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I study those ultramafic and mafic rocks in various types of occurrences such as xenoliths in basalts and kimberlites, ophiolites, orogenic lherzolitic massifs and layered intrusions. All these studies are focusing on the nature and evolution of the magmas and metasomatic melts percolating and accumulating within both the oceanic and sub-continental upper mantle and lower crust both in intraplate and subduction zone settings. For that purpose, I use detailed analyses of major and trace element contents in both bulk rocks and minerals using electron microprobe, and ICP-MS techniques (laser and solution). 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class="affiliations-container fake-truncate js-profile-affiliations"><div><a class="u-tcGrayDarker" href="https://omp.academia.edu/">Observatoire Midi-Pyrénées, Université de Toulouse III Paul Sabatier</a>, <a class="u-tcGrayDarker" href="https://omp.academia.edu/Departments/Geology/Documents">Geology</a>, <span class="u-tcGrayDarker">Faculty Member</span></div></div></div></div><div class="sidebar-cta-container"><button class="ds2-5-button hidden profile-cta-button grow js-profile-follow-button" data-broccoli-component="user-info.follow-button" data-click-track="profile-user-info-follow-button" data-follow-user-fname="Michel" data-follow-user-id="10246740" data-follow-user-source="profile_button" data-has-google="false"><span class="material-symbols-outlined" style="font-size: 20px" translate="no">add</span>Follow</button><button class="ds2-5-button hidden profile-cta-button grow js-profile-unfollow-button" data-broccoli-component="user-info.unfollow-button" 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class="user-bio-container"><div class="profile-bio fake-truncate js-profile-about" style="margin: 0px;">I have broad interests in petrology, mineralogy and geochemistry, with my greatest enthusiasm being in the study of magmatic and mantle ultrabasic and basic rocks. I study those ultramafic and mafic rocks in various types of occurrences such as xenoliths in basalts and kimberlites, ophiolites, orogenic lherzolitic massifs and layered intrusions. All these studies are focusing on the nature and evolution of the magmas and metasomatic melts percolating and accumulating within both the oceanic and sub-continental upper mantle and lower crust both in intraplate and subduction zone settings. For that purpose, I use detailed analyses of major and trace element contents in both bulk rocks and minerals using electron microprobe, and ICP-MS techniques (laser and solution). The final goal of all these studies is to better understand the nature and the evolution of the lower crust and the upper mantle in various settings, and in particular to better understand the nature and evolution of the crust-mantle boundary and the chemical exchanges taking place between these two major earth réservoirs.<br /><span class="u-fw700">Phone: </span>+33 (0)5 61 33 29 77<br /><b>Address: </b>Geosciences Environnement Toulouse, Observatoire Midi Pyrenees, Universite Toulouse III, 14 Av. E. Belin 31400 Toulouse, FRANCE<br /><div class="js-profile-less-about u-linkUnstyled u-tcGrayDarker u-textDecorationUnderline u-displayNone">less</div></div></div><div class="suggested-academics-container"><div class="suggested-academics--header"><h3 class="ds2-5-heading-sans-serif-xs">Related Authors</h3></div><ul class="suggested-user-card-list" data-nosnippet="true"><div class="suggested-user-card"><div class="suggested-user-card__avatar social-profile-avatar-container"><a data-nosnippet="" href="https://bergbaumuseum.academia.edu/NimaNezafati"><img class="profile-avatar u-positionAbsolute" alt="Nima Nezafati related author profile picture" border="0" onerror="if (this.src != '//a.academia-assets.com/images/s200_no_pic.png') this.src = '//a.academia-assets.com/images/s200_no_pic.png';" width="200" height="200" src="https://0.academia-photos.com/58779/17089/2005499/s200_nima.nezafati_.jpg" /></a></div><div class="suggested-user-card__user-info"><a 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Olsen</a><p class="suggested-user-card__user-info__subheader ds2-5-body-xs">Columbia University</p></div></div><div class="suggested-user-card"><div class="suggested-user-card__avatar social-profile-avatar-container"><a