samples are unspiked, and elemental concentration is determined by HR-ICPMS. Isotopic composition is determined by both thermal ionization mass spectrometry (Sr, Nd) and by multi-collector inductively coupled plasma mass spectrometry (Nd, Hf, Pb). Replicate runs of La Jolla Nd standard demonstrate excellent agreement between MC-ICPMS (143Nd/144Nd=0.511846+/-14 [n=100]) and TIMS (0.511850+/-16 [n=67]). Replicate analyses of strontium standard NBS987 yield 86Sr/87Sr values of 0.710256+/-15 [n=130]. Neodymium isotopic analyses (143Nd/144Nd values and Sm/Nd ratios) of previously characterized standards, such as BCR-1 (143Nd/144Nd=0.512623+/-2 [Nu; n=2]; 0.512627+/-8 [Triton; n=8]; Sm/Nd=0.1389) and BHVO-1 (0.512972+/-5 [Nu; n=2]; 0.512973+/-6 [Triton; n=14]; 0.1522-0.1532) are within error of published values. Replicate analyses of previously uncharacterized standards, such as AGV-1 (0.512776+/-4 [Nu; n=4]; 0.512781+/-7 [Triton; n=7]) and RGM-1 (0.512799+/-2 [Triton; n=2]), and second generation standards, such as BCR-2 (0.512639+/-6 [Triton; n=3]), BHVO-2 (0.512984+/-3 [Triton; n=3]), and AGV-2 (0.512792+/-1 [Triton; n=2]), provide the first reproducible data for these standards. Strontium analyses of BCR-1 (87Sr/86Sr= 0.705027+/-8 [Triton; n=4]) and BHVO-1 (0.703482+/-13 [Triton; n=6]) yield 86Sr/87Sr values that replicate known values. Replicate analyses of other standards, such as BCR-2 (0.705024+/-5 [Triton; n=3]), BHVO-2 (0.703487+/-9 [Triton; n=4]) and AGV-1 (0.703997+/-8 [Triton; n=7]) provide the first data for these standards. Hafnium and lead isotopic analyses on the same suite of samples are underway.","internal_url":"https://www.academia.edu/32186924/Comprehensive_and_systematic_MC_ICP_MS_TIMS_isotopic_characterization_of_USGS_Standards","translated_internal_url":"","created_at":"2017-04-01T10:05:31.509-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304490,"work_id":32186924,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176436,"email":"w***s@eos.ubc.ca","display_order":0,"name":"Wilma Pretorius","title":"Comprehensive and systematic MC-ICP-MS/TIMS isotopic characterization of USGS Standards"},{"id":28304499,"work_id":32186924,"tagging_user_id":62411756,"tagged_user_id":62425741,"co_author_invite_id":6176437,"email":"g***i@gmail.com","display_order":4194304,"name":"Gwen Williams","title":"Comprehensive and systematic MC-ICP-MS/TIMS isotopic characterization of USGS Standards"},{"id":28304517,"work_id":32186924,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176439,"email":"k***a@bay.k12.fl.us","display_order":6291456,"name":"B. 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Only a few 176Hf/177Hf results are published on these materials and with the increased use of MC-ICP-MS it is critical to build a solid reference database. Standard</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186923"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186923"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186923; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186923]").text(description); $(".js-view-count[data-work-id=32186923]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186923; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186923']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186923, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186923]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186923,"title":"Hf isotope geochemistry of USGS reference materials and various labware: Insight into potential contaminant sources","translated_title":"","metadata":{"abstract":"We have undertaken a high-precision geochemical and isotopic study of USGS reference materials by HR-ICP-MS, TIMS and MC-ICP-MS, including basalt (BCR-1,2; BHVO-1,2), andesite (AGV-1,2), rhyolite (RGM-1), syenite (STM-1,2), granodiorite (GSP-2), and granite (G-2,3). Only a few 176Hf/177Hf results are published on these materials and with the increased use of MC-ICP-MS it is critical to build a solid reference database. Standard"},"translated_abstract":"We have undertaken a high-precision geochemical and isotopic study of USGS reference materials by HR-ICP-MS, TIMS and MC-ICP-MS, including basalt (BCR-1,2; BHVO-1,2), andesite (AGV-1,2), rhyolite (RGM-1), syenite (STM-1,2), granodiorite (GSP-2), and granite (G-2,3). Only a few 176Hf/177Hf results are published on these materials and with the increased use of MC-ICP-MS it is critical to build a solid reference database. Standard","internal_url":"https://www.academia.edu/32186923/Hf_isotope_geochemistry_of_USGS_reference_materials_and_various_labware_Insight_into_potential_contaminant_sources","translated_internal_url":"","created_at":"2017-04-01T10:05:31.377-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304495,"work_id":32186923,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176436,"email":"w***s@eos.ubc.ca","display_order":0,"name":"Wilma Pretorius","title":"Hf isotope geochemistry of USGS reference materials and various labware: Insight into potential contaminant sources"},{"id":28304515,"work_id":32186923,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176438,"email":"b***r@eos.ubc.ca","display_order":4194304,"name":"Bruno Kieffer","title":"Hf isotope geochemistry of USGS reference materials and various labware: Insight into potential contaminant sources"},{"id":28304558,"work_id":32186923,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176449,"email":"i***e@eos.ubc.ca","display_order":6291456,"name":"Nobre Silva","title":"Hf isotope geochemistry of USGS reference materials and various labware: Insight into potential contaminant sources"}],"downloadable_attachments":[],"slug":"Hf_isotope_geochemistry_of_USGS_reference_materials_and_various_labware_Insight_into_potential_contaminant_sources","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":4107,"name":"High Pressure","url":"https://www.academia.edu/Documents/in/High_Pressure"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":1029721,"name":"Instruments and Techniques","url":"https://www.academia.edu/Documents/in/Instruments_and_Techniques"}],"urls":[]}, dispatcherData: dispatcherData }); 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window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186894]").text(description); $(".js-view-count[data-work-id=32186894]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186894; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186894']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186894, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); 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We present a technique for separating Hf by ion exchange chemistry from high-TiO 2 (\u003e 40% m/m) minerals to achieve precise Hf isotopic composition analyses by MC (multiple collector)-ICP-MS. Following digestion and conversion to chlorides, the first elution column is used to separate iron and the rare earth elements, the second column is designed to separate most of the titanium from Hf, an evaporation step using HClO 4 is then performed to remove any trace of HF in preparation for the third column, which is needed to eliminate any remaining trace of titanium. The modified chemistry helped to improve the yields from \u003c 10 to \u003e 78% as well as the analytical precision of the processed samples (e.g., sample 2033-A1, 176 Hf/ 177 Hf = 0.282251 AE 25 before vs. 0.282225 AE 6 after). The technique was tested on a case study in which the Hf isotopic ratios of ilmenite and rutile (analysed prior to the chemistry improvement) were determined and permitted to evaluate that the origin of rutile-bearing ilmenite deposits is from the same or similar magma than their, respectively, associated Proterozoic anorthosite massifs (Saint-Urbain and Lac Allard) of the Grenville Province in Qu ebec, Canada.","publication_date":{"day":null,"month":null,"year":2013,"errors":{}},"publication_name":"Geostandards and Geoanalytical Research","grobid_abstract_attachment_id":52420506},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186894/Methodology_and_Application_of_Hafnium_Isotopes_in_Ilmenite_and_Rutile_by_MC_ICP_MS","translated_internal_url":"","created_at":"2017-04-01T10:05:27.405-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304406,"work_id":32186894,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Methodology and Application of Hafnium Isotopes in Ilmenite and Rutile by MC-ICP-MS"},{"id":28304485,"work_id":32186894,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176435,"email":"c***t@golder.com","display_order":4194304,"name":"Caroline-Emmanuelle Morisset","title":"Methodology and Application of Hafnium Isotopes in Ilmenite and Rutile by MC-ICP-MS"},{"id":28304641,"work_id":32186894,"tagging_user_id":62411756,"tagged_user_id":62654960,"co_author_invite_id":6176469,"email":"a***r@proximus.be","display_order":6291456,"name":"André Rahier","title":"Methodology and Application of Hafnium Isotopes in Ilmenite and Rutile by MC-ICP-MS"}],"downloadable_attachments":[{"id":52420506,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420506/thumbnails/1.jpg","file_name":"Methodology_and_Application_of_Hafnium_I20170401-6068-agrgsf.pdf","download_url":"https://www.academia.edu/attachments/52420506/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Methodology_and_Application_of_Hafnium_I.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420506/Methodology_and_Application_of_Hafnium_I20170401-6068-agrgsf-libre.pdf?1491067302=\u0026response-content-disposition=attachment%3B+filename%3DMethodology_and_Application_of_Hafnium_I.pdf\u0026Expires=1733097976\u0026Signature=ODsvmKRGsZQTzQVUl~kNPzVQWusIodC9fqH0E1R2EUP9gqJwNlncuWBPa7KcnH4e9lE4E2aT3JwmGmYK8cI-yx~2f0W3idzOfSYqMJe8uPyanDf7RrARv~vsXYU1~Kb-18daafOKy~8jyNjqbUlHr8sNMvQdn03MTjvXMMC2HZtkh6fhxuZkf0akE-7cwbGqH8FXUPUcLET0Bx0Gw8~7DHOCSpqAuML62BdcUVIqEgpUfPU2y~AqXGjKve8Wm8GL-4FAnkMEKLZyUghjvBGl3rtQL27wDQUpu6n~asoNTMuNG4Wco0hJHNj3WzMo4JXZmVnBvaCPAaNrGH2I~~HbFg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Methodology_and_Application_of_Hafnium_Isotopes_in_Ilmenite_and_Rutile_by_MC_ICP_MS","translated_slug":"","page_count":18,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420506,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420506/thumbnails/1.jpg","file_name":"Methodology_and_Application_of_Hafnium_I20170401-6068-agrgsf.pdf","download_url":"https://www.academia.edu/attachments/52420506/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Methodology_and_Application_of_Hafnium_I.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420506/Methodology_and_Application_of_Hafnium_I20170401-6068-agrgsf-libre.pdf?1491067302=\u0026response-content-disposition=attachment%3B+filename%3DMethodology_and_Application_of_Hafnium_I.pdf\u0026Expires=1733097976\u0026Signature=ODsvmKRGsZQTzQVUl~kNPzVQWusIodC9fqH0E1R2EUP9gqJwNlncuWBPa7KcnH4e9lE4E2aT3JwmGmYK8cI-yx~2f0W3idzOfSYqMJe8uPyanDf7RrARv~vsXYU1~Kb-18daafOKy~8jyNjqbUlHr8sNMvQdn03MTjvXMMC2HZtkh6fhxuZkf0akE-7cwbGqH8FXUPUcLET0Bx0Gw8~7DHOCSpqAuML62BdcUVIqEgpUfPU2y~AqXGjKve8Wm8GL-4FAnkMEKLZyUghjvBGl3rtQL27wDQUpu6n~asoNTMuNG4Wco0hJHNj3WzMo4JXZmVnBvaCPAaNrGH2I~~HbFg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186893"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186893/A_Common_Reference_Material_for_Cadmium_Isotope_Studies_NIST_SRM_3108"><img alt="Research paper thumbnail of A Common Reference Material for Cadmium Isotope Studies - NIST SRM 3108" class="work-thumbnail" src="https://attachments.academia-assets.com/52420515/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186893/A_Common_Reference_Material_for_Cadmium_Isotope_Studies_NIST_SRM_3108">A Common Reference Material for Cadmium Isotope Studies - NIST SRM 3108</a></div><div class="wp-workCard_item"><span>Geostandards and Geoanalytical Research</span><span>, 2013</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="87a2b9c817f4acf46417369118a36f1f" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420515,"asset_id":32186893,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420515/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186893"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186893"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186893; 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Methodologies are diverse with MC-ICP-MS favoured by all but one laboratory, which uses thermal ionisation mass spectrometry (TIMS). To quantify the isotope fractionation and correct for instrumental mass bias, double-spike techniques, sample-calibrator bracketing or element doping has been used. However, easy comparison between data sets has been hampered by the multitude of in-house Cd solutions used as zero-delta reference in different laboratories. The lack of a suitable isotopic reference material for Cd is detrimental for progress in the long term. We have conducted a comprehensive round-robin assay of NIST SRM 3108 and the Cd isotope offsets to commonly used in-house reference materials. Here, we advocate NIST SRM 3108 both as an isotope standard and the isotopic reference point for Cd and encourage its use as 'zero-delta' in future studies. The purity of NIST SRM 3108 was evaluated regarding isobaric and polyatomic molecular interferences, and the levels of Zn, Pd and Sn found were not significant. 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wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186882/Effects_of_acid_leaching_on_the_Sr_Nd_Hf_isotopic_compositions_of_ocean_island_basalts">Effects of acid leaching on the Sr-Nd-Hf isotopic compositions of ocean island basalts</a></div><div class="wp-workCard_item"><span>Geochemistry Geophysics Geosystems</span><span>, 2010</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="1874c280b31f55be8558785ae073ae00" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420523,"asset_id":32186882,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420523/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa 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})(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "1874c280b31f55be8558785ae073ae00" } } $('.js-work-strip[data-work-id=32186882]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186882,"title":"Effects of acid leaching on the Sr-Nd-Hf isotopic compositions of ocean island basalts","translated_title":"","metadata":{"grobid_abstract":"1] The ability to conduct multi-isotopic analyses (e.g., Sr-Nd-Hf-Pb) on the same sample is critical for studies that evaluate the mantle source components of oceanic basalts. The isotopic compositions of relatively immobile elements, such as Nd (and other REE) and Hf, are considered to be relatively resistant to alteration, however, accurate Sr and Pb isotopic analyses of oceanic basalts require thorough acid leaching prior to dissolution. A detailed study of the Sr, Nd and Hf isotopic systematics of acid-leached oceanic basalts from Hawaii and Kerguelen was undertaken to assess how acid leaching affects their isotopic compositions. Most of the Sr, Nd and Hf was removed in the first acid leaching steps. Hawaiian basalts lose up to 35% and 40% of their total Sr and Hf contents, respectively, whereas for Kerguelen basalts the corresponding losses are 63% and ∼70%. Acid leaching leads to significant loss of the original Nd content (up to 90%), which cannot be solely explained by the elimination of alteration phases and is likely related to preferential removal of the REE in the constituent silicate minerals (e.g., plagioclase, clinopyroxene). The leached residues yield Sr isotopic ratios significantly less radiogenic than their respective unleached powders and Nd-Hf isotopic compositions that are within analytical uncertainty of the respective unleached powders. This study shows that multi-isotopic analyses on the same acid-leached sample aliquot can produce reliable results for use in the discrimination of mantle source components of oceanic basalts. . Inherent to their emplacement in an oceanic environment, oceanic basalts are susceptible to seawater alteration, and the effects of this alteration on Rb-Sr and U-Pb isotope systematics have long been recognized [e.g.,","publication_date":{"day":null,"month":null,"year":2010,"errors":{}},"publication_name":"Geochemistry Geophysics Geosystems","grobid_abstract_attachment_id":52420523},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186882/Effects_of_acid_leaching_on_the_Sr_Nd_Hf_isotopic_compositions_of_ocean_island_basalts","translated_internal_url":"","created_at":"2017-04-01T10:05:25.745-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304401,"work_id":32186882,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Effects of acid leaching on the Sr-Nd-Hf isotopic compositions of ocean island basalts"},{"id":28305087,"work_id":32186882,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176449,"email":"i***e@eos.ubc.ca","display_order":4194304,"name":"Inês Silva","title":"Effects of acid leaching on the Sr-Nd-Hf isotopic compositions of ocean island basalts"}],"downloadable_attachments":[{"id":52420523,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420523/thumbnails/1.jpg","file_name":"2010gc00317620170401-6068-ycdig8.pdf","download_url":"https://www.academia.edu/attachments/52420523/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Effects_of_acid_leaching_on_the_Sr_Nd_Hf.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420523/2010gc00317620170401-6068-ycdig8-libre.pdf?1491067283=\u0026response-content-disposition=attachment%3B+filename%3DEffects_of_acid_leaching_on_the_Sr_Nd_Hf.pdf\u0026Expires=1733034949\u0026Signature=FHnxRH0TkNFUgo5uaa7iC6c8jsbmjCqA4Xbs~iJbNNcOrigZb05AL4gQ8ofdKv86SBlFdsg8qCJkTWs0vMmTsP6epwwwoBR9c-xRG0002Po056morlFJaHVSRxo0F9p1vq6xrugZBsSjWS9qiXxgjMlj73YPC20a5gf3pxH92vhqHxdb-pmdLvWpe~jDdPJ3B8xTk-yDEVwefOEtUTwy6Dohu3naKgDTjkYeF4bKHtFgtMfsUMtGxrIHiIjS1f7FeFaYY2FzCKmq-ghdMROKHBL9LOQUAHx6rYnu5uni4g-0SEA3yfJe3hkm0mx7UUEpx4bqxf1w0HJg1S~SLHNozg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Effects_of_acid_leaching_on_the_Sr_Nd_Hf_isotopic_compositions_of_ocean_island_basalts","translated_slug":"","page_count":20,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420523,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420523/thumbnails/1.jpg","file_name":"2010gc00317620170401-6068-ycdig8.pdf","download_url":"https://www.academia.edu/attachments/52420523/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Effects_of_acid_leaching_on_the_Sr_Nd_Hf.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420523/2010gc00317620170401-6068-ycdig8-libre.pdf?1491067283=\u0026response-content-disposition=attachment%3B+filename%3DEffects_of_acid_leaching_on_the_Sr_Nd_Hf.pdf\u0026Expires=1733034949\u0026Signature=FHnxRH0TkNFUgo5uaa7iC6c8jsbmjCqA4Xbs~iJbNNcOrigZb05AL4gQ8ofdKv86SBlFdsg8qCJkTWs0vMmTsP6epwwwoBR9c-xRG0002Po056morlFJaHVSRxo0F9p1vq6xrugZBsSjWS9qiXxgjMlj73YPC20a5gf3pxH92vhqHxdb-pmdLvWpe~jDdPJ3B8xTk-yDEVwefOEtUTwy6Dohu3naKgDTjkYeF4bKHtFgtMfsUMtGxrIHiIjS1f7FeFaYY2FzCKmq-ghdMROKHBL9LOQUAHx6rYnu5uni4g-0SEA3yfJe3hkm0mx7UUEpx4bqxf1w0HJg1S~SLHNozg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"},{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":322954,"name":"Chip","url":"https://www.academia.edu/Documents/in/Chip"},{"id":413191,"name":"Reproducibility","url":"https://www.academia.edu/Documents/in/Reproducibility"},{"id":424229,"name":"Sr isotopes","url":"https://www.academia.edu/Documents/in/Sr_isotopes"},{"id":902427,"name":"Acid Leaching","url":"https://www.academia.edu/Documents/in/Acid_Leaching"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186878"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186878/Hf_isotope_compositions_of_U_S_Geological_Survey_reference_materials"><img alt="Research paper thumbnail of Hf isotope compositions of U.S. Geological Survey reference materials" class="work-thumbnail" src="https://attachments.academia-assets.com/52420491/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186878/Hf_isotope_compositions_of_U_S_Geological_Survey_reference_materials">Hf isotope compositions of U.S. Geological Survey reference materials</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/NMattielli">N. Mattielli</a></span></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2007</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="faafa34a9db76e839af4f5c42cdbbf70" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420491,"asset_id":32186878,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420491/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186878"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186878"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186878; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186878]").text(description); $(".js-view-count[data-work-id=32186878]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186878; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186878']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186878, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "faafa34a9db76e839af4f5c42cdbbf70" } } $('.js-work-strip[data-work-id=32186878]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186878,"title":"Hf isotope compositions of U.S. Geological Survey reference materials","translated_title":"","metadata":{"grobid_abstract":"Reproducibility is better than 50 ppm for the granitoid compositions and better than 40 ppm for the basaltic/andesitic compositions. For the isotopic analyses acquired early in this project on glass columns, Hf isotopic analyses from several of the reference materials were significantly less reproducible than Nd and Sr isotopic analyses determined from the same sample dissolution. The 176 Hf/ 177 Hf ratios for relatively radiogenic compositions (BCR-1, 2; BHVO-1, 2; RGM-1) were shifted systematically toward lower values by 100-150 ppm when a borosilicate primary column was used. Although systematic, the shift for felsic compositions was generally within analytical error, except for GSP-2, which has a very low Hf isotopic ratio, where the shift was to higher 176 Hf/ 177 Hf. Trace element and isotopic characterization of the borosilicate glass column, borosilicate frits, and quartz columns reveals extremely variable levels of trace elements. The 176 Hf/ 177 Hf ratios for these materials are very unradiogenic (borosilicate glass \u003c0.28220; frit = 0.28193 ± 4). The borosilicate frit material appears to be the most variable in elemental concentration and isotopic composition. The quartz material has very low levels (\u003cppm) of all trace elements. Low 176 Hf/ 177 Hf and high Hf concentrations of the borosilicate glass column (16 ppm) and frit material (22 ppm) indicate that only small amounts of such unradiogenic material could cause significant contamination of small samples. For the basaltic (BCR-1, 2; BHVO-1, 2) and rhyolitic (RGM-1) samples, approximately 3 ng of Hf from the column or frit would be enough to produce the observed 100-150 ppm shift. Accurate, high-precision 176 Hf/ 177 Hf data can only be acquired if samples are processed using all PTFE Teflon 1 labware, or quartz and polypropylene.","publication_date":{"day":null,"month":null,"year":2007,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420491},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186878/Hf_isotope_compositions_of_U_S_Geological_Survey_reference_materials","translated_internal_url":"","created_at":"2017-04-01T10:05:25.209-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304493,"work_id":32186878,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176436,"email":"w***s@eos.ubc.ca","display_order":0,"name":"Wilma Pretorius","title":"Hf isotope compositions of U.S. Geological Survey reference materials"},{"id":28304511,"work_id":32186878,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176438,"email":"b***r@eos.ubc.ca","display_order":4194304,"name":"Bruno Kieffer","title":"Hf isotope compositions of U.S. Geological Survey reference materials"},{"id":28305116,"work_id":32186878,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":5447447,"email":"c***h@ulb.ac.be","display_order":6291456,"name":"Claude Maerschalk","title":"Hf isotope compositions of U.S. Geological Survey reference materials"},{"id":28305122,"work_id":32186878,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":4581898,"email":"j***g@pop.geol.ku.dk","display_order":7340032,"name":"Jane Barling","title":"Hf isotope compositions of U.S. Geological Survey reference materials"},{"id":28305134,"work_id":32186878,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176605,"email":"j***o@ship.iodp.tamu.edu","display_order":7864320,"name":"Diane Hanano","title":"Hf isotope compositions of U.S. Geological Survey reference materials"},{"id":28580513,"work_id":32186878,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176449,"email":"i***e@eos.ubc.ca","display_order":8126464,"name":"I. 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Unleached samples consistently yield Pb isotopic ratios that reflect the incorporation of foreign material. Leaching removes up to 70-80% of the total Pb content of the samples with corresponding weight losses between 35 and 60%. The older and more altered Kerguelen basalts show better external reproducibility than the Hawaiian basalts, which appears to be due to the presence in the Hawaiian samples of more radiogenic contaminants (e.g., seawater Pb, drilling mud, and related alteration phases). All leached samples purified twice on anion exchange columns show more radiogenic Pb isotopic ratios than those processed once. The difference is larger for tholeiitic basalts (Hawaiian and Kerguelen Plateau) than for transitional to alkalic basalts (Kerguelen Archipelago). The small differences in measured ratios of total procedural triplicates reflect differential elimination of residual alteration via leaching and matrix effects. The effectiveness of matrix elimination depends on the specific basalt composition, and tholeiitic basalts (i.e., low Pb concentrations) require two passes on anion exchange columns. This study shows that all steps in sample processing are critical for achieving accurate high-precision Pb isotopic compositions of ocean island basalts.","publication_date":{"day":null,"month":null,"year":2009,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420485},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186877/Leaching_systematics_and_matrix_elimination_for_the_determination_of_high_precision_Pb_isotope_compositions_of_ocean_island_basalts","translated_internal_url":"","created_at":"2017-04-01T10:05:25.091-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304407,"work_id":32186877,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Leaching systematics and matrix 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Pb-Sr-Nd-Hf isotopic characterization of USGS BHVO-1 and BHVO-2 reference materials"},{"id":28304505,"work_id":32186876,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176438,"email":"b***r@eos.ubc.ca","display_order":4194304,"name":"Bruno Kieffer","title":"High-precision Pb-Sr-Nd-Hf isotopic characterization of USGS BHVO-1 and BHVO-2 reference materials"},{"id":28305051,"work_id":32186876,"tagging_user_id":62411756,"tagged_user_id":39214705,"co_author_invite_id":null,"email":"j***g@eos.ubc.ca","display_order":6291456,"name":"Jane Barling","title":"High-precision Pb-Sr-Nd-Hf isotopic characterization of USGS BHVO-1 and BHVO-2 reference materials"},{"id":28305115,"work_id":32186876,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":5447447,"email":"c***h@ulb.ac.be","display_order":7340032,"name":"Claude Maerschalk","title":"High-precision Pb-Sr-Nd-Hf isotopic characterization of USGS BHVO-1 and BHVO-2 reference 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href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/GwenWilliams8">Gwen Williams</a></span></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2006</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2f0bcdc5f85d9e1003ee7e7052cbe5c6" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420496,"asset_id":32186875,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420496/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper 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class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186862/Hf_and_Lu_isotopic_reference_values_for_the_zircon_standard_91500_by_MC_ICP_MS"><img alt="Research paper thumbnail of Hf and Lu isotopic reference values for the zircon standard 91500 by MC-ICP-MS" class="work-thumbnail" src="https://attachments.academia-assets.com/52420476/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186862/Hf_and_Lu_isotopic_reference_values_for_the_zircon_standard_91500_by_MC_ICP_MS">Hf and Lu isotopic reference values for the zircon standard 91500 by MC-ICP-MS</a></div><div class="wp-workCard_item"><span>Chemical Geology</span><span>, 2004</span></div><div class="wp-workCard_item wp-workCard--actions"><span 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The chemical protocol consists of a high-pressure and hightemperature acid dissolution of zircon followed by optimized two-step ion-exchange chromatography with an overall recovery better than 94%. Instrumental calibration involved an extensive characterization of standard solutions for Hf [JMC-475 250 ppb: 176 Hf/ 177 Hf=0.282161F16 (2 S.D.)] and Lu [JMC standard 50 ppb: 175 Lu/ 176 Lu=37.72F2 (2 S.D.)].","publication_date":{"day":null,"month":null,"year":2004,"errors":{}},"publication_name":"Chemical Geology","grobid_abstract_attachment_id":52420476},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186862/Hf_and_Lu_isotopic_reference_values_for_the_zircon_standard_91500_by_MC_ICP_MS","translated_internal_url":"","created_at":"2017-04-01T10:05:23.383-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304429,"work_id":32186862,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Hf and Lu isotopic reference values for the zircon standard 91500 by MC-ICP-MS"},{"id":28305080,"work_id":32186862,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176603,"email":"a***s@gmail.com","display_order":4194304,"name":"Arnaud Goolaerts","title":"Hf and Lu isotopic reference values for the zircon standard 91500 by MC-ICP-MS"}],"downloadable_attachments":[{"id":52420476,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420476/thumbnails/1.jpg","file_name":"Hf_and_Lu_isotopic_reference_values_for_20170401-6062-e2aa17.pdf","download_url":"https://www.academia.edu/attachments/52420476/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Hf_and_Lu_isotopic_reference_values_for.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420476/Hf_and_Lu_isotopic_reference_values_for_20170401-6062-e2aa17-libre.pdf?1491067327=\u0026response-content-disposition=attachment%3B+filename%3DHf_and_Lu_isotopic_reference_values_for.pdf\u0026Expires=1733097976\u0026Signature=Z60RMf~w5-6hV7ioCbATxYenuTAgigM3~brksAge3uzWjH0yhOK~VTgP6BtiECb9kxNU3Zd9XKqcDbNCDvlh-pPLvfYfOUSFWQZ-CaQBOqiOS4XOmEzDZ~u7pN1d6WLa8tLUotWzm~Rgp4hlSJxkaNoiv5OpN0HGARoTBBtnUeQnjK4MNTyXkJJF98mcCeuIxpNJMdCI7U2MlqsWlY5I0D16R6ru5ORPyoHBbb~qXk6WzmWcVOHSYy0RJgGCNRvwU7e0McqIPG1FuwGYZFSN0ukSPe9fqTwXOkgqWuhfAWp-hCpY0J~qK335Ts0MiQg6n4OVaeR0BG1MOnIQtdWe2Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Hf_and_Lu_isotopic_reference_values_for_the_zircon_standard_91500_by_MC_ICP_MS","translated_slug":"","page_count":9,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420476,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420476/thumbnails/1.jpg","file_name":"Hf_and_Lu_isotopic_reference_values_for_20170401-6062-e2aa17.pdf","download_url":"https://www.academia.edu/attachments/52420476/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Hf_and_Lu_isotopic_reference_values_for.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420476/Hf_and_Lu_isotopic_reference_values_for_20170401-6062-e2aa17-libre.pdf?1491067327=\u0026response-content-disposition=attachment%3B+filename%3DHf_and_Lu_isotopic_reference_values_for.pdf\u0026Expires=1733097976\u0026Signature=Z60RMf~w5-6hV7ioCbATxYenuTAgigM3~brksAge3uzWjH0yhOK~VTgP6BtiECb9kxNU3Zd9XKqcDbNCDvlh-pPLvfYfOUSFWQZ-CaQBOqiOS4XOmEzDZ~u7pN1d6WLa8tLUotWzm~Rgp4hlSJxkaNoiv5OpN0HGARoTBBtnUeQnjK4MNTyXkJJF98mcCeuIxpNJMdCI7U2MlqsWlY5I0D16R6ru5ORPyoHBbb~qXk6WzmWcVOHSYy0RJgGCNRvwU7e0McqIPG1FuwGYZFSN0ukSPe9fqTwXOkgqWuhfAWp-hCpY0J~qK335Ts0MiQg6n4OVaeR0BG1MOnIQtdWe2Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":4107,"name":"High Pressure","url":"https://www.academia.edu/Documents/in/High_Pressure"},{"id":16024,"name":"Chemical Geology","url":"https://www.academia.edu/Documents/in/Chemical_Geology"},{"id":159153,"name":"Laser Ablation","url":"https://www.academia.edu/Documents/in/Laser_Ablation"},{"id":191117,"name":"High Temperature","url":"https://www.academia.edu/Documents/in/High_Temperature"},{"id":203965,"name":"Ion Exchange Chromatography","url":"https://www.academia.edu/Documents/in/Ion_Exchange_Chromatography"},{"id":222413,"name":"Inductively Coupled Plasma Mass Spectrometry","url":"https://www.academia.edu/Documents/in/Inductively_Coupled_Plasma_Mass_Spectrometry"},{"id":1292656,"name":"Reference Value","url":"https://www.academia.edu/Documents/in/Reference_Value"}],"urls":[]}, dispatcherData: dispatcherData }); 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These matrix effects were evaluated by comparing pure Cd and Zn standards and standards doped with bulk column blank from the anion exchange chromatography procedure. Doped standards exhibit signal enhancements (Cd, Ag, Zn and Cu), instrumental mass bias changes and inaccurate isotopic compositions relative to undoped standards, all of which are attributed to the combined presence of resin-derived organics and inorganics. The matrix effect associated with the inorganic component of the column blanks was evaluated separately by doping standards with metals at the trace levels detected in the column blanks. Mass bias effects introduced by the inorganic column blank matrix are smaller than for the bulk column blank matrix but can still lead to significant changes in ion signal intensity, instrumental mass bias and isotopic ratios. Chemical treatment with refluxed HNO 3 or HClO 4 /HNO 3 removes resin-derived organic components resulting in matrix effects similar in magnitude to those associated with the inorganic component of the column blank.","publication_date":{"day":null,"month":null,"year":2009,"errors":{}},"publication_name":"Analytica Chimica 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Alteration mineralogy and the effect of acid-leaching on the Pb-isotope systematics of ocean-island basalts" class="work-thumbnail" src="https://attachments.academia-assets.com/52420475/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186843/Alteration_mineralogy_and_the_effect_of_acid_leaching_on_the_Pb_isotope_systematics_of_ocean_island_basalts">Alteration mineralogy and the effect of acid-leaching on the Pb-isotope systematics of ocean-island basalts</a></div><div class="wp-workCard_item"><span>American Mineralogist</span><span>, 2009</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="4fc209e32e3c7466e788c9cf7af93d21" class="wp-workCard--action" rel="nofollow" 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Pb-isotope systematics of weakly altered basalts from two major ocean islands (Hawaii and Kerguelen) was investigated using scanning electron microscopy (SEM), X-ray diffraction (XRD), and acid-leaching experiments. Alteration within vesicles and as replacement products of olivine and glass consists mainly of phyllosilicate mixtures (most commonly smectite ± talc, serpentine, chlorite, celadonite), goethite, and zeolite with minor pyrolusite, barite, apophyllite, dolomite, pyrite, and chalcopyrite. The presence of distinct alteration assemblages within the Hawaiian and Kerguelen basalts can be related to differences in their eruption environment, age, and sampling method. In particular, the Hawaiian basalts have been contaminated by highly radiogenic components (seawater and drilling mud), demonstrating the importance of acid-leaching prior to Pb-isotopic analysis even for young basalts that appear to be relatively unaltered. However, for some basalts, leaching may not remove the alteration completely or in a reproducible way, which may reflect variable extents of dissolution of secondary minerals that are not readily soluble in HCl (e.g., celadonite) or inconsistencies in the leaching procedure. The incomplete removal of foreign Pb components, which typically have distinct Pb-isotopic signatures, is a major source of uncertainty and may represent the ultimate limitation on high-precision Pb-isotopic compositions of ocean-island basalts. To achieve the highest precision and accuracy, we recommend that Pb-isotope studies of basalts include an investigation of the alteration mineralogy and an evaluation of the effectiveness of the leaching procedure as part of standard quality control protocols.","publication_date":{"day":null,"month":null,"year":2009,"errors":{}},"publication_name":"American Mineralogist","grobid_abstract_attachment_id":52420475},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186843/Alteration_mineralogy_and_the_effect_of_acid_leaching_on_the_Pb_isotope_systematics_of_ocean_island_basalts","translated_internal_url":"","created_at":"2017-04-01T10:05:21.315-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304415,"work_id":32186843,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Alteration mineralogy and the effect of acid-leaching on the Pb-isotope systematics of ocean-island basalts"},{"id":28305128,"work_id":32186843,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176605,"email":"j***o@ship.iodp.tamu.edu","display_order":4194304,"name":"Diane Hanano","title":"Alteration mineralogy and the effect of acid-leaching on the Pb-isotope systematics of ocean-island basalts"}],"downloadable_attachments":[{"id":52420475,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420475/thumbnails/1.jpg","file_name":"Alteration_mineralogy_and_the_effect_of_20170401-6059-13g6ldo.pdf","download_url":"https://www.academia.edu/attachments/52420475/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Alteration_mineralogy_and_the_effect_of.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420475/Alteration_mineralogy_and_the_effect_of_20170401-6059-13g6ldo-libre.pdf?1491067345=\u0026response-content-disposition=attachment%3B+filename%3DAlteration_mineralogy_and_the_effect_of.pdf\u0026Expires=1733034950\u0026Signature=QBgTEha-cUWhIHSVn9cCNS5JP26ujbLZNxmfw2SE9sZFYZjCCb1ufWP2j2vYTGhl94hwG64KnantNXYJNAr5t-cUI2DI4iOHAH1y-f7p6~abl6wUyx03w0TqR-r5dbwDk5KhLCF1VaALl-Ef94l0L0Gv6Unfzd2SfMeR7tr8Bav6SKN4JTZlM1ltpuN46q7XvqVq6Dl3mIFVr1h0sOfPjPEuDVt7kK-EdKlkGu9LetNW8jamnBn29MZQWXu02Svv74LzqmcoGGeVvqE1a7BY1ukeMGp-5Uht~HkSNt84mAWMLisqR0HA5EKGtQcAv2mGSPeIRjK3-D4DSy3k36Symw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Alteration_mineralogy_and_the_effect_of_acid_leaching_on_the_Pb_isotope_systematics_of_ocean_island_basalts","translated_slug":"","page_count":10,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420475,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420475/thumbnails/1.jpg","file_name":"Alteration_mineralogy_and_the_effect_of_20170401-6059-13g6ldo.pdf","download_url":"https://www.academia.edu/attachments/52420475/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Alteration_mineralogy_and_the_effect_of.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420475/Alteration_mineralogy_and_the_effect_of_20170401-6059-13g6ldo-libre.pdf?1491067345=\u0026response-content-disposition=attachment%3B+filename%3DAlteration_mineralogy_and_the_effect_of.pdf\u0026Expires=1733034950\u0026Signature=QBgTEha-cUWhIHSVn9cCNS5JP26ujbLZNxmfw2SE9sZFYZjCCb1ufWP2j2vYTGhl94hwG64KnantNXYJNAr5t-cUI2DI4iOHAH1y-f7p6~abl6wUyx03w0TqR-r5dbwDk5KhLCF1VaALl-Ef94l0L0Gv6Unfzd2SfMeR7tr8Bav6SKN4JTZlM1ltpuN46q7XvqVq6Dl3mIFVr1h0sOfPjPEuDVt7kK-EdKlkGu9LetNW8jamnBn29MZQWXu02Svv74LzqmcoGGeVvqE1a7BY1ukeMGp-5Uht~HkSNt84mAWMLisqR0HA5EKGtQcAv2mGSPeIRjK3-D4DSy3k36Symw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"}],"urls":[]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="6767200" id="kerguelen"><div class="js-work-strip profile--work_container" data-work-id="32187048"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32187048/Geologie_des_iles_Crozet"><img alt="Research paper thumbnail of Geologie des iles Crozet" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32187048/Geologie_des_iles_Crozet">Geologie des iles Crozet</a></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187048"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187048"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187048; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186998"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186998/Ninetyeast_Ridge_Indian_Ocean_A_5000_km_record_of_a_Dupal_mantle_plume"><img alt="Research paper thumbnail of Ninetyeast Ridge (Indian Ocean): A 5000 km record of a Dupal mantle plume" class="work-thumbnail" src="https://attachments.academia-assets.com/52420549/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186998/Ninetyeast_Ridge_Indian_Ocean_A_5000_km_record_of_a_Dupal_mantle_plume">Ninetyeast Ridge (Indian Ocean): A 5000 km record of a Dupal mantle plume</a></div><div class="wp-workCard_item"><span>Geology</span><span>, 1991</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Data and observation from Drifting Program Leg 121 and plate-tectonic reconstructions indicate th...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Data and observation from Drifting Program Leg 121 and plate-tectonic reconstructions indicate that the Ninetyeast Ridge (Indian Ocean) was derived from the interaction of a deep-seated Dupal hotspot and a nearby spreading-ridge axis. The 5000-km-long ridge, from lat 34°S to Rat 10°N, was drilled at three sites during Leg 121. About 178 m of basalt, >38 to >80 Ma, were recovered from a total penetration of ˜310 m. Shipboard petrographic and geochemical studies showed that each site has distinctive characteristics. Most of the cored lavas have a tholeiitic basalt composition. Incompatible-element abundanes and ratios show systematic trends, consistent with an origin for the Ninetyeast Ridge lavas by mixing between a depleted component-Indian Ocean mid-ocean ridge basalt-and an enriched component-oceanic-island basalt similar to that observed in the youngest alkalic basalts from the Kerguelen archipelago. Preliminary shore-based trace element abundance and isotopic data are compatible with this hypothesis, although Pb isotopes indicate the involvement of another component. The long-lasting and more or less continuous activity of the Kerguelen-Heard plume (ca. 115 Ma), now located under Heard Island, south of the Southeast Indian Ridge, provides evidence that the source of the Dupal anomaly is deep seated.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e10b7e05afb71a557cfedd488e5ab346" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420549,"asset_id":32186998,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420549/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186998"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186998"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186998; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186998]").text(description); $(".js-view-count[data-work-id=32186998]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186998; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186998']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186998, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "e10b7e05afb71a557cfedd488e5ab346" } } $('.js-work-strip[data-work-id=32186998]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186998,"title":"Ninetyeast Ridge (Indian Ocean): A 5000 km record of a Dupal mantle plume","translated_title":"","metadata":{"abstract":"Data and observation from Drifting Program Leg 121 and plate-tectonic reconstructions indicate that the Ninetyeast Ridge (Indian Ocean) was derived from the interaction of a deep-seated Dupal hotspot and a nearby spreading-ridge axis. 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Mixing of depleted asthenosphere with the plume in sublithospheric channels during migration of the Southeast the Kerguelen Archipelago (Mont des Ruches and Mont Fontaine) indicates that three distinct magma types erupted within \u003e1 Myr. Indian Ridge axis away from the Kerguelen hotspot is proposed as a suitable explanation to account for the temporal distribution of Low-MgO basalts (\u003e4-6 wt %) in both sections are overlain by high-MgO basalts (\u003e7-13 wt %), mostly present in Mont the depleted component in basalts from the Northern Kerguelen Plateau and the \u003e26 Ma Kerguelen Archipelago flood basalts; Fontaine. Both high-and low-MgO basalts have nearly identical cessation of plume-ridge interactions may explain the absence of low 87 Sr/ 86 Sr and high 143 Nd/ 144 Nd and formed from similar depleted basalts in the youngest sections that erupted further away parental magmas that represent mixtures between a depleted mantle from the ridge axis. component and the Kerguelen plume. The third magma type, predominant in Mont des Ruches, is represented by high-MgO basalts that are isotopically heterogeneous with isotopic ratios that are intermediate between those of the stratigraphically lower basalts KEY WORDS: Kerguelen Archipelago; basalt; geochemistry; depleted comand the Kerguelen plume compositions; this third magma type may ponent; Kerguelen plume; mixing have formed by mixing of similar material, but with a higher contribution from the Kerguelen plume. The depleted component involved in all three magma types is similar to the source for Southeast Indian Ridge basalts and is present in Kerguelen Archipelago basalts * Corresponding author. 