data-nosnippet="" href="https://usal.academia.edu/GabrielGutierrezAlonso"><img class="profile-avatar u-positionAbsolute" alt="Gabriel Gutierrez-Alonso related author profile picture" border="0" onerror="if (this.src != '//a.academia-assets.com/images/s200_no_pic.png') this.src = '//a.academia-assets.com/images/s200_no_pic.png';" width="200" height="200" src="https://0.academia-photos.com/175637/822125/1022101/s200_gabriel.gutierrez-alonso.jpg" /></a></div><div class="suggested-user-card__user-info"><a class="suggested-user-card__user-info__header ds2-5-body-sm-bold ds2-5-body-link" href="https://usal.academia.edu/GabrielGutierrezAlonso">Gabriel Gutierrez-Alonso</a><p class="suggested-user-card__user-info__subheader ds2-5-body-xs">University of Salamanca</p></div></div></ul></div><style type="text/css">.suggested-academics--header h3{font-size:16px;font-weight:500;line-height:20px}</style><div class="ri-section"><div class="ri-section-header"><span>Interests</span><a class="ri-more-link js-profile-ri-list-card" data-click-track="profile-user-info-primary-research-interest" data-has-card-for-ri-list="10246740">View All (22)</a></div><div class="ri-tags-container"><a data-click-track="profile-user-info-expand-research-interests" data-has-card-for-ri-list="10246740" href="https://www.academia.edu/Documents/in/Geology"><div id="js-react-on-rails-context" style="display:none" data-rails-context="{"inMailer":false,"i18nLocale":"en","i18nDefaultLocale":"en","href":"https://omp.academia.edu/MichelGregoire","location":"/MichelGregoire","scheme":"https","host":"omp.academia.edu","port":null,"pathname":"/MichelGregoire","search":null,"httpAcceptLanguage":null,"serverSide":false}"></div> <div class="js-react-on-rails-component" style="display:none" data-component-name="Pill" data-props="{"color":"gray","children":["Geology"]}" data-trace="false" data-dom-id="Pill-react-component-3bf03eb8-d386-488b-8c1f-8cbf03f495ad"></div> <div id="Pill-react-component-3bf03eb8-d386-488b-8c1f-8cbf03f495ad"></div> </a><a data-click-track="profile-user-info-expand-research-interests" data-has-card-for-ri-list="10246740" href="https://www.academia.edu/Documents/in/Earth_Sciences"><div class="js-react-on-rails-component" style="display:none" data-component-name="Pill" data-props="{"color":"gray","children":["Earth Sciences"]}" data-trace="false" data-dom-id="Pill-react-component-564d4363-f2b7-4f6e-b19a-cf6dda9c8bf1"></div> <div id="Pill-react-component-564d4363-f2b7-4f6e-b19a-cf6dda9c8bf1"></div> </a><a data-click-track="profile-user-info-expand-research-interests" data-has-card-for-ri-list="10246740" href="https://www.academia.edu/Documents/in/Geochemistry"><div class="js-react-on-rails-component" style="display:none" data-component-name="Pill" data-props="{"color":"gray","children":["Geochemistry"]}" data-trace="false" data-dom-id="Pill-react-component-5af3e0c7-58ff-4a1f-9669-184edd11ea20"></div> <div id="Pill-react-component-5af3e0c7-58ff-4a1f-9669-184edd11ea20"></div> </a><a data-click-track="profile-user-info-expand-research-interests" data-has-card-for-ri-list="10246740" href="https://www.academia.edu/Documents/in/Mineralogy"><div class="js-react-on-rails-component" style="display:none" data-component-name="Pill" data-props="{"color":"gray","children":["Mineralogy"]}" data-trace="false" data-dom-id="Pill-react-component-b7c51a1b-30f3-492e-9537-aef716ccb458"></div> <div id="Pill-react-component-b7c51a1b-30f3-492e-9537-aef716ccb458"></div> </a><a data-click-track="profile-user-info-expand-research-interests" data-has-card-for-ri-list="10246740" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry"><div class="js-react-on-rails-component" style="display:none" data-component-name="Pill" data-props="{"color":"gray","children":["Petrology and Geochemistry"]}" data-trace="false" data-dom-id="Pill-react-component-90d14ea7-9d1a-44e3-972f-20fd5617e31e"></div> <div id="Pill-react-component-90d14ea7-9d1a-44e3-972f-20fd5617e31e"></div> </a></div></div><div class="external-links-container"><ul class="profile-links new-profile js-UserInfo-social"><li class="left-most js-UserInfo-social-cv" data-broccoli-component="user-info.cv-button" data-click-track="profile-user-info-cv" data-cv-filename="CV_MichelGregoire_2019.pdf" data-placement="top" data-toggle="tooltip" href="/MichelGregoire/CurriculumVitae"><button