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Large variations of trace element concentrations in clinopyroxenes and their INTRODUCTION isotopic compositions reflect the strong imprint of complex, multi-It is now well accepted that the Earth's mantle behaves stage metasomatic episodes during evolution of the lithospheric mantle as a viscous fluid over geologic time-scales. The variation under the Kerguelen Archipelago. Two metasomatic agents have been and amplitude of mantle geochemical heterogeneities identified that have interacted with the mantle peridotite matrix: (1) reflect the efficiency of heat and mass transfer processes a basaltic melt, and a carbonatitic melt that produced extremely as well as the composition of entrained components (e.g. high and variable incompatible element abundances in clinopyroxenes, . The heterogeneous nature of the which are attributed to chromatographic effects associated with convecting mantle has been delineated through the geometasomatic melt transport by porous flow through the mantle. chemical study of (1) mid-ocean ridge basalts (MORB) Isotopic compositions of 12 peridotite xenoliths indicate that both and oceanic island basalts (OIB) (e.g. Zindler \u0026 Hart, types of metasomatic melts are related to the alkaline magmatism 1986; Hofmann, 1997), and (2) mantle xenoliths, typically produced by the Kerguelen plume. In contrast, isotopic data from a characterized by a much greater geochemical variability single dunite xenolith indicate the strong influence of a continental than their host and related basalts (e.g. Hauri et al., lithospheric component, probably derived from Gondwanaland, that 1993). Mantle plumes represent the main mechanism for either forms part of the Kerguelen Plateau or was incorporated into entrainment in the mantle (Hart et al., 1992; Hauri et al., the mantle beneath Kerguelen and mixed with plume-derived 1994).","publication_date":{"day":null,"month":null,"year":1999,"errors":{}},"publication_name":"Journal of Petrology","grobid_abstract_attachment_id":52420521},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186900/Evolution_of_Heterogeneous_Lithospheric_Mantle_in_a_Plume_Environment_Beneath_the_Kerguelen_Archipelago","translated_internal_url":"","created_at":"2017-04-01T10:05:28.266-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304427,"work_id":32186900,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James 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and Mass Transfer","url":"https://www.academia.edu/Documents/in/Heat_and_Mass_Transfer"},{"id":48814,"name":"Indian Ocean","url":"https://www.academia.edu/Documents/in/Indian_Ocean"},{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":281810,"name":"Mantle xenolith","url":"https://www.academia.edu/Documents/in/Mantle_xenolith"},{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186898"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" 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wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/MatthiasFranssens">Matthias Franssens</a></span></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, 2007</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="fc82a21b3ff0fa2c70873f9c40ad64b7" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420508,"asset_id":32186898,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420508/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action 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The 4 km 2 Val gabbro plutonic suite was emplaced at 24Á25 AE 0Á15 Ma (U^Pb zircon) into 25 Ma volcanic rocks of the Southeast Province, locally producing a large zone of overlying basaltic breccia. Cumulate basic^ultrabasic rocks are the dominant lithology in the intrusion, with horizontally layered peridotites at the base of the exposed part of the intrusion, overlain by vertically layered, coarsegrained plagioclase-bearing peridotites, melagabbros and equigranular gabbros. The intrusion was formed by repeated injections of relatively crystal-rich and crystal-poor magmas into an open-system magma reservoir. Strong geochemical and isotopic similarities between the fine-grained marginal microgabbros and cross-cutting felsic rocks and the hosting mildly alkalic basalts and trachytes of the Southeast Province indicate that they were derived from similar alkalic basaltic parental magmas, which were dominated by the enriched component of the Kerguelen mantle plume source. At 25 Ma, the change from tholeiitic^transitional to mildly alkalic basalts marks the terminal stage of flood basalt volcanism on the Kerguelen Archipelago. This compositional change was associated with deeper melting within the Kerguelen plume source, lower extents of melting, a decrease in magma supply, and the emplacement of high-level intrusions such as the Val gabbro plutonic suite.","publication_date":{"day":null,"month":null,"year":2007,"errors":{}},"publication_name":"Journal of 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Archipelago"},{"id":28304637,"work_id":32186898,"tagging_user_id":62411756,"tagged_user_id":62450636,"co_author_invite_id":6176467,"email":"m***s@yahoo.fr","display_order":4194304,"name":"Matthias Franssens","title":"The Val Gabbro Plutonic Suite: A Sub-volcanic Intrusion Emplaced at the End of Flood Basalt Volcanism on the Kerguelen Archipelago"},{"id":28304665,"work_id":32186898,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176477,"email":"h***l@hotmail.com","display_order":6291456,"name":"Heidi Annell","title":"The Val Gabbro Plutonic Suite: A Sub-volcanic Intrusion Emplaced at the End of Flood Basalt Volcanism on the Kerguelen Archipelago"},{"id":28304669,"work_id":32186898,"tagging_user_id":62411756,"tagged_user_id":20819004,"co_author_invite_id":6176478,"email":"n***p@whitman.edu","affiliation":"Whitman College","display_order":7340032,"name":"Kirsten Nicolaysen","title":"The Val Gabbro Plutonic Suite: A Sub-volcanic Intrusion Emplaced at the End of 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wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186897/The_Ninetyeast_Ridge_and_its_Relation_to_the_Kerguelen_Amsterdam_and_St_Paul_Hotspots_in_the_Indian_Ocean">The Ninetyeast Ridge and its Relation to the Kerguelen, Amsterdam and St. Paul Hotspots in the Indian Ocean</a></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, 2013</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="34fc53480932533138c5883e6f474e6e" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420526,"asset_id":32186897,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420526/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i 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})(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "34fc53480932533138c5883e6f474e6e" } } $('.js-work-strip[data-work-id=32186897]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186897,"title":"The Ninetyeast Ridge and its Relation to the Kerguelen, Amsterdam and St. Paul Hotspots in the Indian Ocean","translated_title":"","metadata":{"ai_title_tag":"Isotopic Study of Ninetyeast Ridge and Its Mantle Sources","grobid_abstract":"The Ninetyeast Ridge is an $5500 km long, north^south-oriented, submarine volcanic ridge in the eastern Indian Ocean that formed from magmatism associated with the deep-seated Kerguelen mantle plume as the Indian plate drifted rapidly northward during the Late Cretaceous. Basalts recovered along the ridge have the characteristic Dupal geochemical signature of Indian Ocean basalts, but debate concerning the nature and number of components in their mantle source persists. New multiple collector inductively coupled plasma mass spectrometry (Pb, Hf) and thermal ionization mass spectrometry (Sr, Nd) isotopic analyses were obtained for tholeiites representative of the $180 m of basaltic basement recovered from three drill sites (Site 758, 82 Ma; Site 757, 58 Ma; Site 756, 43 Ma) along the Ninetyeast Ridge during Ocean Drilling Program Leg 121. No systematic isotopic variation is observed along the ridge, which is inconsistent with the hypothesis of an aging mantle plume origin for the ridge. The isotopic compositions are generally intermediate between those of the volcanic products of the Kerguelen and Amsterdam^St. Paul hotspots and define mixing trends between components with relatively enriched and depleted signatures. At least three, possibly four, source components are required to explain the observed isotopic variability along the Ninetyeast Ridge. The unradiogenic signatures of some Ninetyeast Ridge basalts (e.g. 87 Sr/ 86 Sr ¼ 0·70381^0·70438) are not related to the source of Indian MORB and indicate the presence of a relatively depleted component in a deep mantle source. A similar source component is also identified in other Indian Ocean island basalts (e.g. Crozet, Re¤ union) not related to magmatic activity of the Kerguelen hotspot. The Pb^Hf^Sr^Nd isotopic compositions of the Ninetyeast Ridge basalts are consistent with the presence of a mixture of recycled sediments and lower continental crust together with altered oceanic crust in their mantle source, hence supporting a deep origin for the enriched Dupal signature encountered in ocean island basalts.","publication_date":{"day":null,"month":null,"year":2013,"errors":{}},"publication_name":"Journal of Petrology","grobid_abstract_attachment_id":52420526},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186897/The_Ninetyeast_Ridge_and_its_Relation_to_the_Kerguelen_Amsterdam_and_St_Paul_Hotspots_in_the_Indian_Ocean","translated_internal_url":"","created_at":"2017-04-01T10:05:27.786-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304402,"work_id":32186897,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"The Ninetyeast Ridge and its Relation to the Kerguelen, Amsterdam and St. Paul Hotspots in the Indian Ocean"},{"id":28304553,"work_id":32186897,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176449,"email":"i***e@eos.ubc.ca","display_order":4194304,"name":"Nobre Silva","title":"The Ninetyeast Ridge and its Relation to the Kerguelen, Amsterdam and St. Paul Hotspots in the Indian Ocean"}],"downloadable_attachments":[{"id":52420526,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420526/thumbnails/1.jpg","file_name":"The_Ninetyeast_Ridge_and_its_Relation_to20170401-6059-7he7mj.pdf","download_url":"https://www.academia.edu/attachments/52420526/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"The_Ninetyeast_Ridge_and_its_Relation_to.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420526/The_Ninetyeast_Ridge_and_its_Relation_to20170401-6059-7he7mj-libre.pdf?1491067304=\u0026response-content-disposition=attachment%3B+filename%3DThe_Ninetyeast_Ridge_and_its_Relation_to.pdf\u0026Expires=1733034950\u0026Signature=g7j6nnLiyqBa97trIJtkMhpM40AQDhweRlsA9LQ12YuxYlU8qV0Pf95~9oHySR2HycWEkvz-7FHvj8ilwtuCYBDlJJGyetmVGgPeS7EAfNT4fiRdmtGJHip-JRb4Hh1cZXfN-zo6lSlIaCfDtLZeOVTvUPy4FGRTBIzGHQDAibzWNjaQ06k4xrAainVeTvZuJ13KWJ38hjn-0UgxWgKNj9xb-R0IglHawyK39h0nSwEcpwZtQzn0H~PgCXkeI1xCU5bgoapdRBgMVoId5GqrjvX0RZDcH1UV7lZKkUjMbybexTbm9NAWuE9XDHXq4OCJq-9qUZ4tw1M9vE5dKLzlMA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_Ninetyeast_Ridge_and_its_Relation_to_the_Kerguelen_Amsterdam_and_St_Paul_Hotspots_in_the_Indian_Ocean","translated_slug":"","page_count":39,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420526,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420526/thumbnails/1.jpg","file_name":"The_Ninetyeast_Ridge_and_its_Relation_to20170401-6059-7he7mj.pdf","download_url":"https://www.academia.edu/attachments/52420526/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"The_Ninetyeast_Ridge_and_its_Relation_to.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420526/The_Ninetyeast_Ridge_and_its_Relation_to20170401-6059-7he7mj-libre.pdf?1491067304=\u0026response-content-disposition=attachment%3B+filename%3DThe_Ninetyeast_Ridge_and_its_Relation_to.pdf\u0026Expires=1733034950\u0026Signature=g7j6nnLiyqBa97trIJtkMhpM40AQDhweRlsA9LQ12YuxYlU8qV0Pf95~9oHySR2HycWEkvz-7FHvj8ilwtuCYBDlJJGyetmVGgPeS7EAfNT4fiRdmtGJHip-JRb4Hh1cZXfN-zo6lSlIaCfDtLZeOVTvUPy4FGRTBIzGHQDAibzWNjaQ06k4xrAainVeTvZuJ13KWJ38hjn-0UgxWgKNj9xb-R0IglHawyK39h0nSwEcpwZtQzn0H~PgCXkeI1xCU5bgoapdRBgMVoId5GqrjvX0RZDcH1UV7lZKkUjMbybexTbm9NAWuE9XDHXq4OCJq-9qUZ4tw1M9vE5dKLzlMA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); 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It is probably related to the early stages of activity of the Kerguelen hot spot which is also responsible for the Ninetyeast Ridge. It shows all evidence of being an oceanic plateau with an impressive volume of magmatism. The Nd-Sr isotopic systematics of the Plateau basalts show a large spread of values comparable to the systematics shown by the basalts from the Kerguelen Islands. However, while the archipelago basalts have Pb isotopic variations almost within analytical errors, the Plateau basalts show large Pb isotopic variations which overiap the whole range observed amongst Indian Ocean ridge basal\u0026 Contamination of a deep, enriched OIB-type plume, i.e., the Kerguelen hot spot with characteristic Dupal signature, by a depleted, MORBtype reservoir can account for both the trace-element and isotopic geochemistry of the Kerguelen Plateau basalts. This indicates the existence of the Dupal anomaly already I 1.5 Ma ago. In addition, evidence for its involvement in the genesis of Indian Ocean basalts occurs throughout time, including the present day. This favors the hypothesis of a deep-seated source for this major geochemical anomaly which is then probably responsible for the special features of the Indian Ocean. Editorial handling: G. Faure REFERENCES BASSIAS Y., DAVIES H. L., LECLAIRE L., and WEIS D. (1987) Basaltic basement and sedimentary rocks from the southern sector of the Ke~uelen-Hod Plateau: new data and their Mesa-Cenozoic paleoaeosranhic and aeodynamic implications. B\u0026tin du Mus~~rn na\u0026\u0026l ci'Histoire_naturelle, Paris 419, 367-403. CASTILLO P. (1988) The Dupal anomaly as a trace of the upwelling lower mantle. Nature 3X, 667-670. COFFIN M. F., DAVIES H. L., and HAXBY W. F. (1986) Structure of the Kerguelen Plateau province from SEASAT altimetry and seismic reflection data. 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href="https://www.academia.edu/32186883/Trace_of_the_Kerguelen_mantle_plume_Evidence_from_seamounts_between_the_Kerguelen_Archipelago_and_Heard_Island_Indian_Ocean">Trace of the Kerguelen mantle plume: Evidence from seamounts between the Kerguelen Archipelago and Heard Island, Indian Ocean</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ulb.academia.edu/DimitriDamasceno">Dimitri Damasceno</a></span></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2002</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e13d9635edaff3638cc1e7f1ca257025" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186880"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186880/Constraining_the_components_of_the_Kerguelen_mantle_plume_A_Hf_Pb_Sr_Nd_isotopic_study_of_picrites_and_high_MgO_basalts_from_the_Kerguelen_Archipelago"><img alt="Research paper thumbnail of Constraining the components of the Kerguelen mantle plume: A Hf-Pb-Sr-Nd isotopic study of picrites and high-MgO basalts from the Kerguelen Archipelago" class="work-thumbnail" src="https://attachments.academia-assets.com/52420495/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" 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high-MgO volcanic rocks (6-17 wt.% MgO) from the Kerguelen Archipelago, which are rare compared to other oceanic islands, to better constrain the nature and the origin of components present in the Kerguelen mantle plume source. The Sr and Nd isotopic compositions of the transitional to mildly alkalic picrites and high-MgO basalts closely match those of the 24 Ma mildly alkalic basalts from the Courbet Peninsula, whose compositions are considered to reflect the present geochemical expression of the enriched component of the Kerguelen mantle plume. However, linear trends in Pb isotopic compositions in the studied samples reflect involvement of a component with lower 206 Pb/ 204 Pb and 208 Pb/ 204 Pb than that inferred for the enriched Kerguelen plume. Contamination of the MgO-rich magmas by the Kerguelen Plateau cannot account for the observed Hf-Pb-Sr-Nd isotopic variations. Isotopic systematics in the picrites and the high-MgO basalts are inconsistent with simple binary mixing between two distinct end-members and indicate the presence of small-scale heterogeneities within the Kerguelen plume itself as has been observed in other hot spot environments such as Hawaii and Iceland. The 34 to 26 Ma Kerguelen plume-related basalts that formed when the archipelago was close to the ridge axis ($50 to 250 km) show geochemical evidence for significant involvement of a Southeast Indian Ridge (SEIR)-like source. In contrast, the 24-25 Ma mildly alkalic basalts from the eastern and southeastern parts of the archipelago, which erupted about 400 km away from the SEIR, and the picrites and high-MgO basalts from this study show little or no contribution from a SEIR-like component. Thus chemical interaction between the SEIR axis and the Kerguelen plume effectively ceased prior to 25 Ma.","publication_date":{"day":null,"month":null,"year":2005,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420495},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186880/Constraining_the_components_of_the_Kerguelen_mantle_plume_A_Hf_Pb_Sr_Nd_isotopic_study_of_picrites_and_high_MgO_basalts_from_the_Kerguelen_Archipelago","translated_internal_url":"","created_at":"2017-04-01T10:05:25.479-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304405,"work_id":32186880,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Constraining the components of the Kerguelen mantle plume: A Hf-Pb-Sr-Nd isotopic study of picrites and high-MgO basalts from the Kerguelen Archipelago"},{"id":28304609,"work_id":32186880,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176460,"email":"d***t@ipgp.jussieu.fr","display_order":4194304,"name":"Sonia Doucet","title":"Constraining the components of the Kerguelen mantle plume: A Hf-Pb-Sr-Nd isotopic study of picrites and high-MgO basalts from the Kerguelen 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"profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186879"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186879/Flood_basalts_from_Mt_Capitole_in_the_central_Kerguelen_Archipelago_Insights_into_the_growth_of_the_archipelago_and_source_components_contributing_to_plume_related_volcanism"><img alt="Research paper thumbnail of Flood basalts from Mt. Capitole in the central Kerguelen Archipelago: Insights into the growth of the archipelago and source components contributing to plume-related volcanism" class="work-thumbnail" src="https://attachments.academia-assets.com/52420502/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186879/Flood_basalts_from_Mt_Capitole_in_the_central_Kerguelen_Archipelago_Insights_into_the_growth_of_the_archipelago_and_source_components_contributing_to_plume_related_volcanism">Flood basalts from Mt. Capitole in the central Kerguelen Archipelago: Insights into the growth of the archipelago and source components contributing to plume-related volcanism</a></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2007</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="75e65fb4554383ba2acba791e8e3412f" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420502,"asset_id":32186879,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420502/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186879"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186879"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186879; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186879]").text(description); $(".js-view-count[data-work-id=32186879]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186879; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186879']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186879, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "75e65fb4554383ba2acba791e8e3412f" } } $('.js-work-strip[data-work-id=32186879]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186879,"title":"Flood basalts from Mt. Capitole in the central Kerguelen Archipelago: Insights into the growth of the archipelago and source components contributing to plume-related volcanism","translated_title":"","metadata":{"grobid_abstract":"1] The Kerguelen Archipelago, constructed on the submarine Northern Kerguelen Plateau, is attributed to Cenozoic volcanism arising from the Kerguelen hot spot. Geochemical studies of 325 to 1000 m thick lava sections of the $30 to 25 Ma flood basalt forming the bulk of the archipelago show a temporal change from older tholeiitic basalt to younger slightly alkalic basalt. This compositional transition is expressed in a 630 m lava section at Mt. Capitole where the lava sequence is lowermost tholeiitic basalt overlain by slightly alkalic basalt overlain by plagioclase-rich cumulates that are mixtures of plagioclase-phyric basalt and more evolved magmas. During growth of the archipelago, magma supply from the hot spot was variable and at times sufficiently low to enable extensive crystal fractionation; e.g., at Mt. Capitole and nearby Mt. Tourmente only 10 of 120 lava flows have \u003e6 wt% MgO. On the basis of this study and previous isotopic data for the $34 Ma submarine lavas erupted on the Northern Kerguelen Plateau, other flood basalt sections in the Kerguelen Archipelago, and younger lavas erupted in the archipelago and at Heard Island, there is significant Sr, Nd, Hf, and Pb isotopic heterogeneity that can be explained by two stages of mixing. The first mixing event, best shown by the submarine lavas, is between components that are related to Indian Ocean mid-ocean ridge basalt (MORB) and the Kerguelen hot spot. From $34 Ma to \u003c1 Ma, on average the proportion of the MORB-related component decreased. Subsequently, a second mixing process involved addition of a component with relatively high 87 Sr/ 86 Sr (\u003e0.7060) and low 143 Nd/ 144 Nd (\u003c0.5125) and 176 Hf/ 177 Hf (\u003c0.2827) and nonradiogenic Pb isotope ratios (\u003c17.9 for 206 Pb/ 204 Pb). We infer that this component was lower continental crust.","publication_date":{"day":null,"month":null,"year":2007,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420502},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186879/Flood_basalts_from_Mt_Capitole_in_the_central_Kerguelen_Archipelago_Insights_into_the_growth_of_the_archipelago_and_source_components_contributing_to_plume_related_volcanism","translated_internal_url":"","created_at":"2017-04-01T10:05:25.349-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304396,"work_id":32186879,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Flood basalts from Mt. Capitole in the central Kerguelen Archipelago: Insights into the growth of the archipelago and source components contributing to plume-related volcanism"},{"id":28305112,"work_id":32186879,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":355366,"email":"f***y@mit.edu","display_order":4194304,"name":"Frederick Frey","title":"Flood basalts from Mt. 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element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":1993786,"name":"Cumulant","url":"https://www.academia.edu/Documents/in/Cumulant"},{"id":2303517,"name":"Temporal Change","url":"https://www.academia.edu/Documents/in/Temporal_Change"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186871"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186871/Relationship_between_the_early_Kerguelen_plume_and_continental_flood_basalts_of_the_paleo_Eastern_Gondwanan_margins"><img alt="Research paper thumbnail of Relationship between the early Kerguelen plume and continental flood basalts of the paleo-Eastern Gondwanan margins" class="work-thumbnail" 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class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186868/Kerguelen_Archipelago_revisited_geochemical_and_isotopic_study_of_the_Southeast_Province_lavas">Kerguelen Archipelago revisited: geochemical and isotopic study of the Southeast Province lavas</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, 1993</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6b7c3ef492cf7efcced69a5fc63efe1c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420488,"asset_id":32186868,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420488/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa 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Letters</span><span>, 2006</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="cbc16524f2d62a62e4b3462d4d5f9e77" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420492,"asset_id":32186866,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420492/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186866"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div 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{"id":32186866,"title":"Primitive neon and helium isotopic compositions of high-MgO basalts from the Kerguelen Archipelago, Indian Ocean","translated_title":"","metadata":{"grobid_abstract":"The geochemical characteristics of mildly alkalic basalts (24-25 Ma) erupted in the southeastern Kerguelen Archipelago are considered to represent the best estimate for the composition of the enriched Kerguelen plume end-member. A recent study of picrites and high-MgO basalts from this part of the archipelago highlighted the Pb and Hf isotopic variations and suggested the presence of mantle heterogeneities within the Kerguelen plume itself. We present new helium and neon isotopic compositions for olivines from these picrites and high-MgO basalts (6-17 wt.% MgO) both to constrain the enriched composition of the Kerguelen plume and to determine the origin of isotopic heterogeneities involved in the genesis of Kerguelen plume-related basalts. The olivine phenocrysts have extremely variable 4 He / 3 He compositions between MORB and primitive values observed in OIB (~90,000 to 40,000; i.e., R / R a~8 to 18) and they show primitive neon isotopic ratios (average 21 Ne / 21 Ne ext~0 .044). The neon isotopic systematics and the 4 He / 3 He ratios that are lower than MORB values for the Kerguelen basalts clearly suggest that the Kerguelen hotspot belongs to the family of primitive hotspots, such as Iceland and Hawaii. The rare gas signature for the Kerguelen samples, intermediate between MORB and solar, is apparently inconsistent with mixing of a primitive component with a MORB-like source, but may result from sampling a heterogeneous part of the mantle with solar 3 He / 22 Ne and with a higher (U, Th) / 3 He ratio compared to typically high R / R a hotspot basalts such as those from Iceland and Hawaii. D","publication_date":{"day":null,"month":null,"year":2006,"errors":{}},"publication_name":"Earth and Planetary Science Letters","grobid_abstract_attachment_id":52420492},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186866/Primitive_neon_and_helium_isotopic_compositions_of_high_MgO_basalts_from_the_Kerguelen_Archipelago_Indian_Ocean","translated_internal_url":"","created_at":"2017-04-01T10:05:23.817-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304404,"work_id":32186866,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Primitive neon and helium isotopic compositions of high-MgO basalts from the Kerguelen Archipelago, Indian 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href="https://www.academia.edu/32186865/Geochemical_and_Hf_Pb_Sr_Nd_isotopic_constraints_on_the_origin_of_the_Amsterdam_St_Paul_Indian_Ocean_hotspot_basalts"><img alt="Research paper thumbnail of Geochemical and Hf–Pb–Sr–Nd isotopic constraints on the origin of the Amsterdam–St. Paul (Indian Ocean) hotspot basalts" class="work-thumbnail" src="https://attachments.academia-assets.com/52420479/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186865/Geochemical_and_Hf_Pb_Sr_Nd_isotopic_constraints_on_the_origin_of_the_Amsterdam_St_Paul_Indian_Ocean_hotspot_basalts">Geochemical and Hf–Pb–Sr–Nd isotopic constraints on the origin of the Amsterdam–St. Paul (Indian Ocean) hotspot basalts</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, 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{"id":32186865,"title":"Geochemical and Hf–Pb–Sr–Nd isotopic constraints on the origin of the Amsterdam–St. Paul (Indian Ocean) hotspot basalts","translated_title":"","metadata":{"ai_title_tag":"Isotopic and Geochemical Analysis of Amsterdam-St. Paul Hotspot Basalts","grobid_abstract":"The Amsterdam^St. Paul (ASP) Plateau is a recent ( 9 5 Ma) volcanic rise constructed along the Southeast Indian Ridge (SEIR) by the combined effects of a relatively small mantle plume and a mid-oceanic ridge. The Amsterdam and St. Paul islands are located 100 km away from each other and formed during the last 0.4 Myr; they are the only subaerial features of the ASP Plateau and the two islands are structurally separated by the presence of a SW^NE transform fault. New geochemical analyses and Hf^Pb^Sr^Nd isotopic compositions of 20 basaltic rocks from Amsterdam and St. Paul Islands constrain the nature and origin of the sources involved in the genesis of the ASP hotspot basalts. Aphyric basalts from St. Paul are mildly alkalic, incompatible element-enriched and highly fractionated; they are distinct from the tholeiitic basalts from Amsterdam, from the recently discovered Boomerang active seamount on the ASP Plateau, and from the Kerguelen Archipelago basalts on the Antarctic Plate. The St. Paul and Amsterdam basalts have very limited isotopic variations with distinct 206 Pb/ 204 Pb, 207 Pb/ 204 Pb, 208 Pb/ 204 Pb, and 176 Hf/ 177 Hf isotopic compositions (19.08 þ 0.07, 15.61 þ 0.02, 39.45 þ 0.12, 0.28313 þ 0.00003 for Amsterdam, and 18.70 þ 0.08, 15.56 þ 0.01, 38.87 þ 0.05, 0.28306 þ 0.00002 for St. Paul, respectively) that are not compatible with any direct contribution of the enriched Kerguelen plume end-member. Pb^Nd^Sr isotopic compositions of the St.","publication_date":{"day":null,"month":null,"year":2004,"errors":{}},"publication_name":"Earth and Planetary Science Letters","grobid_abstract_attachment_id":52420479},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186865/Geochemical_and_Hf_Pb_Sr_Nd_isotopic_constraints_on_the_origin_of_the_Amsterdam_St_Paul_Indian_Ocean_hotspot_basalts","translated_internal_url":"","created_at":"2017-04-01T10:05:23.705-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304416,"work_id":32186865,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Geochemical and Hf–Pb–Sr–Nd isotopic constraints on the origin of the Amsterdam–St. Paul (Indian Ocean) hotspot 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class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="6767201" id="hawaii"><div class="js-work-strip profile--work_container" data-work-id="32187063"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187063/Submarine_radial_vents_on_Mauna_Loa_Volcano_Hawaii"><img alt="Research paper thumbnail of Submarine radial vents on Mauna Loa Volcano, Hawai'i" class="work-thumbnail" src="https://attachments.academia-assets.com/52420589/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187063/Submarine_radial_vents_on_Mauna_Loa_Volcano_Hawaii">Submarine radial vents on Mauna Loa Volcano, Hawai'i</a></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2006</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="adb10aa95b0504ff592fe68eb808cf34" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420589,"asset_id":32187063,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420589/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187063"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span 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WowProfile.WorkStripView({ el: this, workJSON: {"id":32187063,"title":"Submarine radial vents on Mauna Loa Volcano, Hawai'i","translated_title":"","metadata":{"grobid_abstract":"1] A 2002 multibeam sonar survey of Mauna Loa's western flank revealed ten submarine radial vents and three submarine lava flows. Only one submarine radial vent was known previously. The ages of these vents are constrained by eyewitness accounts, geologic relationships, Mn-Fe coatings, and geochemical stratigraphy; they range from 128 years B.P. to possibly 47 ka. Eight of the radial vents produced degassed lavas despite eruption in water depths sufficient to inhibit sulfur degassing. These vents formed truncated cones and short lava flows. Two vents produced undegassed lavas that created ''irregular'' cones and longer lava flows. Compositionally and isotopically, the submarine radial vent lavas are typical of Mauna Loa lavas, except two cones that erupted alkalic lavas. He-Sr isotopes for the radial vent lavas follow Mauna Loa's evolutionary trend. The compositional and isotopic heterogeneity of these lavas indicates most had distinct parental magmas. Bathymetry and acoustic backscatter results, along with photography and sampling during four JASON2 dives, are used to produce a detailed geologic map to evaluate Mauna Loa's submarine geologic history. The new map shows that the 1877 submarine eruption was much larger than previously thought, resulting in a 10% increase for recent volcanism. Furthermore, although alkalic lavas were found at two radial vents, there is no systematic increase in alkalinity among these or other Mauna Loa lavas as expected for a dying volcano. These results refute an interpretation that Mauna Loa's volcanism is waning. The submarine radial vents and flows cover 29 km 2 of seafloor and comprise a total volume of $2 Â 10 9 m 3 of lava, reinforcing the idea that submarine lava eruptions are important in the growth of oceanic island volcanoes even after they emerged above sea level.","publication_date":{"day":null,"month":null,"year":2006,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420589},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187063/Submarine_radial_vents_on_Mauna_Loa_Volcano_Hawaii","translated_internal_url":"","created_at":"2017-04-01T10:07:17.094-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304741,"work_id":32187063,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176503,"email":"j***s@tamu.edu","display_order":0,"name":"James Rhodes","title":"Submarine radial vents on Mauna Loa Volcano, Hawai'i"},{"id":28304756,"work_id":32187063,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176508,"email":"m***z@nsf.gov","display_order":4194304,"name":"Mark Kurz","title":"Submarine radial vents on Mauna Loa Volcano, Hawai'i"},{"id":28304804,"work_id":32187063,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":6291456,"name":"Michael Garcia","title":"Submarine radial vents on Mauna Loa Volcano, Hawai'i"}],"downloadable_attachments":[{"id":52420589,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420589/thumbnails/1.jpg","file_name":"Submarine_radial_vents_on_Mauna_Loa_Volc20170401-6068-12pgw81.pdf","download_url":"https://www.academia.edu/attachments/52420589/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Submarine_radial_vents_on_Mauna_Loa_Volc.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420589/Submarine_radial_vents_on_Mauna_Loa_Volc20170401-6068-12pgw81-libre.pdf?1491067247=\u0026response-content-disposition=attachment%3B+filename%3DSubmarine_radial_vents_on_Mauna_Loa_Volc.pdf\u0026Expires=1733034951\u0026Signature=f60QCXaw-qdxv6FNHAt1uQqOZGlWOaKlpSsASp3xYuPkVVDg7kUKik6Fzsu7~PfowWMV0aaIgVId-uHMgzjb7f~OKtsYzpG-3qNXgMnyDwcTWRJBmHbJYaVVodGZgGIc2YWFhlCHoPE6AbjEZA-~CLLVW1BQLBtesPLFD8VEkyfnAk9L~HNKulbCQWdRqZXFb4vyVVa3zAarcLiVWWLo2QwqwederuKHBY9LPEh1UgVGlOPibYUUa83S2X2iAajmrQvrMAlXgfi61cD6o5Rh5PSqOlXZySQYqCrqWMsQIxIGLx~m4LINHd~yjehiAO~nMyY8TH62JhTa-~lBXFfmdQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Submarine_radial_vents_on_Mauna_Loa_Volcano_Hawaii","translated_slug":"","page_count":28,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420589,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420589/thumbnails/1.jpg","file_name":"Submarine_radial_vents_on_Mauna_Loa_Volc20170401-6068-12pgw81.pdf","download_url":"https://www.academia.edu/attachments/52420589/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Submarine_radial_vents_on_Mauna_Loa_Volc.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420589/Submarine_radial_vents_on_Mauna_Loa_Volc20170401-6068-12pgw81-libre.pdf?1491067247=\u0026response-content-disposition=attachment%3B+filename%3DSubmarine_radial_vents_on_Mauna_Loa_Volc.pdf\u0026Expires=1733034951\u0026Signature=f60QCXaw-qdxv6FNHAt1uQqOZGlWOaKlpSsASp3xYuPkVVDg7kUKik6Fzsu7~PfowWMV0aaIgVId-uHMgzjb7f~OKtsYzpG-3qNXgMnyDwcTWRJBmHbJYaVVodGZgGIc2YWFhlCHoPE6AbjEZA-~CLLVW1BQLBtesPLFD8VEkyfnAk9L~HNKulbCQWdRqZXFb4vyVVa3zAarcLiVWWLo2QwqwederuKHBY9LPEh1UgVGlOPibYUUa83S2X2iAajmrQvrMAlXgfi61cD6o5Rh5PSqOlXZySQYqCrqWMsQIxIGLx~m4LINHd~yjehiAO~nMyY8TH62JhTa-~lBXFfmdQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"},{"id":424229,"name":"Sr isotopes","url":"https://www.academia.edu/Documents/in/Sr_isotopes"},{"id":604905,"name":"Oceanic Islands","url":"https://www.academia.edu/Documents/in/Oceanic_Islands"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":1242196,"name":"Water Depth","url":"https://www.academia.edu/Documents/in/Water_Depth"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187064"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187064/Major_element_variations_in_Hawaiian_shield_lavas_Source_features_and_perspectives_from_global_ocean_island_basalt_OIB_systematics"><img alt="Research paper thumbnail of Major element variations in Hawaiian shield lavas: Source features and perspectives from global ocean island basalt (OIB) systematics" class="work-thumbnail" src="https://attachments.academia-assets.com/52420594/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187064/Major_element_variations_in_Hawaiian_shield_lavas_Source_features_and_perspectives_from_global_ocean_island_basalt_OIB_systematics">Major element variations in Hawaiian shield lavas: Source features and perspectives from global ocean island basalt (OIB) systematics</a></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2012</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="3585ce037eb0e7c1f57530413a363ec1" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420594,"asset_id":32187064,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420594/download_file?st=MTczMzA5NDM3Niw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187064"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187064"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187064; 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In order to place constraints on the source lithologies of Hawaiian lavas, we explore relationships between major elements and radiogenic isotopes in tholeiitic, shield-building lavas. Olivine-fractionation corrected lava compositions reveal clear trends between radiogenic isotopes and major elements. Individual data points exhibit remarkable trends and there is no need to average the data by volcano. Data form arrays that are anchored by Koolau lava at one end (with high 87 Sr/ 86 Sr, 187 Os/ O concentrations do not correlate with radiogenic isotopes. The Hawaiian data set exhibits correlations that mirror the best correlations between major elements and radiogenic isotope in the global ocean island basalt (OIB) database. We suggest that the mechanism driving the correlations in Hawaii illustrates, in microcosm, a larger global process that generates major element variability in mantle plumes. Like the global arrays, the Hawaiian lavas with radiogenic Pb and SiO 2 -poor lavas are sourced by a SiO 2 -poor mafic component (pyroxenite) admixed with peridotite, while Hawaiian lavas with unradiogenic Pb and high SiO 2 are sourced by a SiO 2 -rich mafic component (eclogite). The variable SiO 2 in the mafic component may result from different degrees of SiO 2 -extraction from the slab during subduction. (2012), Major element variations in Hawaiian shield lavas: Source features and perspectives from global ocean island basalt (OIB) systematics, Geochem. Geophys. 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186928]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186928,"title":"Geochemical, geological and geophysical inferences for the origin of the South Kauai Swell","translated_title":"","metadata":{},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186928/Geochemical_geological_and_geophysical_inferences_for_the_origin_of_the_South_Kauai_Swell","translated_internal_url":"","created_at":"2017-04-01T10:05:32.035-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304534,"work_id":32186928,"tagging_user_id":62411756,"tagged_user_id":62424174,"co_author_invite_id":6176445,"email":"l***d@leapfrog3d.com","display_order":0,"name":"Lisa Swinnard","title":"Geochemical, geological and geophysical inferences for the origin of the South Kauai Swell"},{"id":28304544,"work_id":32186928,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176446,"email":"r***f@soest.hawaii.edu","display_order":4194304,"name":"Todd Bianco","title":"Geochemical, geological and geophysical inferences for the origin of the South Kauai Swell"},{"id":28304546,"work_id":32186928,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176447,"email":"a***s@my.uri.edu","display_order":6291456,"name":"Ashton Flinders","title":"Geochemical, geological and geophysical inferences for the origin of the South Kauai Swell"},{"id":28304799,"work_id":32186928,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":7340032,"name":"Michael Garcia","title":"Geochemical, geological and geophysical inferences for the origin of the South Kauai Swell"}],"downloadable_attachments":[],"slug":"Geochemical_geological_and_geophysical_inferences_for_the_origin_of_the_South_Kauai_Swell","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186927"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186927/Age_geochemistry_and_melt_flux_variations_for_the_Hawaiian_Ridge"><img alt="Research paper thumbnail of Age, geochemistry and melt flux variations for the Hawaiian Ridge" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186927/Age_geochemistry_and_melt_flux_variations_for_the_Hawaiian_Ridge">Age, geochemistry and melt flux variations for the Hawaiian Ridge</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/JonathanTree">Jonathan Tree</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT The Hawaiian Ridge portion of the Hawaiian-Emperor Chain, the classic example of a mantl...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT The Hawaiian Ridge portion of the Hawaiian-Emperor Chain, the classic example of a mantle plume produced linear island chain, is 6000 km in length, active for 80 Myr, and tectonically simple. Despite its importance to our understanding of mantle plumes and Cenozoic plate motion, there are large data gaps for the age and geochemistry of lavas from volcanoes along the Hawaiian Ridge (HR) portion of the Chain. Ages: Only volcanoes near the Hawaiian-Emperor bend and in the Hawaiian Islands have modern Ar-Ar ages, leaving a gap of 2000 km where existing K-Ar ages suggest synchronous volcanism over a 1000 km section. Geochemistry: There is a 2900 km gap in high precision geochemical data for the HR. The Emperor Seamounts (&amp;gt;45 Ma) have better regional coverage of recent isotopic data and show a correlation of Sr isotope composition with age of the underlying oceanic lithosphere (Regelous et al. 2003). The HR has an unexplained, exponential increase in magma flux over the last 30 Myr (Vidal &amp;amp; Bonneville 2004). Potential explanations for the increase in magma flux include: changes in melting conditions (temperature and/or pressure), change in source fertility related to rock type (pyroxenite vs. peridotite) or previous melting history, and/or changes in plate stresses resulting from reconfigurations of plate motion. Our new multi-disciplinary project will: 1) Determine 40Ar/39Ar ages, and whole-rock major, trace element, and Pb, Sr, Nd and Hf isotopic geochemistry for lavas from 20 volcanoes spanning ~2150 km of the HR (NW of the Hawaiian Islands). 2) Use the geochemical data to determine the long-term evolution of the Hawaiian mantle plume source components and to evaluate whether there have been systematic variations in mantle potential temperature, melting pressure, and/or source lithology during the creation of the HR. If so, are they responsible for the 300% variation in melt production along the Ridge? Also, we will assess when the more fertile Loa source component appeared. 3) Reassess models for the origin of the HR using the new 40Ar/39Ar ages. 4) Recompute and compare the magma flux rate for the Hawaiian and Louisville Ridges using our new HR ages and IODP results for Louisville Ridge, and updated bathymetric data for both chains. 5) Utilize the new ages to revise Cenozoic Pacific plate motions and to compute differential motions as proxies for stress changes along the HR with time to evaluate the effects of plate motion on magma flux rate. These studies will have fundamental implications for mantle plume sources, plume dynamics, and plate kinematics. Vidal V, Bonneville A, 2004. J. Geophys. Res., 109, B03104, doi:10.1029/2003JB002559 Regelous M, Hofmann AW, Abouchami W, Galer SJG, 2003. Jour. Petrol. 44, 113-140</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186927"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186927"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186927; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186927]").text(description); $(".js-view-count[data-work-id=32186927]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186927; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186927']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186927, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186927]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186927,"title":"Age, geochemistry and melt flux variations for the Hawaiian Ridge","translated_title":"","metadata":{"abstract":"ABSTRACT The Hawaiian Ridge portion of the Hawaiian-Emperor Chain, the classic example of a mantle plume produced linear island chain, is 6000 km in length, active for 80 Myr, and tectonically simple. Despite its importance to our understanding of mantle plumes and Cenozoic plate motion, there are large data gaps for the age and geochemistry of lavas from volcanoes along the Hawaiian Ridge (HR) portion of the Chain. Ages: Only volcanoes near the Hawaiian-Emperor bend and in the Hawaiian Islands have modern Ar-Ar ages, leaving a gap of 2000 km where existing K-Ar ages suggest synchronous volcanism over a 1000 km section. Geochemistry: There is a 2900 km gap in high precision geochemical data for the HR. The Emperor Seamounts (\u0026amp;gt;45 Ma) have better regional coverage of recent isotopic data and show a correlation of Sr isotope composition with age of the underlying oceanic lithosphere (Regelous et al. 2003). The HR has an unexplained, exponential increase in magma flux over the last 30 Myr (Vidal \u0026amp;amp; Bonneville 2004). Potential explanations for the increase in magma flux include: changes in melting conditions (temperature and/or pressure), change in source fertility related to rock type (pyroxenite vs. peridotite) or previous melting history, and/or changes in plate stresses resulting from reconfigurations of plate motion. Our new multi-disciplinary project will: 1) Determine 40Ar/39Ar ages, and whole-rock major, trace element, and Pb, Sr, Nd and Hf isotopic geochemistry for lavas from 20 volcanoes spanning ~2150 km of the HR (NW of the Hawaiian Islands). 2) Use the geochemical data to determine the long-term evolution of the Hawaiian mantle plume source components and to evaluate whether there have been systematic variations in mantle potential temperature, melting pressure, and/or source lithology during the creation of the HR. If so, are they responsible for the 300% variation in melt production along the Ridge? Also, we will assess when the more fertile Loa source component appeared. 3) Reassess models for the origin of the HR using the new 40Ar/39Ar ages. 4) Recompute and compare the magma flux rate for the Hawaiian and Louisville Ridges using our new HR ages and IODP results for Louisville Ridge, and updated bathymetric data for both chains. 5) Utilize the new ages to revise Cenozoic Pacific plate motions and to compute differential motions as proxies for stress changes along the HR with time to evaluate the effects of plate motion on magma flux rate. These studies will have fundamental implications for mantle plume sources, plume dynamics, and plate kinematics. Vidal V, Bonneville A, 2004. J. Geophys. Res., 109, B03104, doi:10.1029/2003JB002559 Regelous M, Hofmann AW, Abouchami W, Galer SJG, 2003. Jour. Petrol. 44, 113-140"},"translated_abstract":"ABSTRACT The Hawaiian Ridge portion of the Hawaiian-Emperor Chain, the classic example of a mantle plume produced linear island chain, is 6000 km in length, active for 80 Myr, and tectonically simple. Despite its importance to our understanding of mantle plumes and Cenozoic plate motion, there are large data gaps for the age and geochemistry of lavas from volcanoes along the Hawaiian Ridge (HR) portion of the Chain. Ages: Only volcanoes near the Hawaiian-Emperor bend and in the Hawaiian Islands have modern Ar-Ar ages, leaving a gap of 2000 km where existing K-Ar ages suggest synchronous volcanism over a 1000 km section. Geochemistry: There is a 2900 km gap in high precision geochemical data for the HR. The Emperor Seamounts (\u0026amp;gt;45 Ma) have better regional coverage of recent isotopic data and show a correlation of Sr isotope composition with age of the underlying oceanic lithosphere (Regelous et al. 2003). The HR has an unexplained, exponential increase in magma flux over the last 30 Myr (Vidal \u0026amp;amp; Bonneville 2004). Potential explanations for the increase in magma flux include: changes in melting conditions (temperature and/or pressure), change in source fertility related to rock type (pyroxenite vs. peridotite) or previous melting history, and/or changes in plate stresses resulting from reconfigurations of plate motion. Our new multi-disciplinary project will: 1) Determine 40Ar/39Ar ages, and whole-rock major, trace element, and Pb, Sr, Nd and Hf isotopic geochemistry for lavas from 20 volcanoes spanning ~2150 km of the HR (NW of the Hawaiian Islands). 2) Use the geochemical data to determine the long-term evolution of the Hawaiian mantle plume source components and to evaluate whether there have been systematic variations in mantle potential temperature, melting pressure, and/or source lithology during the creation of the HR. If so, are they responsible for the 300% variation in melt production along the Ridge? Also, we will assess when the more fertile Loa source component appeared. 3) Reassess models for the origin of the HR using the new 40Ar/39Ar ages. 4) Recompute and compare the magma flux rate for the Hawaiian and Louisville Ridges using our new HR ages and IODP results for Louisville Ridge, and updated bathymetric data for both chains. 5) Utilize the new ages to revise Cenozoic Pacific plate motions and to compute differential motions as proxies for stress changes along the HR with time to evaluate the effects of plate motion on magma flux rate. These studies will have fundamental implications for mantle plume sources, plume dynamics, and plate kinematics. Vidal V, Bonneville A, 2004. J. Geophys. Res., 109, B03104, doi:10.1029/2003JB002559 Regelous M, Hofmann AW, Abouchami W, Galer SJG, 2003. Jour. 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Wessel","title":"Age, geochemistry and melt flux variations for the Hawaiian Ridge"},{"id":28304810,"work_id":32186927,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":6291456,"name":"Michael Garcia","title":"Age, geochemistry and melt flux variations for the Hawaiian Ridge"}],"downloadable_attachments":[],"slug":"Age_geochemistry_and_melt_flux_variations_for_the_Hawaiian_Ridge","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186920"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186920/Petrology_and_Geochronology_of_Kaula_Volcano_lavas_An_off_axis_window_into_the_Hawaiian_Mantle_Plume"><img alt="Research paper thumbnail of Petrology and Geochronology of Kaula Volcano lavas: An off-axis window into the Hawaiian Mantle Plume" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186920/Petrology_and_Geochronology_of_Kaula_Volcano_lavas_An_off_axis_window_into_the_Hawaiian_Mantle_Plume">Petrology and Geochronology of Kaula Volcano lavas: An off-axis window into the Hawaiian Mantle Plume</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/JonathanTree">Jonathan Tree</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Hawaiian Islands extend NW for 625 km from Lō‘ihi to Ka‘ula island. One anomalous feature cro...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Hawaiian Islands extend NW for 625 km from Lō‘ihi to Ka‘ula island. One anomalous feature cross-cutting the Hawaiian Islands is the Kaua‘i Ridge, a 165 km-long bathymetric high with three well-defined gravity highs. These gravity highs are centered under or near the islands of Ka‘ula, Ni‘ihau and Kaua‘i, and represent the cores of three shield volcanoes whose volumes decrease dramatically with distance from the axis of the Hawaiian Chain (Kaua‘i, 58 x 103 km3, Ni‘ihau x 103 km, Ka‘ula 10 x 103 km; Robinson and Eakins 2006). Ka‘ula Volcano, on the SW end of the Kaua‘i Ridge, is centered 100 km off the axis of the Hawaiian mantle plume. The volcano is capped by a small island, which is a remnant of a nephelinitic tuff cone. The cone contains abundant accidental bombs of lava (tholeiite, phonolite and basanite), peridotite and pyroxenite, and unexploded ordnance from US military bombing. Two JASON dives on the flanks of Ka‘ula recovered only alkalic lavas. Three stage of Ka‘ula vol...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186920"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186920"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186920; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186920]").text(description); $(".js-view-count[data-work-id=32186920]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186920; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186920']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186920, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186920]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186920,"title":"Petrology and Geochronology of Kaula Volcano lavas: An off-axis window into the Hawaiian Mantle Plume","translated_title":"","metadata":{"abstract":"The Hawaiian Islands extend NW for 625 km from Lō‘ihi to Ka‘ula island. 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Three stage of Ka‘ula vol..."},"translated_abstract":"The Hawaiian Islands extend NW for 625 km from Lō‘ihi to Ka‘ula island. One anomalous feature cross-cutting the Hawaiian Islands is the Kaua‘i Ridge, a 165 km-long bathymetric high with three well-defined gravity highs. These gravity highs are centered under or near the islands of Ka‘ula, Ni‘ihau and Kaua‘i, and represent the cores of three shield volcanoes whose volumes decrease dramatically with distance from the axis of the Hawaiian Chain (Kaua‘i, 58 x 103 km3, Ni‘ihau x 103 km, Ka‘ula 10 x 103 km; Robinson and Eakins 2006). Ka‘ula Volcano, on the SW end of the Kaua‘i Ridge, is centered 100 km off the axis of the Hawaiian mantle plume. The volcano is capped by a small island, which is a remnant of a nephelinitic tuff cone. The cone contains abundant accidental bombs of lava (tholeiite, phonolite and basanite), peridotite and pyroxenite, and unexploded ordnance from US military bombing. Two JASON dives on the flanks of Ka‘ula recovered only alkalic lavas. Three stage of Ka‘ula vol...","internal_url":"https://www.academia.edu/32186920/Petrology_and_Geochronology_of_Kaula_Volcano_lavas_An_off_axis_window_into_the_Hawaiian_Mantle_Plume","translated_internal_url":"","created_at":"2017-04-01T10:05:30.989-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304583,"work_id":32186920,"tagging_user_id":62411756,"tagged_user_id":62421480,"co_author_invite_id":6176456,"email":"j***e@hawaii.edu","display_order":0,"name":"Jonathan Tree","title":"Petrology and Geochronology of Kaula Volcano lavas: An off-axis window into the Hawaiian Mantle Plume"},{"id":28304815,"work_id":32186920,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":4194304,"name":"Michael Garcia","title":"Petrology and Geochronology of Kaula Volcano lavas: An off-axis window into the Hawaiian Mantle Plume"}],"downloadable_attachments":[],"slug":"Petrology_and_Geochronology_of_Kaula_Volcano_lavas_An_off_axis_window_into_the_Hawaiian_Mantle_Plume","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186919"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186919/A_Geochemical_Study_of_Magmatic_Processes_and_Evolution_along_the_Submarine_Southwest_Rift_zone_of_Mauna_Loa_Volcano_Hawaii"><img alt="Research paper thumbnail of A Geochemical Study of Magmatic Processes and Evolution along the Submarine Southwest Rift zone of Mauna Loa Volcano, Hawaii" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186919/A_Geochemical_Study_of_Magmatic_Processes_and_Evolution_along_the_Submarine_Southwest_Rift_zone_of_Mauna_Loa_Volcano_Hawaii">A Geochemical Study of Magmatic Processes and Evolution along the Submarine Southwest Rift zone of Mauna Loa Volcano, Hawaii</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://umass.academia.edu/MichaelVollinger">Michael Vollinger</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Mauna Loa&#39;s southwest rift zone (SWR) extends for 102 km from its summit caldera, at an eleva...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Mauna Loa&#39;s southwest rift zone (SWR) extends for 102 km from its summit caldera, at an elevation of 4,170 m above sea level, to submarine depths of over 4,500 m. About 65% of the rift zone is subaerial and 35% submarine. Recent sampling with the Jason II submersible of the `mile-high&#39; (1800 m) Ka Lae submarine landslide scarp and the</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186919"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186919"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186919; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186919]").text(description); $(".js-view-count[data-work-id=32186919]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186919; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186919']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186919, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186919]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186919,"title":"A Geochemical Study of Magmatic Processes and Evolution along the Submarine Southwest Rift zone of Mauna Loa Volcano, Hawaii","translated_title":"","metadata":{"abstract":"Mauna Loa\u0026#39;s southwest rift zone (SWR) extends for 102 km from its summit caldera, at an elevation of 4,170 m above sea level, to submarine depths of over 4,500 m. About 65% of the rift zone is subaerial and 35% submarine. Recent sampling with the Jason II submersible of the `mile-high\u0026#39; (1800 m) Ka Lae submarine landslide scarp and the","publication_date":{"day":null,"month":null,"year":2003,"errors":{}}},"translated_abstract":"Mauna Loa\u0026#39;s southwest rift zone (SWR) extends for 102 km from its summit caldera, at an elevation of 4,170 m above sea level, to submarine depths of over 4,500 m. About 65% of the rift zone is subaerial and 35% submarine. 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These radial vents are located on its northern and western flanks and account for approximately 10% of historic eruptions outside the summit region. Thirty-three subaerial and one submarine vent (active in 1877) were known prior to our work. During a recent Jason2</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186918"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186918"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186918; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186918]").text(description); $(".js-view-count[data-work-id=32186918]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186918; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186918']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186918, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186918]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186918,"title":"Numerous Submarine Radial Vents Revealed on Mauna Loa Volcano","translated_title":"","metadata":{"abstract":"Among Hawaiian shield volcanoes, Mauna Loa is distinct in having vents outside of its summit and rift zones. 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Petrology, Geochemistry and Geochronology of Kaua'i Lavas over 4{middle dot}5 Myr: Implications for the Origin of Rejuvenated Volcanism and the Evolution of the Hawaiian Plume" class="work-thumbnail" src="https://attachments.academia-assets.com/52420528/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186899/Petrology_Geochemistry_and_Geochronology_of_Kauai_Lavas_over_4_middle_dot_5_Myr_Implications_for_the_Origin_of_Rejuvenated_Volcanism_and_the_Evolution_of_the_Hawaiian_Plume">Petrology, Geochemistry and Geochronology of Kaua'i Lavas over 4{middle dot}5 Myr: Implications for the Origin of Rejuvenated Volcanism and the Evolution of the Hawaiian Plume</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/LisaSwinnard">Lisa Swinnard</a></span></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, 2010</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="1027e35fb4078a107b6172c72bbb60e7" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420528,"asset_id":32186899,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420528/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span 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New field, geochronological, petrological and geochemical results for a large suite of shield, post-shield and rejuvenated lavas are used to examine models for the origin of rejuvenated volcanism, and to evaluate the composition and structure of the Hawaiian plume. Kaua'i has the most voluminous ($58 km 3 based on new field and water well interpretations) and longest-lived suite of rejuvenated lavas ($2·5 Myr) in Hawai'i. New K^Ar ages and field work reveal an $1 Myr gap (3·6^2·6 Ma) in volcanism between post-shield and rejuvenated volcanism. Isotopic and trace element ratios, and modeling of major elements of Kaua'i' s rejuvenated lavas require low-degree melting (0·02^2·6%) at $1525 AE 108C and 3·5^4·0 GPa of a heterogeneous, peridotitic plume source. High-precision Pb, Sr, Nd and Hf isotopic, and inductively coupled plasma mass spectrometry trace element data show substantial source variations with a dramatic increase in the depleted component in younger lavas. Some shield, post-shield and rejuvenated lavas (4·3^0·7 Ma) have high 208 Pb*/ 206 Pb* (radiogenic Pb produced since the formation of the Earth) values (40·947) indicative of Loa-type compositions, the first reported Loa values in rocks 43 Ma, questioning previous models for the emergence of the Loa component in Hawaiian lavas. The timing, long duration, temporal variation in rock types and voluminous pulse of rejuvenated volcanism (58 km 3 ), and the synchronous eruption of compositionally similar rejuvenated lavas, indicating tapping of common components along 350 km of the Hawaiian chain, are inconsistent with current models for this volcanism. Combining the lithospheric flexure and secondary zone of melting models provides a physical mechanism to initiate and focus the melting at shallower levels within the plume (flexural uplift) with a means to extend the duration of Ko loa volcanism at higher degrees of partial melting.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}},"publication_name":"Journal of Petrology","grobid_abstract_attachment_id":52420528},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186899/Petrology_Geochemistry_and_Geochronology_of_Kauai_Lavas_over_4_middle_dot_5_Myr_Implications_for_the_Origin_of_Rejuvenated_Volcanism_and_the_Evolution_of_the_Hawaiian_Plume","translated_internal_url":"","created_at":"2017-04-01T10:05:28.132-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304535,"work_id":32186899,"tagging_user_id":62411756,"tagged_user_id":62424174,"co_author_invite_id":6176445,"email":"l***d@leapfrog3d.com","display_order":0,"name":"Lisa Swinnard","title":"Petrology, Geochemistry and Geochronology of Kaua'i Lavas over 4{middle dot}5 Myr: Implications for the Origin of Rejuvenated Volcanism and the Evolution of the Hawaiian Plume"},{"id":28304806,"work_id":32186899,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":4194304,"name":"Michael Garcia","title":"Petrology, Geochemistry and Geochronology of Kaua'i Lavas over 4{middle dot}5 Myr: Implications for the Origin of Rejuvenated Volcanism and the Evolution of the Hawaiian Plume"}],"downloadable_attachments":[{"id":52420528,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420528/thumbnails/1.jpg","file_name":"Petrology_Geochemistry_and_Geochronology20170401-6068-1l89v1q.pdf","download_url":"https://www.academia.edu/attachments/52420528/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Petrology_Geochemistry_and_Geochronology.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420528/Petrology_Geochemistry_and_Geochronology20170401-6068-1l89v1q-libre.pdf?1491067486=\u0026response-content-disposition=attachment%3B+filename%3DPetrology_Geochemistry_and_Geochronology.pdf\u0026Expires=1733034952\u0026Signature=X9lWuG6rJCSvEZlcYaPW5Dw3p4avsxz4IT-r5UQ77AZdJNp1bWMe7g572gQ42dEcMdwhIsNT5b1VpJCtPNpaKNh5TNqz2REDynR1X8HFzVeycXh2cS0VQGkk8Jo2sofbKtZZMkO~LG3reYf6N2z491BiQT2COzRHyC029SNmrGB02kC5sfvIddjVtsne2GIqa1ejbkIOmjlgnHqErxzr0hOSXNsy5UhK8f9KqlhOFpcqXV0aLWJWVR8gMwZkemUQl-pePmqhbqQMwv7JlRxKp85aYLRodzLSk2bu8S292d6UFia6gaJqQQLu5VE~1ORmVsiPhD1MCJh37o~CKXHncA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Petrology_Geochemistry_and_Geochronology_of_Kauai_Lavas_over_4_middle_dot_5_Myr_Implications_for_the_Origin_of_Rejuvenated_Volcanism_and_the_Evolution_of_the_Hawaiian_Plume","translated_slug":"","page_count":48,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420528,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420528/thumbnails/1.jpg","file_name":"Petrology_Geochemistry_and_Geochronology20170401-6068-1l89v1q.pdf","download_url":"https://www.academia.edu/attachments/52420528/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Petrology_Geochemistry_and_Geochronology.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420528/Petrology_Geochemistry_and_Geochronology20170401-6068-1l89v1q-libre.pdf?1491067486=\u0026response-content-disposition=attachment%3B+filename%3DPetrology_Geochemistry_and_Geochronology.pdf\u0026Expires=1733034952\u0026Signature=X9lWuG6rJCSvEZlcYaPW5Dw3p4avsxz4IT-r5UQ77AZdJNp1bWMe7g572gQ42dEcMdwhIsNT5b1VpJCtPNpaKNh5TNqz2REDynR1X8HFzVeycXh2cS0VQGkk8Jo2sofbKtZZMkO~LG3reYf6N2z491BiQT2COzRHyC029SNmrGB02kC5sfvIddjVtsne2GIqa1ejbkIOmjlgnHqErxzr0hOSXNsy5UhK8f9KqlhOFpcqXV0aLWJWVR8gMwZkemUQl-pePmqhbqQMwv7JlRxKp85aYLRodzLSk2bu8S292d6UFia6gaJqQQLu5VE~1ORmVsiPhD1MCJh37o~CKXHncA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186885"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186885/Hawaiian_hot_spot_dynamics_as_inferred_from_the_Hf_and_Pb_isotope_evolution_of_Mauna_Kea_volcano"><img alt="Research paper thumbnail of Hawaiian hot spot dynamics as inferred from the Hf and Pb isotope evolution of Mauna Kea volcano" class="work-thumbnail" src="https://attachments.academia-assets.com/52420505/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186885/Hawaiian_hot_spot_dynamics_as_inferred_from_the_Hf_and_Pb_isotope_evolution_of_Mauna_Kea_volcano">Hawaiian hot spot dynamics as inferred from the Hf and Pb isotope evolution of Mauna Kea volcano</a></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2003</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="426a717e13285627339f55984e971be9" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420505,"asset_id":32186885,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420505/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186885"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186885"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186885; 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class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186884/A_low_relief_shield_volcano_origin_for_the_South_Kaua_i_Swell">A low-relief shield volcano origin for the South Kaua‘i Swell</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/LisaSwinnard">Lisa Swinnard</a></span></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2013</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="8bbc1b831c23755f0241f865086331f8" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" 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waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "8bbc1b831c23755f0241f865086331f8" } } $('.js-work-strip[data-work-id=32186884]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186884,"title":"A low-relief shield volcano origin for the South Kaua‘i Swell","translated_title":"","metadata":{"grobid_abstract":"1] The South Kaua'i Swell (SKS) is a 110 km x 80 km ovoid bathymetric feature that stands \u003e2 km high and abuts the southern flank of the island of Kaua'i. The origin of the SKS was investigated using multibeam bathymetry and acoustic backscatter, gravity data, radiometric ages, and geochemistry of rock samples. Most of the SKS rock samples are tholeiitic in composition with ages of 3.9-5.4 Ma indicating they were derived from shield volcanism. The ages and compositions of the SKS rocks partially overlap with those of the nearby Ni'ihau, Kaua'i and West Ka'ena volcano complexes. The SKS was originally described as a landslide; however, this interpretation is problematic given the ovoid shape of SKS, its relatively smooth, flat-to-convex surface, and the lack of an obvious source region that could accommodate what would be one of Earth's most voluminous (6 x 10 3 km 3 ) landslides. The morphology, size, and the surrounding gravity anomaly are more consistent with the SKS being a low-relief shield volcano, which was partially covered with a small volume of landside debris from south Kaua'i and later with some secondary volcanic seamounts. A shield origin would imply that Hawaiian and possibly other hotspot shield volcanoes can take on a wider variety of forms than is commonly thought, ranging from tall island-building shields, to smaller edifices such as Ka'ena Ridge and Mahukona, to even lower-relief volcanoes represented by the SKS and possibly the South West O'ahu Volcanic Field.","publication_date":{"day":null,"month":null,"year":2013,"errors":{}},"publication_name":"Geochemistry, Geophysics, 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Swell"},{"id":28304813,"work_id":32186884,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":6291456,"name":"Michael Garcia","title":"A low-relief shield volcano origin for the South Kaua‘i Swell"},{"id":28305055,"work_id":32186884,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":1435011,"email":"b***a@geology.wisc.edu","display_order":7340032,"name":"Brian Jicha","title":"A low-relief shield volcano origin for the South Kaua‘i Swell"},{"id":28305056,"work_id":32186884,"tagging_user_id":62411756,"tagged_user_id":42774443,"co_author_invite_id":null,"email":"b***e@gmail.com","display_order":7864320,"name":"Brian Taylor","title":"A low-relief shield volcano origin for the South Kaua‘i Swell"},{"id":28305057,"work_id":32186884,"tagging_user_id":62411756,"tagged_user_id":39703952,"co_author_invite_id":null,"email":"t***k@aloha.net","display_order":8126464,"name":"Charles Blay","title":"A low-relief shield volcano origin for the South Kaua‘i Swell"},{"id":28305058,"work_id":32186884,"tagging_user_id":62411756,"tagged_user_id":459154,"co_author_invite_id":null,"email":"j***h@learningalliances.net","display_order":8257536,"name":"John Smith","title":"A low-relief shield volcano origin for the South Kaua‘i Swell"},{"id":28305095,"work_id":32186884,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":2068964,"email":"g***o@soest.hawaii.edu","display_order":8323072,"name":"Garrett Ito","title":"A low-relief shield volcano origin for the South Kaua‘i Swell"},{"id":28305127,"work_id":32186884,"tagging_user_id":62411756,"tagged_user_id":33010082,"co_author_invite_id":null,"email":"m***a@hawaii.edu","display_order":8355840,"name":"m g","title":"A low-relief shield volcano origin for the South Kaua‘i Swell"}],"downloadable_attachments":[{"id":52420519,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420519/thumbnails/1.jpg","file_name":"A_low-relief_shield_volcano_origin_for_t20170401-6059-dbve0p.pdf","download_url":"https://www.academia.edu/attachments/52420519/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"A_low_relief_shield_volcano_origin_for_t.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420519/A_low-relief_shield_volcano_origin_for_t20170401-6059-dbve0p-libre.pdf?1491067292=\u0026response-content-disposition=attachment%3B+filename%3DA_low_relief_shield_volcano_origin_for_t.pdf\u0026Expires=1733034952\u0026Signature=MNbEhi4qtgfhs2z1QERAgtCSpPHgpnOqYfCndk6Vh3vssypOLozOeZ-emaogJtcl9WIPtcY4bX87-gbMX~~yYkVpl~oJYTg3--4oTjE0j4k~5oCfsnkiPfjO24jrlakbRh5n7ygJRz7Xsq9-ikLjO5JE4x7ckBYuNtnHcYa7w-5xx1vyn4xiZZtkodilFsVaaAWykV8QU1oNh~yTqlue~Gw7Y2lInIVpGtxip2mNBYhEmBthQZPbKijfkgPVsItO1Go-49ufNd6H-mgZtifmjR8mEZ87jCDy-AQzDLCK96HqeAJbBxBcHQY4EeX51Jz6-DxYrqVTqqKStN1QlCaXRw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"A_low_relief_shield_volcano_origin_for_the_South_Kaua_i_Swell","translated_slug":"","page_count":21,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique 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Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186874"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186874/Horizontal_and_vertical_zoning_of_heterogeneities_in_the_Hawaiian_mantle_plume_from_the_geochemistry_of_consecutive_postshield_volcano_pairs_Kohala_Mahukona_and_Mauna_Kea_Hualalai"><img alt="Research paper thumbnail of Horizontal and vertical zoning of heterogeneities in the Hawaiian mantle plume from the geochemistry of consecutive postshield volcano pairs: Kohala-Mahukona and Mauna Kea-Hualalai" class="work-thumbnail" src="https://attachments.academia-assets.com/52420522/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186874/Horizontal_and_vertical_zoning_of_heterogeneities_in_the_Hawaiian_mantle_plume_from_the_geochemistry_of_consecutive_postshield_volcano_pairs_Kohala_Mahukona_and_Mauna_Kea_Hualalai">Horizontal and vertical zoning of heterogeneities in the Hawaiian mantle plume from the geochemistry of consecutive postshield volcano pairs: Kohala-Mahukona and Mauna Kea-Hualalai</a></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2010</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="9fde22c210c196cbe1b8cede074c90ba" class="wp-workCard--action" 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id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "9fde22c210c196cbe1b8cede074c90ba" } } $('.js-work-strip[data-work-id=32186874]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186874,"title":"Horizontal and vertical zoning of heterogeneities in the Hawaiian mantle plume from the geochemistry of consecutive postshield volcano pairs: Kohala-Mahukona and Mauna Kea-Hualalai","translated_title":"","metadata":{"grobid_abstract":"1] Sr-Nd-Pb-Hf isotopic compositions of postshield lavas from two pairs of Hawaiian volcanoes, Mauna Kea and Kohala (Kea trend) and Hualalai and Mahukona (Loa trend), allow for identification of smallscale (tens of kilometers) heterogeneities in the Hawaiian mantle plume and provide constraints on their distribution. The postshield lavas range from transitional/alkalic basalt to trachyte and are enriched in incompatible trace elements (e.g., La N /Yb N = 6.0-16.2). These lavas are characterized by a limited range of Sr-Nd-Hf isotopic compositions ( 87 Sr/ 86 Sr = 0.70343-0.70365, 143 Nd/ 144 Nd = 0.51292-0.51301, and 176 Hf/ 177 Hf = 0.28311-0.28314) and have distinct Pb isotopic compositions ( 206 Pb/ 204 Pb = 17. and 208 Pb/ 204 Pb = 37.68-38.01) that correspond to their respective Kea or Loa side of the Pb-Pb isotopic boundary. Mauna Kea lavas show a systematic shift to less radiogenic Pb isotopic compositions from the shield to postshield stage and they trend to low 87 Sr/ 86 Sr toward, but not as extreme as, compositions characteristic of rejuvenated stage lavas. Hualalai postshield lavas lie distinctly above the Hf-Nd Hawaiian array and have much lower Pb isotopic ratios than shield lavas, including some of the least radiogenic values (e.g., 206 Pb/ 204 Pb = 17.89-18.01) of recent Hawaiian volcanoes. In contrast, comparison of Kohala with the adjacent Mahukona volcano shows that these older postshield lavas become more radiogenic in Pb during the late stages of volcanism. The isotope systematics of the postshield lavas cannot be explained by mixing between Hawaiian plume end-members (e.g., Kea, Koolau, and Loihi) or by assimilation of Pacific lithosphere and are consistent with the presence of ancient recycled lower oceanic crust (±sediments) in their source. More than one depleted component is sampled by the postshield lavas and these components are long-lived features of the Hawaiian plume that are present in both the Kea and Loa source regions. The depleted components in the postshield lavas, particularly as sampled at Hualalai, are different from the much more homogeneous component present in rejuvenated lavas. The geochemistry of the postshield lavas provides evidence for a bilateral symmetry to the plume where the compositional boundary between the Kea and Loa sources is complex and vertical components of heterogeneity are significant.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}},"publication_name":"Geochemistry, Geophysics, 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from Kīlauea's Pu‘u ‘Ō‘ō eruption (1983-2010): Cyclic variations from melting of source heterogeneities</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://umass.academia.edu/MichaelVollinger">Michael Vollinger</a></span></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2013</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="30dfbcc53ad8de4cf5e343bf5e8c4f5c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420487,"asset_id":32186873,"asset_type":"Work","button_location":"profile"}" 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source components of Mauna Kea volcano. We report high-precision Pb-Sr-Nd isotopic compositions of 40 basalts from the last 408 m of the final drilling phase (HSDP2-B and HSDP2-C) and show that these lowermost basalts represent the early shield stage of Mauna Kea's growth history. Two sample groups are distinguished based on their isotopic variability compared to the rest of the core. Over a depth interval of 210 m (3098.2-3308.2 mbsl), the basalts show very restricted isotopic variation and represent sampling of a relatively homogeneous source. Samples from the bottom 192 m record the largest range of 206 Pb/ 204 Pb and 208 Pb/ 204 Pb in the core, reflecting the greater isotopic variability of the earlier stages of volcanism compared to subsequent stages. The heterogeneity of Mauna Kea lavas is explained by mixing variable proportions of four distinct components intrinsic to the Hawaiian mantle plume. One of these components, Kea, is a prevalent and long-lived composition within the Hawaiian plume, whereas the other three components are involved at different stages of the volcano's history and contribute to the short-term isotopic variability of Mauna Kea. The compositional similarity of the Kea component to \"C\" and to the super-chondritic bulk-silicate Earth suggests that Kea may be part of the primitive mantle of a non-chondritic Earth. Other Pacific oceanic island basalts share Kea-like compositions, indicating that the Kea component is a common, widespread composition within the Pacific deep mantle.","publication_date":{"day":null,"month":null,"year":2013,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420483},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186872/Isotopic_systematics_of_the_early_Mauna_Kea_shield_phase_and_insight_into_the_deep_mantle_beneath_the_Pacific_Ocean","translated_internal_url":"","created_at":"2017-04-01T10:05:24.479-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304421,"work_id":32186872,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Isotopic systematics of the early Mauna Kea shield phase and insight into the deep mantle beneath the Pacific Ocean"},{"id":28305086,"work_id":32186872,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176449,"email":"i***e@eos.ubc.ca","display_order":4194304,"name":"Inês Silva","title":"Isotopic systematics of the early Mauna Kea shield phase and insight into the deep mantle beneath the Pacific Ocean"}],"downloadable_attachments":[{"id":52420483,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420483/thumbnails/1.jpg","file_name":"Isotopic_systematics_of_the_early_Mauna_20170401-6059-iiunoh.pdf","download_url":"https://www.academia.edu/attachments/52420483/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Isotopic_systematics_of_the_early_Mauna.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420483/Isotopic_systematics_of_the_early_Mauna_20170401-6059-iiunoh-libre.pdf?1491067351=\u0026response-content-disposition=attachment%3B+filename%3DIsotopic_systematics_of_the_early_Mauna.pdf\u0026Expires=1733097977\u0026Signature=NCSDPH7HBNbWNwkp3zJNtEgnMv4eo9GLxfdVYDlHnX59pOh9U7ApqWjEF~YLy5qPSuDEOmo-tNqtS52xfR6vqjfu53FBeaoWqpIYZSfOkV5Jpl6G0Rsm69Y0qiYRv0mb8boNBftpgiB8pAd2m5ISL~Jmww3JoaCamzO5FKN8lN-z4bLmo4O7BNi39qx2XAnw55-B1DLsTyB-6jOLJitdEV~c0D1ftzqpGNKHKREaSIk8de1x9jamvxUbv6t2AEdnuZRMmLjFita9Ymr~wgdIVlQof-XzZ2Mw8TKlaDMGhLwse2uXzROLk7Dvtrd1oDG~PibvPEBW5OwFRtRVcevjYA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Isotopic_systematics_of_the_early_Mauna_Kea_shield_phase_and_insight_into_the_deep_mantle_beneath_the_Pacific_Ocean","translated_slug":"","page_count":18,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420483,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420483/thumbnails/1.jpg","file_name":"Isotopic_systematics_of_the_early_Mauna_20170401-6059-iiunoh.pdf","download_url":"https://www.academia.edu/attachments/52420483/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Isotopic_systematics_of_the_early_Mauna.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420483/Isotopic_systematics_of_the_early_Mauna_20170401-6059-iiunoh-libre.pdf?1491067351=\u0026response-content-disposition=attachment%3B+filename%3DIsotopic_systematics_of_the_early_Mauna.pdf\u0026Expires=1733097977\u0026Signature=NCSDPH7HBNbWNwkp3zJNtEgnMv4eo9GLxfdVYDlHnX59pOh9U7ApqWjEF~YLy5qPSuDEOmo-tNqtS52xfR6vqjfu53FBeaoWqpIYZSfOkV5Jpl6G0Rsm69Y0qiYRv0mb8boNBftpgiB8pAd2m5ISL~Jmww3JoaCamzO5FKN8lN-z4bLmo4O7BNi39qx2XAnw55-B1DLsTyB-6jOLJitdEV~c0D1ftzqpGNKHKREaSIk8de1x9jamvxUbv6t2AEdnuZRMmLjFita9Ymr~wgdIVlQof-XzZ2Mw8TKlaDMGhLwse2uXzROLk7Dvtrd1oDG~PibvPEBW5OwFRtRVcevjYA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186870"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186870/Rapid_passage_of_a_small_scale_mantle_heterogeneity_through_the_melting_regions_of_Kilauea_and_Mauna_Loa_Volcanoes"><img alt="Research paper thumbnail of Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes" class="work-thumbnail" src="https://attachments.academia-assets.com/52420497/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186870/Rapid_passage_of_a_small_scale_mantle_heterogeneity_through_the_melting_regions_of_Kilauea_and_Mauna_Loa_Volcanoes">Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, 2007</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="4e2c274b2d5576b5bc32ef8bc74b3bc6" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420497,"asset_id":32186870,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420497/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186870"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186870"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186870; 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "4e2c274b2d5576b5bc32ef8bc74b3bc6" } } $('.js-work-strip[data-work-id=32186870]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186870,"title":"Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes","translated_title":"","metadata":{"grobid_abstract":"Recent Kilauea and Mauna Loa lavas provide a snapshot of the size, shape, and distribution of compositional heterogeneities within the Hawaiian mantle plume. Here we present a study of the Pb, Sr, and Nd isotope ratios of two suites of young prehistoric lavas from these volcanoes: (1) Kilauea summit lavas erupted from AD 900 to 1400, and (2) 14 C-dated Mauna Loa flows erupted from ∼ 2580-140 yr before present (relative to AD 1950). These lavas display systematic isotopic fluctuations, and the Kilauea lavas span the Pb isotopic divide that was previously thought to exist between these two volcanoes. For a brief period from AD 250 to 1400, the 206 Pb/ 204 Pb and 87 Sr/ 86 Sr isotope ratios and ε Nd values of Kilauea and Mauna Loa lavas departed from values typical for each volcano (based on historical and other young prehistoric lavas), moved towards an intermediate composition, and subsequently returned to typical values. This is the only known period in the eruptive history of these volcanoes when such a simultaneous convergence of Pb, Sr, and Nd isotope ratios has occurred. The common isotopic composition of lavas erupted from both Kilauea and Mauna Loa during this transient magmatic event was probably caused by the rapid passage of a small-scale compositional heterogeneity through the melting regions of both volcanoes. This heterogeneity is thought to have been either a single body (∼ 35 km long based on the distance between the summits of these volcanoes) or the plume matrix itself (which would be expected to be present beneath both volcanoes). The time scale of this event (centuries) is much shorter than previously noted for variations in the isotopic composition of Hawaiian lavas due to the upwelling of heterogeneities within the plume (thousands to tens of thousands of years). Calculations based on the timing of the isotopic convergence suggest a maximum thickness for the melting region (and thus, the heterogeneity) of ∼ 5-10 km. The small size of the heterogeneity indicates that melt can be extracted from small regions within the Hawaiian plume with minimal subsequent chemical modification (beyond the effects of crystal","publication_date":{"day":null,"month":null,"year":2007,"errors":{}},"publication_name":"Earth and Planetary Science Letters","grobid_abstract_attachment_id":52420497},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186870/Rapid_passage_of_a_small_scale_mantle_heterogeneity_through_the_melting_regions_of_Kilauea_and_Mauna_Loa_Volcanoes","translated_internal_url":"","created_at":"2017-04-01T10:05:24.256-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304561,"work_id":32186870,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176450,"email":"j***e@carnegiescience.edu","display_order":0,"name":"Jared Marske","title":"Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes"},{"id":28304801,"work_id":32186870,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":4194304,"name":"Michael Garcia","title":"Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes"},{"id":28305042,"work_id":32186870,"tagging_user_id":62411756,"tagged_user_id":197661874,"co_author_invite_id":6176598,"email":"j***s@geo.umass.edu","display_order":6291456,"name":"John Rhodes","title":"Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes"},{"id":28305043,"work_id":32186870,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":2068962,"email":"a***s@geology.sdsu.edu","display_order":7340032,"name":"Aaron Pietruszka","title":"Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes"},{"id":28305125,"work_id":32186870,"tagging_user_id":62411756,"tagged_user_id":33010082,"co_author_invite_id":null,"email":"m***a@hawaii.edu","display_order":7864320,"name":"m g","title":"Rapid passage of a small-scale mantle heterogeneity through the melting regions of Kilauea and Mauna Loa Volcanoes"}],"downloadable_attachments":[{"id":52420497,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420497/thumbnails/1.jpg","file_name":"Rapid_passage_of_a_small-scale_mantle_he20170401-6059-12ahwk.pdf","download_url":"https://www.academia.edu/attachments/52420497/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Rapid_passage_of_a_small_scale_mantle_he.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420497/Rapid_passage_of_a_small-scale_mantle_he20170401-6059-12ahwk-libre.pdf?1491067312=\u0026response-content-disposition=attachment%3B+filename%3DRapid_passage_of_a_small_scale_mantle_he.pdf\u0026Expires=1733034952\u0026Signature=NX5rJ2ZUANqaeZuVYXlLZyk21o0AmFAoQhHpK0ORc1PYrlBETqqlq~5soICC7hgZ9lFqeV5J7~tIR8~s8i-Dn0AxSADe-6XwDXwieKPJcR7qi4kNK8~m-t2v-xU9COPED6g8fUqqkoJY4W8c-UfPeXPpMk71BLc4v-BW8q0VuqzunbIOSxRCSIUbRRrKoVJZgYADwpCrFuAfsXqMw8~20XDQD9KwqfpVK21fhq~BYX6WRTMQAcMEDUjgX~KlUWY9Yr65gAfBCKfIQ7i7IMqnhrgt-lLGNyzofX7KHIzOQNaGokCKLx52YhNz8mnOuSNc17gopyPFhvowgmxZ8G8fgA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Rapid_passage_of_a_small_scale_mantle_heterogeneity_through_the_melting_regions_of_Kilauea_and_Mauna_Loa_Volcanoes","translated_slug":"","page_count":17,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420497,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420497/thumbnails/1.jpg","file_name":"Rapid_passage_of_a_small-scale_mantle_he20170401-6059-12ahwk.pdf","download_url":"https://www.academia.edu/attachments/52420497/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Rapid_passage_of_a_small_scale_mantle_he.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420497/Rapid_passage_of_a_small-scale_mantle_he20170401-6059-12ahwk-libre.pdf?1491067312=\u0026response-content-disposition=attachment%3B+filename%3DRapid_passage_of_a_small_scale_mantle_he.pdf\u0026Expires=1733034952\u0026Signature=NX5rJ2ZUANqaeZuVYXlLZyk21o0AmFAoQhHpK0ORc1PYrlBETqqlq~5soICC7hgZ9lFqeV5J7~tIR8~s8i-Dn0AxSADe-6XwDXwieKPJcR7qi4kNK8~m-t2v-xU9COPED6g8fUqqkoJY4W8c-UfPeXPpMk71BLc4v-BW8q0VuqzunbIOSxRCSIUbRRrKoVJZgYADwpCrFuAfsXqMw8~20XDQD9KwqfpVK21fhq~BYX6WRTMQAcMEDUjgX~KlUWY9Yr65gAfBCKfIQ7i7IMqnhrgt-lLGNyzofX7KHIzOQNaGokCKLx52YhNz8mnOuSNc17gopyPFhvowgmxZ8G8fgA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":241723,"name":"Earth and Planetary Science","url":"https://www.academia.edu/Documents/in/Earth_and_Planetary_Science"},{"id":424229,"name":"Sr isotopes","url":"https://www.academia.edu/Documents/in/Sr_isotopes"},{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"},{"id":1418721,"name":"Chemical Modification","url":"https://www.academia.edu/Documents/in/Chemical_Modification"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186853"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186853/Age_geology_geophysics_and_geochemistry_of_Mahukona_Volcano_Hawaii"><img alt="Research paper thumbnail of Age, geology, geophysics, and geochemistry of Mahukona Volcano, Hawai`i" class="work-thumbnail" src="https://attachments.academia-assets.com/52420490/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186853/Age_geology_geophysics_and_geochemistry_of_Mahukona_Volcano_Hawaii">Age, geology, geophysics, and geochemistry of Mahukona Volcano, Hawai`i</a></div><div class="wp-workCard_item"><span>Bulletin of Volcanology</span><span>, 2012</span></div><div 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{"id":32186853,"title":"Age, geology, geophysics, and geochemistry of Mahukona Volcano, Hawai`i","translated_title":"","metadata":{"grobid_abstract":"The size, shape, and magmatic history of the most recently discovered shield volcano in the Hawaiian Islands, Mahukona, have been controversial. Mahukona corresponds to what was thought to be a gap in the paired sequence (Loa and Kea trends) of younger Hawaiian volcanoes (\u003c4 Ma). Here, we present the results of marine expeditions to Mahukona where new bathymetry, sidescan sonar, gravity data, and lava samples were collected to address these controversies. Modeling of bathymetric and gravity data indicate that Mahukona is one of the smallest Hawaiian volcanoes (∼6,000 km 3 ) and that its magmatic system was not focused in a long-lived central reservoir like most other Hawaiian volcanoes. This lack of a long-lived magmatic reservoir is reflected by the absence of a central residual gravity high and the random distribution of cones on Mahukona Volcano. Our reconstructed subsidence history for Mahukona suggests it grew to at least ∼270 m below sea level but probably did not form an island. New 40 Ar-39 Ar plateau ages range from 350 to 654 ka providing temporal constraints for Mahukona's post-shield and shield stages of volcanism, which ended prematurely. Mahukona post-shield lavas have high 3 He/ 4 He ratios (16-21 Ra), which have not been observed in post-shield lavas from other Hawaiian volcanoes. Lava compositions range widely at Mahukona, including Pb isotopic values that straddle the boundary between Kea and Loa sequences of volcanoes. The compositional diversity of Mahukona lavas may be related to its relatively small size (less extensive melting) and the absence of a central magma reservoir where magmas would have been homogenized.","publication_date":{"day":null,"month":null,"year":2012,"errors":{}},"publication_name":"Bulletin of Volcanology","grobid_abstract_attachment_id":52420490},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186853/Age_geology_geophysics_and_geochemistry_of_Mahukona_Volcano_Hawaii","translated_internal_url":"","created_at":"2017-04-01T10:05:22.414-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304547,"work_id":32186853,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176447,"email":"a***s@my.uri.edu","display_order":0,"name":"Ashton Flinders","title":"Age, geology, geophysics, and geochemistry of Mahukona Volcano, Hawai`i"},{"id":28304757,"work_id":32186853,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176508,"email":"m***z@nsf.gov","display_order":4194304,"name":"Mark Kurz","title":"Age, geology, geophysics, and geochemistry of Mahukona Volcano, Hawai`i"},{"id":28304805,"work_id":32186853,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":6291456,"name":"Michael Garcia","title":"Age, geology, geophysics, and geochemistry of Mahukona Volcano, Hawai`i"},{"id":28305094,"work_id":32186853,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":2068964,"email":"g***o@soest.hawaii.edu","display_order":7340032,"name":"Garrett Ito","title":"Age, geology, geophysics, and geochemistry of Mahukona Volcano, Hawai`i"},{"id":28305124,"work_id":32186853,"tagging_user_id":62411756,"tagged_user_id":33010082,"co_author_invite_id":null,"email":"m***a@hawaii.edu","display_order":7864320,"name":"m 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dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="6767202" id="abstracts"><div class="js-work-strip profile--work_container" data-work-id="32186956"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186956/Isotopic_evolution_of_Hawaiian_shield_basalts_over_4_5_million_years_and_implications_for_plume_structure"><img alt="Research paper thumbnail of Isotopic evolution of Hawaiian shield basalts over 4.5 million years and implications for plume structure" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186956/Isotopic_evolution_of_Hawaiian_shield_basalts_over_4_5_million_years_and_implications_for_plume_structure">Isotopic evolution of Hawaiian shield basalts over 4.5 million years and implications for plume structure</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Improved analytical precision for radiogenic isotopes (down to ~100 ppm for Pb and to &lt;50 ppm ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Improved analytical precision for radiogenic isotopes (down to ~100 ppm for Pb and to &lt;50 ppm for Sr, Nd and Hf), combined with statistical data treatment, allow for detailed investigations into the geochemical variations of basalts related to mantle plumes. For the main Hawaiian Islands, representing 4.5 myr of volcanism, we compiled high-precision Pb isotopic data (MC-ICP-MS or DS, TS TIMS) for 845 samples, integrated with Sr, Nd and Hf isotopic data on 500-600 samples for shield stage (67%), post-shield/late shield (22%) and rejuvenated lavas (10%). All data were normalized to the same standard values to avoid inter-laboratory biases and 30% of the analyses were determined at UBC. The Kea trend volcanoes have higher 206Pb/204Pb and 208Pb/204Pb, higher epsilon Nd, epsilon Hf, and lower 87Sr/86Sr than Loa trend volcanoes. This dichotomy does not stop at O`ahu as Loa characteristics are identified in the ~4.5 Ma Kaua`i lavas. Pb isotopes present the sharpest boundary between the ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186956"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186956"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186956; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186956]").text(description); $(".js-view-count[data-work-id=32186956]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186956; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186956']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186956, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186956]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186956,"title":"Isotopic evolution of Hawaiian shield basalts over 4.5 million years and implications for plume structure","translated_title":"","metadata":{"abstract":"Improved analytical precision for radiogenic isotopes (down to ~100 ppm for Pb and to \u0026lt;50 ppm for Sr, Nd and Hf), combined with statistical data treatment, allow for detailed investigations into the geochemical variations of basalts related to mantle plumes. For the main Hawaiian Islands, representing 4.5 myr of volcanism, we compiled high-precision Pb isotopic data (MC-ICP-MS or DS, TS TIMS) for 845 samples, integrated with Sr, Nd and Hf isotopic data on 500-600 samples for shield stage (67%), post-shield/late shield (22%) and rejuvenated lavas (10%). All data were normalized to the same standard values to avoid inter-laboratory biases and 30% of the analyses were determined at UBC. The Kea trend volcanoes have higher 206Pb/204Pb and 208Pb/204Pb, higher epsilon Nd, epsilon Hf, and lower 87Sr/86Sr than Loa trend volcanoes. This dichotomy does not stop at O`ahu as Loa characteristics are identified in the ~4.5 Ma Kaua`i lavas. Pb isotopes present the sharpest boundary between the ..."},"translated_abstract":"Improved analytical precision for radiogenic isotopes (down to ~100 ppm for Pb and to \u0026lt;50 ppm for Sr, Nd and Hf), combined with statistical data treatment, allow for detailed investigations into the geochemical variations of basalts related to mantle plumes. For the main Hawaiian Islands, representing 4.5 myr of volcanism, we compiled high-precision Pb isotopic data (MC-ICP-MS or DS, TS TIMS) for 845 samples, integrated with Sr, Nd and Hf isotopic data on 500-600 samples for shield stage (67%), post-shield/late shield (22%) and rejuvenated lavas (10%). All data were normalized to the same standard values to avoid inter-laboratory biases and 30% of the analyses were determined at UBC. The Kea trend volcanoes have higher 206Pb/204Pb and 208Pb/204Pb, higher epsilon Nd, epsilon Hf, and lower 87Sr/86Sr than Loa trend volcanoes. This dichotomy does not stop at O`ahu as Loa characteristics are identified in the ~4.5 Ma Kaua`i lavas. Pb isotopes present the sharpest boundary between the ...","internal_url":"https://www.academia.edu/32186956/Isotopic_evolution_of_Hawaiian_shield_basalts_over_4_5_million_years_and_implications_for_plume_structure","translated_internal_url":"","created_at":"2017-04-01T10:05:36.312-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304457,"work_id":32186956,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Isotopic evolution of Hawaiian shield basalts over 4.5 million years and implications for plume structure"},{"id":28304822,"work_id":32186956,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":4194304,"name":"Michael Garcia","title":"Isotopic evolution of Hawaiian shield basalts over 4.5 million years and implications for plume structure"}],"downloadable_attachments":[],"slug":"Isotopic_evolution_of_Hawaiian_shield_basalts_over_4_5_million_years_and_implications_for_plume_structure","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"},{"id":984993,"name":"Residence Time","url":"https://www.academia.edu/Documents/in/Residence_Time"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186939"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32186939/Small_scale_heterogeneities_in_the_enriched_component_of_the_Kerguelen_mantle_plume_Pb_Hf_Sr_Nd_isotopic_constraints_from_the_Kerguelen_Baie_Charrier_section"><img alt="Research paper thumbnail of Small-scale heterogeneities in the enriched component of the Kerguelen mantle plume: Pb-Hf-Sr-Nd isotopic constraints from the Kerguelen Baie Charrier section" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32186939/Small_scale_heterogeneities_in_the_enriched_component_of_the_Kerguelen_mantle_plume_Pb_Hf_Sr_Nd_isotopic_constraints_from_the_Kerguelen_Baie_Charrier_section">Small-scale heterogeneities in the enriched component of the Kerguelen mantle plume: Pb-Hf-Sr-Nd isotopic constraints from the Kerguelen Baie Charrier section</a></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186939"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186939"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186939; 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Marion Dufresne, Kerguelen Archipelago, southern Indian Ocean" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32186934/Evidence_for_a_depleted_mantle_component_in_mildly_alkalic_high_MgO_basalts_from_Mt_Marion_Dufresne_Kerguelen_Archipelago_southern_Indian_Ocean">Evidence for a depleted mantle component in mildly alkalic high-MgO basalts from Mt. Marion Dufresne, Kerguelen Archipelago, southern Indian Ocean</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Kerguelen Archipelago flood basalts (29-24 Ma) were erupted onto the Northern Kerguelen Plateau w...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Kerguelen Archipelago flood basalts (29-24 Ma) were erupted onto the Northern Kerguelen Plateau when the Southeast Indian Ridge was 200-400 km northeast of the Kerguelen hotspot. A depleted mantle component is evident in older (28-29 Ma) transitional-tholeiitic basalts on the archipelago, but is absent in younger (24-25 Ma) mildly alkalic lavas. This trend towards more alkalic volcanism primarily reflects decreasing</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186934"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186934"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186934; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186934]").text(description); $(".js-view-count[data-work-id=32186934]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186934; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186934']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186934, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186934]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186934,"title":"Evidence for a depleted mantle component in mildly alkalic high-MgO basalts from Mt. 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This trend towards more alkalic volcanism primarily reflects decreasing","internal_url":"https://www.academia.edu/32186934/Evidence_for_a_depleted_mantle_component_in_mildly_alkalic_high_MgO_basalts_from_Mt_Marion_Dufresne_Kerguelen_Archipelago_southern_Indian_Ocean","translated_internal_url":"","created_at":"2017-04-01T10:05:32.804-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304440,"work_id":32186934,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Evidence for a depleted mantle component in mildly alkalic high-MgO basalts from Mt. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186852"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32186852/Ongoing_Isotopic_Characterization_of_USGS_Standards_MC_ICPMS_and_TIMS_data_from_The_Pacific_Centre_for_Isotopic_and_Geochemical_Research_University_of_British_"><img alt="Research paper thumbnail of Ongoing Isotopic Characterization of USGS Standards: MC-ICPMS and TIMS data from The Pacific Centre for Isotopic and Geochemical Research, University of British …" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32186852/Ongoing_Isotopic_Characterization_of_USGS_Standards_MC_ICPMS_and_TIMS_data_from_The_Pacific_Centre_for_Isotopic_and_Geochemical_Research_University_of_British_">Ongoing Isotopic Characterization of USGS Standards: MC-ICPMS and TIMS data from The Pacific Centre for Isotopic and Geochemical Research, University of British …</a></div><div class="wp-workCard_item"><span>Annual …</span><span>, 2003</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The PCIGR at the University of British Columbia has undertaken a systematic analysis of isotopic ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The PCIGR at the University of British Columbia has undertaken a systematic analysis of isotopic (Nd, Sr, Hf, Pb) composition and concentration of a broad compositional range of United States Geological Survey standards, including basalt (BCR-1, 2; BHVO-1, 2; BIR-1), dunite ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186852"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186852"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186852; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186852]").text(description); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186847"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186847/Flood_basalts_of_the_Wrangellia_Terrane_southwest_Yukon_Implications_for_the_formation_of_oceanic_plateaus_continental_crust_and_Ni_Cu_PGE_mineralization"><img alt="Research paper thumbnail of Flood basalts of the Wrangellia Terrane, southwest Yukon: Implications for the formation of oceanic plateaus, continental crust and Ni-Cu-PGE mineralization" class="work-thumbnail" src="https://attachments.academia-assets.com/52420467/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186847/Flood_basalts_of_the_Wrangellia_Terrane_southwest_Yukon_Implications_for_the_formation_of_oceanic_plateaus_continental_crust_and_Ni_Cu_PGE_mineralization">Flood basalts of the Wrangellia Terrane, southwest Yukon: Implications for the formation of oceanic plateaus, continental crust and Ni-Cu-PGE mineralization</a></div><div class="wp-workCard_item"><span>Yukon Exploration and …</span><span>, 2004</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="fedc4269bf139550595ce77085e2c6f8" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420467,"asset_id":32186847,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420467/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186847"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186847"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186847; 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These volcanic sequences erupted onto an extinct island arc in less than 5 million years at ca. 230 Ma. Triassic Wrangellia basalts and intrusions form a 1 to 10 km-wide linear belt of mafic and ultramafic rocks extending 300 km across southwest Yukon. A total of 85 samples were collected for geochemical and isotopic analysis from 10 widespread areas along the entire length of the linear belt. Field observations during the summer of 2004, and a synthesis of previous research for the Yukon portion of Wrangellia, are part of a larger research project involving Wrangellia basalts extending from Vancouver Island to central Alaska. The Wrangellia volcanic sequences represent one of the finest examples of an accreted oceanic plateau worldwide. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186845"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186845/Evolution_of_the_Hawaiian_Mantle_Plume_Shield_and_Rejuvenescent_Magmatism_at_Middle_Bank_the_Youngest_Sunken_Hawaiian_Volcano"><img alt="Research paper thumbnail of Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186845/Evolution_of_the_Hawaiian_Mantle_Plume_Shield_and_Rejuvenescent_Magmatism_at_Middle_Bank_the_Youngest_Sunken_Hawaiian_Volcano">Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT Post-shield volcanism provides unique insight into the structure of mantle plumes and th...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT Post-shield volcanism provides unique insight into the structure of mantle plumes and the magmatic processes responsible for the evolution of ocean islands. Middle Bank is the closest seamount to the main Hawaiian archipelago, thus providing a perspective into the processes related to the dying phase of a Hawaiian volcano. We conducted a detailed survey of the volcano in 2007 using multibeam sonar coupled with Jason2 ROV imaging and sampling. According to plate tectonic models, Middle Bank volcano should be about 9.6 Ma, if it formed near the present location of Kilauea. Middle Bank is 100 km in diameter and rises nearly 5000 m from base level. Its morphology is dominated by three major rift zones that emanate to the east, west, and south from the beveled summit platform. The rifts are separated by talus fans, and the volcano is surrounded by dozens of satellite cones. Many of the satellite cones are covered by remarkably unsedimented lavas that were erupted in the submarine environment, which we interpret as a rejuvenated stage of volcanism. Most of the sampled rocks are strongly alkaline and range from basanite to hawaiite and trachyte. Samples from two sites are tholeiitic, which is consistent with them forming during the shield stage of volcanism. If so, then most of the late history of volcanism, from shield building to rejuvenated volcanism is preserved at Middle Bank. The alkaline basalts and basanites have La/Sm and La/Yb ratios that are higher than the tholeiites, and all of the rocks are strongly LREE enriched. Major and trace element compositions of hawaiites and trachytes are consistent with large amounts of crystal fractionation, which especially affected magmas erupted on the outer flanks of the volcano. The tholeiites have Sr/Nb and Zr/Nb that suggest that the Middle Bank shield is akin to the modern-day &amp;quot;Kea&amp;quot; trend geochemically. Thus, Middle Bank has preserved the archetypical tholeiitic-shield to alkaline-rejuvenated evolutionary stages that characterize the subaerial Hawaiian volcanoes.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186845"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186845"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186845; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186845]").text(description); $(".js-view-count[data-work-id=32186845]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186845; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186845']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186845, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186845]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186845,"title":"Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano","translated_title":"","metadata":{"abstract":"ABSTRACT Post-shield volcanism provides unique insight into the structure of mantle plumes and the magmatic processes responsible for the evolution of ocean islands. Middle Bank is the closest seamount to the main Hawaiian archipelago, thus providing a perspective into the processes related to the dying phase of a Hawaiian volcano. We conducted a detailed survey of the volcano in 2007 using multibeam sonar coupled with Jason2 ROV imaging and sampling. According to plate tectonic models, Middle Bank volcano should be about 9.6 Ma, if it formed near the present location of Kilauea. Middle Bank is 100 km in diameter and rises nearly 5000 m from base level. Its morphology is dominated by three major rift zones that emanate to the east, west, and south from the beveled summit platform. The rifts are separated by talus fans, and the volcano is surrounded by dozens of satellite cones. Many of the satellite cones are covered by remarkably unsedimented lavas that were erupted in the submarine environment, which we interpret as a rejuvenated stage of volcanism. Most of the sampled rocks are strongly alkaline and range from basanite to hawaiite and trachyte. Samples from two sites are tholeiitic, which is consistent with them forming during the shield stage of volcanism. If so, then most of the late history of volcanism, from shield building to rejuvenated volcanism is preserved at Middle Bank. The alkaline basalts and basanites have La/Sm and La/Yb ratios that are higher than the tholeiites, and all of the rocks are strongly LREE enriched. Major and trace element compositions of hawaiites and trachytes are consistent with large amounts of crystal fractionation, which especially affected magmas erupted on the outer flanks of the volcano. The tholeiites have Sr/Nb and Zr/Nb that suggest that the Middle Bank shield is akin to the modern-day \u0026amp;quot;Kea\u0026amp;quot; trend geochemically. Thus, Middle Bank has preserved the archetypical tholeiitic-shield to alkaline-rejuvenated evolutionary stages that characterize the subaerial Hawaiian volcanoes.","publication_date":{"day":null,"month":null,"year":2008,"errors":{}}},"translated_abstract":"ABSTRACT Post-shield volcanism provides unique insight into the structure of mantle plumes and the magmatic processes responsible for the evolution of ocean islands. Middle Bank is the closest seamount to the main Hawaiian archipelago, thus providing a perspective into the processes related to the dying phase of a Hawaiian volcano. We conducted a detailed survey of the volcano in 2007 using multibeam sonar coupled with Jason2 ROV imaging and sampling. According to plate tectonic models, Middle Bank volcano should be about 9.6 Ma, if it formed near the present location of Kilauea. Middle Bank is 100 km in diameter and rises nearly 5000 m from base level. Its morphology is dominated by three major rift zones that emanate to the east, west, and south from the beveled summit platform. The rifts are separated by talus fans, and the volcano is surrounded by dozens of satellite cones. Many of the satellite cones are covered by remarkably unsedimented lavas that were erupted in the submarine environment, which we interpret as a rejuvenated stage of volcanism. Most of the sampled rocks are strongly alkaline and range from basanite to hawaiite and trachyte. Samples from two sites are tholeiitic, which is consistent with them forming during the shield stage of volcanism. If so, then most of the late history of volcanism, from shield building to rejuvenated volcanism is preserved at Middle Bank. The alkaline basalts and basanites have La/Sm and La/Yb ratios that are higher than the tholeiites, and all of the rocks are strongly LREE enriched. Major and trace element compositions of hawaiites and trachytes are consistent with large amounts of crystal fractionation, which especially affected magmas erupted on the outer flanks of the volcano. The tholeiites have Sr/Nb and Zr/Nb that suggest that the Middle Bank shield is akin to the modern-day \u0026amp;quot;Kea\u0026amp;quot; trend geochemically. Thus, Middle Bank has preserved the archetypical tholeiitic-shield to alkaline-rejuvenated evolutionary stages that characterize the subaerial Hawaiian volcanoes.","internal_url":"https://www.academia.edu/32186845/Evolution_of_the_Hawaiian_Mantle_Plume_Shield_and_Rejuvenescent_Magmatism_at_Middle_Bank_the_Youngest_Sunken_Hawaiian_Volcano","translated_internal_url":"","created_at":"2017-04-01T10:05:21.536-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304530,"work_id":32186845,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176444,"email":"d***t@nsf.gov","display_order":0,"name":"Dennis Geist","title":"Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano"},{"id":28304814,"work_id":32186845,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176530,"email":"m***a@mdanderson.org","display_order":4194304,"name":"Michael Garcia","title":"Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano"},{"id":28305072,"work_id":32186845,"tagging_user_id":62411756,"tagged_user_id":34403155,"co_author_invite_id":null,"email":"k***p@colgate.edu","affiliation":"Colgate University","display_order":6291456,"name":"Karen Harpp","title":"Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano"},{"id":28305093,"work_id":32186845,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":2068964,"email":"g***o@soest.hawaii.edu","display_order":7340032,"name":"Garrett Ito","title":"Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano"},{"id":28305123,"work_id":32186845,"tagging_user_id":62411756,"tagged_user_id":33010082,"co_author_invite_id":null,"email":"m***a@hawaii.edu","display_order":7864320,"name":"m g","title":"Evolution of the Hawaiian Mantle Plume: Shield and Rejuvenescent Magmatism at Middle Bank, the Youngest Sunken Hawaiian Volcano"}],"downloadable_attachments":[],"slug":"Evolution_of_the_Hawaiian_Mantle_Plume_Shield_and_Rejuvenescent_Magmatism_at_Middle_Bank_the_Youngest_Sunken_Hawaiian_Volcano","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":814934,"name":"Plate tectonic","url":"https://www.academia.edu/Documents/in/Plate_tectonic"}],"urls":[]}, dispatcherData: dispatcherData }); 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Carbon reduction offers the potential to avoid the use of hazardous gases; however, it has been plagued by low yields and variable isotopic fractionation leading to significant differences in isotopic composition compared to conventional fluorination techniques (CFT). We adopt a carbon reduction method, which includes a fluorinated graphite polymer (F>60%) to help oxidize the silicate, thus increasing the percent yield as well as the precision of the analyses. Three silicate standards (NBS-28; UWG-2; GBW044190) were analyzed to compare this method against CFT. Silicate samples of 0.2mg are combined with 2mg of fluorinated graphite and sealed in a silver cup. The cups are then heated instantaneously to 1470°C in a high temperature conversion elemental analyzer (TC/EA). The evolved oxygen reacts with carbon in the furnace resulting in carbon monoxide which is transported via a helium carrier gas to a series of chemical and cold traps prior to introduction into the gas chromatograph. An Ascarite II and Mg(ClO4)2 chemical trap removes acids (e.g. HF) and water, followed by an LN2 cold trap to remove SiF4. The He carrier gas flow is kept low (0.7bar) to maximize reaction time, whereas He flow to the open split is increased (0.7bar) in order to reduce peak tailing in the IRMS. Using this method individual analysis can be completed in ~7 minutes. Oxygen yields range from 54-92%; however reproducibility better than 0.5‰ is normally achievable. Measured values are consistently enriched in 18O compared with accepted values; however, this offset is systematic and can be corrected for using a linear correction factor. Corrected values are: 9.11±0.3‰, 5.95±0.5‰, and -1.78±0.4‰ for NBS-28, UWG-2, and GBW044190 respectively. As the number of laboratories with CF-IRMS and TC/EA apparatus increases the development of this method has the potential to make δ18O analysis of silicates more widely available.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187112"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187112"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187112; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187112]").text(description); $(".js-view-count[data-work-id=32187112]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187112; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187112']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187112, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187112]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187112,"title":"The use of Fluorinated Graphite Polymer in the Oxygen-Isotope Analysis of Silicates by Continuous Flow Isotope Ratio Mass Spectrometry (CF-IRMS)","translated_title":"","metadata":{"abstract":"To date the majority of analytical procedures for δ18O analysis of silicates require relatively expensive apparatus involving the use of hazardous fluorine or halogen fluoride gases. Carbon reduction offers the potential to avoid the use of hazardous gases; however, it has been plagued by low yields and variable isotopic fractionation leading to significant differences in isotopic composition compared to conventional fluorination techniques (CFT). We adopt a carbon reduction method, which includes a fluorinated graphite polymer (F\u003e60%) to help oxidize the silicate, thus increasing the percent yield as well as the precision of the analyses. Three silicate standards (NBS-28; UWG-2; GBW044190) were analyzed to compare this method against CFT. Silicate samples of 0.2mg are combined with 2mg of fluorinated graphite and sealed in a silver cup. The cups are then heated instantaneously to 1470°C in a high temperature conversion elemental analyzer (TC/EA). The evolved oxygen reacts with carbon in the furnace resulting in carbon monoxide which is transported via a helium carrier gas to a series of chemical and cold traps prior to introduction into the gas chromatograph. An Ascarite II and Mg(ClO4)2 chemical trap removes acids (e.g. HF) and water, followed by an LN2 cold trap to remove SiF4. The He carrier gas flow is kept low (0.7bar) to maximize reaction time, whereas He flow to the open split is increased (0.7bar) in order to reduce peak tailing in the IRMS. Using this method individual analysis can be completed in ~7 minutes. Oxygen yields range from 54-92%; however reproducibility better than 0.5‰ is normally achievable. Measured values are consistently enriched in 18O compared with accepted values; however, this offset is systematic and can be corrected for using a linear correction factor. Corrected values are: 9.11±0.3‰, 5.95±0.5‰, and -1.78±0.4‰ for NBS-28, UWG-2, and GBW044190 respectively. As the number of laboratories with CF-IRMS and TC/EA apparatus increases the development of this method has the potential to make δ18O analysis of silicates more widely available.","publication_date":{"day":null,"month":null,"year":2008,"errors":{}}},"translated_abstract":"To date the majority of analytical procedures for δ18O analysis of silicates require relatively expensive apparatus involving the use of hazardous fluorine or halogen fluoride gases. Carbon reduction offers the potential to avoid the use of hazardous gases; however, it has been plagued by low yields and variable isotopic fractionation leading to significant differences in isotopic composition compared to conventional fluorination techniques (CFT). We adopt a carbon reduction method, which includes a fluorinated graphite polymer (F\u003e60%) to help oxidize the silicate, thus increasing the percent yield as well as the precision of the analyses. Three silicate standards (NBS-28; UWG-2; GBW044190) were analyzed to compare this method against CFT. Silicate samples of 0.2mg are combined with 2mg of fluorinated graphite and sealed in a silver cup. The cups are then heated instantaneously to 1470°C in a high temperature conversion elemental analyzer (TC/EA). The evolved oxygen reacts with carbon in the furnace resulting in carbon monoxide which is transported via a helium carrier gas to a series of chemical and cold traps prior to introduction into the gas chromatograph. An Ascarite II and Mg(ClO4)2 chemical trap removes acids (e.g. HF) and water, followed by an LN2 cold trap to remove SiF4. The He carrier gas flow is kept low (0.7bar) to maximize reaction time, whereas He flow to the open split is increased (0.7bar) in order to reduce peak tailing in the IRMS. Using this method individual analysis can be completed in ~7 minutes. Oxygen yields range from 54-92%; however reproducibility better than 0.5‰ is normally achievable. Measured values are consistently enriched in 18O compared with accepted values; however, this offset is systematic and can be corrected for using a linear correction factor. Corrected values are: 9.11±0.3‰, 5.95±0.5‰, and -1.78±0.4‰ for NBS-28, UWG-2, and GBW044190 respectively. As the number of laboratories with CF-IRMS and TC/EA apparatus increases the development of this method has the potential to make δ18O analysis of silicates more widely available.","internal_url":"https://www.academia.edu/32187112/The_use_of_Fluorinated_Graphite_Polymer_in_the_Oxygen_Isotope_Analysis_of_Silicates_by_Continuous_Flow_Isotope_Ratio_Mass_Spectrometry_CF_IRMS_","translated_internal_url":"","created_at":"2017-04-01T10:07:26.755-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304783,"work_id":32187112,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176520,"email":"a***n@eos.ubc.ca","display_order":0,"name":"Andrew Kingston","title":"The use of Fluorinated Graphite Polymer in the Oxygen-Isotope Analysis of Silicates by Continuous Flow Isotope Ratio Mass Spectrometry (CF-IRMS)"}],"downloadable_attachments":[],"slug":"The_use_of_Fluorinated_Graphite_Polymer_in_the_Oxygen_Isotope_Analysis_of_Silicates_by_Continuous_Flow_Isotope_Ratio_Mass_Spectrometry_CF_IRMS_","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":12971,"name":"Isotope Ratio Mass Spectrometry","url":"https://www.academia.edu/Documents/in/Isotope_Ratio_Mass_Spectrometry"},{"id":71905,"name":"Carbon Monoxide","url":"https://www.academia.edu/Documents/in/Carbon_Monoxide"},{"id":91257,"name":"Stable Isotope","url":"https://www.academia.edu/Documents/in/Stable_Isotope"},{"id":119665,"name":"Reaction Time","url":"https://www.academia.edu/Documents/in/Reaction_Time"},{"id":191117,"name":"High Temperature","url":"https://www.academia.edu/Documents/in/High_Temperature"},{"id":275177,"name":"Oxygen Isotope","url":"https://www.academia.edu/Documents/in/Oxygen_Isotope"},{"id":417933,"name":"Continuous Flow","url":"https://www.academia.edu/Documents/in/Continuous_Flow"},{"id":640682,"name":"Isotope fractionation","url":"https://www.academia.edu/Documents/in/Isotope_fractionation"},{"id":897122,"name":"Gas Flow","url":"https://www.academia.edu/Documents/in/Gas_Flow"},{"id":1029721,"name":"Instruments and Techniques","url":"https://www.academia.edu/Documents/in/Instruments_and_Techniques"}],"urls":[{"id":8041971,"url":"http://adsabs.harvard.edu/abs/2008agufm.v13a2099k"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187115"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187115/Lack_of_Correlated_Isotopic_and_Compositional_Variations_in_Mauna_Loa_Lavas_A_Serious_Problem_for_Pyroxenite_Eclogite_Plume_Source_Models"><img alt="Research paper thumbnail of Lack of Correlated Isotopic and Compositional Variations in Mauna Loa Lavas: A Serious Problem for Pyroxenite/Eclogite Plume Source Models" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187115/Lack_of_Correlated_Isotopic_and_Compositional_Variations_in_Mauna_Loa_Lavas_A_Serious_Problem_for_Pyroxenite_Eclogite_Plume_Source_Models">Lack of Correlated Isotopic and Compositional Variations in Mauna Loa Lavas: A Serious Problem for Pyroxenite/Eclogite Plume Source Models</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The long held notion that basaltic magmas are produced by decompressional melting of peridotite i...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The long held notion that basaltic magmas are produced by decompressional melting of peridotite is under challenge. Recent models for the Hawaiian and other plumes argue that they consist of a heterogeneous mix of peridotite and discrete eclogite blobs, the latter derived from recycled subducted crust. Eclogite melting produces relatively siliceous magmas (dacite to andesite) which either mix with picritic melts from the peridotite, or, more plausibly, react with the peridotite to produce pyroxenite. Melting of varying proportions of the peridotite/pyroxenite mix is thought to produce the correlated compositional and isotopic characteristics of Hawaiian volcanoes. Magmas from Mauna Loa and Koolau volcanoes are thought to contain more of the recycled component; those from Loihi and Kilauea volcanoes contain less. A simple test of these mixed source models examines whether isotopic changes within the long magmatic history of a single volcano are accompanied by corresponding changes in major and trace element characteristics. Mauna Loa, where we have sampled around 400 - 500 ka of the volcano's eruptive history, provides an excellent opportunity for such a test. During this time, Mauna Loa will have traversed almost half the Hawaiian plume. According to the models, it should have erupted magmas produced from a range of pyroxenite/peridotite mixes with corresponding differences in both isotopic ratios and major and trace elements. Our data show that there is only minor isotopic (Sr, Pb, Nd, Hf) diversity in young lavas (<100 ka), but older lavas are highly diverse, ranging from modern values to those that are close to, and overlap with, those of Loihi volcano. If this isotopic diversity is a consequence of different proportions of pyroxenite and peridotite in the plume source, as the new models predict, we should expect to see correlated changes in bulk composition, particularly. in normalized SiO2, CaO/Al2O3, FeO/MgO and Ni - MgO relationships, as well as changes in Ni - Sc - V relationships. We do not. These parameters remain remarkably uniform over the 400 to 500 ka magmatic history of the volcano, with no correlated variation with isotopic ratios. We conclude that the isotopic heterogeneity within the Hawaiian plume is intrinsic to the peridotite plume source and not dependent on variable contributions from entrained, lithologically-discrete units.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187115"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187115"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187115; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187115]").text(description); $(".js-view-count[data-work-id=32187115]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187115; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187115']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187115, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187115]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187115,"title":"Lack of Correlated Isotopic and Compositional Variations in Mauna Loa Lavas: A Serious Problem for Pyroxenite/Eclogite Plume Source Models","translated_title":"","metadata":{"abstract":"The long held notion that basaltic magmas are produced by decompressional melting of peridotite is under challenge. Recent models for the Hawaiian and other plumes argue that they consist of a heterogeneous mix of peridotite and discrete eclogite blobs, the latter derived from recycled subducted crust. Eclogite melting produces relatively siliceous magmas (dacite to andesite) which either mix with picritic melts from the peridotite, or, more plausibly, react with the peridotite to produce pyroxenite. Melting of varying proportions of the peridotite/pyroxenite mix is thought to produce the correlated compositional and isotopic characteristics of Hawaiian volcanoes. Magmas from Mauna Loa and Koolau volcanoes are thought to contain more of the recycled component; those from Loihi and Kilauea volcanoes contain less. A simple test of these mixed source models examines whether isotopic changes within the long magmatic history of a single volcano are accompanied by corresponding changes in major and trace element characteristics. Mauna Loa, where we have sampled around 400 - 500 ka of the volcano's eruptive history, provides an excellent opportunity for such a test. During this time, Mauna Loa will have traversed almost half the Hawaiian plume. According to the models, it should have erupted magmas produced from a range of pyroxenite/peridotite mixes with corresponding differences in both isotopic ratios and major and trace elements. Our data show that there is only minor isotopic (Sr, Pb, Nd, Hf) diversity in young lavas (\u003c100 ka), but older lavas are highly diverse, ranging from modern values to those that are close to, and overlap with, those of Loihi volcano. If this isotopic diversity is a consequence of different proportions of pyroxenite and peridotite in the plume source, as the new models predict, we should expect to see correlated changes in bulk composition, particularly. in normalized SiO2, CaO/Al2O3, FeO/MgO and Ni - MgO relationships, as well as changes in Ni - Sc - V relationships. We do not. These parameters remain remarkably uniform over the 400 to 500 ka magmatic history of the volcano, with no correlated variation with isotopic ratios. We conclude that the isotopic heterogeneity within the Hawaiian plume is intrinsic to the peridotite plume source and not dependent on variable contributions from entrained, lithologically-discrete units.","publication_date":{"day":1,"month":12,"year":2007,"errors":{}}},"translated_abstract":"The long held notion that basaltic magmas are produced by decompressional melting of peridotite is under challenge. Recent models for the Hawaiian and other plumes argue that they consist of a heterogeneous mix of peridotite and discrete eclogite blobs, the latter derived from recycled subducted crust. Eclogite melting produces relatively siliceous magmas (dacite to andesite) which either mix with picritic melts from the peridotite, or, more plausibly, react with the peridotite to produce pyroxenite. Melting of varying proportions of the peridotite/pyroxenite mix is thought to produce the correlated compositional and isotopic characteristics of Hawaiian volcanoes. Magmas from Mauna Loa and Koolau volcanoes are thought to contain more of the recycled component; those from Loihi and Kilauea volcanoes contain less. A simple test of these mixed source models examines whether isotopic changes within the long magmatic history of a single volcano are accompanied by corresponding changes in major and trace element characteristics. Mauna Loa, where we have sampled around 400 - 500 ka of the volcano's eruptive history, provides an excellent opportunity for such a test. During this time, Mauna Loa will have traversed almost half the Hawaiian plume. According to the models, it should have erupted magmas produced from a range of pyroxenite/peridotite mixes with corresponding differences in both isotopic ratios and major and trace elements. Our data show that there is only minor isotopic (Sr, Pb, Nd, Hf) diversity in young lavas (\u003c100 ka), but older lavas are highly diverse, ranging from modern values to those that are close to, and overlap with, those of Loihi volcano. If this isotopic diversity is a consequence of different proportions of pyroxenite and peridotite in the plume source, as the new models predict, we should expect to see correlated changes in bulk composition, particularly. in normalized SiO2, CaO/Al2O3, FeO/MgO and Ni - MgO relationships, as well as changes in Ni - Sc - V relationships. We do not. These parameters remain remarkably uniform over the 400 to 500 ka magmatic history of the volcano, with no correlated variation with isotopic ratios. We conclude that the isotopic heterogeneity within the Hawaiian plume is intrinsic to the peridotite plume source and not dependent on variable contributions from entrained, lithologically-discrete units.","internal_url":"https://www.academia.edu/32187115/Lack_of_Correlated_Isotopic_and_Compositional_Variations_in_Mauna_Loa_Lavas_A_Serious_Problem_for_Pyroxenite_Eclogite_Plume_Source_Models","translated_internal_url":"","created_at":"2017-04-01T10:07:27.276-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304748,"work_id":32187115,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176503,"email":"j***s@tamu.edu","display_order":0,"name":"James Rhodes","title":"Lack of Correlated Isotopic and Compositional Variations in Mauna Loa Lavas: A Serious Problem for Pyroxenite/Eclogite Plume Source Models"}],"downloadable_attachments":[],"slug":"Lack_of_Correlated_Isotopic_and_Compositional_Variations_in_Mauna_Loa_Lavas_A_Serious_Problem_for_Pyroxenite_Eclogite_Plume_Source_Models","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"}],"urls":[{"id":8041973,"url":"http://adsabs.harvard.edu/abs/2007agufm.v33a1156r"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187117"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187117/Submarine_Tholeiitic_Volcanism_ca_3_6_to_4_9_Ma_West_of_Kaena_Ridge_Hawaiian_Islands_Implications_of_Low_Magma_Productivity_in_the_Evolution_of_the_Hawaiian_Plume"><img alt="Research paper thumbnail of Submarine Tholeiitic Volcanism (ca. 3.6 to 4.9 Ma) West of Ka`ena Ridge, Hawaiian Islands: Implications of Low Magma Productivity in the Evolution of the Hawaiian Plume" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187117/Submarine_Tholeiitic_Volcanism_ca_3_6_to_4_9_Ma_West_of_Kaena_Ridge_Hawaiian_Islands_Implications_of_Low_Magma_Productivity_in_the_Evolution_of_the_Hawaiian_Plume">Submarine Tholeiitic Volcanism (ca. 3.6 to 4.9 Ma) West of Ka`ena Ridge, Hawaiian Islands: Implications of Low Magma Productivity in the Evolution of the Hawaiian Plume</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Submarine tholeiitic and transitional basaltic lavas from volcanic cones west of Ka‘ena Ridge bet...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Submarine tholeiitic and transitional basaltic lavas from volcanic cones west of Ka‘ena Ridge between the Hawaiian Islands of Oah‘u and Kaua‘i were generated by the Hawaiian plume during a time of low magma productivity. Geochemical and Sr, Nd, Hf, and Pb isotopic compositions of West Ka‘ena lavas compared to basalts from Hawaiian shield volcanoes and volume calculations along axis of the Hawaiian Islands provide insights on the relationship between magmatic flux and source composition in the Hawaiian plume in the last 5 Myr. Ka‘ena Ridge is an elongate, relatively flat-topped submerged terrace 35-55 km wide that extends ~80 km from the western edge of Oah‘u The volcanic cones west of Ka‘ena Ridge were sampled by Jason II from R/V Kilo Moana in 2007. The flat-topped and conical cones are <400 m high and <2 km in diameter at water depths ranging between ~2700 to 4300 m, and consist predominantly of pillowed flows and mounds. Ar-Ar ages of eight lavas are between 4.9 and 3.6 Ma; three additional K-Ar ages range from 4.7 to 4.3 Ma. These ages overlap with shield volcanism on Kaua‘i (5.1-4.1 Ma) and Waianae volcano shield basalts (3.9-3.1 Ma) on Oah‘u. Half of the volcanic cones contain high-SiO2 basalts (51.0 to 53.5 wt% SiO_{2}). Isotopic compositions of West Ka‘ena lavas diverge from the main Ko‘olau-Kea mixing trend in binary isotope diagrams and extend to lower 206Pb/^{204}Pb and 208Pb/^{204}Pb ratios than any Hawaiian tholeiitic lava. Several West Ka‘ena samples are similar to SiO2-enriched, Loa-trend lavas of Ko‘olau Makapuu stage, Lanai, and Kahoolawe. However, compared to basalts from these volcanoes the lavas from West Ka‘ena have higher Hf and Nd and lower Sr isotope ratios and do not trend to high ^{208}Pb/$^{204}Pb. A correlation is apparent between magma productivity and isotopic compositions. Thus, west of Ka‘ena Ridge samples may have been generated from a source with a relatively high proportion of eclogite due to decreased plume flux, having formed further from the plume axis, and/or a different distribution of compositional heterogeneities.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187117"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187117"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187117; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187117]").text(description); $(".js-view-count[data-work-id=32187117]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187117; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187117']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187117, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187117]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187117,"title":"Submarine Tholeiitic Volcanism (ca. 3.6 to 4.9 Ma) West of Ka`ena Ridge, Hawaiian Islands: Implications of Low Magma Productivity in the Evolution of the Hawaiian Plume","translated_title":"","metadata":{"abstract":"Submarine tholeiitic and transitional basaltic lavas from volcanic cones west of Ka‘ena Ridge between the Hawaiian Islands of Oah‘u and Kaua‘i were generated by the Hawaiian plume during a time of low magma productivity. Geochemical and Sr, Nd, Hf, and Pb isotopic compositions of West Ka‘ena lavas compared to basalts from Hawaiian shield volcanoes and volume calculations along axis of the Hawaiian Islands provide insights on the relationship between magmatic flux and source composition in the Hawaiian plume in the last 5 Myr. Ka‘ena Ridge is an elongate, relatively flat-topped submerged terrace 35-55 km wide that extends ~80 km from the western edge of Oah‘u The volcanic cones west of Ka‘ena Ridge were sampled by Jason II from R/V Kilo Moana in 2007. The flat-topped and conical cones are \u003c400 m high and \u003c2 km in diameter at water depths ranging between ~2700 to 4300 m, and consist predominantly of pillowed flows and mounds. Ar-Ar ages of eight lavas are between 4.9 and 3.6 Ma; three additional K-Ar ages range from 4.7 to 4.3 Ma. These ages overlap with shield volcanism on Kaua‘i (5.1-4.1 Ma) and Waianae volcano shield basalts (3.9-3.1 Ma) on Oah‘u. Half of the volcanic cones contain high-SiO2 basalts (51.0 to 53.5 wt% SiO_{2}). Isotopic compositions of West Ka‘ena lavas diverge from the main Ko‘olau-Kea mixing trend in binary isotope diagrams and extend to lower 206Pb/^{204}Pb and 208Pb/^{204}Pb ratios than any Hawaiian tholeiitic lava. Several West Ka‘ena samples are similar to SiO2-enriched, Loa-trend lavas of Ko‘olau Makapuu stage, Lanai, and Kahoolawe. However, compared to basalts from these volcanoes the lavas from West Ka‘ena have higher Hf and Nd and lower Sr isotope ratios and do not trend to high ^{208}Pb/$^{204}Pb. A correlation is apparent between magma productivity and isotopic compositions. Thus, west of Ka‘ena Ridge samples may have been generated from a source with a relatively high proportion of eclogite due to decreased plume flux, having formed further from the plume axis, and/or a different distribution of compositional heterogeneities.","publication_date":{"day":null,"month":null,"year":2009,"errors":{}}},"translated_abstract":"Submarine tholeiitic and transitional basaltic lavas from volcanic cones west of Ka‘ena Ridge between the Hawaiian Islands of Oah‘u and Kaua‘i were generated by the Hawaiian plume during a time of low magma productivity. Geochemical and Sr, Nd, Hf, and Pb isotopic compositions of West Ka‘ena lavas compared to basalts from Hawaiian shield volcanoes and volume calculations along axis of the Hawaiian Islands provide insights on the relationship between magmatic flux and source composition in the Hawaiian plume in the last 5 Myr. Ka‘ena Ridge is an elongate, relatively flat-topped submerged terrace 35-55 km wide that extends ~80 km from the western edge of Oah‘u The volcanic cones west of Ka‘ena Ridge were sampled by Jason II from R/V Kilo Moana in 2007. The flat-topped and conical cones are \u003c400 m high and \u003c2 km in diameter at water depths ranging between ~2700 to 4300 m, and consist predominantly of pillowed flows and mounds. Ar-Ar ages of eight lavas are between 4.9 and 3.6 Ma; three additional K-Ar ages range from 4.7 to 4.3 Ma. These ages overlap with shield volcanism on Kaua‘i (5.1-4.1 Ma) and Waianae volcano shield basalts (3.9-3.1 Ma) on Oah‘u. Half of the volcanic cones contain high-SiO2 basalts (51.0 to 53.5 wt% SiO_{2}). Isotopic compositions of West Ka‘ena lavas diverge from the main Ko‘olau-Kea mixing trend in binary isotope diagrams and extend to lower 206Pb/^{204}Pb and 208Pb/^{204}Pb ratios than any Hawaiian tholeiitic lava. Several West Ka‘ena samples are similar to SiO2-enriched, Loa-trend lavas of Ko‘olau Makapuu stage, Lanai, and Kahoolawe. However, compared to basalts from these volcanoes the lavas from West Ka‘ena have higher Hf and Nd and lower Sr isotope ratios and do not trend to high ^{208}Pb/$^{204}Pb. A correlation is apparent between magma productivity and isotopic compositions. Thus, west of Ka‘ena Ridge samples may have been generated from a source with a relatively high proportion of eclogite due to decreased plume flux, having formed further from the plume axis, and/or a different distribution of compositional heterogeneities.","internal_url":"https://www.academia.edu/32187117/Submarine_Tholeiitic_Volcanism_ca_3_6_to_4_9_Ma_West_of_Kaena_Ridge_Hawaiian_Islands_Implications_of_Low_Magma_Productivity_in_the_Evolution_of_the_Hawaiian_Plume","translated_internal_url":"","created_at":"2017-04-01T10:07:27.788-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304723,"work_id":32187117,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176493,"email":"r***g@state.gov","display_order":0,"name":"John Robinson","title":"Submarine Tholeiitic Volcanism (ca. 3.6 to 4.9 Ma) West of Ka`ena Ridge, Hawaiian Islands: Implications of Low Magma Productivity in the Evolution of the Hawaiian Plume"}],"downloadable_attachments":[],"slug":"Submarine_Tholeiitic_Volcanism_ca_3_6_to_4_9_Ma_West_of_Kaena_Ridge_Hawaiian_Islands_Implications_of_Low_Magma_Productivity_in_the_Evolution_of_the_Hawaiian_Plume","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":241896,"name":"Hawaiian Islands","url":"https://www.academia.edu/Documents/in/Hawaiian_Islands"},{"id":424229,"name":"Sr isotopes","url":"https://www.academia.edu/Documents/in/Sr_isotopes"},{"id":1242196,"name":"Water Depth","url":"https://www.academia.edu/Documents/in/Water_Depth"}],"urls":[{"id":8041975,"url":"http://adsabs.harvard.edu/abs/2009agufm.v41f..07g"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187233"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187233/High_Precision_Pb_Isotope_Systematics_of_Basalts_from_the_Kerguelen_Archipelago_New_Insights_on_the_Kerguelen_Plume_Components"><img alt="Research paper thumbnail of High-Precision Pb Isotope Systematics of Basalts from the Kerguelen Archipelago: New Insights on the Kerguelen Plume Components" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187233/High_Precision_Pb_Isotope_Systematics_of_Basalts_from_the_Kerguelen_Archipelago_New_Insights_on_the_Kerguelen_Plume_Components">High-Precision Pb Isotope Systematics of Basalts from the Kerguelen Archipelago: New Insights on the Kerguelen Plume Components</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The number and origin of components involved in mantle plumes continues to be a subject of intens...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The number and origin of components involved in mantle plumes continues to be a subject of intense debate amongst geochemists. New analytical techniques are now allowing for a more refined analysis of individual oceanic islands. About 60 samples of Kerguelen Archipelago basalts (MgO &gt; 2.3 wt.%) were re-analyzed for their Pb isotopic compositions by MC-ICP-MS (Nu Plasma 015). We carefully selected the samples on the basis of their Sr-Nd-Hf and Pb (TIMS) characteristics in order to cover the range of age, geographic and compositional variations observed on the archipelago. These new high-precision Pb isotopic compositions (2sigma: 100-150 ppm for 206Pb/204Pb and 207Pb/204Pb and 150 ppm for 208Pb/204Pb) reduce the total range of 207Pb/204Pb variations among Kerguelen basalts by a factor of 2. This provides an important new perspective on Kerguelen plume systematics and allows for the clear distinction of three groups: the 29-25 Ma tholeiitic-transitional basalts, the 25-24 Ma mildly alkalic basalts, and the &lt;10 Ma more evolved, alkalic lavas and intrusions. This age and compositional evolution also corresponds to a geographic trend, where the older basalts are closest to the Southeast Indian Ridge (~300-400 km) while the mildly alkalic basalts are further away. The younger, more evolved alkalic rocks occur mainly in the same areas as the mildly alkalic basalts. These alkalic rocks result from lower degrees of melting and their distinctly lower 206Pb/204Pb (and 176Hf/177Hf) together with their significantly younger age indicate some interaction with the older Kerguelen Plateau. These important differences clearly reflect a Miocene change of regime of the Kerguelen plume (Mattielli et al., JP, 2002). Among the flood basalts that cover &gt;80% of the Kerguelen Archipelago, the mildly alkalic basalts of the 24 Ma Crozier volcanic section stand out with distinctly higher 206Pb/204Pb. The isotopic compositions of the Crozier basalts are interpreted as representative of those of the Kerguelen plume. These basaltic magmas had little, if any, interaction with either the surrounding depleted mantle or the Kerguelen Plateau during ascent, either because their magma conduits became isolated or/and because by 24 Ma, the Southeast Indian Ridge was too far away. Our study confirms that the high-precision Pb isotope systematics of basaltic lavas represent an excellent tool to decipher components in major mantle plumes, as has also recently been shown in Hawaii (Eisele et al., G3, submitted; Blichert-Toft et al., G3, submitted).</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187233"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187233"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187233; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187233]").text(description); $(".js-view-count[data-work-id=32187233]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187233; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187233']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187233, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187233]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187233,"title":"High-Precision Pb Isotope Systematics of Basalts from the Kerguelen Archipelago: New Insights on the Kerguelen Plume Components","translated_title":"","metadata":{"abstract":"The number and origin of components involved in mantle plumes continues to be a subject of intense debate amongst geochemists. New analytical techniques are now allowing for a more refined analysis of individual oceanic islands. About 60 samples of Kerguelen Archipelago basalts (MgO \u0026gt; 2.3 wt.%) were re-analyzed for their Pb isotopic compositions by MC-ICP-MS (Nu Plasma 015). We carefully selected the samples on the basis of their Sr-Nd-Hf and Pb (TIMS) characteristics in order to cover the range of age, geographic and compositional variations observed on the archipelago. These new high-precision Pb isotopic compositions (2sigma: 100-150 ppm for 206Pb/204Pb and 207Pb/204Pb and 150 ppm for 208Pb/204Pb) reduce the total range of 207Pb/204Pb variations among Kerguelen basalts by a factor of 2. This provides an important new perspective on Kerguelen plume systematics and allows for the clear distinction of three groups: the 29-25 Ma tholeiitic-transitional basalts, the 25-24 Ma mildly alkalic basalts, and the \u0026lt;10 Ma more evolved, alkalic lavas and intrusions. This age and compositional evolution also corresponds to a geographic trend, where the older basalts are closest to the Southeast Indian Ridge (~300-400 km) while the mildly alkalic basalts are further away. The younger, more evolved alkalic rocks occur mainly in the same areas as the mildly alkalic basalts. These alkalic rocks result from lower degrees of melting and their distinctly lower 206Pb/204Pb (and 176Hf/177Hf) together with their significantly younger age indicate some interaction with the older Kerguelen Plateau. These important differences clearly reflect a Miocene change of regime of the Kerguelen plume (Mattielli et al., JP, 2002). Among the flood basalts that cover \u0026gt;80% of the Kerguelen Archipelago, the mildly alkalic basalts of the 24 Ma Crozier volcanic section stand out with distinctly higher 206Pb/204Pb. The isotopic compositions of the Crozier basalts are interpreted as representative of those of the Kerguelen plume. These basaltic magmas had little, if any, interaction with either the surrounding depleted mantle or the Kerguelen Plateau during ascent, either because their magma conduits became isolated or/and because by 24 Ma, the Southeast Indian Ridge was too far away. Our study confirms that the high-precision Pb isotope systematics of basaltic lavas represent an excellent tool to decipher components in major mantle plumes, as has also recently been shown in Hawaii (Eisele et al., G3, submitted; Blichert-Toft et al., G3, submitted).","publication_date":{"day":null,"month":null,"year":2002,"errors":{}}},"translated_abstract":"The number and origin of components involved in mantle plumes continues to be a subject of intense debate amongst geochemists. New analytical techniques are now allowing for a more refined analysis of individual oceanic islands. About 60 samples of Kerguelen Archipelago basalts (MgO \u0026gt; 2.3 wt.%) were re-analyzed for their Pb isotopic compositions by MC-ICP-MS (Nu Plasma 015). We carefully selected the samples on the basis of their Sr-Nd-Hf and Pb (TIMS) characteristics in order to cover the range of age, geographic and compositional variations observed on the archipelago. These new high-precision Pb isotopic compositions (2sigma: 100-150 ppm for 206Pb/204Pb and 207Pb/204Pb and 150 ppm for 208Pb/204Pb) reduce the total range of 207Pb/204Pb variations among Kerguelen basalts by a factor of 2. This provides an important new perspective on Kerguelen plume systematics and allows for the clear distinction of three groups: the 29-25 Ma tholeiitic-transitional basalts, the 25-24 Ma mildly alkalic basalts, and the \u0026lt;10 Ma more evolved, alkalic lavas and intrusions. This age and compositional evolution also corresponds to a geographic trend, where the older basalts are closest to the Southeast Indian Ridge (~300-400 km) while the mildly alkalic basalts are further away. The younger, more evolved alkalic rocks occur mainly in the same areas as the mildly alkalic basalts. These alkalic rocks result from lower degrees of melting and their distinctly lower 206Pb/204Pb (and 176Hf/177Hf) together with their significantly younger age indicate some interaction with the older Kerguelen Plateau. These important differences clearly reflect a Miocene change of regime of the Kerguelen plume (Mattielli et al., JP, 2002). Among the flood basalts that cover \u0026gt;80% of the Kerguelen Archipelago, the mildly alkalic basalts of the 24 Ma Crozier volcanic section stand out with distinctly higher 206Pb/204Pb. The isotopic compositions of the Crozier basalts are interpreted as representative of those of the Kerguelen plume. These basaltic magmas had little, if any, interaction with either the surrounding depleted mantle or the Kerguelen Plateau during ascent, either because their magma conduits became isolated or/and because by 24 Ma, the Southeast Indian Ridge was too far away. Our study confirms that the high-precision Pb isotope systematics of basaltic lavas represent an excellent tool to decipher components in major mantle plumes, as has also recently been shown in Hawaii (Eisele et al., G3, submitted; Blichert-Toft et al., G3, submitted).","internal_url":"https://www.academia.edu/32187233/High_Precision_Pb_Isotope_Systematics_of_Basalts_from_the_Kerguelen_Archipelago_New_Insights_on_the_Kerguelen_Plume_Components","translated_internal_url":"","created_at":"2017-04-01T10:16:03.261-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"High_Precision_Pb_Isotope_Systematics_of_Basalts_from_the_Kerguelen_Archipelago_New_Insights_on_the_Kerguelen_Plume_Components","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"},{"id":604905,"name":"Oceanic Islands","url":"https://www.academia.edu/Documents/in/Oceanic_Islands"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187237"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187237/Isotopic_Variations_in_the_Post_Shield_Lavas_of_Mauna_Kea_Hualalai_and_Kohala_Evidence_for_a_Koolau_Component"><img alt="Research paper thumbnail of Isotopic Variations in the Post-Shield Lavas of Mauna Kea, Hualalai and Kohala: Evidence for a Koolau Component" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187237/Isotopic_Variations_in_the_Post_Shield_Lavas_of_Mauna_Kea_Hualalai_and_Kohala_Evidence_for_a_Koolau_Component">Isotopic Variations in the Post-Shield Lavas of Mauna Kea, Hualalai and Kohala: Evidence for a Koolau Component</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We have measured O, He, Pb, Sr, and Nd isotope ratios in olivine separates and whole rock powders...