class="ds2-5-text-link ds2-5-text-link--small" style="font-size: 20px; 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height: 88px !important; box-sizing: content-box; } .thumbnail-image { height: 100%; width: 100%; object-fit: cover; } .play-icon { position: absolute; width: 40px; height: 40px; top: calc(50% - 20px); left: calc(50% - 20px); } .video-duration { position: absolute; bottom: 2px; right: 2px; color: #ffffff; background-color: #000000; font-size: 12px; font-weight: 500; line-height: 12px; padding: 2px; }</style><div class="js-work-strip profile--work_container" data-video-id="3270"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" href="https://www.academia.edu/video/jZvDMj"><div class="work-thumbnail video-thumbnail-container"><img class="thumbnail-image" onerror="this.src='//a.academia-assets.com/images/videoicon.svg'" src="https://academia-edu-videos.s3.amazonaws.com/transcoded/jZvDMj/thumbnail.jpg?response-content-disposition=inline%3B%20filename%3D%22thumbnail.jpg%22%3B%20filename%2A%3DUTF-8%27%27thumbnail.jpg&response-content-type=image%2Fjpeg&X-Amz-Algorithm=AWS4-HMAC-SHA256&X-Amz-Credential=ASIATUSBJ6BAKB6DFY6Z%2F20250329%2Fus-east-1%2Fs3%2Faws4_request&X-Amz-Date=20250329T031340Z&X-Amz-Expires=10220&X-Amz-Security-Token=IQoJb3JpZ2luX2VjEAAaCXVzLWVhc3QtMSJIMEYCIQDdBobUjPLmWGvuVeWFsvkDeicB1xMPyT%2Fq5iz3IBFZhgIhAKCz6w4JFeOjurGqxbyqJZosLiAakjn8SY5ahrOZnKSyKo0ECGkQABoMMjUwMzE4ODExMjAwIgxiVEqORWt9W6MWcOEq6gMyQxnTFvTtS7cF%2B4k5iWNS8e8dR7Gi6LB8GkshyZr7lSTXr3hyGWQlAdo58lJ9TgV5n95FxJEibGMDTFH%2BbVhqP0yZ5Y88X1iXtpZdFsX58LKhU4JJa59QuV0ctC%2F5RbY8MSTo6eEi4HKhLIfFruNt97A%2B%2B4OzmOoasblc3UXb8o32yKPLs5zyE6jFPqZvz%2F13d6MwylKPmvAXOi7WBbb97rJY2IWONNotcKd7%2BiPfOpaHrUXqxQkEyNExEU%2Ba73RfkV30gBmB31InENQh%2F1REQGXV5OawrA0yCwzRwNaPyMTpk9JUn7d6qtDrTEt5RFGdK5xIkONsX5rxVET8bz3UUIAxWyk%2FpD7DhDvBSNN8tnAXYVt4g%2FaNahscMO9%2FBoPxEZvXzXt5BkGyFrHmLVn1K2bnEB4YD2eriFzr6MqnLKI68uFDG%2FL6r%2BL1k9RmAP5J5JwgpMc61%2Bn95LRl0jdNGNynNAFfUGHCfLLpGHDHZ1MTD7oVqRl7kpHkjsTTzii0lU6JeVbggmZguwHEblxTatC39NdHR2cTmu0c1HYfRA8j7dBoE%2FIf28Vu4%2FH6%2FK2oE8tPdnR5%2FdvFBhMEBPcjoJCMnvQml545Vm90IuZlfFOlhOwjA%2BGWMbXPdsfFw8XSR2bjGSF%2BrZKuMPDxnL8GOqQBpocFRMOxDltbvW8f4vf3p93JbRC21ud7zDaCDLDfwLFAgjPOURMhcDrcJWwDF7DFgb38MYfCdRxELRRt75LZO%2FvWGruiMFAtUyNcSWH9ajZnwWFK%2FrfCz6D3f3Fj%2FzFKdUcLvdxMWQFTv65zOaTlYEuM4xJ9U9DMs2ZjGn0BcHAr6i04qxUhII9ZtNldODSisUyr4Rs3Gy8ZpOP%2BnJzB7Wa71rc%3D&X-Amz-SignedHeaders=host&X-Amz-Signature=9fa54bdf8224eb23572609914dc8de3fe4022182e7cbf757cea4cb1b5d391601" /><img alt="Play" class="play-icon" src="//a.academia-assets.com/images/video-play-icon.svg" /><div class="video-duration">07:22</div></div></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" href="https://www.academia.edu/video/jZvDMj">The Midi Pyrenees Observatory and Geosciences Environnement Toulouse Research Laboratory (in 2014)</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Presentation of the "Observatoire Midi-Pyrénées" and of the laboratory Geosciences Environnement ...</span><a class="js-work-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">Presentation of the "Observatoire Midi-Pyrénées" and of the laboratory Geosciences Environnement Toulouse. Presented at the 2014 Geological Society of America (GSA) Annual Meeting (Vancouver, Canada)</span></div><div class="wp-workCard_item wp-workCard--actions"><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-video-id="jZvDMj"><a class="js-profile-work-strip-edit-button" href="https://omp.academia.edu/video/edit/jZvDMj" rel="nofollow" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-video-id="jZvDMj">12 views</span></span></span></div></div></div><div class="profile--tab_heading_container js-section-heading" data-section="Papers" id="Papers"><h3 class="profile--tab_heading_container">Papers by Michel Gregoire</h3></div><div class="js-work-strip profile--work_container" data-work-id="127478319"><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/127478319/Sustainability2025"><img alt="Research paper thumbnail of Sustainability2025" 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/127478319/Sustainability2025">Sustainability2025</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://omp.academia.edu/MichelGregoire">Michel Gregoire</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/JessicaKlar1">Jessica Klar</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/PCourjaultRad%C3%A9">Pierre Courjault-Radé</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/SebastienFabre1">Sébastien Fabre</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This study investigates uranium (U) and thorium (Th) levels in surface beach sediments from the ...