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">We have measured O, He, Pb, Sr, and Nd isotope ratios in olivine separates and whole rock powders from post-shield lavas of the island of Hawaii. These small-volume eruptions, which presumably correspond to small-volume source regions in the mantle, serve as high resolution probes of geochemical heterogeneity to complement data available from shield-stage tholeiites that originate in the primary melting region. He, Sr, and Nd ratios show small amplitude variations, well within the range of previously published data indicating little evidence for isotopically anomalous material in the melting region - either recycled sediments or oceanic crust. These data suggest that the plume does not contain large-amplitude isotopic variations at the scale of the source volume of post-shield lavas, which is likely to be about 100 times smaller than the volume averaged during main stage tholeiite production. However, the oxygen and lead isotope data indicate consistent, large amplitude differences between Hualalai and the other volcanoes. Samples from Hualalai have high delta18O (+5.5) and low 206Pb/204Pb (17.888-18.028). The only other volcanoes in the Hawaiian chain with such correlated extreme values are Koolau and Lanai, which have enriched radiogenic isotopic Sr and Nd compositions not seen in the data from Hualalai. Furthermore, correlated low helium values (8-10R/Ra)- high delta18O from Hualalai are consistent with a Koolau component in the source region for this volcano. The high delta18O contra-indicates a significant lithospheric interaction that would probably decrease delta18O rather than increase it to the values we measure. Samples from Mauna Kea and Kohala are consistently lower in delta18O (+4.8-5.12) than those from Hualalai, and fall within the range of previously measured values for late shield-stage lavas. The multiple isotope systems measured on the same post-shield samples indicate that simple models for Kea and Loa trends based on main stage tholeiitic lavas do not capture some of the most significant geochemical features. In particular, there are large temporal variations in the Loa trend, so that the difference between the Loa and Kea trends varies with time.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187237"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187237"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187237; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187237]").text(description); $(".js-view-count[data-work-id=32187237]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187237; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187237']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187237, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187237]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187237,"title":"Isotopic Variations in the Post-Shield Lavas of Mauna Kea, Hualalai and Kohala: Evidence for a Koolau Component","translated_title":"","metadata":{"abstract":"We have measured O, He, Pb, Sr, and Nd isotope ratios in olivine separates and whole rock powders from post-shield lavas of the island of Hawaii. These small-volume eruptions, which presumably correspond to small-volume source regions in the mantle, serve as high resolution probes of geochemical heterogeneity to complement data available from shield-stage tholeiites that originate in the primary melting region. He, Sr, and Nd ratios show small amplitude variations, well within the range of previously published data indicating little evidence for isotopically anomalous material in the melting region - either recycled sediments or oceanic crust. These data suggest that the plume does not contain large-amplitude isotopic variations at the scale of the source volume of post-shield lavas, which is likely to be about 100 times smaller than the volume averaged during main stage tholeiite production. However, the oxygen and lead isotope data indicate consistent, large amplitude differences between Hualalai and the other volcanoes. Samples from Hualalai have high delta18O (+5.5) and low 206Pb/204Pb (17.888-18.028). The only other volcanoes in the Hawaiian chain with such correlated extreme values are Koolau and Lanai, which have enriched radiogenic isotopic Sr and Nd compositions not seen in the data from Hualalai. Furthermore, correlated low helium values (8-10R/Ra)- high delta18O from Hualalai are consistent with a Koolau component in the source region for this volcano. The high delta18O contra-indicates a significant lithospheric interaction that would probably decrease delta18O rather than increase it to the values we measure. Samples from Mauna Kea and Kohala are consistently lower in delta18O (+4.8-5.12) than those from Hualalai, and fall within the range of previously measured values for late shield-stage lavas. The multiple isotope systems measured on the same post-shield samples indicate that simple models for Kea and Loa trends based on main stage tholeiitic lavas do not capture some of the most significant geochemical features. In particular, there are large temporal variations in the Loa trend, so that the difference between the Loa and Kea trends varies with time.","publication_date":{"day":null,"month":null,"year":2005,"errors":{}}},"translated_abstract":"We have measured O, He, Pb, Sr, and Nd isotope ratios in olivine separates and whole rock powders from post-shield lavas of the island of Hawaii. These small-volume eruptions, which presumably correspond to small-volume source regions in the mantle, serve as high resolution probes of geochemical heterogeneity to complement data available from shield-stage tholeiites that originate in the primary melting region. He, Sr, and Nd ratios show small amplitude variations, well within the range of previously published data indicating little evidence for isotopically anomalous material in the melting region - either recycled sediments or oceanic crust. These data suggest that the plume does not contain large-amplitude isotopic variations at the scale of the source volume of post-shield lavas, which is likely to be about 100 times smaller than the volume averaged during main stage tholeiite production. However, the oxygen and lead isotope data indicate consistent, large amplitude differences between Hualalai and the other volcanoes. Samples from Hualalai have high delta18O (+5.5) and low 206Pb/204Pb (17.888-18.028). The only other volcanoes in the Hawaiian chain with such correlated extreme values are Koolau and Lanai, which have enriched radiogenic isotopic Sr and Nd compositions not seen in the data from Hualalai. Furthermore, correlated low helium values (8-10R/Ra)- high delta18O from Hualalai are consistent with a Koolau component in the source region for this volcano. The high delta18O contra-indicates a significant lithospheric interaction that would probably decrease delta18O rather than increase it to the values we measure. Samples from Mauna Kea and Kohala are consistently lower in delta18O (+4.8-5.12) than those from Hualalai, and fall within the range of previously measured values for late shield-stage lavas. The multiple isotope systems measured on the same post-shield samples indicate that simple models for Kea and Loa trends based on main stage tholeiitic lavas do not capture some of the most significant geochemical features. In particular, there are large temporal variations in the Loa trend, so that the difference between the Loa and Kea trends varies with time.","internal_url":"https://www.academia.edu/32187237/Isotopic_Variations_in_the_Post_Shield_Lavas_of_Mauna_Kea_Hualalai_and_Kohala_Evidence_for_a_Koolau_Component","translated_internal_url":"","created_at":"2017-04-01T10:16:04.225-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Isotopic_Variations_in_the_Post_Shield_Lavas_of_Mauna_Kea_Hualalai_and_Kohala_Evidence_for_a_Koolau_Component","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":80308,"name":"Extreme Value Theory","url":"https://www.academia.edu/Documents/in/Extreme_Value_Theory"},{"id":91257,"name":"Stable Isotope","url":"https://www.academia.edu/Documents/in/Stable_Isotope"},{"id":309086,"name":"High Resolution","url":"https://www.academia.edu/Documents/in/High_Resolution"},{"id":702522,"name":"Tethys Oceanic Crust","url":"https://www.academia.edu/Documents/in/Tethys_Oceanic_Crust"}],"urls":[]}, dispatcherData: dispatcherData }); 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The shield of East Molokai volcano, at greater than 1.5 Ma, is the oldest volcano on the Kea trend. Sequences of older tholeiitic to younger alkalic basalt that erupted as this volcano evolved from the shield to postshield stage of volcanism are well exposed. Much younger, $0.34-0.57 Ma, alkalic basalt and basanite erupted during rejuvenated stage volcanism. Like rejuvenated stage lavas erupted at other Hawaiian volcanoes, rejuvenated stage East Molokai lavas have relatively low 87 Sr/ 86 Sr and high 143 Nd/ 144 Nd. Such ratios reflect a source component with a long-term depletion in abundance of incompatible elements. On the basis of positive correlations of 87 Sr/ 86 Sr versus 206 Pb/ 204 Pb and negative correlations of these isotopic ratios with Nb/Zr, a smaller proportion of this depleted component also contributed to the late shield/postshield lavas erupted at East Molokai and the other Kea-trend volcanoes, Haleakala and Mauna Kea. At each of these Kea-trend volcanoes, as the volcano moved away from the hot spot, the extent of melting and magma supply from the mantle decreased, the depth of melt segregation increased, and there was an increasing role for a component with long-term relative depletion in incompatible elements. This depleted component has Kea-trend Pb isotopic characteristics and relatively low 208 Pb/ 204 Pb at a given 206 Pb/ 204 Pb, and it is probably not related to oceanic lithosphere or the source of mid-ocean ridge basalt. The overlap in Sr, Nd, and Pb isotope ratios of recent Kilauea shield lavas and 550 ka Mauna Kea shield lavas has been used to argue that Kea-trend shield volcanism samples a vertically continuous, geochemically distinct stripe which persisted in the hot spot source for 550 kyr . As Kea-trend volcanoes migrate away from the hot spot and evolve from the shield to postshield stage, there are systematic changes in Sr, Nd, and Pb isotope ratios. However, the overlap of Sr, Nd, and Pb isotope ratios in late shield/postshield lavas from Mauna Kea (\u003c350 ka) and East Molokai ($1.5 Ma) show that the periphery of the hot spot sampled by Kea-trend postshield lavas also had long-term geochemical homogeneity.","publication_date":{"day":null,"month":null,"year":2005,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420742},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187261/East_Molokai_and_other_Kea_trend_volcanoes_Magmatic_processes_and_sources_as_they_migrate_away_from_the_Hawaiian_hot_spot","translated_internal_url":"","created_at":"2017-04-01T10:16:10.834-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420742,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420742/thumbnails/1.jpg","file_name":"2004gc00083020170401-6068-tlheki.pdf","download_url":"https://www.academia.edu/attachments/52420742/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"East_Molokai_and_other_Kea_trend_volcano.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420742/2004gc00083020170401-6068-tlheki-libre.pdf?1491067590=\u0026response-content-disposition=attachment%3B+filename%3DEast_Molokai_and_other_Kea_trend_volcano.pdf\u0026Expires=1733034953\u0026Signature=QG2uGeHEw3TiBE0YXnP8Rhf6W1xuVHaBmLHZWnZFr8O84O1CLkpEek8HBsKGgyLf0nixGWuXY0Yllou2NrfNBDXksiHNxktVcn2CB1F8Ts9dwPAB4b-xo4NyDTntsVL~ML~7qIKJsG3Oyj2S7EqUvdtLTaOw8wtPlhI8OPfTMKEZbezOSo0nxHh6R-w4A4QcoLfIWc-hZQKzhfi~u7vVTwlUEMtHQJ1PmM32k8An-oTb3Oche~jQ3B0TkmblgVEQe2CK0cmSDxGcvJqBdthzkmiAq2Bk3fkl6BYGrEGFe77PktmME3lrwfg236FLTqhnNgUV85S~SGNARKnkiY7BoA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"East_Molokai_and_other_Kea_trend_volcanoes_Magmatic_processes_and_sources_as_they_migrate_away_from_the_Hawaiian_hot_spot","translated_slug":"","page_count":28,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420742,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420742/thumbnails/1.jpg","file_name":"2004gc00083020170401-6068-tlheki.pdf","download_url":"https://www.academia.edu/attachments/52420742/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"East_Molokai_and_other_Kea_trend_volcano.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420742/2004gc00083020170401-6068-tlheki-libre.pdf?1491067590=\u0026response-content-disposition=attachment%3B+filename%3DEast_Molokai_and_other_Kea_trend_volcano.pdf\u0026Expires=1733034953\u0026Signature=QG2uGeHEw3TiBE0YXnP8Rhf6W1xuVHaBmLHZWnZFr8O84O1CLkpEek8HBsKGgyLf0nixGWuXY0Yllou2NrfNBDXksiHNxktVcn2CB1F8Ts9dwPAB4b-xo4NyDTntsVL~ML~7qIKJsG3Oyj2S7EqUvdtLTaOw8wtPlhI8OPfTMKEZbezOSo0nxHh6R-w4A4QcoLfIWc-hZQKzhfi~u7vVTwlUEMtHQJ1PmM32k8An-oTb3Oche~jQ3B0TkmblgVEQe2CK0cmSDxGcvJqBdthzkmiAq2Bk3fkl6BYGrEGFe77PktmME3lrwfg236FLTqhnNgUV85S~SGNARKnkiY7BoA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":224577,"name":"Trace Elements","url":"https://www.academia.edu/Documents/in/Trace_Elements"},{"id":342071,"name":"Hot Spot","url":"https://www.academia.edu/Documents/in/Hot_Spot"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"}],"urls":[]}, dispatcherData: dispatcherData }); 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new insights from high-precision Pb isotopes</a></div><div class="wp-workCard_item"><span>Geochimica et Cosmochimica Acta</span><span>, 2006</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187263"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187263"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187263; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186912"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186912/Significance_of_Picritic_and_Tholeiitic_Lavas_Within_Wrangellia_Flood_Basalts_on_Vancouver_Island_for_the_Melting_History_and_Magmatic_Evolution_of_a_Major_Oceanic_Plateau"><img alt="Research paper thumbnail of Significance of Picritic and Tholeiitic Lavas Within Wrangellia Flood Basalts on Vancouver Island for the Melting History and Magmatic Evolution of a Major Oceanic Plateau" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186912/Significance_of_Picritic_and_Tholeiitic_Lavas_Within_Wrangellia_Flood_Basalts_on_Vancouver_Island_for_the_Melting_History_and_Magmatic_Evolution_of_a_Major_Oceanic_Plateau">Significance of Picritic and Tholeiitic Lavas Within Wrangellia Flood Basalts on Vancouver Island for the Melting History and Magmatic Evolution of a Major Oceanic Plateau</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Geochemical studies of lavas from the accreted Wrangellia oceanic plateau forming a large part of...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Geochemical studies of lavas from the accreted Wrangellia oceanic plateau forming a large part of Vancouver Island (~20,000 km2) in the Pacific Northwest of North America offer a view of the melting history of plume-derived magmas that does not involve continental lithosphere and where source heterogeneity does not play a major role. The Late Triassic Wrangellia flood basalts (~229-226 Ma) are predominantly homogeneous tholeiitic basalt. However, the lower submarine part of the 6 km-thick stratigraphy, on northern Vancouver Island, contains picritic pillow basalts. These high-MgO (9-20 wt%) lavas are depleted in LREE (La/YbCN= 0.5 ± 0.2), whereas the tholeiitic lavas (6-8 wt% MgO) are LREE-enriched (La/YbCN= 2.2 ± 0.3). Both lava groups have overlapping initial εHf (+10.3 ± 2.1) and εHf Nd (+7.7 ± 1.3), indicating a common, depleted (but not MORB) Pacific mantle source similar to the source of basalts from the Ontong Java and Caribbean Plateaus. The presence of picritic lavas indica...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186912"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186912"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186912; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186912]").text(description); $(".js-view-count[data-work-id=32186912]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186912; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186912']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186912, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186912]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186912,"title":"Significance of Picritic and Tholeiitic Lavas Within Wrangellia Flood Basalts on Vancouver Island for the Melting History and Magmatic Evolution of a Major Oceanic Plateau","translated_title":"","metadata":{"abstract":"Geochemical studies of lavas from the accreted Wrangellia oceanic plateau forming a large part of Vancouver Island (~20,000 km2) in the Pacific Northwest of North America offer a view of the melting history of plume-derived magmas that does not involve continental lithosphere and where source heterogeneity does not play a major role. 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The presence of picritic lavas indica...","publication_date":{"day":null,"month":null,"year":2007,"errors":{}}},"translated_abstract":"Geochemical studies of lavas from the accreted Wrangellia oceanic plateau forming a large part of Vancouver Island (~20,000 km2) in the Pacific Northwest of North America offer a view of the melting history of plume-derived magmas that does not involve continental lithosphere and where source heterogeneity does not play a major role. The Late Triassic Wrangellia flood basalts (~229-226 Ma) are predominantly homogeneous tholeiitic basalt. However, the lower submarine part of the 6 km-thick stratigraphy, on northern Vancouver Island, contains picritic pillow basalts. These high-MgO (9-20 wt%) lavas are depleted in LREE (La/YbCN= 0.5 ± 0.2), whereas the tholeiitic lavas (6-8 wt% MgO) are LREE-enriched (La/YbCN= 2.2 ± 0.3). 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Sco...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... a , Corresponding Author Contact Information , E-mail The Corresponding Author , James S. Scoates a , Dominique Weis a and Steve Israel b. ... is predominantly massive tholeiitic subaerial flows (~ 1000 m) with no intervening sediments and a thin zone of pillow breccia along the ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186906"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186906"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186906; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186906]").text(description); $(".js-view-count[data-work-id=32186906]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186906; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186906']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186906, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186906]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186906,"title":"Geochemistry of Triassic flood basalts from the Yukon (Canada) segment of the accreted Wrangellia oceanic plateau","translated_title":"","metadata":{"abstract":"... a , Corresponding Author Contact Information , E-mail The Corresponding Author , James S. Scoates a , Dominique Weis a and Steve Israel b. ... is predominantly massive tholeiitic subaerial flows (~ 1000 m) with no intervening sediments and a thin zone of pillow breccia along the ...","publication_date":{"day":null,"month":null,"year":2009,"errors":{}},"publication_name":"Lithos"},"translated_abstract":"... a , Corresponding Author Contact Information , E-mail The Corresponding Author , James S. Scoates a , Dominique Weis a and Steve Israel b. ... is predominantly massive tholeiitic subaerial flows (~ 1000 m) with no intervening sediments and a thin zone of pillow breccia along the ...","internal_url":"https://www.academia.edu/32186906/Geochemistry_of_Triassic_flood_basalts_from_the_Yukon_Canada_segment_of_the_accreted_Wrangellia_oceanic_plateau","translated_internal_url":"","created_at":"2017-04-01T10:05:29.081-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304418,"work_id":32186906,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Geochemistry of Triassic flood basalts from the Yukon (Canada) segment of the accreted Wrangellia oceanic plateau"}],"downloadable_attachments":[],"slug":"Geochemistry_of_Triassic_flood_basalts_from_the_Yukon_Canada_segment_of_the_accreted_Wrangellia_oceanic_plateau","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":11404,"name":"Titanium","url":"https://www.academia.edu/Documents/in/Titanium"},{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186905"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186905/Caribbean_island_arc_rifting_and_back_arc_basin_development_in_the_Late_Cretaceous_Geochemical_isotopic_and_geochronological_evidence_from_Central_Hispaniola"><img alt="Research paper thumbnail of Caribbean island-arc rifting and back-arc basin development in the Late Cretaceous: Geochemical, isotopic and geochronological evidence from Central Hispaniola" class="work-thumbnail" src="https://attachments.academia-assets.com/52420542/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186905/Caribbean_island_arc_rifting_and_back_arc_basin_development_in_the_Late_Cretaceous_Geochemical_isotopic_and_geochronological_evidence_from_Central_Hispaniola">Caribbean island-arc rifting and back-arc basin development in the Late Cretaceous: Geochemical, isotopic and geochronological evidence from Central Hispaniola</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/MarcJoubert">Marc Joubert</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a></span></div><div class="wp-workCard_item"><span>Lithos</span><span>, 2008</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="652a33a2067ec8c7b5fcb6e8b820a084" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420542,"asset_id":32186905,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420542/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186905"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186905"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186905; 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "652a33a2067ec8c7b5fcb6e8b820a084" } } $('.js-work-strip[data-work-id=32186905]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186905,"title":"Caribbean island-arc rifting and back-arc basin development in the Late Cretaceous: Geochemical, isotopic and geochronological evidence from Central Hispaniola","translated_title":"","metadata":{"ai_title_tag":"Late Cretaceous Caribbean Arc Rifting in Hispaniola","grobid_abstract":"We present new regional petrologic, geochemical, Sr-Nd isotopic, and U-Pb geochronological data on the Turonian-Campanian mafic igneous rocks of Central Hispaniola that provide important clues on the development of the Caribbean island-arc. Central Hispaniola is made up of three main tectonic blocks-Jicomé, Jarabacoa and Bonao-that include four broad geochemical groups of Late Cretaceous mafic igneous rocks: group I, tholeiitic to calc-alkaline basalts and andesites; group II, low-Ti high-Mg andesites and basalts; group III, tholeiitic basalts and gabbros/ dolerites; and group IV, tholeiitic to transitional and alkalic basalts. These igneous rocks show significant differences in time and space, from arclike to non-arc-like characteristics, suggesting that they were derived from different mantle sources. We interpret these groups as the record of Caribbean arc-rifting and back-arc basin development in the Late Cretaceous. TheN 90 Ma group I volcanic rocks and associated cumulate complexes preserved in the Jicomé and Jarabacoa blocks represent the Albian to Cenomanian Caribbean island-arc material. The arc rift stage magmatism in these blocks took place during the deposition of the Restauración Formation from the Turonian-Coniacian transition (~90 Ma) to Santonian/Lower Campanian, particularly in its lower part with extrusion at 90-88 Ma of group II low-Ti, high-Mg andesites/basalts. During this time or slightly afterwards adakitic rhyolites erupted in the Jarabacoa block. Group III tholeiitic lavas represent the initiation of Coniacian-Lower Campanian back-arc spreading. In the Bonao block, this stage is represented by back-arc basin-like basalts, gabbros and dolerite/diorite dykes intruded into the Loma Caribe peridotite, as well as the Peralvillo Sur Formation basalts, capped by tuffs, shales and Campanian cherts. This dismembered ophiolitic stratigraphy indicates that the Bonao block is a fragment of an ensimatic back-arc basin. In the Jicomé and Jarabacoa blocks, the mainly Campanian group IV basalts of the Peña Blanca, Siete Cabezas and Pelona-Pico Duarte Formation, represent the subsequent stage of back-arc spreading and off-axis non-arc-like magmatism, caused by migration of the arc toward the northeast. These basalts have geochemical affinities with the mantle domain influenced by the Caribbean plume, suggesting that mantle was flowing toward the NE, beneath the extended Caribbean island-arc, in response to rollback of the subducting proto-Caribbean slab.","publication_date":{"day":null,"month":null,"year":2008,"errors":{}},"publication_name":"Lithos","grobid_abstract_attachment_id":52420542},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186905/Caribbean_island_arc_rifting_and_back_arc_basin_development_in_the_Late_Cretaceous_Geochemical_isotopic_and_geochronological_evidence_from_Central_Hispaniola","translated_internal_url":"","created_at":"2017-04-01T10:05:28.946-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304386,"work_id":32186905,"tagging_user_id":62411756,"tagged_user_id":62863314,"co_author_invite_id":6176432,"email":"m***t@hotmail.com","display_order":0,"name":"Marc Joubert","title":"Caribbean island-arc rifting and back-arc basin development in the Late Cretaceous: Geochemical, isotopic and geochronological evidence from Central Hispaniola"},{"id":28304393,"work_id":32186905,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176433,"email":"t***h@nps.gov","display_order":4194304,"name":"Thomas Ulrich","title":"Caribbean island-arc rifting and back-arc basin development in the Late Cretaceous: Geochemical, isotopic and geochronological evidence from Central Hispaniola"}],"downloadable_attachments":[{"id":52420542,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420542/thumbnails/1.jpg","file_name":"Caribbean_island-arc_rifting_and_back-ar20170401-6059-qz13pv.pdf","download_url":"https://www.academia.edu/attachments/52420542/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Caribbean_island_arc_rifting_and_back_ar.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420542/Caribbean_island-arc_rifting_and_back-ar20170401-6059-qz13pv-libre.pdf?1491067266=\u0026response-content-disposition=attachment%3B+filename%3DCaribbean_island_arc_rifting_and_back_ar.pdf\u0026Expires=1733034953\u0026Signature=CmdGrJ0PPbAjlZXEn23k4U-MvYsW2eqUgEN53ATzywuUxE6PREmcAXhmeeJRo0uNiZB5z4xAUaWonsvhtChxnSSrIFlyzSQ5oUGCw-MWU9RXrB3pdQCpWjVCw3wF-isl8dE55rNAfN9e-TuScoraRrJ6CBI7B3f2-vnaR3ZAFTdKihFlNj8sFldKieq97bRw9VkhXnrDJpICDxpwudt-lmkpPbgsSmUZtDWBvSFED5tNc4-oDivwewr9it-MvevkJ4nYCILOoG0pCbcsnadIh-t2fiJcK26rPs3cBSR~yAgA-900SM4MoDQe5QAy-RkGAF~LCaDIqsEdsmLyHGMm~A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Caribbean_island_arc_rifting_and_back_arc_basin_development_in_the_Late_Cretaceous_Geochemical_isotopic_and_geochronological_evidence_from_Central_Hispaniola","translated_slug":"","page_count":28,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420542,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420542/thumbnails/1.jpg","file_name":"Caribbean_island-arc_rifting_and_back-ar20170401-6059-qz13pv.pdf","download_url":"https://www.academia.edu/attachments/52420542/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Caribbean_island_arc_rifting_and_back_ar.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420542/Caribbean_island-arc_rifting_and_back-ar20170401-6059-qz13pv-libre.pdf?1491067266=\u0026response-content-disposition=attachment%3B+filename%3DCaribbean_island_arc_rifting_and_back_ar.pdf\u0026Expires=1733034953\u0026Signature=CmdGrJ0PPbAjlZXEn23k4U-MvYsW2eqUgEN53ATzywuUxE6PREmcAXhmeeJRo0uNiZB5z4xAUaWonsvhtChxnSSrIFlyzSQ5oUGCw-MWU9RXrB3pdQCpWjVCw3wF-isl8dE55rNAfN9e-TuScoraRrJ6CBI7B3f2-vnaR3ZAFTdKihFlNj8sFldKieq97bRw9VkhXnrDJpICDxpwudt-lmkpPbgsSmUZtDWBvSFED5tNc4-oDivwewr9it-MvevkJ4nYCILOoG0pCbcsnadIh-t2fiJcK26rPs3cBSR~yAgA-900SM4MoDQe5QAy-RkGAF~LCaDIqsEdsmLyHGMm~A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":142791,"name":"Caribou","url":"https://www.academia.edu/Documents/in/Caribou"},{"id":148652,"name":"Late Cretaceous","url":"https://www.academia.edu/Documents/in/Late_Cretaceous"},{"id":281807,"name":"Mantle melting","url":"https://www.academia.edu/Documents/in/Mantle_melting"},{"id":688910,"name":"Volcanic Rock","url":"https://www.academia.edu/Documents/in/Volcanic_Rock"},{"id":840115,"name":"Island Arc","url":"https://www.academia.edu/Documents/in/Island_Arc"},{"id":1993786,"name":"Cumulant","url":"https://www.academia.edu/Documents/in/Cumulant"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186896"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186896/Melting_History_and_Magmatic_Evolution_of_Basalts_and_Picrites_from_the_Accreted_Wrangellia_Oceanic_Plateau_Vancouver_Island_Canada"><img alt="Research paper thumbnail of Melting History and Magmatic Evolution of Basalts and Picrites from the Accreted Wrangellia Oceanic Plateau, Vancouver Island, Canada" class="work-thumbnail" src="https://attachments.academia-assets.com/52420567/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186896/Melting_History_and_Magmatic_Evolution_of_Basalts_and_Picrites_from_the_Accreted_Wrangellia_Oceanic_Plateau_Vancouver_Island_Canada">Melting History and Magmatic Evolution of Basalts and Picrites from the Accreted Wrangellia Oceanic Plateau, Vancouver Island, Canada</a></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, 2009</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d538e9828f7f1359fa7810b746c39acd" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420567,"asset_id":32186896,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420567/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186896"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186896"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186896; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186896]").text(description); $(".js-view-count[data-work-id=32186896]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186896; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186896']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186896, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d538e9828f7f1359fa7810b746c39acd" } } $('.js-work-strip[data-work-id=32186896]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186896,"title":"Melting History and Magmatic Evolution of Basalts and Picrites from the Accreted Wrangellia Oceanic Plateau, Vancouver Island, Canada","translated_title":"","metadata":{"grobid_abstract":"The accreted Wrangellia oceanic plateau in the Pacific Northwest of North America provides important insights into the volcanic architecture of major oceanic plateaus, as well as the nature of their mantle source, conditions of melting and subsequent magmatic evolution. The $20 000 km 2 Karmutsen Formation flood basalts (Vancouver Island) were emplaced at c. 225^230 Ma onto Middle Triassic marine sediments and Late Devonian to Early Permian island-arc volcanic and sedimentary sequences, and are overlain by Late Triassic platformal carbonates. The basalts form an emergent sequence consisting of a basal sediment^sill complex (600^900 m thick), pillowed and massive submarine flows (42Á5 km), pillow breccia and hyaloclastite (51Á5 km), and massive subaerial flows (52Á5 km). Although the Karmutsen Formation is predominantly composed of tholeiitic basalt, the submarine part of the stratigraphy on northern Vancouver Island also contains picritic basalts. These high-MgO (9^20 wt %) lavas are depleted in light rare earth elements (LREE; La/Yb CN ¼ 0Á5 AE 0Á2), whereas the tholeiitic lavas (6^8 wt % MgO) are LREE-enriched (La/Yb CN ¼ 2Á2 AE 0Á3). Both lava groups have overlapping initial e Hf (þ10Á3 AE 2Á1) and e Nd (þ7Á7 AE1Á3), indicating a common, plume-type Pacific mantle source with geochemical characteristics similar to the source of basalts from the Ontong Java and Caribbean plateaus. Major-element modeling results indicate that the picrites formed by extensive melting (23^27%) of anomalously hot mantle ($15008C), which is consistent with a mantle plume initiation model for formation of the Karmutsen flood basalts on Vancouver Island. Trace element constraints indicate that the picrites require melting of a depleted spinel lherzolite source, whereas the tholeiitic basalts involved melting of garnet and spinel lherzolite. The tholeiitic basalts underwent significant fractional crystallization (450%) and the fractionated residues may be represented by high-velocity rocks beneath Vancouver Island identified from seismic reflection studies.","publication_date":{"day":null,"month":null,"year":2009,"errors":{}},"publication_name":"Journal of Petrology","grobid_abstract_attachment_id":52420567},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186896/Melting_History_and_Magmatic_Evolution_of_Basalts_and_Picrites_from_the_Accreted_Wrangellia_Oceanic_Plateau_Vancouver_Island_Canada","translated_internal_url":"","created_at":"2017-04-01T10:05:27.660-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304408,"work_id":32186896,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Melting History and Magmatic Evolution of Basalts and Picrites from the Accreted Wrangellia Oceanic Plateau, Vancouver Island, Canada"},{"id":28304506,"work_id":32186896,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176438,"email":"b***r@eos.ubc.ca","display_order":4194304,"name":"Bruno Kieffer","title":"Melting History and Magmatic Evolution of Basalts and Picrites from the Accreted Wrangellia Oceanic Plateau, Vancouver Island, Canada"},{"id":28304661,"work_id":32186896,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176476,"email":"g***n@gov.bc.ca","display_order":6291456,"name":"Graham Nixon","title":"Melting History and Magmatic Evolution of Basalts and Picrites from the Accreted Wrangellia Oceanic Plateau, Vancouver Island, Canada"}],"downloadable_attachments":[{"id":52420567,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420567/thumbnails/1.jpg","file_name":"Melting_History_and_Magmatic_Evolution_o20170401-6068-1byfjkf.pdf","download_url":"https://www.academia.edu/attachments/52420567/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Melting_History_and_Magmatic_Evolution_o.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420567/Melting_History_and_Magmatic_Evolution_o20170401-6068-1byfjkf-libre.pdf?1491067492=\u0026response-content-disposition=attachment%3B+filename%3DMelting_History_and_Magmatic_Evolution_o.pdf\u0026Expires=1733097977\u0026Signature=P48ZhEJ3lhvyOXWQ8P1D1ecNdzdRa876N4fvIPExmQzo01Bq2k-KiXkq25FXbxiT8um4ICN2mP44oRZE5NVQVkpvoPLLHVCn0TSbWGM3yj7WyNaQBcGYu-XmLRvHpOJE76qNfUOyM0lbktTxITci~dsSRclx4JHmylgUZF4Mn0r1OYFoyhvElqec3kUUPKmrB9O9b3~BbBZF6fmj4WZ83~4blv58c2XcvBEz0gQyuG5FkBTAblcocirsIgeOwpirXlubTG3FbhcddyHQSuG8U0rVeSDtK7LdyZGytfEw-DbVDL-b0tqvkEAIzIfbdgIY5MPpYciakNhCWtKCmS8UgQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Melting_History_and_Magmatic_Evolution_of_Basalts_and_Picrites_from_the_Accreted_Wrangellia_Oceanic_Plateau_Vancouver_Island_Canada","translated_slug":"","page_count":50,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420567,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420567/thumbnails/1.jpg","file_name":"Melting_History_and_Magmatic_Evolution_o20170401-6068-1byfjkf.pdf","download_url":"https://www.academia.edu/attachments/52420567/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Melting_History_and_Magmatic_Evolution_o.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420567/Melting_History_and_Magmatic_Evolution_o20170401-6068-1byfjkf-libre.pdf?1491067492=\u0026response-content-disposition=attachment%3B+filename%3DMelting_History_and_Magmatic_Evolution_o.pdf\u0026Expires=1733097977\u0026Signature=P48ZhEJ3lhvyOXWQ8P1D1ecNdzdRa876N4fvIPExmQzo01Bq2k-KiXkq25FXbxiT8um4ICN2mP44oRZE5NVQVkpvoPLLHVCn0TSbWGM3yj7WyNaQBcGYu-XmLRvHpOJE76qNfUOyM0lbktTxITci~dsSRclx4JHmylgUZF4Mn0r1OYFoyhvElqec3kUUPKmrB9O9b3~BbBZF6fmj4WZ83~4blv58c2XcvBEz0gQyuG5FkBTAblcocirsIgeOwpirXlubTG3FbhcddyHQSuG8U0rVeSDtK7LdyZGytfEw-DbVDL-b0tqvkEAIzIfbdgIY5MPpYciakNhCWtKCmS8UgQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology"},{"id":235502,"name":"Vancouver Island","url":"https://www.academia.edu/Documents/in/Vancouver_Island"}],"urls":[]}, dispatcherData: dispatcherData }); 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Geochemical, Sr-Nd isotope, and 40 Ar-39 Ar radiometric age data combined with detailed mapping have shown that the Duarte Complex includes two lithostratigraphic units, composed of four geochemical groups of metavolcanic rocks: Group Ia, low-Ti high-Mg basalts, and group Ib, high-Ti picrites and primitive high-Mg basalts, occur interlayered in the lowermost levels of the lower unit; group II, light rare earth element (LREE)-enriched picrites, ferropicrites and high-Mg basalts, forms the main lava sequence of the lower unit; and group III, LREE-enriched Fe-Ti basalts, is present exclusively in the upper unit. Nd isotope and incompatible trace element patterns are diverse in the Duarte Complex metavolcanics and are consistent with mantle sources related to a heterogeneous plume. Mantle melt modeling suggests that an early, extensive melting (10-20%) of shallow mantle resulted in the formation of relatively depleted group I and II magmas, whereas the late, more enriched group III magmas were the product of deeper, low-degree (\u003c3%) melting of a heterogeneous plume. Therefore plume mantle sources were more enriched and deeper through time. Foliated amphibolites of the Duarte Complex yield 40 Ar-39 Ar hornblende plateau ages of 93.9 ± 1.4 and 95.8 ± 1.9 Ma (Cenomanian, 99.6-93.5 Ma) that demonstrate an older age of the protholiths, probably Albian (\u003e96 Ma). Hence an Early Cretaceous phase of the Caribbean-Colombian oceanic plateau construction is recorded in Hispaniola.","publication_date":{"day":null,"month":null,"year":2007,"errors":{}},"publication_name":"Journal of Geophysical Research","grobid_abstract_attachment_id":52420514},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186895/Plume_mantle_source_heterogeneity_through_time_Insights_from_the_Duarte_Complex_Hispaniola_northeastern_Caribbean","translated_internal_url":"","created_at":"2017-04-01T10:05:27.545-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304385,"work_id":32186895,"tagging_user_id":62411756,"tagged_user_id":62863314,"co_author_invite_id":6176432,"email":"m***t@hotmail.com","display_order":0,"name":"Marc Joubert","title":"Plume mantle source heterogeneity through time: Insights from the Duarte Complex, Hispaniola, 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hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186881/Wrangellia_flood_basalts_in_Alaska_A_record_of_plume_lithosphere_interaction_in_a_Late_Triassic_accreted_oceanic_plateau"><img alt="Research paper thumbnail of Wrangellia flood basalts in Alaska: A record of plume-lithosphere interaction in a Late Triassic accreted oceanic plateau" class="work-thumbnail" src="https://attachments.academia-assets.com/52420501/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186881/Wrangellia_flood_basalts_in_Alaska_A_record_of_plume_lithosphere_interaction_in_a_Late_Triassic_accreted_oceanic_plateau">Wrangellia flood basalts in Alaska: A record of plume-lithosphere interaction in a Late Triassic accreted oceanic plateau</a></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2008</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="f3acddcc928b9bddf4a3ce616a76eb74" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420501,"asset_id":32186881,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420501/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186881"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa 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They provide important constraints on the construction of these vast submarine edifices and the source and temporal evolution of magmas for a plume head impinging beneath oceanic lithosphere. Wrangellia flood basalts ($231-225 Ma) extend $450 km across southern Alaska (Wrangell Mountains and Alaska Range) where $3.5 km of mostly subaerial flows are bounded by late Paleozoic arc volcanics and Late Triassic limestone. The vast majority of the flood basalts are light rare earth element (LREE) -enriched high-Ti basalt (1.6-2.4 wt % TiO 2 ) with uniform ocean island basalt (OIB) -type Pacific mantle isotopic compositions (e Hf (t) = +9.7 to +10.7; e Nd (t) = +6.0 to +8.1; t = 230 Ma). However, the lowest $400 m of stratigraphy in the Alaska Range is LREE-depleted low-Ti basalt (0.4-1.2 wt % TiO 2 ) with pronounced negative high field strength element (HFSE) anomalies and Hf isotopic compositions (e Hf (t) = +13.7 to +18.4) that are decoupled from Nd (e Nd (t) = +4.6 to +5.4) and displaced well above the OIB mantle array (De Hf = +4 to +8). The radiogenic Hf of the low-Ti basalts indicates involvement of a component that evolved with high Lu/Hf over time but not with a correspondingly high Sm/Nd. The radiogenic Hf and HFSE-depleted signature of the low-Ti basalts suggest pre-existing arc lithosphere was involved in the formation of flood basalts that erupted early in construction of part of the Wrangellia plateau in Alaska. Thermal and mechanical erosion of the base of the lithosphere by the impinging plume head may have led to melting of arc lithosphere or interaction of plume-derived melts and subduction-modified mantle. The high-Ti lavas dominate the main phase of construction of the plateau and were derived from a depleted mantle source distinct from the source of MORB and with compositional similarities to that of ocean islands (e.g., Hawaii) and plateaus (e.g., Ontong Java) in the Pacific Ocean.","publication_date":{"day":null,"month":null,"year":2008,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420501},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186881/Wrangellia_flood_basalts_in_Alaska_A_record_of_plume_lithosphere_interaction_in_a_Late_Triassic_accreted_oceanic_plateau","translated_internal_url":"","created_at":"2017-04-01T10:05:25.609-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304400,"work_id":32186881,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"Wrangellia flood basalts in Alaska: A record of plume-lithosphere interaction in a Late Triassic accreted oceanic plateau"},{"id":28305104,"work_id":32186881,"tagging_user_id":62411756,"tagged_user_id":62620760,"co_author_invite_id":6176604,"email":"a***e@soest.hawaii.edu","display_order":4194304,"name":"Andrew Greene","title":"Wrangellia flood basalts in Alaska: A record of plume-lithosphere interaction in a Late Triassic accreted oceanic plateau"}],"downloadable_attachments":[{"id":52420501,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420501/thumbnails/1.jpg","file_name":"Wrangellia_flood_basalts_in_Alaska_A_rec20170401-6068-gfh704.pdf","download_url":"https://www.academia.edu/attachments/52420501/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Wrangellia_flood_basalts_in_Alaska_A_rec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420501/Wrangellia_flood_basalts_in_Alaska_A_rec20170401-6068-gfh704-libre.pdf?1491067328=\u0026response-content-disposition=attachment%3B+filename%3DWrangellia_flood_basalts_in_Alaska_A_rec.pdf\u0026Expires=1733097977\u0026Signature=R0Nbmi2hJbYjWm5BfDKXM8jjBlPbxelzBqpyZ6EcbYMkYycyIke6fscjrSo2SDO5D2dwbrpsNWcaGsEpncfpJGwbgI5Ei7R1GIyNal4g9mPRsgPH95kOpTUWikWRroQfLh1xvNv7qKk2H36HNHhmtut~86ShEI0IaE0g2KZXihYVfmsPG-Mk5MN-pTBmWXI2-5CGAOC69UEPt1iPIQZs7hskf9VlCD~X93nc5fJXUREIekmfkqVMIS6-Wohn1qe9JX~j841Gkq3OgLABCxNHZyJCZ66J~skBQOnZoyTiu7WhKj9EACpSBGsyESdbU7hr9qj7WNuFC~NIKMkHn5ZdNw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Wrangellia_flood_basalts_in_Alaska_A_record_of_plume_lithosphere_interaction_in_a_Late_Triassic_accreted_oceanic_plateau","translated_slug":"","page_count":34,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420501,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420501/thumbnails/1.jpg","file_name":"Wrangellia_flood_basalts_in_Alaska_A_rec20170401-6068-gfh704.pdf","download_url":"https://www.academia.edu/attachments/52420501/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Wrangellia_flood_basalts_in_Alaska_A_rec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420501/Wrangellia_flood_basalts_in_Alaska_A_rec20170401-6068-gfh704-libre.pdf?1491067328=\u0026response-content-disposition=attachment%3B+filename%3DWrangellia_flood_basalts_in_Alaska_A_rec.pdf\u0026Expires=1733097977\u0026Signature=R0Nbmi2hJbYjWm5BfDKXM8jjBlPbxelzBqpyZ6EcbYMkYycyIke6fscjrSo2SDO5D2dwbrpsNWcaGsEpncfpJGwbgI5Ei7R1GIyNal4g9mPRsgPH95kOpTUWikWRroQfLh1xvNv7qKk2H36HNHhmtut~86ShEI0IaE0g2KZXihYVfmsPG-Mk5MN-pTBmWXI2-5CGAOC69UEPt1iPIQZs7hskf9VlCD~X93nc5fJXUREIekmfkqVMIS6-Wohn1qe9JX~j841Gkq3OgLABCxNHZyJCZ66J~skBQOnZoyTiu7WhKj9EACpSBGsyESdbU7hr9qj7WNuFC~NIKMkHn5ZdNw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"}],"urls":[]}, dispatcherData: dispatcherData }); 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La secuencia magmática del Jurásico Superior-Cretácico superior de la Cordillera Central, República Dominicana. Boletín Geológico y Minero, 118 (2): 243-268 (5) I.C.T. Jaume Almera-CSIC. Lluís Solé i Sabarís s/n. 08028 Barcelona. 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data-work-id="32179578"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32179578/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area"><img alt="Research paper thumbnail of Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area" class="work-thumbnail" src="https://attachments.academia-assets.com/52414196/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32179578/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area">Whole-rock geochemistry and Sr-, Nd-, and Pb-isotopic characteristics of undeformed, deformed, and recrystallized gabbros from Sites 921, 922, and 923 in the MARK area</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/Hertogen">Jan Hertogen</a></span></div><div class="wp-workCard_item"><span>Proceedings of the Ocean Drilling Program Scientific Results</span><span>, 1997</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="8e57eea26151ab0d1373cffb4b28bdb9" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52414196,"asset_id":32179578,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52414196/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32179578"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32179578"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var 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area","translated_title":"","metadata":{"grobid_abstract":"Gabbros and diabases from Layer 3 of the oceanic lithosphere were recovered from the western wall of the Mid-Atlantic Rift Valley near the Kane Fracture Zone (23.5°N, 45°W) during Ocean Drilling Program Leg 153. Thirty-five gabbroic samples from Sites 921 to 923 and three diabases from Sites 920 and 921 have been analyzed for major and trace elements. The gabbroic samples were chosen to be representative of range of composition and variation in degree of deformation. Sr-, Nd-, and Pb-isotope ratios were measured for 19 of the gabbros and a single diabase.","publication_date":{"day":null,"month":null,"year":1997,"errors":{}},"publication_name":"Proceedings of the Ocean Drilling Program Scientific Results","grobid_abstract_attachment_id":52414196},"translated_abstract":null,"internal_url":"https://www.academia.edu/32179578/Whole_rock_geochemistry_and_Sr_Nd_and_Pb_isotopic_characteristics_of_undeformed_deformed_and_recrystallized_gabbros_from_Sites_921_922_and_923_in_the_MARK_area","translated_internal_url":"","created_at":"2017-04-01T01:03:38.095-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62397373,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28298630,"work_id":32179578,"tagging_user_id":62397373,"tagged_user_id":62411756,"co_author_invite_id":6175232,"email":"d***s@eos.ubc.ca","affiliation":"University of British Columbia","display_order":0,"name":"Dominique 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187119"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187119/Fault_controlled_hydrothermal_fluid_flow_at_the_EPR"><img alt="Research paper thumbnail of Fault-controlled hydrothermal fluid flow at the EPR" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187119/Fault_controlled_hydrothermal_fluid_flow_at_the_EPR">Fault-controlled hydrothermal fluid flow at the EPR</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Investigation of an axial mid-ocean ridge fault to determine the character of focused hydrotherma...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Investigation of an axial mid-ocean ridge fault to determine the character of focused hydrothermal fluid flow. Tectonic escarpments at Pito Deep expose ocean crust formed at the super-fast spreading portion of the southern EPR (ca. 3 Ma). Ocean crust from Pito Deep is cut by high angle axial faults striking NE-SW parallel to the sheeted dykes. We focus on trace element and Sr isotopic compositional variations across an approximately 35 m fault zone within the sheeted dyke complex, ca. 100m below the lava-dyke transition, to explore the relationship between fluid flow, alteration and deformation. Samples from across this axial fault can be divided into 1) wall-rock basalts, 2) fault zone basalts and 3) fault zone breccias, ranging from simple cataclasites, veined cataclasites to quartz cataclasites. Breccias and basalts occur closely juxtaposed within the fault zone suggesting heterogeneous, highly localized deformation and fluid flow. Wall-rock basalts have been sampled a few to 30 m away from the fault zone and show extents of alteration typical of dykes away from fault zones with dominant replacement of primary phases by amphibole. The alteration in the fault zone basalts is also amphibole dominated with wider veins than the wall-rocks of quartz, chlorite ± amphibole. The fault zone breccias range in alteration mineralogy from chlorite to quartz dominated assemblages. Wall rock and fault zone basalts have similar trace element compositions to fresh crust. Breccias show large deviations in trace element compositions in comparison to adjacent altered basalts, with depletion of highly mobile elements such as K, Sr and both enrichment and depletion of Cu and Zn. 87Sr/86Sr of the dykes away from the fault zones are slightly elevated over fresh oceanic crust (0.7025- 0.7029) and fault zone samples have similar to higher 87Sr/86Sr. Quartz-epidote veins precipitated from fluids at Pito Deep have 87Sr/86Sr of approximately 0.7040. These new data provide insight into the chemical evolution of axial hydrothermal fluids during focused fluid flow.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187119"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187119"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187119; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187119]").text(description); $(".js-view-count[data-work-id=32187119]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187119; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187119']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187119, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187119]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187119,"title":"Fault-controlled hydrothermal fluid flow at the EPR","translated_title":"","metadata":{"abstract":"Investigation of an axial mid-ocean ridge fault to determine the character of focused hydrothermal fluid flow. Tectonic escarpments at Pito Deep expose ocean crust formed at the super-fast spreading portion of the southern EPR (ca. 3 Ma). Ocean crust from Pito Deep is cut by high angle axial faults striking NE-SW parallel to the sheeted dykes. We focus on trace element and Sr isotopic compositional variations across an approximately 35 m fault zone within the sheeted dyke complex, ca. 100m below the lava-dyke transition, to explore the relationship between fluid flow, alteration and deformation. Samples from across this axial fault can be divided into 1) wall-rock basalts, 2) fault zone basalts and 3) fault zone breccias, ranging from simple cataclasites, veined cataclasites to quartz cataclasites. Breccias and basalts occur closely juxtaposed within the fault zone suggesting heterogeneous, highly localized deformation and fluid flow. Wall-rock basalts have been sampled a few to 30 m away from the fault zone and show extents of alteration typical of dykes away from fault zones with dominant replacement of primary phases by amphibole. The alteration in the fault zone basalts is also amphibole dominated with wider veins than the wall-rocks of quartz, chlorite ± amphibole. The fault zone breccias range in alteration mineralogy from chlorite to quartz dominated assemblages. Wall rock and fault zone basalts have similar trace element compositions to fresh crust. Breccias show large deviations in trace element compositions in comparison to adjacent altered basalts, with depletion of highly mobile elements such as K, Sr and both enrichment and depletion of Cu and Zn. 87Sr/86Sr of the dykes away from the fault zones are slightly elevated over fresh oceanic crust (0.7025- 0.7029) and fault zone samples have similar to higher 87Sr/86Sr. Quartz-epidote veins precipitated from fluids at Pito Deep have 87Sr/86Sr of approximately 0.7040. These new data provide insight into the chemical evolution of axial hydrothermal fluids during focused fluid flow.","publication_date":{"day":1,"month":12,"year":2007,"errors":{}}},"translated_abstract":"Investigation of an axial mid-ocean ridge fault to determine the character of focused hydrothermal fluid flow. Tectonic escarpments at Pito Deep expose ocean crust formed at the super-fast spreading portion of the southern EPR (ca. 3 Ma). Ocean crust from Pito Deep is cut by high angle axial faults striking NE-SW parallel to the sheeted dykes. We focus on trace element and Sr isotopic compositional variations across an approximately 35 m fault zone within the sheeted dyke complex, ca. 100m below the lava-dyke transition, to explore the relationship between fluid flow, alteration and deformation. Samples from across this axial fault can be divided into 1) wall-rock basalts, 2) fault zone basalts and 3) fault zone breccias, ranging from simple cataclasites, veined cataclasites to quartz cataclasites. Breccias and basalts occur closely juxtaposed within the fault zone suggesting heterogeneous, highly localized deformation and fluid flow. Wall-rock basalts have been sampled a few to 30 m away from the fault zone and show extents of alteration typical of dykes away from fault zones with dominant replacement of primary phases by amphibole. The alteration in the fault zone basalts is also amphibole dominated with wider veins than the wall-rocks of quartz, chlorite ± amphibole. The fault zone breccias range in alteration mineralogy from chlorite to quartz dominated assemblages. Wall rock and fault zone basalts have similar trace element compositions to fresh crust. Breccias show large deviations in trace element compositions in comparison to adjacent altered basalts, with depletion of highly mobile elements such as K, Sr and both enrichment and depletion of Cu and Zn. 87Sr/86Sr of the dykes away from the fault zones are slightly elevated over fresh oceanic crust (0.7025- 0.7029) and fault zone samples have similar to higher 87Sr/86Sr. Quartz-epidote veins precipitated from fluids at Pito Deep have 87Sr/86Sr of approximately 0.7040. These new data provide insight into the chemical evolution of axial hydrothermal fluids during focused fluid flow.","internal_url":"https://www.academia.edu/32187119/Fault_controlled_hydrothermal_fluid_flow_at_the_EPR","translated_internal_url":"","created_at":"2017-04-01T10:07:28.208-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304651,"work_id":32187119,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176472,"email":"s***r@uvic.ca","display_order":0,"name":"Kathryn Gillis","title":"Fault-controlled hydrothermal fluid flow at the EPR"},{"id":28304657,"work_id":32187119,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176473,"email":"l***8@leicester.ac.uk","display_order":4194304,"name":"Laurence Coogan","title":"Fault-controlled hydrothermal fluid flow at the EPR"}],"downloadable_attachments":[],"slug":"Fault_controlled_hydrothermal_fluid_flow_at_the_EPR","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":14920,"name":"Chemical Evolution","url":"https://www.academia.edu/Documents/in/Chemical_Evolution"},{"id":70919,"name":"Mid Ocean Ridge","url":"https://www.academia.edu/Documents/in/Mid_Ocean_Ridge"},{"id":215076,"name":"Fluid flow","url":"https://www.academia.edu/Documents/in/Fluid_flow"},{"id":424229,"name":"Sr isotopes","url":"https://www.academia.edu/Documents/in/Sr_isotopes"},{"id":702522,"name":"Tethys Oceanic Crust","url":"https://www.academia.edu/Documents/in/Tethys_Oceanic_Crust"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"}],"urls":[{"id":8041976,"url":"http://adsabs.harvard.edu/abs/2007agufm.t23b1414b"}]}, dispatcherData: dispatcherData }); 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Jaume Almera-CSIC. Lluís Solé i Sabarís s/n. 08028 Barcelona. España. andres@ija.csic.es RESUMEN Localizada en el NO de la Cordillera Central, la Formación Amina comprende una secuencia de protolitos volcánicos de edad Cretácico Inferior variablemente deformados y metamorfizados. La deformación fue heterogénea y consistió en un cizallamiento dúctil regional oblicuo dirigido al N y NO, que produjo una fábrica plano-linear Sp-Lp penetrativa de características miloníticas y una macroestructura consistente en un apilamiento de láminas cabalgantes de espesor kilométrico inclinadas hacia el SO. El metamorfismo sin-Sp fue en condiciones de la facies de los esquistos verdes de baja-T y localmente de la prenhita-pumpellita. Los estudios combinados cartográfico, geoquímico e isotópico Sr-Nd de la Fm Amina permiten identificar cuatro protolitos básicos y un tipo adicional de ácidos: toleítas de arco isla; toleítas de arco isla pobres en Ti y LREE; boninitas; basaltos de afinidad calco-alcalina; y riolitas. La fuente de estas rocas fue un manto variablemente empobrecido, al que se superpone un componente subductivo. Desde un punto de vista geoquímico, isotópico y petrogenético, existe una gran similitud entre los protolitos de las Formaciones Amina y Maimón con las rocas volcánicas de la Formación Los Ranchos, que implica que las rocas del primer grupo son los equivalentes tectonometamórficos del segundo. Todas ellas tienen las características típicas de series ígneas de arcos isla intraoceánicos, por lo que en conjunto representan la formación y desarrollo del arco isla Caribeño primitivo en el segmento de La Española durante el Aptiense-Albiense. Los mapas geoquímicos y transversales regionales de elementos traza seleccionados para el conjunto de las tres formaciones, permiten inferir, para la de la zona de subducción relacionada, una localización al O, NO y N respecto a la actual posición del dominio de Amina-Maimón.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}},"publication_name":"Boletín Geológico y …","grobid_abstract_attachment_id":52420731},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187246/Tect%C3%B3nica_y_geoqu%C3%ADmica_de_la_Formaci%C3%B3n_Amina_registro_del_arco_isla_Caribe%C3%B1o_primitivo_en_la","translated_internal_url":"","created_at":"2017-04-01T10:16:07.579-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420731,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420731/thumbnails/1.jpg","file_name":"Tectnica_y_geoqumica_de_la_Formacin_Amin20170401-6068-24349n.pdf","download_url":"https://www.academia.edu/attachments/52420731/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Tectonica_y_geoquimica_de_la_Formacion_A.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420731/Tectnica_y_geoqumica_de_la_Formacin_Amin20170401-6068-24349n-libre.pdf?1491067581=\u0026response-content-disposition=attachment%3B+filename%3DTectonica_y_geoquimica_de_la_Formacion_A.pdf\u0026Expires=1733097977\u0026Signature=ZTziQAr9wHymZzR~CrU9v064F2dyzuPx5qalAuI3Wt8aKvWAQieQB~i6T-aIwnMtF5GzXTUs2XOWnd3IxJlHNQe974hdKPPPLNuC98ya-dvTMRxmetDV3Z~hDdojJUGKZvMddmvMX5lHDuojRzR7JeJyCNZuZvmUTsN9aoU6qo41h4C5s7jiKDoMLAFzgIhJYhSpkwj4Cx826EE3G3WofgEvLXKwtwRmVdHgKankuVCyXXBS4FfRJjLN0uihDsc2KHJWiE8x7depim-V4bTcLdY9kCCDLtPOSqkNg3AN1hD9ebcoT-JRH2Y9nVdJerK53HaDhZwz1Bo93sCwij2dbA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Tectónica_y_geoquímica_de_la_Formación_Amina_registro_del_arco_isla_Caribeño_primitivo_en_la","translated_slug":"","page_count":22,"language":"es","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420731,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420731/thumbnails/1.jpg","file_name":"Tectnica_y_geoqumica_de_la_Formacin_Amin20170401-6068-24349n.pdf","download_url":"https://www.academia.edu/attachments/52420731/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Tectonica_y_geoquimica_de_la_Formacion_A.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420731/Tectnica_y_geoqumica_de_la_Formacin_Amin20170401-6068-24349n-libre.pdf?1491067581=\u0026response-content-disposition=attachment%3B+filename%3DTectonica_y_geoquimica_de_la_Formacion_A.pdf\u0026Expires=1733097977\u0026Signature=ZTziQAr9wHymZzR~CrU9v064F2dyzuPx5qalAuI3Wt8aKvWAQieQB~i6T-aIwnMtF5GzXTUs2XOWnd3IxJlHNQe974hdKPPPLNuC98ya-dvTMRxmetDV3Z~hDdojJUGKZvMddmvMX5lHDuojRzR7JeJyCNZuZvmUTsN9aoU6qo41h4C5s7jiKDoMLAFzgIhJYhSpkwj4Cx826EE3G3WofgEvLXKwtwRmVdHgKankuVCyXXBS4FfRJjLN0uihDsc2KHJWiE8x7depim-V4bTcLdY9kCCDLtPOSqkNg3AN1hD9ebcoT-JRH2Y9nVdJerK53HaDhZwz1Bo93sCwij2dbA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); 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The data are used to evaluate the source of the xenoliths which formed two differentiation suites: the acidic and intermediate xenoliths together with most of the lavas on the one hand, and the gabbroic xenoliths and a basaltic tuff on the other hand. The Pb isotopic compositions imply a mantle origin for the source magmas of the xenoliths and confirm the possibility of generating granitic rocks in an oceanic environment by fractional crystallization of a mantle-derived magma whose geochemical and isotopic characteristics are comparable to the source magmas of oceanic island basalts.","publication_date":{"day":null,"month":null,"year":1983,"errors":{}},"publication_name":"Earth and Planetary Science Letters","grobid_abstract_attachment_id":52420734},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187260/Pb_isotopes_in_Ascension_Island_rocks_oceanic_origin_for_the_gabbroic_to_granitic_plutonic_xenoliths","translated_internal_url":"","created_at":"2017-04-01T10:16:10.600-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420734,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420734/thumbnails/1.jpg","file_name":"0012-821x_2883_2990090-020170401-6059-pgu498.pdf","download_url":"https://www.academia.edu/attachments/52420734/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Pb_isotopes_in_Ascension_Island_rocks_oc.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420734/0012-821x_2883_2990090-020170401-6059-pgu498-libre.pdf?1491067584=\u0026response-content-disposition=attachment%3B+filename%3DPb_isotopes_in_Ascension_Island_rocks_oc.pdf\u0026Expires=1733097977\u0026Signature=AAYTZi1vmh-1j6QRxgncwckxAB0LCHZPniL4ZMIH4P-vt1b9AATsMao7~AbMd6XdIBzP~FHJuvY7X12nRecl38bkSfSoRw8X27NAm6Mk1grQJKetFPkbYVQMEiLCGOHYb8exdx0svtqm3kpY~K-SaLhbf6UiWj9k6pyJMQER~G8iBs4oJzkzvXqcuz2MIpHLjosh3sbVjPVHRkebj4RivH~jGd2-iuvnBORK61YrfYUQfdajNiPTVHxaM7KssEm2Jjww8Pbztx9IXQUac7fl~iWubJjZ6lzdZGBWc1~qG-KlKp5krXhwioQQOg8q057uqd69I6bgCngnOg9vqBdB9Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Pb_isotopes_in_Ascension_Island_rocks_oceanic_origin_for_the_gabbroic_to_granitic_plutonic_xenoliths","translated_slug":"","page_count":10,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420734,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420734/thumbnails/1.jpg","file_name":"0012-821x_2883_2990090-020170401-6059-pgu498.pdf","download_url":"https://www.academia.edu/attachments/52420734/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Pb_isotopes_in_Ascension_Island_rocks_oc.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420734/0012-821x_2883_2990090-020170401-6059-pgu498-libre.pdf?1491067584=\u0026response-content-disposition=attachment%3B+filename%3DPb_isotopes_in_Ascension_Island_rocks_oc.pdf\u0026Expires=1733097977\u0026Signature=AAYTZi1vmh-1j6QRxgncwckxAB0LCHZPniL4ZMIH4P-vt1b9AATsMao7~AbMd6XdIBzP~FHJuvY7X12nRecl38bkSfSoRw8X27NAm6Mk1grQJKetFPkbYVQMEiLCGOHYb8exdx0svtqm3kpY~K-SaLhbf6UiWj9k6pyJMQER~G8iBs4oJzkzvXqcuz2MIpHLjosh3sbVjPVHRkebj4RivH~jGd2-iuvnBORK61YrfYUQfdajNiPTVHxaM7KssEm2Jjww8Pbztx9IXQUac7fl~iWubJjZ6lzdZGBWc1~qG-KlKp5krXhwioQQOg8q057uqd69I6bgCngnOg9vqBdB9Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"}],"urls":[]}, dispatcherData: dispatcherData }); 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "952c844bce82815cc7f3141d217ae561" } } $('.js-work-strip[data-work-id=32187271]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187271,"title":"Geochemical implications of gabbro from the slow-spreading Northern Central Indian Ocean Ridge, Indian Ocean","translated_title":"","metadata":{"grobid_abstract":"Gabbro samples (ca. \u003c 0.4 Ma old) dredged from close to the \"Vityaz Megamullion\" on the slow spreading Northern Central Indian Ridge (NCIR, 18-22 mm/yr) include mostly olivine gabbro and Fe-Ti oxide gabbro. The cumulate olivine-gabbro shows ophitic to subophitic texture with early formed plagioclase crystals in mutual contact with each other, and narrow range of compositions of olivine (Fo 80-81 ), clinopyroxene (magnesium number: 85-87) and plagioclase (An 67-70 ). This olivine gabbro could be geochemically co-genetic with the evolved oxide-gabbro. These gabbro samples are geochemically distinct from the CIR gabbro occurring along the Vema, Argo and Marie Celeste transform faults and can further be discriminated from the associated NCIR basalts by their clinopyroxene (augite in gabbro, and diopsidic in basalts) and olivine (gabbro: Fo 80-81 , basalts: Fo 82-88 ) compositions. Our major oxide, trace element and REE geochemistry suggest that the gabbro and the NCIR basalts are also not co-genetic and had experienced different trends of geochemical evolution. The clinopyroxenes of the present NCIR gabbros are geochemically similar to primitive melt that is in equilibrium with mantle peridotite, and do not show any poikilitic texture with resorbed plagioclase, which negate the possibility of these gabbros being a pre-existing cumulate that has been brought up to the shallower oceanic crust and interacted with the NCIR basalt. The Sr, Pb and Nd isotopic data of the gabbro substantially differ from those of the NCIR basalts and suggest significant contamination of its depleted mantle source most likely by the Indian Ocean pelagic sediments. The proportion of pelagic sediment that mixed in the depleted mantle source of the NCIR gabbro is much higher than the level of contamination observed for the Indian Ocean MORBs.","publication_date":{"day":null,"month":null,"year":2011,"errors":{}},"publication_name":"Geological Magazine","grobid_abstract_attachment_id":52420739},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187271/Geochemical_implications_of_gabbro_from_the_slow_spreading_Northern_Central_Indian_Ocean_Ridge_Indian_Ocean","translated_internal_url":"","created_at":"2017-04-01T10:16:13.416-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420739,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420739/thumbnails/1.jpg","file_name":"Geochemical_implications_of_gabbro_from_20170401-6059-6c3dsz.pdf","download_url":"https://www.academia.edu/attachments/52420739/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_implications_of_gabbro_from.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420739/Geochemical_implications_of_gabbro_from_20170401-6059-6c3dsz-libre.pdf?1491067591=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_implications_of_gabbro_from.pdf\u0026Expires=1733034954\u0026Signature=VPlgBdJLHqMdz52OG0V0Pw13vtpHyGX2zqCa7bnx~c~BVhX~nWhexOs2OkUWA5qY0wkBihr9~nIBskwBkjYNRCZFoyYrUHhsOBjOPmlyYOJD1mZcNyxsYFAlmVA-IOT8hMtZK4b3fMi1jn3fJc7jIg3VQ30PE3lYTKNCz3hzne7SwLrCnDTBZSiAcmdO-S2WgIGp9iI9eG2XZMd-Hf8Ef4aqdeFVbOuHV~0CEMmeqVKouNkKhM76gKD2iyCjDscbGc7g30RICpKSWOMiXgx7a3jJ4DzJBH7HtGjjiykw4hkw4O-bj9ysinRElbhuWaf4mQLo3gIWzPgtFGhi4Cihag__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Geochemical_implications_of_gabbro_from_the_slow_spreading_Northern_Central_Indian_Ocean_Ridge_Indian_Ocean","translated_slug":"","page_count":43,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420739,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420739/thumbnails/1.jpg","file_name":"Geochemical_implications_of_gabbro_from_20170401-6059-6c3dsz.pdf","download_url":"https://www.academia.edu/attachments/52420739/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_implications_of_gabbro_from.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420739/Geochemical_implications_of_gabbro_from_20170401-6059-6c3dsz-libre.pdf?1491067591=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_implications_of_gabbro_from.pdf\u0026Expires=1733034954\u0026Signature=VPlgBdJLHqMdz52OG0V0Pw13vtpHyGX2zqCa7bnx~c~BVhX~nWhexOs2OkUWA5qY0wkBihr9~nIBskwBkjYNRCZFoyYrUHhsOBjOPmlyYOJD1mZcNyxsYFAlmVA-IOT8hMtZK4b3fMi1jn3fJc7jIg3VQ30PE3lYTKNCz3hzne7SwLrCnDTBZSiAcmdO-S2WgIGp9iI9eG2XZMd-Hf8Ef4aqdeFVbOuHV~0CEMmeqVKouNkKhM76gKD2iyCjDscbGc7g30RICpKSWOMiXgx7a3jJ4DzJBH7HtGjjiykw4hkw4O-bj9ysinRElbhuWaf4mQLo3gIWzPgtFGhi4Cihag__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":646312,"name":"Geological","url":"https://www.academia.edu/Documents/in/Geological"}],"urls":[]}, dispatcherData: dispatcherData }); 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The Arctic ridges (Gakkel Ridge and Lena Trough) are ultraslow-spreading ridges with low melt productivity and are thus the best locations to investigate mantle heterogeneity. We report the major and trace element and Sr^Nd^Pb^Hf isotope compositions of basalts generated along the Lena Trough and the westernmost part of the Gakkel Ridge in the Arctic Ocean. Basalts from the northern Lena Trough and westernmost Gakkel Ridge (NLT^WGR) have compositions close to normal MORB. The geochemical composition of the NLTŴ GR lavas confirms a binary mixing model involving melts from a depleted MORB mantle source and a Spitsbergen amphibole-bearing subcontinental lithospheric mantle (SCLM) source. In contrast, in the central part of the Lena Trough (CLT), the basalts are alkalic with relatively high Mg-number (60^65), high SiO 2 (51·0^51·6 wt %), Al 2 O 3 (18·1^18·4 wt %), Na 2 O (4·0^4·2 wt %), K 2 O (1·0^1·6 wt %), K 2 O/TiO 2 (0·6^0·9) and (La/Sm) PM (1·4^1·8), and low FeO (6·5^6·8 wt %) contents. These basalts display isotope variations with 87 Sr/ 86 Sr ranging from 0·70361 to 0·70390, 143 Nd/ 144 Nd from 0·51283 to 0·51290 (e Nd þ 3·7 to þ5·2), 176 Hf/ 177 Hf from 0·28313 to 0·28322 (e Hf þ 11·6 to þ14·9) and 206 Pb/ 204 Pb from 17·752 to 17·884, 207 Pb/ 204 Pb from 15·410 to 15·423 and 208 Pb/ 204 Pb from 37·544 to 37·670. These isotope compositions clearly distinguish the CLT lavas from those generated along the Gakkel Ridge. For the CLT lavas, involvement of a phlogopite-or amphibole-and (possibly garnet)-bearing SCLM source component is proposed. Owing to SCLM contamination along the entire length of the Lena Trough, we classify the LenaTrough as an ocean^continent transition boundary. Magmatism similar to that observed in the Lena Trough would be expected to occur wherever ocean spreading initiates.","publication_date":{"day":null,"month":null,"year":2011,"errors":{}},"publication_name":"Journal of Petrology","grobid_abstract_attachment_id":52420741},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187274/Geochemical_Composition_of_K_rich_Lavas_from_the_Lena_Trough_Arctic_Ocean_","translated_internal_url":"","created_at":"2017-04-01T10:16:14.192-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420741,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420741/thumbnails/1.jpg","file_name":"1185.full.pdf","download_url":"https://www.academia.edu/attachments/52420741/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_Composition_of_K_rich_Lavas.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420741/1185.full-libre.pdf?1491067597=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_Composition_of_K_rich_Lavas.pdf\u0026Expires=1733034954\u0026Signature=WUuCV2NUKuxkuYVFFO0HzShb8TssQdTsq3CIJiwygrrUpdXQQjWFFOeytnp55sab1EWwdsc7PagwkVeORabcIaGNRYqChOwCpDXjqMYhEa4aQRaT2kspCBrciv8kyjzeDjkk4r2SVCY2eTFF1Kef4UD9QYmmLud6FKjZ6kzt3ZbK-WSBKwUcyHqd-HyM-YqkWwaBh1ufxmYjChbMcSv2rHDtTEEl65T3fIuCRdYBwzCxjcqZHeUPcmans1yps5jvxWq0KGZC8dOyqCsup2C79QKVZma0aPn36yLdfIu6FlO~Znc~L5Vc2--Xc9o~BW8GYyJsL~QrIfdJGIUzsQS8tA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Geochemical_Composition_of_K_rich_Lavas_from_the_Lena_Trough_Arctic_Ocean_","translated_slug":"","page_count":22,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420741,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420741/thumbnails/1.jpg","file_name":"1185.full.pdf","download_url":"https://www.academia.edu/attachments/52420741/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_Composition_of_K_rich_Lavas.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420741/1185.full-libre.pdf?1491067597=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_Composition_of_K_rich_Lavas.pdf\u0026Expires=1733034954\u0026Signature=WUuCV2NUKuxkuYVFFO0HzShb8TssQdTsq3CIJiwygrrUpdXQQjWFFOeytnp55sab1EWwdsc7PagwkVeORabcIaGNRYqChOwCpDXjqMYhEa4aQRaT2kspCBrciv8kyjzeDjkk4r2SVCY2eTFF1Kef4UD9QYmmLud6FKjZ6kzt3ZbK-WSBKwUcyHqd-HyM-YqkWwaBh1ufxmYjChbMcSv2rHDtTEEl65T3fIuCRdYBwzCxjcqZHeUPcmans1yps5jvxWq0KGZC8dOyqCsup2C79QKVZma0aPn36yLdfIu6FlO~Znc~L5Vc2--Xc9o~BW8GYyJsL~QrIfdJGIUzsQS8tA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187282"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187282/Geochemical_characteristics_of_the_R%C3%ADo_Verde_Complex_Central_Hispaniola_Implications_for_the_paleotectonic_reconstruction_of_the_Lower_Cretaceous_Caribbean_island_arc"><img alt="Research paper thumbnail of Geochemical characteristics of the Río Verde Complex, Central Hispaniola: Implications for the paleotectonic reconstruction of the Lower Cretaceous Caribbean island-arc" class="work-thumbnail" src="https://attachments.academia-assets.com/52420774/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187282/Geochemical_characteristics_of_the_R%C3%ADo_Verde_Complex_Central_Hispaniola_Implications_for_the_paleotectonic_reconstruction_of_the_Lower_Cretaceous_Caribbean_island_arc">Geochemical characteristics of the Río Verde Complex, Central Hispaniola: Implications for the paleotectonic reconstruction of the Lower Cretaceous Caribbean island-arc</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, 2010</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="b3fbb8a6fcf809f2332f738bd5a06bfc" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420774,"asset_id":32187282,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420774/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187282"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187282"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187282; 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U-Pb and 40 Ar/ 39 Ar age data show that the Río Verde Complex protoliths were in part coeval with volcanic rocks of the Los Ranchos Formation (Upper Aptian to Lower Albian). The geochemical data establish the existence of gradients in trace element parameters (Nb/Yb, Th/Yb, Zr/Yb, Zr/ Ba, and normalized Ti, Sm, Y and Yb abundances) and Nd isotope compositions from throughout Hispaniola, which reflect differences in the degree of mantle wedge depletion and contributions from the subducting slab. The Río Verde Complex mafic rocks and some mafic sills and dykes intruding in the Loma Caribe Peridotite, have a transitional IAT to N-MORB geochemistry and a weak subduction-related signature, and are interpreted to form in a rifted arc or evolving back-arc basin setting. The Los Ranchos, Amina and Maimón Formations volcanic rocks have arc-like characteristics and represent magmatism in the volcanic front. Trace element and Nd isotope modeling reproduce observed data trends from arc to back-arc and suggest that the variations in several geochemical parameters observed in a SW direction across the Caribbean subduction system can be explained from the progressively lower subduction flux into a progressively less depleted mantle source. The low Nb contents and high (ε Nd ) i values in both arc and backarc mafic rocks imply, however, the absence of a significant Lower Cretaceous plume enriched component. In order to explain these observations, a model of proto-Caribbean oceanic lithosphere subducting to the SW at least in the 120-110 Ma interval, is proposed to cause the observed magmatic variations in the Lower Cretaceous Caribbean island-arc-back-arc system. In this context, arc rifting and initial sea-floor spreading to form the Río Verde Complex protoliths occurred in the back-arc setting of this primitive island-arc, built on the NE edge of the Caribbean 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href="https://independent.academia.edu/MurielTournay">Muriel Tournay</a></span></div><div class="wp-workCard_item"><span>Annales De La Societe Geologique De Belgique</span><span>, Jul 29, 2010</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6b3a4b97a2f9388bc40a53da95c7bbcf" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52414195,"asset_id":32179582,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52414195/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32179582"><a class="js-profile-work-strip-edit-button" 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elementbearing Little Nahanni Pegmatite Group, NWT, and whole rock samples from nearby granitic intrusions were measured. Correlation of the Li isotopic values from the pegmatite dikes with whole rock trace element geochemistry, mineralogy and primary textural evidence reflect mechanisms of Li isotopic fractionation during pegmatite formation. The heavier δ 7 Li signatures within the broad range measured from whole rock LNPG samples (− 0.94‰ to + 11.36‰) are related to the consolidation of the final~15% melt fraction of a volatilerich peraluminous magma in the late stages of magmatic fractionation. Rock-forming minerals (quartz, albite, spodumene and mica) display δ 7 Li signatures that indicate consolidation of the dikes under variable, nonequilibrium conditions. Lithium isotope signatures of relatively cool, highly evolved peraluminous magmas reflect the build-up of fluxes (e.g., H 2 O and F) and provide a qualitative assessment of the state of mineral/ melt chemical equilibrium. (E.M. Barnes), dweis@eos.ubc.ca (D. Weis), lgroat@eos.ubc.ca (L.A. Groat). 1 'Flux' is used as defined in London (2005b; and references therein) as components that 'lower the melting and crystallization temperatures…and enhance miscibility among otherwise less soluble constituents'. 2 The term 'rare element' as used here for the LNPG is an accepted pegmatite classification denoting an increased abundance of rare elements such as Li, Rb, Cs, Be, Sn, Nb and Ta (Černý, 1991a, 1991b). It should be not confused with 'rare earth elements' (the lanthanides) that are highly depleted in the LNPG samples.","publication_date":{"day":null,"month":null,"year":2012,"errors":{}},"publication_name":"Lithos","grobid_abstract_attachment_id":52420540},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186914/Significant_Li_isotope_fractionation_in_geochemically_evolved_rare_element_bearing_pegmatites_from_the_Little_Nahanni_Pegmatite_Group_NWT_Canada","translated_internal_url":"","created_at":"2017-04-01T10:05:30.156-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304518,"work_id":32186914,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176440,"email":"e***s@eos.ubc.ca","display_order":0,"name":"Elspeth Barnes","title":"Significant Li isotope fractionation in geochemically evolved rare element-bearing pegmatites from the Little Nahanni Pegmatite Group, NWT, Canada"}],"downloadable_attachments":[{"id":52420540,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420540/thumbnails/1.jpg","file_name":"j.lithos.2011.11.01420170401-6062-1k0ug8e.pdf","download_url":"https://www.academia.edu/attachments/52420540/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Significant_Li_isotope_fractionation_in.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420540/j.lithos.2011.11.01420170401-6062-1k0ug8e-libre.pdf?1491067261=\u0026response-content-disposition=attachment%3B+filename%3DSignificant_Li_isotope_fractionation_in.pdf\u0026Expires=1733097977\u0026Signature=VlnJ55A~O7pXNUtw7RcG7ufzcP165mEe61izRGXnYkghpRSl42cktUQo~b8~2fwyaYHARzwNun1gq009yJ4ev-WtbISOeIAw2J7PG3AzuGJVZAdawS5X3bhZnwfWts0spJm54gnVuFN44IZ8khwcJoBlpZJMGLncwKGwpy30SuFOKI724QkjnY1VvIIpQlJxtJ-5G5R4Q4tlkgHNjK3vTJta5AOIqnkedCehnbw4k0CwHhoDQgqF4Eu161XcLgQaEbYOkk8hVxKdNDENd1jEUe9vTtZkmaObhWSb0S06Nwleu8cXVN0QQfYlcJPE7J5zhwHTN-SC4nzfLp-IbGyEhA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Significant_Li_isotope_fractionation_in_geochemically_evolved_rare_element_bearing_pegmatites_from_the_Little_Nahanni_Pegmatite_Group_NWT_Canada","translated_slug":"","page_count":16,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420540,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420540/thumbnails/1.jpg","file_name":"j.lithos.2011.11.01420170401-6062-1k0ug8e.pdf","download_url":"https://www.academia.edu/attachments/52420540/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Significant_Li_isotope_fractionation_in.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420540/j.lithos.2011.11.01420170401-6062-1k0ug8e-libre.pdf?1491067261=\u0026response-content-disposition=attachment%3B+filename%3DSignificant_Li_isotope_fractionation_in.pdf\u0026Expires=1733097977\u0026Signature=VlnJ55A~O7pXNUtw7RcG7ufzcP165mEe61izRGXnYkghpRSl42cktUQo~b8~2fwyaYHARzwNun1gq009yJ4ev-WtbISOeIAw2J7PG3AzuGJVZAdawS5X3bhZnwfWts0spJm54gnVuFN44IZ8khwcJoBlpZJMGLncwKGwpy30SuFOKI724QkjnY1VvIIpQlJxtJ-5G5R4Q4tlkgHNjK3vTJta5AOIqnkedCehnbw4k0CwHhoDQgqF4Eu161XcLgQaEbYOkk8hVxKdNDENd1jEUe9vTtZkmaObhWSb0S06Nwleu8cXVN0QQfYlcJPE7J5zhwHTN-SC4nzfLp-IbGyEhA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":1186733,"name":"Pegmatite","url":"https://www.academia.edu/Documents/in/Pegmatite"}],"urls":[]}, dispatcherData: dispatcherData }); 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Aside from dilution by biogenic components, their chemical compositions reflect those of nearby continental masses. This study focuses on oceanic sediments coming from the juvenile Canadian Cordillera and highlights systematic differences between detritus deriving from juvenile crust and detritus from old and mature crust. We report major and trace element concentrations for 68 sediments from the northernmost part of the Cascade forearc, drilled at ODP Sites 888 and 1027. The calculated weighted averages for each site can then be used in the future to quantify the contribution of subducted sediments to Cascades volcanism. The two sites have similar compositions but Site 888, located closer to the continent, has higher sandy turbidite contents and displays higher bulk SiO 2 /Al 2 O 3 with lower bulk Nb/Zr, attributed to the presence of zircons in the coarse sands. Comparison with published data for other oceanic sedimentary piles demonstrates the existence of systematic differences between modern sediments deriving from juvenile terranes (juvenile sediments) and modern sediments derived from mature continental areas (cratonic sediments). The most striking systematic difference is for Th/Nb, Th/U, Nb/U and Th/Rb ratios: juvenile sediments have much lower ratios than cratonic sediments. The small enrichment of Th over Nb in cratonic sediments may be explained by intracrustal magmatic and metamorphic differentiation processes. In contrast, their elevated Th/U and Nb/U ratios (average values of 6.87 and 7.95, respectively) in comparison to juvenile sediments (Th/U~3.09, Nb/U~5.15) suggest extensive U and Rb losses on old cratons. Uranium and Rb losses are attributed to long-term leaching by rain and river water during exposure of the continental crust at the surface. Over geological times, the weathering effects create a slow but systematic increase of Th/U with exposure time.","publication_date":{"day":null,"month":null,"year":2013,"errors":{}},"publication_name":"Chemical Geology","grobid_abstract_attachment_id":52420494},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186857/Large_U_loss_during_weathering_of_upper_continental_crust_The_sedimentary_record","translated_internal_url":"","created_at":"2017-04-01T10:05:22.831-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304569,"work_id":32186857,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176454,"email":"m***r@eos.ubc.ca","display_order":0,"name":"Marion Carpentier","title":"Large U loss during weathering of upper continental crust: The sedimentary record"},{"id":28305026,"work_id":32186857,"tagging_user_id":62411756,"tagged_user_id":32756050,"co_author_invite_id":6176595,"email":"c***l@univ-grenoble-alpes.fr","affiliation":"Joseph Fourier University","display_order":4194304,"name":"Catherine Chauvel","title":"Large U loss during weathering of upper continental crust: The sedimentary record"},{"id":28305027,"work_id":32186857,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176596,"email":"m***t@eos.ubc.ca","display_order":6291456,"name":"Marion Carpent","title":"Large U loss during weathering of upper continental crust: The sedimentary record"}],"downloadable_attachments":[{"id":52420494,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420494/thumbnails/1.jpg","file_name":"Large_U_loss_during_weathering_of_upper_20170401-6062-14e518v.pdf","download_url":"https://www.academia.edu/attachments/52420494/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Large_U_loss_during_weathering_of_upper.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420494/Large_U_loss_during_weathering_of_upper_20170401-6062-14e518v-libre.pdf?1491067320=\u0026response-content-disposition=attachment%3B+filename%3DLarge_U_loss_during_weathering_of_upper.pdf\u0026Expires=1733034954\u0026Signature=VA3NyYZqNRAkhIFV4rpNapxdFZuOhpZSSMZUM7agsxeTVkIXbuCoOdS00gVuOSiIXc~RxmAlgk2tB7vuGRBqS8TKqcVtZt42GfUQnVVpEvDGyQuVTaamlalPNurt~LO6zZV-YowewDqakK8LTrejzbNCMSAUce1YP3pKKIANHB8s17ygcw9An9Cnbxsmcb4RXwsizWBGsrQBf0fE63cBhuCiftUPV8p37v93I8eznC2DsLtcJ0X1sysBcBPmbF3d7VlF-VA2iRHcP6fwUedje4Lx9xVTbwDt4FiBsp0Fa41-83Qj7NYjyGnVNmmGNiVboOSn9ALF7tpFx~2ShvL6sQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Large_U_loss_during_weathering_of_upper_continental_crust_The_sedimentary_record","translated_slug":"","page_count":14,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420494,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420494/thumbnails/1.jpg","file_name":"Large_U_loss_during_weathering_of_upper_20170401-6062-14e518v.pdf","download_url":"https://www.academia.edu/attachments/52420494/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Large_U_loss_during_weathering_of_upper.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420494/Large_U_loss_during_weathering_of_upper_20170401-6062-14e518v-libre.pdf?1491067320=\u0026response-content-disposition=attachment%3B+filename%3DLarge_U_loss_during_weathering_of_upper.pdf\u0026Expires=1733034954\u0026Signature=VA3NyYZqNRAkhIFV4rpNapxdFZuOhpZSSMZUM7agsxeTVkIXbuCoOdS00gVuOSiIXc~RxmAlgk2tB7vuGRBqS8TKqcVtZt42GfUQnVVpEvDGyQuVTaamlalPNurt~LO6zZV-YowewDqakK8LTrejzbNCMSAUce1YP3pKKIANHB8s17ygcw9An9Cnbxsmcb4RXwsizWBGsrQBf0fE63cBhuCiftUPV8p37v93I8eznC2DsLtcJ0X1sysBcBPmbF3d7VlF-VA2iRHcP6fwUedje4Lx9xVTbwDt4FiBsp0Fa41-83Qj7NYjyGnVNmmGNiVboOSn9ALF7tpFx~2ShvL6sQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":16024,"name":"Chemical Geology","url":"https://www.academia.edu/Documents/in/Chemical_Geology"}],"urls":[]}, dispatcherData: dispatcherData }); 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Nevertheless, recent petrological, geochemical and isotopic studies (Mi-chot and Deutsch, 197...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... Nevertheless, recent petrological, geochemical and isotopic studies (Mi-chot and Deutsch, 1977; Demaiffe et al., 1985) show the alkaline character of the Seychelles granites to ... I~:ocn es : B anch sseuseTr mpeuse Roch.Requin &amp;amp;quot; ~ANELLES $1LHOU ET TE ~&amp;amp;quot;&amp;amp;quot; Roches Brizards ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187120"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187120"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187120; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187120]").text(description); $(".js-view-count[data-work-id=32187120]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187120; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187120']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187120, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187120]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187120,"title":"Nd and Pb isotope evidence from the Seychelles granites and their xenoliths: Mantle origin with slight upper-crust interaction for alkaline anorogenic complexes","translated_title":"","metadata":{"abstract":"... Nevertheless, recent petrological, geochemical and isotopic studies (Mi-chot and Deutsch, 1977; Demaiffe et al., 1985) show the alkaline character of the Seychelles granites to ... I~:ocn es : B anch sseuseTr mpeuse Roch.Requin \u0026amp;amp;quot; ~ANELLES $1LHOU ET TE ~\u0026amp;amp;quot;\u0026amp;amp;quot; Roches Brizards ...","publication_date":{"day":30,"month":4,"year":1984,"errors":{}},"publication_name":"Chemical Geology"},"translated_abstract":"... Nevertheless, recent petrological, geochemical and isotopic studies (Mi-chot and Deutsch, 1977; Demaiffe et al., 1985) show the alkaline character of the Seychelles granites to ... I~:ocn es : B anch sseuseTr mpeuse Roch.Requin \u0026amp;amp;quot; ~ANELLES $1LHOU ET TE ~\u0026amp;amp;quot;\u0026amp;amp;quot; Roches Brizards ...","internal_url":"https://www.academia.edu/32187120/Nd_and_Pb_isotope_evidence_from_the_Seychelles_granites_and_their_xenoliths_Mantle_origin_with_slight_upper_crust_interaction_for_alkaline_anorogenic_complexes","translated_internal_url":"","created_at":"2017-04-01T10:07:28.504-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304642,"work_id":32187120,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176470,"email":"s***h@odu.edu","display_order":0,"name":"Alexander Deutsch","title":"Nd and Pb isotope evidence from the Seychelles granites and their xenoliths: Mantle origin with slight upper-crust interaction for alkaline anorogenic complexes"}],"downloadable_attachments":[],"slug":"Nd_and_Pb_isotope_evidence_from_the_Seychelles_granites_and_their_xenoliths_Mantle_origin_with_slight_upper_crust_interaction_for_alkaline_anorogenic_complexes","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":16024,"name":"Chemical Geology","url":"https://www.academia.edu/Documents/in/Chemical_Geology"},{"id":83087,"name":"Isotopes","url":"https://www.academia.edu/Documents/in/Isotopes"},{"id":179031,"name":"Mantle","url":"https://www.academia.edu/Documents/in/Mantle"},{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":198066,"name":"Contamination","url":"https://www.academia.edu/Documents/in/Contamination"},{"id":205590,"name":"Xenoliths","url":"https://www.academia.edu/Documents/in/Xenoliths"},{"id":361750,"name":"Isotope","url":"https://www.academia.edu/Documents/in/Isotope"},{"id":421956,"name":"Continental Crust","url":"https://www.academia.edu/Documents/in/Continental_Crust"},{"id":965094,"name":"Origin","url":"https://www.academia.edu/Documents/in/Origin"}],"urls":[{"id":8041977,"url":"http://cat.inist.fr/?aModele=afficheN\u0026cpsidt=9532984"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187232"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187232/Trace_Element_and_Os_Hf_Nd_Sr_Isotope_Systematics_of_Pervasively_Metasomatised_Ancient_Lithospheric_Mantle_at_the_Southeastern_rim_of_the_Siberian_Craton"><img alt="Research paper thumbnail of Trace Element and Os-Hf-Nd-Sr Isotope Systematics of Pervasively Metasomatised Ancient Lithospheric Mantle at the Southeastern rim of the Siberian Craton" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187232/Trace_Element_and_Os_Hf_Nd_Sr_Isotope_Systematics_of_Pervasively_Metasomatised_Ancient_Lithospheric_Mantle_at_the_Southeastern_rim_of_the_Siberian_Craton">Trace Element and Os-Hf-Nd-Sr Isotope Systematics of Pervasively Metasomatised Ancient Lithospheric Mantle at the Southeastern rim of the Siberian Craton</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects of Meso-Cenozoic tectonic re-activation and magmatism on the ancient lithospheric mantle. Most of the xenoliths are harzburgites and cpx-poor lherzolites; less common are fertile lherzolites and olivine-rich cumulates. Petrographic and chemical data indicate profound metasomatic alteration of the refractory peridotites, possibly due to interaction with evolved magmatic liquids: precipitation of secondary clinopyroxene and gabbroic interstitial material, low Mg-numbers of olivine and whole-rocks in combination with high Cr in spinel; high whole-rock Ca/Al, enrichments in highly incompatible elements and/or inversely U-shaped REE patterns. Re abundances in all xenoliths are &lt;0.06 ppb; Os abundances range from 0.1 to 4 ppb. Re and Os (0.9-3 ppb) in a subset of samples (including all cpx-rich lherzolites) that show no or limited metasomatism are positively correlated with modal clinopyroxene or whole-rock Al. 187/188Os in those xenoliths show linear correlations with Al or modal cpx consistent with a depletion age about 2 Ga and the formation of the lithosphere in the Precambrian. By contrast, the metasomatised refractory (2-7% cpx) xenoliths show a broad range in Os abundances and 187/188Os values (0.116-0.127), possibly due to disturbance of the Re-Os system during metasomatism. 176/177Hf is above the N-MORB average in one clinopyroxene separate and range between BSE and MORB values in the few other samples analysed. The 176/177Hf variations could be explained by mixing of ancient depleted mantle with an OIB-type metasomatic agent. We conclude that the xenoliths represent cratonic mantle strongly modified by metasomatism in hot-spot or subduction-related environments, possibly following removal of the cratonic keel and involving underplating of basaltic melts and their cumulates.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187232"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187232"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187232; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187232]").text(description); $(".js-view-count[data-work-id=32187232]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187232; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187232']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187232, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187232]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187232,"title":"Trace Element and Os-Hf-Nd-Sr Isotope Systematics of Pervasively Metasomatised Ancient Lithospheric Mantle at the Southeastern rim of the Siberian Craton","translated_title":"","metadata":{"abstract":"Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects of Meso-Cenozoic tectonic re-activation and magmatism on the ancient lithospheric mantle. Most of the xenoliths are harzburgites and cpx-poor lherzolites; less common are fertile lherzolites and olivine-rich cumulates. Petrographic and chemical data indicate profound metasomatic alteration of the refractory peridotites, possibly due to interaction with evolved magmatic liquids: precipitation of secondary clinopyroxene and gabbroic interstitial material, low Mg-numbers of olivine and whole-rocks in combination with high Cr in spinel; high whole-rock Ca/Al, enrichments in highly incompatible elements and/or inversely U-shaped REE patterns. Re abundances in all xenoliths are \u0026lt;0.06 ppb; Os abundances range from 0.1 to 4 ppb. Re and Os (0.9-3 ppb) in a subset of samples (including all cpx-rich lherzolites) that show no or limited metasomatism are positively correlated with modal clinopyroxene or whole-rock Al. 187/188Os in those xenoliths show linear correlations with Al or modal cpx consistent with a depletion age about 2 Ga and the formation of the lithosphere in the Precambrian. By contrast, the metasomatised refractory (2-7% cpx) xenoliths show a broad range in Os abundances and 187/188Os values (0.116-0.127), possibly due to disturbance of the Re-Os system during metasomatism. 176/177Hf is above the N-MORB average in one clinopyroxene separate and range between BSE and MORB values in the few other samples analysed. The 176/177Hf variations could be explained by mixing of ancient depleted mantle with an OIB-type metasomatic agent. We conclude that the xenoliths represent cratonic mantle strongly modified by metasomatism in hot-spot or subduction-related environments, possibly following removal of the cratonic keel and involving underplating of basaltic melts and their cumulates.","publication_date":{"day":null,"month":null,"year":2001,"errors":{}}},"translated_abstract":"Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects of Meso-Cenozoic tectonic re-activation and magmatism on the ancient lithospheric mantle. Most of the xenoliths are harzburgites and cpx-poor lherzolites; less common are fertile lherzolites and olivine-rich cumulates. Petrographic and chemical data indicate profound metasomatic alteration of the refractory peridotites, possibly due to interaction with evolved magmatic liquids: precipitation of secondary clinopyroxene and gabbroic interstitial material, low Mg-numbers of olivine and whole-rocks in combination with high Cr in spinel; high whole-rock Ca/Al, enrichments in highly incompatible elements and/or inversely U-shaped REE patterns. Re abundances in all xenoliths are \u0026lt;0.06 ppb; Os abundances range from 0.1 to 4 ppb. Re and Os (0.9-3 ppb) in a subset of samples (including all cpx-rich lherzolites) that show no or limited metasomatism are positively correlated with modal clinopyroxene or whole-rock Al. 187/188Os in those xenoliths show linear correlations with Al or modal cpx consistent with a depletion age about 2 Ga and the formation of the lithosphere in the Precambrian. By contrast, the metasomatised refractory (2-7% cpx) xenoliths show a broad range in Os abundances and 187/188Os values (0.116-0.127), possibly due to disturbance of the Re-Os system during metasomatism. 176/177Hf is above the N-MORB average in one clinopyroxene separate and range between BSE and MORB values in the few other samples analysed. The 176/177Hf variations could be explained by mixing of ancient depleted mantle with an OIB-type metasomatic agent. We conclude that the xenoliths represent cratonic mantle strongly modified by metasomatism in hot-spot or subduction-related environments, possibly following removal of the cratonic keel and involving underplating of basaltic melts and their cumulates.","internal_url":"https://www.academia.edu/32187232/Trace_Element_and_Os_Hf_Nd_Sr_Isotope_Systematics_of_Pervasively_Metasomatised_Ancient_Lithospheric_Mantle_at_the_Southeastern_rim_of_the_Siberian_Craton","translated_internal_url":"","created_at":"2017-04-01T10:16:02.978-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Trace_Element_and_Os_Hf_Nd_Sr_Isotope_Systematics_of_Pervasively_Metasomatised_Ancient_Lithospheric_Mantle_at_the_Southeastern_rim_of_the_Siberian_Craton","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":342071,"name":"Hot Spot","url":"https://www.academia.edu/Documents/in/Hot_Spot"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":1993786,"name":"Cumulant","url":"https://www.academia.edu/Documents/in/Cumulant"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187242"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187242/The_Timedjealen_alkaline_ring_complex_and_related_N_1bS_dyke_swarms_Adrar_des_Iforas_Mali_A_Pb_1bSr_1bO_isotopic_study"><img alt="Research paper thumbnail of The Timedjealen alkaline ring-complex and related N/1bS dyke swarms (Adrar des Iforas, Mali) — A Pb/1bSr/1bO isotopic study" class="work-thumbnail" src="https://attachments.academia-assets.com/52420729/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187242/The_Timedjealen_alkaline_ring_complex_and_related_N_1bS_dyke_swarms_Adrar_des_Iforas_Mali_A_Pb_1bSr_1bO_isotopic_study">The Timedjealen alkaline ring-complex and related N/1bS dyke swarms (Adrar des Iforas, Mali) — A Pb/1bSr/1bO isotopic study</a></div><div class="wp-workCard_item"><span>Chemical Geology</span><span>, 1986</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="75c168e0c41540ea52ad244e73d4976f" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420729,"asset_id":32187242,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420729/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187242"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187242"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187242; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187247"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32187247/Lithospheric_mantle_beneath_the_south_eastern_Siberian_craton_petrology_of_peridotite_xenoliths_in_basalts_from_the_Tokinsky_Stanovik"><img alt="Research paper thumbnail of Lithospheric mantle beneath the south-eastern Siberian craton: petrology of peridotite xenoliths in basalts from the Tokinsky Stanovik" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32187247/Lithospheric_mantle_beneath_the_south_eastern_Siberian_craton_petrology_of_peridotite_xenoliths_in_basalts_from_the_Tokinsky_Stanovik">Lithospheric mantle beneath the south-eastern Siberian craton: petrology of peridotite xenoliths in basalts from the Tokinsky Stanovik</a></div><div class="wp-workCard_item"><span>Contributions to Mineralogy and Petrology</span><span>, 2005</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We provide petrographic, major and trace element data for over 30 spinel peridotite xenoliths fro...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">We provide petrographic, major and trace element data for over 30 spinel peridotite xenoliths from the Tokinsky Stanovik (Tok) volcanic field on the Aldan shield to characterize the lithospheric mantle beneath the south-eastern margin of the Siberian craton, which formed in the Mesoproterozoic. High equilibration temperatures (870–1,010°C) of the xenoliths and the absence of garnet-bearing peridotites indicate a much thinner</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187247"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187247"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187247; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187247]").text(description); $(".js-view-count[data-work-id=32187247]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187247; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187247']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187247, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187247]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187247,"title":"Lithospheric mantle beneath the south-eastern Siberian craton: petrology of peridotite xenoliths in basalts from the Tokinsky Stanovik","translated_title":"","metadata":{"abstract":"We provide petrographic, major and trace element data for over 30 spinel peridotite xenoliths from the Tokinsky Stanovik (Tok) volcanic field on the Aldan shield to characterize the lithospheric mantle beneath the south-eastern margin of the Siberian craton, which formed in the Mesoproterozoic. High equilibration temperatures (870–1,010°C) of the xenoliths and the absence of garnet-bearing peridotites indicate a much thinner","publication_date":{"day":null,"month":null,"year":2005,"errors":{}},"publication_name":"Contributions to Mineralogy and Petrology"},"translated_abstract":"We provide petrographic, major and trace element data for over 30 spinel peridotite xenoliths from the Tokinsky Stanovik (Tok) volcanic field on the Aldan shield to characterize the lithospheric mantle beneath the south-eastern margin of the Siberian craton, which formed in the Mesoproterozoic. High equilibration temperatures (870–1,010°C) of the xenoliths and the absence of garnet-bearing peridotites indicate a much thinner","internal_url":"https://www.academia.edu/32187247/Lithospheric_mantle_beneath_the_south_eastern_Siberian_craton_petrology_of_peridotite_xenoliths_in_basalts_from_the_Tokinsky_Stanovik","translated_internal_url":"","created_at":"2017-04-01T10:16:07.820-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Lithospheric_mantle_beneath_the_south_eastern_Siberian_craton_petrology_of_peridotite_xenoliths_in_basalts_from_the_Tokinsky_Stanovik","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187252"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187252/Os_Hf_Sr_Nd_isotope_and_PGE_systematics_of_spinel_peridotite_xenoliths_from_Tok_SE_Siberian_craton_Effects_of_pervasive_metasomatism_in_shallow_refractory_mantle"><img alt="Research paper thumbnail of Os–Hf–Sr–Nd isotope and PGE systematics of spinel peridotite xenoliths from Tok, SE Siberian craton: Effects of pervasive metasomatism in shallow refractory mantle" class="work-thumbnail" src="https://attachments.academia-assets.com/52420735/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187252/Os_Hf_Sr_Nd_isotope_and_PGE_systematics_of_spinel_peridotite_xenoliths_from_Tok_SE_Siberian_craton_Effects_of_pervasive_metasomatism_in_shallow_refractory_mantle">Os–Hf–Sr–Nd isotope and PGE systematics of spinel peridotite xenoliths from Tok, SE Siberian craton: Effects of pervasive metasomatism in shallow refractory mantle</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, 2006</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="806a23dc4059cd8a566de51f27a56a51" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420735,"asset_id":32187252,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420735/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187252"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187252"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187252; 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "806a23dc4059cd8a566de51f27a56a51" } } $('.js-work-strip[data-work-id=32187252]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187252,"title":"Os–Hf–Sr–Nd isotope and PGE systematics of spinel peridotite xenoliths from Tok, SE Siberian craton: Effects of pervasive metasomatism in shallow refractory mantle","translated_title":"","metadata":{"grobid_abstract":"Os-Hf-Sr-Nd isotopes and PGE were determined in peridotite xenoliths carried to the surface by Quaternary alkali basaltic magmas in the Tokinsky Stanovik Range on the Aldan shield. These data constrain the timing and nature of partial melting and metasomatism in the lithospheric mantle beneath SE Siberian craton. The xenoliths range from the rare fertile spinel lherzolites to the more abundant, strongly metasomatised olivine-rich (70-84%) rocks. Hf-Sr-Nd isotope compositions of the xenoliths are mainly within the fields of oceanic basalts. Most metasomatised xenoliths have lower 143 Nd / 144 Nd and 176 Hf / 177 Hf and higher 87 Sr / 86 Sr than the host basalts indicating that the metasomatism is older and has distinct sources. A few xenoliths have elevated 176 Hf / 177 Hf (up to 0.2838) and plot above the Hf-Nd mantle array defined by oceanic basalts. 187 Os / 188 Os in the poorly metasomatised, fertile to moderately refractory (Al 2 O 3 z 1.6%) Tok peridotites range from 0.1156 to 0.1282, with oldest rhenium depletion ages being about 2 Ga. The 187 Os / 188 Os in these rocks show good correlations with partial melting indices (e.g. Al 2 O 3 , modal cpx); the intercept of the Al-187 Os / 188 Os correlation with lowest Al 2 O 3 estimates for melting residues (~0.3-0.5%) has a 187 Os / 188 Os of~0.109 suggesting that these peridotites may have experienced melt extraction as early as 2.8 Gy ago. 187 Os / 188 Os in the strongly metasomatised, olivine-rich xenoliths (0.6-1.3% Al 2 O 3 ) ranges from 0.1164 to 0.1275 and shows no apparent links to modal or chemical compositions. Convex-upward REE patterns and high abundances of heavy to middle REE in these refractory rocks indicate equilibration with evolved silicate melts at high melt / rock ratios, which may have also variably elevated their 187 Os / 188 Os. This inference is supported by enrichments in Pd and Pt on chondrite-normalised PGE abundance patterns in some of the rocks. The melt extraction ages for the Tok suite of 2.0 to 2.8 Ga are younger than oldest Os ages reported for central Siberian craton, but they must be considered minimum estimates because of the extensive metasomatism of the most refractory Tok peridotites. This metasomatism could have occurred in the late Mesozoic to early Cenozoic when the Tok region was close to the subduction-related Pacific margin of Siberia and experienced large-scale 0012-821X/$ -see front matter D (D.A. Ionov). www.elsevier.com/locate/epsl tectonic and magmatic activity. This study indicates that metasomatic effects on the Re-Os system in the shallow lithospheric mantle can be dramatic. 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The existence of these isochrons indicates that in favorable conditions U (and Pb) can be immobile. This can be due either to the lack of hard oxidizing conditions and/or to the location of U, in very low concentrations, in weathering-resistant minerals. The initial ratios (2°6pb/2°4 Pb = 18.714 _+ 70 and 2°7pb/2°4 Pb = 15.589 _+ 16), corrected for their Permian age, lie in the range observed for oceanic island basalts or continental alkali basalts and indicate an origin in a similar mantle, without any significant crustal contamination. This was also suggested by the initial 87Sr/86 Sr ratio of 0.70457 ± 4. Moreover, these Sr and Pb isotopic characteristics belong to the field of the so-called \"Dupal\" anomaly and indicate that it existed already 270 Ma ago. This study shows the potential interest of isotopic investigations of within-plate alkaline ring-complexes to characterize subcontinental mantle compositions, particularly in the past.","publication_date":{"day":null,"month":null,"year":1987,"errors":{}},"publication_name":"Earth and Planetary Science Letters","grobid_abstract_attachment_id":52420751},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187255/Tadhak_alkaline_ring_complex_Mali_existence_of_UPb_isochrons_and_Dupal_signature_270_Ma_ago","translated_internal_url":"","created_at":"2017-04-01T10:16:09.820-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420751,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420751/thumbnails/1.jpg","file_name":"0012-821x_2887_2990205-620170401-6059-cs6aiz.pdf","download_url":"https://www.academia.edu/attachments/52420751/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Tadhak_alkaline_ring_complex_Mali_existe.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420751/0012-821x_2887_2990205-620170401-6059-cs6aiz-libre.pdf?1491067573=\u0026response-content-disposition=attachment%3B+filename%3DTadhak_alkaline_ring_complex_Mali_existe.pdf\u0026Expires=1733034954\u0026Signature=PRTcxEH~kVVoAuC~B0GxVauPFd12aicHeUp~qBTqGRJMLHEshdExl~DoH9mAJZZjQXqxF5NWlu69MnrIPOpXcgNwUAcaQsjhRHI0m4~aEW1v3KhMt5uc5mPtLe8c6buOnRVgrcmNDfsXrU7WB3Y~LABFwXSMMb5ECRMvW5p9uEom8YKAjAYRqxHeoMFK3kA8sD97qUSqxVzll5Zcxiky1ROBgeB2keE6XxN-o8nbe6aHRVBsx-i3r4mEoHj-TKue5wVYjTY6oBFHbJdZmEQwuNPW5Ac3KlBTmqL3L2pUjVowIPoPV-TZDQXUXden2F9PQfD-ynfV4zQRpJ8krz4MqA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Tadhak_alkaline_ring_complex_Mali_existence_of_UPb_isochrons_and_Dupal_signature_270_Ma_ago","translated_slug":"","page_count":7,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420751,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420751/thumbnails/1.jpg","file_name":"0012-821x_2887_2990205-620170401-6059-cs6aiz.pdf","download_url":"https://www.academia.edu/attachments/52420751/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Tadhak_alkaline_ring_complex_Mali_existe.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420751/0012-821x_2887_2990205-620170401-6059-cs6aiz-libre.pdf?1491067573=\u0026response-content-disposition=attachment%3B+filename%3DTadhak_alkaline_ring_complex_Mali_existe.pdf\u0026Expires=1733034954\u0026Signature=PRTcxEH~kVVoAuC~B0GxVauPFd12aicHeUp~qBTqGRJMLHEshdExl~DoH9mAJZZjQXqxF5NWlu69MnrIPOpXcgNwUAcaQsjhRHI0m4~aEW1v3KhMt5uc5mPtLe8c6buOnRVgrcmNDfsXrU7WB3Y~LABFwXSMMb5ECRMvW5p9uEom8YKAjAYRqxHeoMFK3kA8sD97qUSqxVzll5Zcxiky1ROBgeB2keE6XxN-o8nbe6aHRVBsx-i3r4mEoHj-TKue5wVYjTY6oBFHbJdZmEQwuNPW5Ac3KlBTmqL3L2pUjVowIPoPV-TZDQXUXden2F9PQfD-ynfV4zQRpJ8krz4MqA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":23013,"name":"Carbonatites","url":"https://www.academia.edu/Documents/in/Carbonatites"},{"id":83087,"name":"Isotopes","url":"https://www.academia.edu/Documents/in/Isotopes"},{"id":101506,"name":"Permian","url":"https://www.academia.edu/Documents/in/Permian"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"},{"id":171492,"name":"Paleozoic","url":"https://www.academia.edu/Documents/in/Paleozoic"},{"id":179031,"name":"Mantle","url":"https://www.academia.edu/Documents/in/Mantle"},{"id":191165,"name":"Pb isotopes","url":"https://www.academia.edu/Documents/in/Pb_isotopes"},{"id":361750,"name":"Isotope","url":"https://www.academia.edu/Documents/in/Isotope"},{"id":555338,"name":"Crustal contamination","url":"https://www.academia.edu/Documents/in/Crustal_contamination"},{"id":965094,"name":"Origin","url":"https://www.academia.edu/Documents/in/Origin"},{"id":976618,"name":"Igneous Rocks","url":"https://www.academia.edu/Documents/in/Igneous_Rocks"},{"id":1464622,"name":"Carbonatite","url":"https://www.academia.edu/Documents/in/Carbonatite"}],"urls":[]}, dispatcherData: dispatcherData }); 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Peridotite xenoliths from Vitim (southern Siberia) and Mongolia provide some of the best samples of garnet and garnet-spinel facies off-craton lithospheric mantle. Garnets in those fertile to moderately depleted lherzolites show a surprisingly broad range of HREE abundances, which poorly correlate with modal and major oxide compositions. Some garnets are zoned and have Lu-rich cores. We argue that these features indicate HREE redistribution after the partial melting, possibly related to spinel-garnet phase transition on isobaric cooling. Most peridotites from Vitim have depleted to ultra-depleted Hf isotope compositions (calculated from mineral analyses: Hf(0) ϭ ϩ17 to ϩ45). HREE-rich garnets have the most radiogenic Hf values and plot above the mantle Hf-Nd isotope array while xenoliths with normal HREE abundances usually fall within or near the depleted end of the MORB field. Model Hf isotope ages for the normal peridotites indicate an origin by ancient partial melt extraction from primitive mantle, most likely in the Proterozoic. By contrast, an HREE-rich peridotite yields a Phanerozoic model age, possibly reflecting overprinting of the ancient partial melting record with that related to a recent enrichment in Lu. Clinopyroxene-garnet Lu-Hf isochron ages (31-84 Ma) are higher than the likely eruption age of the host volcanic rocks (ϳ16 Ma). Garnet-controlled HREE migration during spinel-garnet and garnet-spinel phase transitions may be one explanation for extremely radiogenic 176 Hf/ 177 Hf reported for some mantle peridotites; it may also contribute to Hf isotope variations in sub-lithospheric source regions of mantle-derived magmas.","publication_date":{"day":null,"month":null,"year":2005,"errors":{}},"publication_name":"Geochimica et Cosmochimica Acta","grobid_abstract_attachment_id":52420768},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187266/Hf_isotope_compositions_and_HREE_variations_in_off_craton_garnet_and_spinel_peridotite_xenoliths_from_central_Asia","translated_internal_url":"","created_at":"2017-04-01T10:16:12.125-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420768,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420768/thumbnails/1.jpg","file_name":"Hf_isotope_compositions_and_HREE_variati20170401-6062-s6ps6g.pdf","download_url":"https://www.academia.edu/attachments/52420768/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Hf_isotope_compositions_and_HREE_variati.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420768/Hf_isotope_compositions_and_HREE_variati20170401-6062-s6ps6g-libre.pdf?1491068010=\u0026response-content-disposition=attachment%3B+filename%3DHf_isotope_compositions_and_HREE_variati.pdf\u0026Expires=1733034954\u0026Signature=GxbAQQjbV~SzpAAafxxZu1xsJ4ukN~h5~KM7NK-VIi~AK9in-nwchW6X4FwuRYNZDgwlL6K0kK1hk-TA47Tsj9CdBnjQ9HtoV44gxb9g7VU41MLg4EJW5Cc0vUTiz9aCv1GSWwTPWyeYPrmthltfpJO48Gs3~FWlXTafX~hlqtupuOAjU1e43j~Absrg9jkE33PN5hMZl1jUprO1e-hMGPjAwP1KfggqHYlmQo5Hm8ZB7ht1vMEpfZmo1q66gCoRmOWmGqJ52To4H~zOt-9k4yAkaMpoySBMEGH93NXv0sUPA0vrKlzBKnq7Dre4ABSDuH~VbPtZn7EWN-~0aVoUBg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Hf_isotope_compositions_and_HREE_variations_in_off_craton_garnet_and_spinel_peridotite_xenoliths_from_central_Asia","translated_slug":"","page_count":20,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420768,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420768/thumbnails/1.jpg","file_name":"Hf_isotope_compositions_and_HREE_variati20170401-6062-s6ps6g.pdf","download_url":"https://www.academia.edu/attachments/52420768/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Hf_isotope_compositions_and_HREE_variati.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420768/Hf_isotope_compositions_and_HREE_variati20170401-6062-s6ps6g-libre.pdf?1491068010=\u0026response-content-disposition=attachment%3B+filename%3DHf_isotope_compositions_and_HREE_variati.pdf\u0026Expires=1733034954\u0026Signature=GxbAQQjbV~SzpAAafxxZu1xsJ4ukN~h5~KM7NK-VIi~AK9in-nwchW6X4FwuRYNZDgwlL6K0kK1hk-TA47Tsj9CdBnjQ9HtoV44gxb9g7VU41MLg4EJW5Cc0vUTiz9aCv1GSWwTPWyeYPrmthltfpJO48Gs3~FWlXTafX~hlqtupuOAjU1e43j~Absrg9jkE33PN5hMZl1jUprO1e-hMGPjAwP1KfggqHYlmQo5Hm8ZB7ht1vMEpfZmo1q66gCoRmOWmGqJ52To4H~zOt-9k4yAkaMpoySBMEGH93NXv0sUPA0vrKlzBKnq7Dre4ABSDuH~VbPtZn7EWN-~0aVoUBg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":173963,"name":"Phase transition","url":"https://www.academia.edu/Documents/in/Phase_transition"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":281810,"name":"Mantle xenolith","url":"https://www.academia.edu/Documents/in/Mantle_xenolith"},{"id":688910,"name":"Volcanic Rock","url":"https://www.academia.edu/Documents/in/Volcanic_Rock"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187284"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32187284/Coeval_potassic_and_sodic_calc_alkaline_series_in_the_post_collisional_Hercynian_Tanncherfi_intrusive_complex_northeastern_Morocco_geochemical_isotopic_and_geochronological_evidence"><img alt="Research paper thumbnail of Coeval potassic and sodic calc-alkaline series in the post-collisional Hercynian Tanncherfi intrusive complex, northeastern Morocco: geochemical, isotopic and geochronological evidence" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32187284/Coeval_potassic_and_sodic_calc_alkaline_series_in_the_post_collisional_Hercynian_Tanncherfi_intrusive_complex_northeastern_Morocco_geochemical_isotopic_and_geochronological_evidence">Coeval potassic and sodic calc-alkaline series in the post-collisional Hercynian Tanncherfi intrusive complex, northeastern Morocco: geochemical, isotopic and geochronological evidence</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, 1998</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The post-collisional late Hercynian Tanncherfi intrusive complex (TIC) is part of a widespread in...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The post-collisional late Hercynian Tanncherfi intrusive complex (TIC) is part of a widespread intrusive episode in the Moroccan Meseta. The complex contains a wide range of rock types, from monzogabbros to monzogranites. Two distinct magmatic series are ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187284"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187284"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187284; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187284]").text(description); $(".js-view-count[data-work-id=32187284]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187284; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187284']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187284, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187284]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187284,"title":"Coeval potassic and sodic calc-alkaline series in the post-collisional Hercynian Tanncherfi intrusive complex, northeastern Morocco: geochemical, isotopic and geochronological evidence","translated_title":"","metadata":{"abstract":"The post-collisional late Hercynian Tanncherfi intrusive complex (TIC) is part of a widespread intrusive episode in the Moroccan Meseta. The complex contains a wide range of rock types, from monzogabbros to monzogranites. Two distinct magmatic series are ...","publication_date":{"day":null,"month":null,"year":1998,"errors":{}},"publication_name":"Lithos"},"translated_abstract":"The post-collisional late Hercynian Tanncherfi intrusive complex (TIC) is part of a widespread intrusive episode in the Moroccan Meseta. The complex contains a wide range of rock types, from monzogabbros to monzogranites. 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Only the central part of the large Feda unit is rather homogeneous and poorly ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... ably deformed. Only the central part of the large Feda unit is rather homogeneous and poorly de-formed. There ... alkaline affinity. The average FeOto /MgO ratio for theFeda augen gneiss (Cpx zone) is 2.3 ± 1.0 (2o-). 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Hfisotope compositions were determined on a Nu Plasma MC-ICPMS instrument at the University of Brussels. The new data are considered together with results earlier reported for xenoliths from central and NE Asia [Baikal region and SE Siberian craton; Ionov et al. (2001); Blichert-Toft et al. (2000)]. The 176/177Hf values in off-cratonic peridotites range from 0.2830 to 0.2842 and are negatively correlated with Hf abundances. The Hf-Nd-Sr isotope relationships define 3 major fields. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187396"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187396/Whole_Rock_Lithium_Isotopic_Signatures_of_a_Pegmatite_Swarm_and_Their_Variation_With_Increasing_Magmatic_Fractionation_Evidence_From_the_Little_Nahanni_Pegmatite_Group_Northwest_Territories"><img alt="Research paper thumbnail of Whole Rock Lithium Isotopic Signatures of a Pegmatite Swarm and Their Variation With Increasing Magmatic Fractionation: Evidence From the Little Nahanni Pegmatite Group, Northwest Territories" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187396/Whole_Rock_Lithium_Isotopic_Signatures_of_a_Pegmatite_Swarm_and_Their_Variation_With_Increasing_Magmatic_Fractionation_Evidence_From_the_Little_Nahanni_Pegmatite_Group_Northwest_Territories">Whole Rock Lithium Isotopic Signatures of a Pegmatite Swarm and Their Variation With Increasing Magmatic Fractionation: Evidence From the Little Nahanni Pegmatite Group, Northwest Territories</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Variations in the δ7Li values of individual dikes of the Little Nahanni Pegmatite Group (LNPG) in...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Variations in the δ7Li values of individual dikes of the Little Nahanni Pegmatite Group (LNPG) in the Northwest Territories correlate with variations in the mineralogy and whole rock geochemistry suggesting compositional evolution of the melt during emplacement of the pegmatites. A better understanding of the relationship between these aspects may help clarify some of the processes involved in pegmatite formation. Quartz, K-feldspar, plagioclase, spodumene and mica are the major rock-forming minerals of the majority of the > 200 LNPG pegmatites, with accessory phases including columbite-group minerals, cassiterite, tourmaline, beryl, lithiophilite and garnet. A minority of dikes contain no spodumene but significantly more mica than the others. Major element whole rock geochemistry of 23 samples show high abundance and variability in SiO2 (67.2 - 78.5 wt.%) and Al2O3 (12.7 - 19.6 wt.%), moderate abundance and variability in Na2O (2.5 - 5.4 wt.%) and K2O (2.1-4.4 wt.%) and extremely low abundance in FeO (or Fe2O3), CaO, MgO and MnO (< 1 wt.%). However, Harker diagrams show little correlation between the oxides. In contrast, trace element analyses provide a wealth of information with high (e.g. Li, Cs, Ta, Sn) or low (e.g. rare earth element (REE), Sr, Ba) abundances relative to continental crust, strong fractionation trends in Nb/Ta, Ce/Pb and Zr/Hf, and distinctive REE patterns. Less fractionated spodumene-bearing rocks exclusively correlate with `tetrad effect' REE patterns with strongly negative Eu anomalies. The more fractionated spodumene-free samples display LREE enriched, relatively straight or listric REE patterns. The pegmatites at LNPG are high in H2O, F, P, and Li, all of which are capable of postponing the onset of crystallisation by depolymerizing the cooling silicate melt, potentially to within the temperature range of Li isotope fractionation. Measurements by MC-ICP-MS of 6Li and 7Li in the LNPG whole rock samples range between δ7Li -0.73 and 11.36, with the least fractionated samples having among the lowest F, P, and δ7Li values. Higher δ7Li values for the more evolved pegmatite samples may be due to 7Li being preferentially retained in the fluid of the increasingly fractionated silicate melt. The data from LNPG record a range of mineralogical, geochemical and isotopic signatures indicating that the composition of the pegmatites evolved during crystallisation. Ongoing analysis is expected to shed more light on the mechanisms involved and their association with the δ7Li values of the pegmatites.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187396"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187396"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187396; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187396]").text(description); $(".js-view-count[data-work-id=32187396]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187396; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187396']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187396, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187396]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187396,"title":"Whole Rock Lithium Isotopic Signatures of a Pegmatite Swarm and Their Variation With Increasing Magmatic Fractionation: Evidence From the Little Nahanni Pegmatite Group, Northwest Territories","translated_title":"","metadata":{"abstract":"Variations in the δ7Li values of individual dikes of the Little Nahanni Pegmatite Group (LNPG) in the Northwest Territories correlate with variations in the mineralogy and whole rock geochemistry suggesting compositional evolution of the melt during emplacement of the pegmatites. A better understanding of the relationship between these aspects may help clarify some of the processes involved in pegmatite formation. Quartz, K-feldspar, plagioclase, spodumene and mica are the major rock-forming minerals of the majority of the \u003e 200 LNPG pegmatites, with accessory phases including columbite-group minerals, cassiterite, tourmaline, beryl, lithiophilite and garnet. A minority of dikes contain no spodumene but significantly more mica than the others. Major element whole rock geochemistry of 23 samples show high abundance and variability in SiO2 (67.2 - 78.5 wt.%) and Al2O3 (12.7 - 19.6 wt.%), moderate abundance and variability in Na2O (2.5 - 5.4 wt.%) and K2O (2.1-4.4 wt.%) and extremely low abundance in FeO (or Fe2O3), CaO, MgO and MnO (\u003c 1 wt.%). However, Harker diagrams show little correlation between the oxides. In contrast, trace element analyses provide a wealth of information with high (e.g. Li, Cs, Ta, Sn) or low (e.g. rare earth element (REE), Sr, Ba) abundances relative to continental crust, strong fractionation trends in Nb/Ta, Ce/Pb and Zr/Hf, and distinctive REE patterns. Less fractionated spodumene-bearing rocks exclusively correlate with `tetrad effect' REE patterns with strongly negative Eu anomalies. The more fractionated spodumene-free samples display LREE enriched, relatively straight or listric REE patterns. The pegmatites at LNPG are high in H2O, F, P, and Li, all of which are capable of postponing the onset of crystallisation by depolymerizing the cooling silicate melt, potentially to within the temperature range of Li isotope fractionation. Measurements by MC-ICP-MS of 6Li and 7Li in the LNPG whole rock samples range between δ7Li -0.73 and 11.36, with the least fractionated samples having among the lowest F, P, and δ7Li values. Higher δ7Li values for the more evolved pegmatite samples may be due to 7Li being preferentially retained in the fluid of the increasingly fractionated silicate melt. The data from LNPG record a range of mineralogical, geochemical and isotopic signatures indicating that the composition of the pegmatites evolved during crystallisation. Ongoing analysis is expected to shed more light on the mechanisms involved and their association with the δ7Li values of the pegmatites.","publication_date":{"day":null,"month":null,"year":2008,"errors":{}}},"translated_abstract":"Variations in the δ7Li values of individual dikes of the Little Nahanni Pegmatite Group (LNPG) in the Northwest Territories correlate with variations in the mineralogy and whole rock geochemistry suggesting compositional evolution of the melt during emplacement of the pegmatites. A better understanding of the relationship between these aspects may help clarify some of the processes involved in pegmatite formation. Quartz, K-feldspar, plagioclase, spodumene and mica are the major rock-forming minerals of the majority of the \u003e 200 LNPG pegmatites, with accessory phases including columbite-group minerals, cassiterite, tourmaline, beryl, lithiophilite and garnet. A minority of dikes contain no spodumene but significantly more mica than the others. Major element whole rock geochemistry of 23 samples show high abundance and variability in SiO2 (67.2 - 78.5 wt.%) and Al2O3 (12.7 - 19.6 wt.%), moderate abundance and variability in Na2O (2.5 - 5.4 wt.%) and K2O (2.1-4.4 wt.%) and extremely low abundance in FeO (or Fe2O3), CaO, MgO and MnO (\u003c 1 wt.%). However, Harker diagrams show little correlation between the oxides. In contrast, trace element analyses provide a wealth of information with high (e.g. Li, Cs, Ta, Sn) or low (e.g. rare earth element (REE), Sr, Ba) abundances relative to continental crust, strong fractionation trends in Nb/Ta, Ce/Pb and Zr/Hf, and distinctive REE patterns. Less fractionated spodumene-bearing rocks exclusively correlate with `tetrad effect' REE patterns with strongly negative Eu anomalies. The more fractionated spodumene-free samples display LREE enriched, relatively straight or listric REE patterns. The pegmatites at LNPG are high in H2O, F, P, and Li, all of which are capable of postponing the onset of crystallisation by depolymerizing the cooling silicate melt, potentially to within the temperature range of Li isotope fractionation. Measurements by MC-ICP-MS of 6Li and 7Li in the LNPG whole rock samples range between δ7Li -0.73 and 11.36, with the least fractionated samples having among the lowest F, P, and δ7Li values. Higher δ7Li values for the more evolved pegmatite samples may be due to 7Li being preferentially retained in the fluid of the increasingly fractionated silicate melt. The data from LNPG record a range of mineralogical, geochemical and isotopic signatures indicating that the composition of the pegmatites evolved during crystallisation. Ongoing analysis is expected to shed more light on the mechanisms involved and their association with the δ7Li values of the pegmatites.","internal_url":"https://www.academia.edu/32187396/Whole_Rock_Lithium_Isotopic_Signatures_of_a_Pegmatite_Swarm_and_Their_Variation_With_Increasing_Magmatic_Fractionation_Evidence_From_the_Little_Nahanni_Pegmatite_Group_Northwest_Territories","translated_internal_url":"","created_at":"2017-04-01T10:16:37.953-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Whole_Rock_Lithium_Isotopic_Signatures_of_a_Pegmatite_Swarm_and_Their_Variation_With_Increasing_Magmatic_Fractionation_Evidence_From_the_Little_Nahanni_Pegmatite_Group_Northwest_Territories","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":91257,"name":"Stable Isotope","url":"https://www.academia.edu/Documents/in/Stable_Isotope"},{"id":274263,"name":"Rare Earth Element Mineralization","url":"https://www.academia.edu/Documents/in/Rare_Earth_Element_Mineralization"},{"id":421956,"name":"Continental Crust","url":"https://www.academia.edu/Documents/in/Continental_Crust"},{"id":627481,"name":"Northwest Territories","url":"https://www.academia.edu/Documents/in/Northwest_Territories"},{"id":640682,"name":"Isotope fractionation","url":"https://www.academia.edu/Documents/in/Isotope_fractionation"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"}],"urls":[{"id":8042009,"url":"http://adsabs.harvard.edu/abs/2008agufm.v43c2174b"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187398"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187398/Trace_Element_and_Os_Hf_Nd_Sr_Isotope_Systematics_of_Pervasively_Metasomatised_Ancient_Lithospheric_Mantle_at_the_Southeastern_rim_of_the_Siberian_Craton"><img alt="Research paper thumbnail of Trace Element and Os-Hf-Nd-Sr Isotope Systematics of Pervasively Metasomatised Ancient Lithospheric Mantle at the Southeastern rim of the Siberian Craton" class="work-thumbnail" src="https://attachments.academia-assets.com/52420793/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187398/Trace_Element_and_Os_Hf_Nd_Sr_Isotope_Systematics_of_Pervasively_Metasomatised_Ancient_Lithospheric_Mantle_at_the_Southeastern_rim_of_the_Siberian_Craton">Trace Element and Os-Hf-Nd-Sr Isotope Systematics of Pervasively Metasomatised Ancient Lithospheric Mantle at the Southeastern rim of the Siberian Craton</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects of Meso-Cenozoic tectonic re-activation and magmatism on the ancient lithospheric mantle. Most of the xenoliths are harzburgites and cpx-poor lherzolites; less common are fertile lherzolites and olivine-rich cumulates. Petrographic and chemical data indicate profound metasomatic alteration of the refractory peridotites, possibly due to interaction with evolved magmatic liquids: precipitation of secondary clinopyroxene and gabbroic interstitial material, low Mg-numbers of olivine and whole-rocks in combination with high Cr in spinel; high whole-rock Ca/Al, enrichments in highly incompatible elements and/or inversely U-shaped REE patterns. Re abundances in all xenoliths are <0.06 ppb; Os abundances range from 0.1 to 4 ppb. Re and Os (0.9-3 ppb) in a subset of samples (including all cpx-rich lherzolites) that show no or limited metasomatism are positively correlated with modal clinopyroxene or whole-rock Al. 187/188Os in those xenoliths show linear correlations with Al or modal cpx consistent with a depletion age about 2 Ga and the formation of the lithosphere in the Precambrian. By contrast, the metasomatised refractory (2-7% cpx) xenoliths show a broad range in Os abundances and 187/188Os values (0.116-0.127), possibly due to disturbance of the Re-Os system during metasomatism. 176/177Hf is above the N-MORB average in one clinopyroxene separate and range between BSE and MORB values in the few other samples analysed. The 176/177Hf variations could be explained by mixing of ancient depleted mantle with an OIB-type metasomatic agent. We conclude that the xenoliths represent cratonic mantle strongly modified by metasomatism in hot-spot or subduction-related environments, possibly following removal of the cratonic keel and involving underplating of basaltic melts and their cumulates.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="47c64957c1bcfe91717fe57738f44c92" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420793,"asset_id":32187398,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420793/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187398"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187398"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187398; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187398]").text(description); $(".js-view-count[data-work-id=32187398]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187398; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187398']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187398, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "47c64957c1bcfe91717fe57738f44c92" } } $('.js-work-strip[data-work-id=32187398]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187398,"title":"Trace Element and Os-Hf-Nd-Sr Isotope Systematics of Pervasively Metasomatised Ancient Lithospheric Mantle at the Southeastern rim of the Siberian Craton","translated_title":"","metadata":{"abstract":"Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects of Meso-Cenozoic tectonic re-activation and magmatism on the ancient lithospheric mantle. Most of the xenoliths are harzburgites and cpx-poor lherzolites; less common are fertile lherzolites and olivine-rich cumulates. Petrographic and chemical data indicate profound metasomatic alteration of the refractory peridotites, possibly due to interaction with evolved magmatic liquids: precipitation of secondary clinopyroxene and gabbroic interstitial material, low Mg-numbers of olivine and whole-rocks in combination with high Cr in spinel; high whole-rock Ca/Al, enrichments in highly incompatible elements and/or inversely U-shaped REE patterns. Re abundances in all xenoliths are \u003c0.06 ppb; Os abundances range from 0.1 to 4 ppb. Re and Os (0.9-3 ppb) in a subset of samples (including all cpx-rich lherzolites) that show no or limited metasomatism are positively correlated with modal clinopyroxene or whole-rock Al. 187/188Os in those xenoliths show linear correlations with Al or modal cpx consistent with a depletion age about 2 Ga and the formation of the lithosphere in the Precambrian. By contrast, the metasomatised refractory (2-7% cpx) xenoliths show a broad range in Os abundances and 187/188Os values (0.116-0.127), possibly due to disturbance of the Re-Os system during metasomatism. 176/177Hf is above the N-MORB average in one clinopyroxene separate and range between BSE and MORB values in the few other samples analysed. The 176/177Hf variations could be explained by mixing of ancient depleted mantle with an OIB-type metasomatic agent. We conclude that the xenoliths represent cratonic mantle strongly modified by metasomatism in hot-spot or subduction-related environments, possibly following removal of the cratonic keel and involving underplating of basaltic melts and their cumulates.","publication_date":{"day":1,"month":12,"year":2001,"errors":{}}},"translated_abstract":"Spinel peridotite xenoliths in Late Cenozoic basalts from the Aldan-Stanovoi shield show effects of Meso-Cenozoic tectonic re-activation and magmatism on the ancient lithospheric mantle. Most of the xenoliths are harzburgites and cpx-poor lherzolites; less common are fertile lherzolites and olivine-rich cumulates. Petrographic and chemical data indicate profound metasomatic alteration of the refractory peridotites, possibly due to interaction with evolved magmatic liquids: precipitation of secondary clinopyroxene and gabbroic interstitial material, low Mg-numbers of olivine and whole-rocks in combination with high Cr in spinel; high whole-rock Ca/Al, enrichments in highly incompatible elements and/or inversely U-shaped REE patterns. Re abundances in all xenoliths are \u003c0.06 ppb; Os abundances range from 0.1 to 4 ppb. Re and Os (0.9-3 ppb) in a subset of samples (including all cpx-rich lherzolites) that show no or limited metasomatism are positively correlated with modal clinopyroxene or whole-rock Al. 187/188Os in those xenoliths show linear correlations with Al or modal cpx consistent with a depletion age about 2 Ga and the formation of the lithosphere in the Precambrian. By contrast, the metasomatised refractory (2-7% cpx) xenoliths show a broad range in Os abundances and 187/188Os values (0.116-0.127), possibly due to disturbance of the Re-Os system during metasomatism. 176/177Hf is above the N-MORB average in one clinopyroxene separate and range between BSE and MORB values in the few other samples analysed. The 176/177Hf variations could be explained by mixing of ancient depleted mantle with an OIB-type metasomatic agent. 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Despite low levels of incompatible elements, many cumulate samples contain both baddeleyite (ZrO2) and zircon (ZrSiO4). As part of a larger study on the age of the Stillwater Complex and duration of emplacement,</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186936"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186936"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186936; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186936]").text(description); $(".js-view-count[data-work-id=32186936]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186936; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186936']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186936, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186936]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186936,"title":"Baddeleyite-Zircon Relationships in Cumulates of the Archean Stillwater Complex: Evidence from U-Pb Geochronology and Hf Isotope Systematics","translated_title":"","metadata":{"abstract":"The Stillwater Complex is a large mafic-ultramafic layered intrusion in the Beartooth Mountains of Montana (USA) and host to the world-class J-M Reef platinum group element deposit. 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "bd2e93ce11a7efeed28159d8408a1837" } } $('.js-work-strip[data-work-id=32186910]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186910,"title":"U–Pb and 40Ar/39Ar geochronology of the Saint-Urbain and Lac Allard (Havre-Saint-Pierre) anorthosites and their associated Fe–Ti oxide ores, Québec: Evidence for emplacement and slow cooling during the collisional Ottawan orogeny in the Grenville Province","translated_title":"","metadata":{"grobid_abstract":"Intrusive suites containing anorthosite-mangerite-charnockite-granite (AMCG) are a characteristic feature of Mesoproterozoic magmatic activity in the Grenville Province of eastern North America. In this study, the U-Pb and 40 Ar/ 39 Ar geochronology of two AMCG suites (Saint-Urbain and Havre-Saint-Pierre), and associated rutile-bearing hemo-ilmenite deposits, within the allochthonous polycyclic belt of the Grenville Province in Québec are used to constrain their crystallization ages and cooling histories, and to assess their tectonic setting. Both AMCG suites, separated by 700 km along the St. Lawrence River, have similar crystallization ages (ca. 1050-1060 Ma) and durations of magmatism (10-15 million years). The 450 km 2 Saint-Urbain anorthosite is a composite intrusion with a distinctly younger central leuconorite (1046.2 ± 3.1 Ma) compared with anorthosite to the north and south (1055.0 ± 2.4 Ma and 1053.6 ± 2.6 Ma, respectively). The age of a deformed oxide-apatite gabbronorite (1057.4 ± 1.5 Ma) along the northwest margin of the intrusion is within analytical uncertainty of the anorthosites, whereas the oldest intrusion in the Saint-Urbain area is the regionally extensive Saint-Anne du Nord orthopyroxene granodiorite (1060.8 ± 2.8 Ma). The large 11,000 km 2 Havre-Saint-Pierre anorthosite suite comprises a number of intrusive phases, including the 2700 km 2 Lac Allard anorthosite, which contains the giant Lac Tio ilmenite deposit and Big Island ilmenitite dyke. U-Pb zircon ages of three anorthosites from the Lac Allard intrusion, including the host to the Lac Tio deposit, overlap within error (1061.6 ± 3.0 Ma, 1060.5 ± 1.9 Ma, 1057.4 ± 8.4 Ma) and the crosscutting Big Island dyke yields an age of 1052.9 ± 6.5 Ma. These results indicate that the Havre-Saint-Pierre anorthosite should be divided into an older geon 11 part (ca. 1129 Ma) and a younger geon 10 part (ca. 1060 Ma). Average cooling rates of 3-4 • C/million years were estimated for the two AMCG suites by combining crystallization ages (U-Pb zircon) and cooling ages (U-Pb rutile, 40 Ar/ 39 Ar biotite/plagioclase) and reflect emplacement of the intrusions into a hot, long-duration orogen. Emplacement of these two AMCG suites at ca. 1050-1060 Ma is related to regional extensional tectonics near the end of peak metamorphism associated with the collisional Ottawan orogenic phase of the Grenville orogeny. The results of this study provide strong support for proposals that link AMCG magmatism associated with the Grenville orogeny to convective thinning or delamination of the lithosphere and subsequent melting of upwelling asthenospheric mantle. (C.-E. Morisset). 1990) to ca. 975 Ma (Vieux Fort, Heaman et al., 2004). A fundamental issue concerning the origin of AMCG suites in the Proterozoic involves resolving the tectonic setting in which they were generated. Although once considered to be anorogenic, recent proposals now link the origin of specific suites of anorthosite and related rocks to active plate margin orogenic processes, including extension within a collisional orogen following delamination of the continental lithosphere (e.g. , transtension along a terrane boundary during late arc-continent collision (e.g. Scoates and Chamberlain, 1997), and back-arc extension related to a continental margin setting (e.g. . Determining precise crystallization ages and cooling 0301-9268/$ -see front matter","publication_date":{"day":null,"month":null,"year":2009,"errors":{}},"publication_name":"Precambrian Research","grobid_abstract_attachment_id":52420569},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186910/U_Pb_and_40Ar_39Ar_geochronology_of_the_Saint_Urbain_and_Lac_Allard_Havre_Saint_Pierre_anorthosites_and_their_associated_Fe_Ti_oxide_ores_Qu%C3%A9bec_Evidence_for_emplacement_and_slow_cooling_during_the_collisional_Ottawan_orogeny_in_the_Grenville_Province","translated_internal_url":"","created_at":"2017-04-01T10:05:29.611-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304397,"work_id":32186910,"tagging_user_id":62411756,"tagged_user_id":34531449,"co_author_invite_id":6176434,"email":"j***s@eos.ubc.ca","display_order":0,"name":"James Scoates","title":"U–Pb and 40Ar/39Ar geochronology of the Saint-Urbain and Lac Allard (Havre-Saint-Pierre) anorthosites and their associated Fe–Ti oxide ores, Québec: Evidence for emplacement and slow cooling during the collisional Ottawan orogeny in the Grenville Province"},{"id":28304484,"work_id":32186910,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176435,"email":"c***t@golder.com","display_order":4194304,"name":"Caroline-Emmanuelle Morisset","title":"U–Pb and 40Ar/39Ar geochronology of the Saint-Urbain and Lac Allard (Havre-Saint-Pierre) anorthosites and their associated Fe–Ti oxide ores, Québec: Evidence for emplacement and slow cooling during the collisional Ottawan orogeny in the Grenville 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href="https://www.academia.edu/32186909/Age_and_Nd_Hf_isotopic_constraints_on_the_origin_of_marginal_rocks_from_the_Muskox_layered_intrusion_Nunavut_Canada_and_implications_for_the_evolution_of_the_1_27Ga_Mackenzie_large_igneous_province"><img alt="Research paper thumbnail of Age and Nd–Hf isotopic constraints on the origin of marginal rocks from the Muskox layered intrusion (Nunavut, Canada) and implications for the evolution of the 1.27Ga Mackenzie large igneous province" class="work-thumbnail" src="https://attachments.academia-assets.com/52420558/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" 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$a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32186867"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186867/Geochemical_and_isotopic_Sr_Nd_and_Pb_evidence_on_the_origin_of_the_anorthosite_bearing_anorogenic_complexes_of_the_A%C3%AFr_Province_Niger"><img alt="Research paper thumbnail of Geochemical and isotopic (Sr, Nd and Pb) evidence on the origin of the anorthosite-bearing anorogenic complexes of the Aïr Province, Niger" class="work-thumbnail" src="https://attachments.academia-assets.com/52420472/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186867/Geochemical_and_isotopic_Sr_Nd_and_Pb_evidence_on_the_origin_of_the_anorthosite_bearing_anorogenic_complexes_of_the_A%C3%AFr_Province_Niger">Geochemical and isotopic (Sr, Nd and Pb) evidence on the origin of the anorthosite-bearing anorogenic complexes of the Aïr Province, Niger</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, 1991</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="f518d7c0a78aa003b7cab4975fb5a265" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420472,"asset_id":32186867,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420472/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action 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The leucogabbroic rocks are plagioclase cumulates, whereas troctolites and melatroctolites in the Meugueur-Meugueur ring dyke are olivine cumulates. The plagioclase cumulates are strongly laminated but generally unlayered and have positive europium anomalies. Fine-grained marginal gabbros and monzogabbros without europium anomalies are interpreted as having been close to magmatic liquids, as are the other felsic rocks, which have complementary negative europium anomalies. The fine-grained basic rocks are mildly alkaline with a troctolitic tendency with high Ti, P and incompatible elements and low transition elements. Cumulus mineral compositions (-An65 and -Fo65 55) are moderately differentiated. The felsic syenites and granites are alkaline to rarely peralkaline. 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class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32186855/Rutile_Bearing_Ilmenite_Deposits_Associated_with_the_Proterozoic_Saint_Urbain_and_Lac_Allard_Anorthosite_Massifs_Grenville_Province_Quebec"><img alt="Research paper thumbnail of Rutile-Bearing Ilmenite Deposits Associated with the Proterozoic Saint-Urbain and Lac Allard Anorthosite Massifs, Grenville Province, Quebec" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32186855/Rutile_Bearing_Ilmenite_Deposits_Associated_with_the_Proterozoic_Saint_Urbain_and_Lac_Allard_Anorthosite_Massifs_Grenville_Province_Quebec">Rutile-Bearing Ilmenite Deposits Associated with the Proterozoic Saint-Urbain and Lac Allard Anorthosite Massifs, Grenville Province, Quebec</a></div><div class="wp-workCard_item"><span>The Canadian Mineralogist</span><span>, 2010</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract Deposits of concentrated Fe–Ti oxide minerals are a characteristic component of many Pro...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract Deposits of concentrated Fe–Ti oxide minerals are a characteristic component of many Proterozoic anorthosite massifs. 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Norway)" class="work-thumbnail" src="https://attachments.academia-assets.com/52420761/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187264/Pb_isotope_geochemistry_of_a_massif_type_anorthositic_charnockitic_body_The_Hidra_Massif_Rogaland_S_W_Norway_">Pb isotope geochemistry of a massif-type anorthositic-charnockitic body: The Hidra Massif (Rogaland, S.W. Norway)</a></div><div class="wp-workCard_item"><span>Geochimica et Cosmochimica Acta</span><span>, 1983</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="7d333b058d4982ad37ee1ab56c0dd5fd" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420761,"asset_id":32187264,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420761/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187264"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187264"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187264; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187264]").text(description); $(".js-view-count[data-work-id=32187264]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187264; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187264']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187264, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "7d333b058d4982ad37ee1ab56c0dd5fd" } } $('.js-work-strip[data-work-id=32187264]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187264,"title":"Pb isotope geochemistry of a massif-type anorthositic-charnockitic body: The Hidra Massif (Rogaland, S.W. Norway)","translated_title":"","metadata":{"grobid_abstract":"The Hidra Massif(Rogaland complex, S.W. Norway) is a massif-type anorthositic-chamockitic body. It consists of undeformed anorthosites and leuconorites, grading into fine-grained jotunites at the contact with the granulite facies gneisses of the metamorphic envelope. A stockwork of charnockitic dykes cross-cuts the massif. The Pb isotopic compositions of the anorthosites and leuconorites are comparable or stightiy less radiogenic than those of the jotunites (*~Pb/~Pb from 18.079 to 19.307, M7Pb/ *04Pb from 15.568 to 15.657 and 2D8Pb/2@'Pb from 37.6 17 to 38.493). These vafues are compatible with an upper mantle origin for the parental magma ofjotunitic composition and for the plagiociasic cumulates, but show the incorporation of lower crustal material (U-depleted and thus less radiogenic). The charnockitic dykes have significantly less radiogenic Pb isotopic compositions (206Pb/204Pb from 17.472 to","publication_date":{"day":null,"month":null,"year":1983,"errors":{}},"publication_name":"Geochimica et Cosmochimica Acta","grobid_abstract_attachment_id":52420761},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187264/Pb_isotope_geochemistry_of_a_massif_type_anorthositic_charnockitic_body_The_Hidra_Massif_Rogaland_S_W_Norway_","translated_internal_url":"","created_at":"2017-04-01T10:16:11.596-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420761,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420761/thumbnails/1.jpg","file_name":"Pb_isotope_geochemistry_of_a_massif-type20170401-6068-c3semt.pdf","download_url":"https://www.academia.edu/attachments/52420761/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Pb_isotope_geochemistry_of_a_massif_type.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420761/Pb_isotope_geochemistry_of_a_massif-type20170401-6068-c3semt-libre.pdf?1491068017=\u0026response-content-disposition=attachment%3B+filename%3DPb_isotope_geochemistry_of_a_massif_type.pdf\u0026Expires=1733097977\u0026Signature=UR8jkNGsRTPTg4wVyQwX2hSen3QvhlUWmPkLaT~iExoZNlKOR24KOJTooHAhA3-SnKgwqYQbIAE~K9Z4jU4Wv8BdWEzfIckGs0Fh0QUpbon86WwrbNDQ6Vb5x0lg97yxBD1nZ3MdPOJRwEkOb2swie4UCsUy7kT7TtpEMf9kFon3P0kFR3RjRa3UHVbQxewXmuTEQwERSGVWTIT91gakkUip2YxZJJuPSeo5m12-QEiHVFkvdWhleEpQ67jyxxYQ3mCOzg1Rj4adJl0yPKKOxkcpfQZ9gk8Qx9BDxRp9qDHU5VaB850u6gzacuX6nLR2plw89So-8BkeASezTO2V1g__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Pb_isotope_geochemistry_of_a_massif_type_anorthositic_charnockitic_body_The_Hidra_Massif_Rogaland_S_W_Norway_","translated_slug":"","page_count":9,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420761,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420761/thumbnails/1.jpg","file_name":"Pb_isotope_geochemistry_of_a_massif-type20170401-6068-c3semt.pdf","download_url":"https://www.academia.edu/attachments/52420761/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Pb_isotope_geochemistry_of_a_massif_type.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420761/Pb_isotope_geochemistry_of_a_massif-type20170401-6068-c3semt-libre.pdf?1491068017=\u0026response-content-disposition=attachment%3B+filename%3DPb_isotope_geochemistry_of_a_massif_type.pdf\u0026Expires=1733097977\u0026Signature=UR8jkNGsRTPTg4wVyQwX2hSen3QvhlUWmPkLaT~iExoZNlKOR24KOJTooHAhA3-SnKgwqYQbIAE~K9Z4jU4Wv8BdWEzfIckGs0Fh0QUpbon86WwrbNDQ6Vb5x0lg97yxBD1nZ3MdPOJRwEkOb2swie4UCsUy7kT7TtpEMf9kFon3P0kFR3RjRa3UHVbQxewXmuTEQwERSGVWTIT91gakkUip2YxZJJuPSeo5m12-QEiHVFkvdWhleEpQ67jyxxYQ3mCOzg1Rj4adJl0yPKKOxkcpfQZ9gk8Qx9BDxRp9qDHU5VaB850u6gzacuX6nLR2plw89So-8BkeASezTO2V1g__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":1993786,"name":"Cumulant","url":"https://www.academia.edu/Documents/in/Cumulant"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187283"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187283/Marginal_mafic_intrusions_as_indicators_of_downslope_draining_of_dense_residual_melts_in_anorthositic_diapirs"><img alt="Research paper thumbnail of Marginal mafic intrusions as indicators of downslope draining of dense residual melts in anorthositic diapirs?" class="work-thumbnail" src="https://attachments.academia-assets.com/52420767/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187283/Marginal_mafic_intrusions_as_indicators_of_downslope_draining_of_dense_residual_melts_in_anorthositic_diapirs">Marginal mafic intrusions as indicators of downslope draining of dense residual melts in anorthositic diapirs?</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, 2006</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="fd1f0626d592c6e924862f27b2b9656b" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420767,"asset_id":32187283,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420767/download_file?st=MTczMzA5NDM3Nyw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187283"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187283"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187283; 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These layered mafic intrusions are essentially of norite, gabbronorite as well as leuconorite and display conspicuous evidence of subsolidus recrystallization. In Løyning and Hogstad, the modal layering is parallel to the subvertical foliation in the enclosing anorthosite. The northern part of the Koldal intrusion cuts across the foliation of the anorthosite, whereas in its southern part the subvertical layering is parallel to the anorthosite's foliation. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187381"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187381/Small_mafic_intrusions_as_indicators_of_downslope_draining_of_dense_residual_liquids_in_anorthositic_diapirs"><img alt="Research paper thumbnail of Small mafic intrusions as indicators of downslope draining of dense residual liquids in anorthositic diapirs" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187381/Small_mafic_intrusions_as_indicators_of_downslope_draining_of_dense_residual_liquids_in_anorthositic_diapirs">Small mafic intrusions as indicators of downslope draining of dense residual liquids in anorthositic diapirs</a></div><div class="wp-workCard_item"><span>Egs Agu Eug Joint Assembly</span><span>, Apr 1, 2003</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">To investigate the differentiation and emplacement mechanisms of massif type anorthosites, we hav...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">To investigate the differentiation and emplacement mechanisms of massif type anorthosites, we have undertaken a petrological study of three small elongated mafic intrusions (Loyning:1250×150m; Hogstad: 2000×200m; Koldal: 1250×500m) occurring in the marginal zone of two massif-type anorthosites of the Rogaland Anorthositic Province (South Norway) (930 Ma). They are essentially made of norites, melanorites, leuconorites and locally mangerites (Koldal intrusion): these hypersthene-bearing lithologies are typical of Proterozoic AMCG (Anorthosite-Mangerite-Charnockite-Granite) suites. In Loyning, the rocks display a well-defined layering, thoroughly recrystallized and parrallel to the subvertical foliation in the enclosing anorthosite. Hogstad displays a less recrystallized vertical modal layering. In Koldal, the intrusion cuts across the foliation of the anorthosite. The least differentiated compositions of orthopyroxene and plagioclase (Loyning: Ens68-An52 - Hogstad: Ens64-An49 - Koldal: Ens66-An44) are close to those experimentally obtained on jotunites (hypersthene-bearing monzodiorites) suggesting that such liquids are possible parent magmas of these intrusions. Nevertheless, the orthopyroxene and plagioclase megacrysts of the enclosing anorthosites display slightly more primitive compositions (Ens74 to Ens75, An49 to An55), indicating that the parent magmas of the three mafic intrusions are residual after (some) anorthosite crystallization. This conclusion is supported by isotopic data as the 87Sr/86Sr (930Ma) and εNd(t) (Loyning: 87Sr/86Sr : 0.70406-0.70457, εNd : +7.6 to +3.4 - Hogstad: 87Sr/86Sr : 0.70537-0.70590, εNd : +2.59 to -0.23 - Koldal: 87Sr/86Sr : 0.70606-0.70805, εNd : +3.48 to -1.67) partly overlap the observed range in the enclosing anorthosites (87Sr/86Sr : 0.7033-0.7063, εNd : +5.9 to -1.8). Calculated densities of jotunites (at FMQ, 0%H_2O, 1150^oC) demonstrate that they are much denser (2.77) than the plagioclase of the surrounding anorthosite (2.625). We thus suggest that the limited spatial occurrence of these small intrusions in the marginal zone of the enclosing massif type anorthosites results from the crystallization of batches of dense liquids which were drained through the anorthositic crystal mush and crystallized in short-lived magma chambers at various stages of the evolution of the anorthosite diapir. A sloping floor is required for the draining of this dense liquid.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187381"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187381"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187381; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187381]").text(description); $(".js-view-count[data-work-id=32187381]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187381; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187381']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187381, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187381]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187381,"title":"Small mafic intrusions as indicators of downslope draining of dense residual liquids in anorthositic diapirs","translated_title":"","metadata":{"abstract":"To investigate the differentiation and emplacement mechanisms of massif type anorthosites, we have undertaken a petrological study of three small elongated mafic intrusions (Loyning:1250×150m; Hogstad: 2000×200m; Koldal: 1250×500m) occurring in the marginal zone of two massif-type anorthosites of the Rogaland Anorthositic Province (South Norway) (930 Ma). They are essentially made of norites, melanorites, leuconorites and locally mangerites (Koldal intrusion): these hypersthene-bearing lithologies are typical of Proterozoic AMCG (Anorthosite-Mangerite-Charnockite-Granite) suites. In Loyning, the rocks display a well-defined layering, thoroughly recrystallized and parrallel to the subvertical foliation in the enclosing anorthosite. Hogstad displays a less recrystallized vertical modal layering. In Koldal, the intrusion cuts across the foliation of the anorthosite. The least differentiated compositions of orthopyroxene and plagioclase (Loyning: Ens68-An52 - Hogstad: Ens64-An49 - Koldal: Ens66-An44) are close to those experimentally obtained on jotunites (hypersthene-bearing monzodiorites) suggesting that such liquids are possible parent magmas of these intrusions. Nevertheless, the orthopyroxene and plagioclase megacrysts of the enclosing anorthosites display slightly more primitive compositions (Ens74 to Ens75, An49 to An55), indicating that the parent magmas of the three mafic intrusions are residual after (some) anorthosite crystallization. This conclusion is supported by isotopic data as the 87Sr/86Sr (930Ma) and εNd(t) (Loyning: 87Sr/86Sr : 0.70406-0.70457, εNd : +7.6 to +3.4 - Hogstad: 87Sr/86Sr : 0.70537-0.70590, εNd : +2.59 to -0.23 - Koldal: 87Sr/86Sr : 0.70606-0.70805, εNd : +3.48 to -1.67) partly overlap the observed range in the enclosing anorthosites (87Sr/86Sr : 0.7033-0.7063, εNd : +5.9 to -1.8). Calculated densities of jotunites (at FMQ, 0%H_2O, 1150^oC) demonstrate that they are much denser (2.77) than the plagioclase of the surrounding anorthosite (2.625). We thus suggest that the limited spatial occurrence of these small intrusions in the marginal zone of the enclosing massif type anorthosites results from the crystallization of batches of dense liquids which were drained through the anorthositic crystal mush and crystallized in short-lived magma chambers at various stages of the evolution of the anorthosite diapir. A sloping floor is required for the draining of this dense liquid.","publication_date":{"day":1,"month":4,"year":2003,"errors":{}},"publication_name":"Egs Agu Eug Joint Assembly"},"translated_abstract":"To investigate the differentiation and emplacement mechanisms of massif type anorthosites, we have undertaken a petrological study of three small elongated mafic intrusions (Loyning:1250×150m; Hogstad: 2000×200m; Koldal: 1250×500m) occurring in the marginal zone of two massif-type anorthosites of the Rogaland Anorthositic Province (South Norway) (930 Ma). They are essentially made of norites, melanorites, leuconorites and locally mangerites (Koldal intrusion): these hypersthene-bearing lithologies are typical of Proterozoic AMCG (Anorthosite-Mangerite-Charnockite-Granite) suites. In Loyning, the rocks display a well-defined layering, thoroughly recrystallized and parrallel to the subvertical foliation in the enclosing anorthosite. Hogstad displays a less recrystallized vertical modal layering. In Koldal, the intrusion cuts across the foliation of the anorthosite. The least differentiated compositions of orthopyroxene and plagioclase (Loyning: Ens68-An52 - Hogstad: Ens64-An49 - Koldal: Ens66-An44) are close to those experimentally obtained on jotunites (hypersthene-bearing monzodiorites) suggesting that such liquids are possible parent magmas of these intrusions. Nevertheless, the orthopyroxene and plagioclase megacrysts of the enclosing anorthosites display slightly more primitive compositions (Ens74 to Ens75, An49 to An55), indicating that the parent magmas of the three mafic intrusions are residual after (some) anorthosite crystallization. This conclusion is supported by isotopic data as the 87Sr/86Sr (930Ma) and εNd(t) (Loyning: 87Sr/86Sr : 0.70406-0.70457, εNd : +7.6 to +3.4 - Hogstad: 87Sr/86Sr : 0.70537-0.70590, εNd : +2.59 to -0.23 - Koldal: 87Sr/86Sr : 0.70606-0.70805, εNd : +3.48 to -1.67) partly overlap the observed range in the enclosing anorthosites (87Sr/86Sr : 0.7033-0.7063, εNd : +5.9 to -1.8). Calculated densities of jotunites (at FMQ, 0%H_2O, 1150^oC) demonstrate that they are much denser (2.77) than the plagioclase of the surrounding anorthosite (2.625). We thus suggest that the limited spatial occurrence of these small intrusions in the marginal zone of the enclosing massif type anorthosites results from the crystallization of batches of dense liquids which were drained through the anorthositic crystal mush and crystallized in short-lived magma chambers at various stages of the evolution of the anorthosite diapir. A sloping floor is required for the draining of this dense liquid.","internal_url":"https://www.academia.edu/32187381/Small_mafic_intrusions_as_indicators_of_downslope_draining_of_dense_residual_liquids_in_anorthositic_diapirs","translated_internal_url":"","created_at":"2017-04-01T10:16:33.760-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Small_mafic_intrusions_as_indicators_of_downslope_draining_of_dense_residual_liquids_in_anorthositic_diapirs","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[{"id":415322,"name":"Magma Chamber","url":"https://www.academia.edu/Documents/in/Magma_Chamber"}],"urls":[{"id":8042001,"url":"http://adsabs.harvard.edu/abs/2003EAEJA.....3817V"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="6767212" id="environmentalgeochemistry"><div class="js-work-strip profile--work_container" data-work-id="32186965"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32186965/Trace_Element_Signatures_of_Particles_in_the_Fraser_River_Estuary"><img alt="Research paper thumbnail of Trace Element Signatures of Particles in the Fraser River Estuary" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32186965/Trace_Element_Signatures_of_Particles_in_the_Fraser_River_Estuary">Trace Element Signatures of Particles in the Fraser River Estuary</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/DominiqueWeis">Dominique Weis</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ubc.academia.edu/ASnauffer">A. Snauffer</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186965"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32186965"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32186965; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32186965]").text(description); $(".js-view-count[data-work-id=32186965]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32186965; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32186965']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32186965, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32186965]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186965,"title":"Trace Element Signatures of Particles in the Fraser River Estuary","translated_title":"","metadata":{"abstract":"ABSTRACT"},"translated_abstract":"ABSTRACT","internal_url":"https://www.academia.edu/32186965/Trace_Element_Signatures_of_Particles_in_the_Fraser_River_Estuary","translated_internal_url":"","created_at":"2017-04-01T10:05:37.691-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304513,"work_id":32186965,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176438,"email":"b***r@eos.ubc.ca","display_order":0,"name":"Bruno Kieffer","title":"Trace Element Signatures of Particles in the Fraser River Estuary"},{"id":28304830,"work_id":32186965,"tagging_user_id":62411756,"tagged_user_id":62712480,"co_author_invite_id":6176531,"email":"a***r@eoas.ubc.ca","affiliation":"University of British Columbia","display_order":4194304,"name":"A. 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Significant fractionation of Zn and Cd isotopes during processing of ZnS and PbS ore concentrates is demonstrated by the total variation in δ 66/64 Zn and δ 114/110 Cd values of 0.42‰ and 1.04‰, respectively, among all smelter samples. No significant difference is observed between the isotopic compositions of the Zn ore concentrates (δ 66/64 Zn = 0.09 to 0.17‰; δ 114/110 Cd = −0.13 to 0.18‰) and the roasting product, calcine (δ 66/64 Zn =0.17‰; δ 114/110 Cd= 0.05‰), due to ∼100% recovery from roasting. The overall Zn recovery from metallurgical processing is ∼98%, thus the refined Zn metal (δ 66/64 Zn = 0.22‰) is not significantly fractionated relative to the starting materials despite significantly fractionated fume (δ 66/64 Zn = 0.43‰) and effluent (δ 66/64 Zn=0.41 to 0.51‰). Calculated Cd recovery from metallurgical processing is 72-92%, with the majority of the unrecovered Cd lost during Pb operations (δ 114/110 Cd= −0.38‰). The refined Cd metal is heavy (δ 114/110 Cd =0.39 to 0.52‰) relative to the starting materials. In addition, significant fractionation of Cd isotopes is evidenced by the relatively light and heavy isotopic compositions of the fume (δ 114/110 Cd= −0.52‰) and effluent (δ 114/110 Cd =0.31 to 0.46‰). In contrast to Zn and Cd, Pb isotopes are homogenized by mixing during processing. The total variation observed in the Pb isotopic compositions of smelter samples is attributed to mixing of ore sources with different radiogenic signatures.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}},"publication_name":"Science of The Total Environment","grobid_abstract_attachment_id":52420529},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186911/Evaluation_of_zinc_cadmium_and_lead_isotope_fractionation_during_smelting_and_refining","translated_internal_url":"","created_at":"2017-04-01T10:05:29.732-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304377,"work_id":32186911,"tagging_user_id":62411756,"tagged_user_id":14778951,"co_author_invite_id":6176431,"email":"a***l@coas.oregonstate.edu","affiliation":"Oregon State University","display_order":0,"name":"Alyssa Shiel","title":"Evaluation of zinc, cadmium 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href="https://www.academia.edu/32186889/Tracing_cadmium_zinc_and_lead_sources_in_bivalves_from_the_coasts_of_western_Canada_and_the_USA_using_isotopes">Tracing cadmium, zinc and lead sources in bivalves from the coasts of western Canada and the USA using isotopes</a></div><div class="wp-workCard_item"><span>Geochimica et Cosmochimica Acta</span><span>, 2012</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="c1af3d825d93787206b9b6d73b7bb6b4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420527,"asset_id":32186889,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420527/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: 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href="https://www.academia.edu/32186863/Iron_isotopic_fractionation_in_industrial_emissions_and_urban_aerosols"><img alt="Research paper thumbnail of Iron isotopic fractionation in industrial emissions and urban aerosols" class="work-thumbnail" src="https://attachments.academia-assets.com/52420489/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186863/Iron_isotopic_fractionation_in_industrial_emissions_and_urban_aerosols">Iron isotopic fractionation in industrial emissions and urban aerosols</a></div><div class="wp-workCard_item"><span>Chemosphere</span><span>, 2008</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="053b9d7966b5e2086f5ba3bae169978c" class="wp-workCard--action" rel="nofollow" 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id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "053b9d7966b5e2086f5ba3bae169978c" } } $('.js-work-strip[data-work-id=32186863]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32186863,"title":"Iron isotopic fractionation in industrial emissions and urban aerosols","translated_title":"","metadata":{"grobid_abstract":"A study on tropospheric aerosols involving Fe particles with an industrial origin is tackled here. Aerosols were collected at the largest exhausts of a major European steel metallurgy plant and around its near urban environment. A combination of bulk and individual particle analysis performed by SEM-EDX provides the chemical composition of Fe-bearing aerosols emitted within the factory process (hematite, magnetite and agglomerates of these oxides with sylvite (KCl), calcite (CaCO 3 ) and graphite carbon). Fe isotopic compositions of those emissions fall within the range (0.08‰ \u003c d 56 Fe \u003c +0.80‰) of enriched ores processed by the manufacturer (À0.16‰ \u003c d 56 Fe \u003c +1.19‰). No significant evolution of Fe fractionation during steelworks processes is observed. At the industrial source, Fe is mainly present as oxide particles, to some extent in 3-4 lm aggregates. In the close urban area, 5 km away from the steel plant, individual particle analysis of collected aerosols presents, in addition to the industrial particle type, aluminosilicates and related natural particles (gypsum, quartz, calcite and reacted sea salt). The Fe isotopic composition (d 56 Fe = 0.14 ± 0.11‰) measured in the close urban environment of the steel metallurgy plant appears coherent with an external mixing of industrial and continental Fe-containing tropospheric aerosols, as evidenced by individual particle chemical analysis. Our isotopic data provide a first estimation of an anthropogenic source term as part of the study of photochemically promoted dissolution processes and related Fe fractionations in tropospheric aerosols.","publication_date":{"day":null,"month":null,"year":2008,"errors":{}},"publication_name":"Chemosphere","grobid_abstract_attachment_id":52420489},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186863/Iron_isotopic_fractionation_in_industrial_emissions_and_urban_aerosols","translated_internal_url":"","created_at":"2017-04-01T10:05:23.493-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304523,"work_id":32186863,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176442,"email":"j***z@tech-brest-iroise.fr","display_order":0,"name":"Juliette Rimetz-Planchon","title":"Iron isotopic fractionation in industrial emissions 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hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32186851/Zn_isotope_study_of_atmospheric_emissions_and_dry_depositions_within_a_5_km_radius_of_a_Pb_Zn_refinery"><img alt="Research paper thumbnail of Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery" class="work-thumbnail" src="https://attachments.academia-assets.com/52420484/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32186851/Zn_isotope_study_of_atmospheric_emissions_and_dry_depositions_within_a_5_km_radius_of_a_Pb_Zn_refinery">Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery</a></div><div class="wp-workCard_item"><span>Atmospheric Environment</span><span>, 2009</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="a9065319f17bc2f103c8e9b48513f3f0" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420484,"asset_id":32186851,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420484/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32186851"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div 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{"id":32186851,"title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery","translated_title":"","metadata":{"grobid_abstract":"The present paper examines the use of zinc isotopes as tracers of atmospheric sources and focuses on the potential fractionation of Zn isotopes through anthropogenic processes. In order to do so, Zn isotopic ratios are measured in enriched ores and airborne particles associated with pyrometallurgical activities of one of the major Pb-Zn refineries in France. Supporting the isotopic investigation, this paper also compares morphological and chemical characteristics of Zn particles collected on dry deposition plates (''environmental samples'') placed within a 5 km radius of the smelter, with those of Zn particles collected inside the plant (''process samples''), i.e. dust collected from the main exhaust system of the plant. To ensure a constant isotopic ''supply'', the refinery processed a specific set of ores during the sampling campaigns, as agreed with the executive staff of the plant. Enriched ores and dust produced by the successive Zn extraction steps show strong isotope fractionation (from À0.66 to þ0.22\u0026) mainly related to evaporation processes within the blast furnaces. Dust from the main chimney displays a d 66 Zn value of À0.67\u0026. Application of the Rayleigh equation to evaluate the fractionation factor associated with the Zn vapor produced after a free evaporation gives a range of a ore/vapor from 1.0004 to 1.0008. The dry deposits, collected on plates downwind of the refinery, display d 66 Zn variations of up to þ0.7\u0026. However, it is to be noted that between 190 and 1250 m from the main chimney of the refinery, the dry deposits show a high level of large (\u003e10 mm) Zn, S, Fe and O bearing aggregates characterized by positive d 66 Zn values (þ0.02 to þ0.19\u0026). These airborne particles probably derive from the re-suspension of slag heaps and local emissions from the working-units. In contrast, from 1720 to 4560 m, the dry deposits are comprised of small (PM10) particles, including spherical Zn-bearing aggregates, showing negative d 66 Zn values (À0.52 to À0.02\u0026). Our results suggest that the source of the distal dry fallouts is the main chimney plume, whose light Zn isotopic signature they preserve. Based on Zn isotopic analysis in combination with morphological and chemical characteristics of airborne particles, the present study suggests the traceability of smelter dusts by Zn isotopes.","publication_date":{"day":null,"month":null,"year":2009,"errors":{}},"publication_name":"Atmospheric Environment","grobid_abstract_attachment_id":52420484},"translated_abstract":null,"internal_url":"https://www.academia.edu/32186851/Zn_isotope_study_of_atmospheric_emissions_and_dry_depositions_within_a_5_km_radius_of_a_Pb_Zn_refinery","translated_internal_url":"","created_at":"2017-04-01T10:05:22.194-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":28304521,"work_id":32186851,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176441,"email":"a***z@ulb.ac.be","display_order":0,"name":"Aurélien Taillez","title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery"},{"id":28304522,"work_id":32186851,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":6176442,"email":"j***z@tech-brest-iroise.fr","display_order":4194304,"name":"Juliette Rimetz-Planchon","title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery"},{"id":28305013,"work_id":32186851,"tagging_user_id":62411756,"tagged_user_id":32803471,"co_author_invite_id":null,"email":"n***l@ulb.ac.be","display_order":6291456,"name":"N. Mattielli","title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery"},{"id":28305014,"work_id":32186851,"tagging_user_id":62411756,"tagged_user_id":40707795,"co_author_invite_id":null,"email":"e***x@mines-douai.fr","display_order":7340032,"name":"Espéranza Perdrix","title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery"},{"id":28305015,"work_id":32186851,"tagging_user_id":62411756,"tagged_user_id":21265063,"co_author_invite_id":null,"email":"j***t@gmail.com","affiliation":"Université de Bordeaux","display_order":7864320,"name":"Jérôme Petit","title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery"},{"id":28305076,"work_id":32186851,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":323565,"email":"p***l@mren2.univ-littoral.fr","display_order":8126464,"name":"Pascal Flament","title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery"},{"id":28305078,"work_id":32186851,"tagging_user_id":62411756,"tagged_user_id":null,"co_author_invite_id":1714213,"email":"k***t@mren2.univ-littoral.fr","display_order":8257536,"name":"Karine Deboudt","title":"Zn isotope study of atmospheric emissions and dry depositions within a 5 km radius of a Pb–Zn refinery"}],"downloadable_attachments":[{"id":52420484,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420484/thumbnails/1.jpg","file_name":"Zn_isotope_study_of_atmospheric_emission20170401-6059-ovuyft.pdf","download_url":"https://www.academia.edu/attachments/52420484/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Zn_isotope_study_of_atmospheric_emission.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420484/Zn_isotope_study_of_atmospheric_emission20170401-6059-ovuyft-libre.pdf?1491067321=\u0026response-content-disposition=attachment%3B+filename%3DZn_isotope_study_of_atmospheric_emission.pdf\u0026Expires=1732900770\u0026Signature=H3PbUfykdReMgDb5zR6D7aZxDsDj9uVB1uRQcS96ObX70nHfotPizQLUBiTkO5eVTyrrJMcGSx0Izz0Ru9Tupmp1OqXqy3Dd5yuWx2CItoYV2FfYF8GAN2smOctelLVi5ViiKhLOG3kLMW6ap9RqI~O16fwUkDQbKmhz3uzNqIh3-85zdORGTtQl1X-bzbNIOwF3ckublUzXFFahoCTf2ZHH~85Rz5j7HalDziM6rj7L0nOTxT6LndYuxfiv-r7rs6ngToUoHEMo9D4pD6cuo3NuRjteWJMguZ2J-XbAGBSyUXEBH4J7CimL2Qs0txCWJcMFw86WjHscHcl3pBOZ8Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Zn_isotope_study_of_atmospheric_emissions_and_dry_depositions_within_a_5_km_radius_of_a_Pb_Zn_refinery","translated_slug":"","page_count":8,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420484,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420484/thumbnails/1.jpg","file_name":"Zn_isotope_study_of_atmospheric_emission20170401-6059-ovuyft.pdf","download_url":"https://www.academia.edu/attachments/52420484/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Zn_isotope_study_of_atmospheric_emission.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420484/Zn_isotope_study_of_atmospheric_emission20170401-6059-ovuyft-libre.pdf?1491067321=\u0026response-content-disposition=attachment%3B+filename%3DZn_isotope_study_of_atmospheric_emission.pdf\u0026Expires=1732900770\u0026Signature=H3PbUfykdReMgDb5zR6D7aZxDsDj9uVB1uRQcS96ObX70nHfotPizQLUBiTkO5eVTyrrJMcGSx0Izz0Ru9Tupmp1OqXqy3Dd5yuWx2CItoYV2FfYF8GAN2smOctelLVi5ViiKhLOG3kLMW6ap9RqI~O16fwUkDQbKmhz3uzNqIh3-85zdORGTtQl1X-bzbNIOwF3ckublUzXFFahoCTf2ZHH~85Rz5j7HalDziM6rj7L0nOTxT6LndYuxfiv-r7rs6ngToUoHEMo9D4pD6cuo3NuRjteWJMguZ2J-XbAGBSyUXEBH4J7CimL2Qs0txCWJcMFw86WjHscHcl3pBOZ8Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":55,"name":"Environmental Engineering","url":"https://www.academia.edu/Documents/in/Environmental_Engineering"},{"id":4310,"name":"Speciation","url":"https://www.academia.edu/Documents/in/Speciation"},{"id":60285,"name":"Atmospheric sciences","url":"https://www.academia.edu/Documents/in/Atmospheric_sciences"},{"id":108679,"name":"PM","url":"https://www.academia.edu/Documents/in/PM"},{"id":158165,"name":"Zinc","url":"https://www.academia.edu/Documents/in/Zinc"},{"id":640682,"name":"Isotope fractionation","url":"https://www.academia.edu/Documents/in/Isotope_fractionation"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":2490855,"name":"Dry Deposition","url":"https://www.academia.edu/Documents/in/Dry_Deposition"}],"urls":[]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187300"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187300/Isotopic_study_of_two_biolimiting_metals_Zn_and_Cu_in_industrial_aerosols"><img alt="Research paper thumbnail of Isotopic study of two biolimiting metals (Zn and Cu) in industrial aerosols" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187300/Isotopic_study_of_two_biolimiting_metals_Zn_and_Cu_in_industrial_aerosols">Isotopic study of two biolimiting metals (Zn and Cu) in industrial aerosols</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT The goal of the present isotopic study is to characterize atmospheric Zn and Cu flux fro...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT The goal of the present isotopic study is to characterize atmospheric Zn and Cu flux from industrial activities. Zn and Cu belong to traditional biolimiting elements. The geochemical cycle of these elements in the Earth superficial envelopes influences the biological productivity in oceans or in soils and, in turn, the global environment (Maréchal et al., 2000; Pichat et al., 2003). Other than Zn and Cu arising from minor geogenic processes, all other sources of Zn and Cu are anthropogenic. Among world-wide anthropogenic sources of Cu and Zn aerosols, metallurgical processing for Cu and steel production, as well as coal production are among the major sources (Pacyna, 1998). Samples from two metallurgical plants, a Pb-Zn refinery and an integrated steel mill located in Northern France not far away from the southern bight of the North Sea, are investigated in the present study. Samples are ores and dusts directly collected on filtration devices mounted on the main exhaust systems of the plants. Dry deposi-tion plates were positioned near working units previously recognized as major aerosol emission sources (cf. Franssens et al., 2004): sintering plant and steel shop unit, and the main chimneystack.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187300"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187300"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187300; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187300]").text(description); $(".js-view-count[data-work-id=32187300]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187300; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187300']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187300, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=32187300]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187300,"title":"Isotopic study of two biolimiting metals (Zn and Cu) in industrial aerosols","translated_title":"","metadata":{"abstract":"ABSTRACT The goal of the present isotopic study is to characterize atmospheric Zn and Cu flux from industrial activities. Zn and Cu belong to traditional biolimiting elements. The geochemical cycle of these elements in the Earth superficial envelopes influences the biological productivity in oceans or in soils and, in turn, the global environment (Maréchal et al., 2000; Pichat et al., 2003). Other than Zn and Cu arising from minor geogenic processes, all other sources of Zn and Cu are anthropogenic. Among world-wide anthropogenic sources of Cu and Zn aerosols, metallurgical processing for Cu and steel production, as well as coal production are among the major sources (Pacyna, 1998). Samples from two metallurgical plants, a Pb-Zn refinery and an integrated steel mill located in Northern France not far away from the southern bight of the North Sea, are investigated in the present study. Samples are ores and dusts directly collected on filtration devices mounted on the main exhaust systems of the plants. Dry deposi-tion plates were positioned near working units previously recognized as major aerosol emission sources (cf. Franssens et al., 2004): sintering plant and steel shop unit, and the main chimneystack."},"translated_abstract":"ABSTRACT The goal of the present isotopic study is to characterize atmospheric Zn and Cu flux from industrial activities. Zn and Cu belong to traditional biolimiting elements. The geochemical cycle of these elements in the Earth superficial envelopes influences the biological productivity in oceans or in soils and, in turn, the global environment (Maréchal et al., 2000; Pichat et al., 2003). Other than Zn and Cu arising from minor geogenic processes, all other sources of Zn and Cu are anthropogenic. Among world-wide anthropogenic sources of Cu and Zn aerosols, metallurgical processing for Cu and steel production, as well as coal production are among the major sources (Pacyna, 1998). Samples from two metallurgical plants, a Pb-Zn refinery and an integrated steel mill located in Northern France not far away from the southern bight of the North Sea, are investigated in the present study. Samples are ores and dusts directly collected on filtration devices mounted on the main exhaust systems of the plants. Dry deposi-tion plates were positioned near working units previously recognized as major aerosol emission sources (cf. Franssens et al., 2004): sintering plant and steel shop unit, and the main chimneystack.","internal_url":"https://www.academia.edu/32187300/Isotopic_study_of_two_biolimiting_metals_Zn_and_Cu_in_industrial_aerosols","translated_internal_url":"","created_at":"2017-04-01T10:16:22.992-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Isotopic_study_of_two_biolimiting_metals_Zn_and_Cu_in_industrial_aerosols","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); 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window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187369]").text(description); $(".js-view-count[data-work-id=32187369]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187369; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187369']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187369, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187394"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/32187394/Chemical_composition_of_tropospheric_particulate_matter_in_West_Africa_Natural_and_pollution_source_assessment"><img alt="Research paper thumbnail of Chemical composition of tropospheric particulate matter in West Africa: Natural and pollution source assessment" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/32187394/Chemical_composition_of_tropospheric_particulate_matter_in_West_Africa_Natural_and_pollution_source_assessment">Chemical composition of tropospheric particulate matter in West Africa: Natural and pollution source assessment</a></div><div class="wp-workCard_item"><span>Geochmica Et Cosmochimica Acta</span><span>, Jul 1, 2008</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187394"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187394"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187394; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187121"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187121/Multi_stage_mixing_in_subduction_zones_Application_to_Merapi_volcano_Java_island_Sunda_arc_"><img alt="Research paper thumbnail of Multi-stage mixing in subduction zones: Application to Merapi volcano (Java island, Sunda arc)" class="work-thumbnail" src="https://attachments.academia-assets.com/52420629/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187121/Multi_stage_mixing_in_subduction_zones_Application_to_Merapi_volcano_Java_island_Sunda_arc_">Multi-stage mixing in subduction zones: Application to Merapi volcano (Java island, Sunda arc)</a></div><div class="wp-workCard_item"><span>Geochimica Et Cosmochimica Acta Acta Geochimica Et Cosmochimica Acta Acta Geochimica Et Cosmochimica Acta Acta Geochimica Et Cosmochimica Acta Acta</span><span>, Feb 1, 2006</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Many studies have argued for the contribution of at least three components, namely the mantle wed...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Many studies have argued for the contribution of at least three components, namely the mantle wedge, the subducted oceanic crust, and its sediment cover, to describe the geochemistry of island arc volcanics. However, isotope correlations reflecting a simple binary mixing can be observed at the scale of a single arc island or volcano. Here we investigate the possibility that these trends reflect pseudo-binary mixing relationships in a three-component system. We present a simplified, two-stage model for the systematic isotope modelling of a cogenetic suite of arc lavas. This includes metasomatism of portions of the mantle wedge by hydrous phases released from the down-going oceanic crust, and sediments, followed by progressive mixing and melting. A consequence of this model is that it leads to a two end-member mixing process from the mantle wedge, oceanic crust, and sediment components. To solve the model we reduce it to a step-by-step procedure combined with a Monte-Carlo simulation. The procedure consists of: (i) producing a large number of random values on each variable of the model; (ii) using the computed values to calculate the isotopic compositions of lavas; and (iii) comparing the obtained isotopic compositions with measured data. Applied to a new set of Sr, Nd, and Pb isotope data for volcanics (basalts, basaltic andesites, trachybasalts, and basaltic trachyandesites) from Merapi volcano (Java island, Sunda arc), the model successfully reproduces the binary mixing relationships previously documented for the medium-K and high-K lava series from this volcano, thus giving further support to the hypothesis that this distinction is inherited from the primary magmas and primarily reflects a property of the mantle source. The results allow identification of a set of numerical values for bulk partition coefficients (solid/hydrous fluid, and solid/H 2O-rich melt) and variables (e.g., the mass ratio between the metasomatizing phase and the mantle wedge), which can be used for quantitative arc-lava petrogenetic calculations. They also require a direct relationship between dehydration of the slab and melting of the metasomatized mantle wedge. Finally, our evaluation shows that for isotope modelling of the Merapi lavas, the two-stage procedure is controlled more by the considered source components (mantle wedge, oceanic crust, sediments, and their derivatives) than by the various processes involved (dehydration, melting, and mixing).</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6bb3e938dfa5f595dc8b7addbd1ce38d" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420629,"asset_id":32187121,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420629/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187121"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187121"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187121; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32187121]").text(description); $(".js-view-count[data-work-id=32187121]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32187121; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='32187121']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 32187121, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "6bb3e938dfa5f595dc8b7addbd1ce38d" } } $('.js-work-strip[data-work-id=32187121]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":32187121,"title":"Multi-stage mixing in subduction zones: Application to Merapi volcano (Java island, Sunda arc)","translated_title":"","metadata":{"abstract":"Many studies have argued for the contribution of at least three components, namely the mantle wedge, the subducted oceanic crust, and its sediment cover, to describe the geochemistry of island arc volcanics. 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Applied to a new set of Sr, Nd, and Pb isotope data for volcanics (basalts, basaltic andesites, trachybasalts, and basaltic trachyandesites) from Merapi volcano (Java island, Sunda arc), the model successfully reproduces the binary mixing relationships previously documented for the medium-K and high-K lava series from this volcano, thus giving further support to the hypothesis that this distinction is inherited from the primary magmas and primarily reflects a property of the mantle source. The results allow identification of a set of numerical values for bulk partition coefficients (solid/hydrous fluid, and solid/H 2O-rich melt) and variables (e.g., the mass ratio between the metasomatizing phase and the mantle wedge), which can be used for quantitative arc-lava petrogenetic calculations. They also require a direct relationship between dehydration of the slab and melting of the metasomatized mantle wedge. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="32187262"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/32187262/Sr_Nd_Hf_Pb_isotope_and_trace_element_evidence_for_the_origin_of_alkalic_basalts_in_the_Garibaldi_Belt_northern_Cascade_arc"><img alt="Research paper thumbnail of Sr-Nd-Hf-Pb isotope and trace element evidence for the origin of alkalic basalts in the Garibaldi Belt, northern Cascade arc" class="work-thumbnail" src="https://attachments.academia-assets.com/52420738/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/32187262/Sr_Nd_Hf_Pb_isotope_and_trace_element_evidence_for_the_origin_of_alkalic_basalts_in_the_Garibaldi_Belt_northern_Cascade_arc">Sr-Nd-Hf-Pb isotope and trace element evidence for the origin of alkalic basalts in the Garibaldi Belt, northern Cascade arc</a></div><div class="wp-workCard_item"><span>Geochemistry, Geophysics, Geosystems</span><span>, 2013</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="320b923b20fa40896ca64b87d5c57549" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":52420738,"asset_id":32187262,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/52420738/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="32187262"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="32187262"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32187262; 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Meager (BSM volcanic centers) are alkalic, atypical for an arc setting. Subduction signatures are negligible or absent from primitive alkalic basalts from Salal Glacier and Bridge River, while altered oceanic crust may have contributed a minimal amount of fluid at Mt. Meager. More evolved BSM basalts display trace element signatures considered typical of arc lavas, but this is a consequence of deep crustal assimilation rather than primary input from the subducted slab. Primary BSM basalts represent 3-8% melts that segregated from enriched garnet lherzolite at significantly higher temperatures and pressures (70-105 km) than calc-alkaline Cascade arc basalts. The BSM mantle source is significantly more incompatible element-enriched than the depleted mantle tapped by calc-alkaline Cascade arc basalts. The BSM basalts are also isotopically distinct from calc-alkaline Cascade arc basalts, more similar to MORB and intraplate basalts of the NE Pacific and NW North America. The relatively deep, hot, and geochemically distinct mantle source for BSM basalts is consistent with upwelling asthenosphere. The BSM volcanic centers are close to the projected trace of the Nootka fault, which forms the boundary between the subducting Juan de Fuca plate and the near-stagnant Explorer plate. A gap or attenuated zone between the plates may promote upwelling of enriched asthenosphere that undergoes low-degree decompression melting to generate alkalic basalts that are essentially free of slab input yet occur in an arc setting.","publication_date":{"day":null,"month":null,"year":2013,"errors":{}},"publication_name":"Geochemistry, Geophysics, Geosystems","grobid_abstract_attachment_id":52420738},"translated_abstract":null,"internal_url":"https://www.academia.edu/32187262/Sr_Nd_Hf_Pb_isotope_and_trace_element_evidence_for_the_origin_of_alkalic_basalts_in_the_Garibaldi_Belt_northern_Cascade_arc","translated_internal_url":"","created_at":"2017-04-01T10:16:11.079-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":62411756,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":52420738,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420738/thumbnails/1.jpg","file_name":"Sr-Nd-Hf-Pb_isotope_and_trace_element_ev20170401-6059-11cpmet.pdf","download_url":"https://www.academia.edu/attachments/52420738/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Sr_Nd_Hf_Pb_isotope_and_trace_element_ev.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420738/Sr-Nd-Hf-Pb_isotope_and_trace_element_ev20170401-6059-11cpmet-libre.pdf?1491067589=\u0026response-content-disposition=attachment%3B+filename%3DSr_Nd_Hf_Pb_isotope_and_trace_element_ev.pdf\u0026Expires=1733097978\u0026Signature=NlmViQvfa8Tvlc5VpblvaeBDglmJoJDojgYquIAHJqCAvE~b917PibasMAjG-gFRXzuIiX1ofnzS8WjUKbr42zQlSwybGVQCKXOvqR5AZB1fSRkP0YlzWmjc1xy1fN1wEutfbvhoWmaI8KtpdHlKhVJTtmVRgZmTLalIzSBEkda0ZwNMm6~~xef1HUBP8bYOa3lYlEV57sxaX4l3Nlg0QASKSDZImbWL4QJPuFcFk-egTEK-n927Qq7lSLsK45XZR-n1fBJL-fDI-OIkWNxt-THC0P3F2HPVQbpFgEbXlC-di4aBwRfQnqDa37EMwOFb48n8gSYIkQWgkm4-2PEmRQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Sr_Nd_Hf_Pb_isotope_and_trace_element_evidence_for_the_origin_of_alkalic_basalts_in_the_Garibaldi_Belt_northern_Cascade_arc","translated_slug":"","page_count":30,"language":"en","content_type":"Work","owner":{"id":62411756,"first_name":"Dominique","middle_initials":"","last_name":"Weis","page_name":"DominiqueWeis","domain_name":"ubc","created_at":"2017-04-01T10:04:05.164-07:00","display_name":"Dominique Weis","url":"https://ubc.academia.edu/DominiqueWeis"},"attachments":[{"id":52420738,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/52420738/thumbnails/1.jpg","file_name":"Sr-Nd-Hf-Pb_isotope_and_trace_element_ev20170401-6059-11cpmet.pdf","download_url":"https://www.academia.edu/attachments/52420738/download_file?st=MTczMzA5NDM3OCw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Sr_Nd_Hf_Pb_isotope_and_trace_element_ev.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/52420738/Sr-Nd-Hf-Pb_isotope_and_trace_element_ev20170401-6059-11cpmet-libre.pdf?1491067589=\u0026response-content-disposition=attachment%3B+filename%3DSr_Nd_Hf_Pb_isotope_and_trace_element_ev.pdf\u0026Expires=1733097978\u0026Signature=NlmViQvfa8Tvlc5VpblvaeBDglmJoJDojgYquIAHJqCAvE~b917PibasMAjG-gFRXzuIiX1ofnzS8WjUKbr42zQlSwybGVQCKXOvqR5AZB1fSRkP0YlzWmjc1xy1fN1wEutfbvhoWmaI8KtpdHlKhVJTtmVRgZmTLalIzSBEkda0ZwNMm6~~xef1HUBP8bYOa3lYlEV57sxaX4l3Nlg0QASKSDZImbWL4QJPuFcFk-egTEK-n927Qq7lSLsK45XZR-n1fBJL-fDI-OIkWNxt-THC0P3F2HPVQbpFgEbXlC-di4aBwRfQnqDa37EMwOFb48n8gSYIkQWgkm4-2PEmRQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences"},{"id":224577,"name":"Trace Elements","url":"https://www.academia.edu/Documents/in/Trace_Elements"}],"urls":[]}, dispatcherData: dispatcherData }); 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