</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">This study investigates uranium (U) and thorium (Th) levels in surface beach <br />sediments from the Central Gulf of Gabes (SE Tunisia), aiming to identify concentration zones, geochemical behaviors, and enrichment factors. U concentrations ranged from 0.71 to 38.00 mg/kg, exceeding Th levels, which ranged from 1.00 to 10.60 mg/kg. A positive correlation between U and Th indicates a common source, which is most likely phosphogypsum wastes, and similar geochemical behaviors. The central sector near Gabes’ fertilizer factories showed the highest U and Th concentrations, with factors such as,proximity to industrial discharge, port structures’ influence, organic matter enrichment, low seawater pH, and high phosphorus levels affecting the spatial distribution of these elements. Thermochemical analysis suggests that U and Th exhibit parallel chemical behaviors in low-pH, phosphate-rich conditions. This is the first study to document U and Th presence in phosphogypsum-contaminated beach sediments in Gabes, underlining potential risks to the environment and human health. The findings of this work contribute to the international database of U and Th contamination in coastal sediments, providing essential data to support sustainable strategies aimed at safeguarding human health and preserving local environments affected by phosphate fertilizer industry pollution.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="7895ea4cbffc1c09e4c01474bbcec4c6" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":121204659,"asset_id":127478319,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/121204659/download_file?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="127478319"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="127478319"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 127478319; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=127478319]").text(description); $(".js-view-count[data-work-id=127478319]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 127478319; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='127478319']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "7895ea4cbffc1c09e4c01474bbcec4c6" } } $('.js-work-strip[data-work-id=127478319]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":127478319,"title":"Sustainability2025","translated_title":"","metadata":{"abstract":"This study investigates uranium (U) and thorium (Th) levels in surface beach\r\nsediments from the Central Gulf of Gabes (SE Tunisia), aiming to identify concentration zones, geochemical behaviors, and enrichment factors. 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The findings of this work contribute to the international database of U and Th contamination in coastal sediments, providing essential data to support sustainable strategies aimed at safeguarding human health and preserving local environments affected by phosphate fertilizer industry pollution.","internal_url":"https://www.academia.edu/127478319/Sustainability2025","translated_internal_url":"","created_at":"2025-02-05T05:49:28.415-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":43079435,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":339069122,"co_author_invite_id":8334967,"email":"j***r@gmail.com","display_order":1,"name":"Jessica Klar","title":"Sustainability2025"},{"id":43079436,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":66204658,"co_author_invite_id":null,"email":"s***t@get.omp.eu","display_order":2,"name":"Sylvie castet","title":"Sustainability2025"},{"id":43079437,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":187138830,"co_author_invite_id":null,"email":"c***e@gmail.com","display_order":4,"name":"Pierre Courjault-Radé","title":"Sustainability2025"},{"id":43079438,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":339018268,"co_author_invite_id":8334968,"email":"s***e@irap.omp.eu","display_order":5,"name":"Sébastien Fabre","title":"Sustainability2025"}],"downloadable_attachments":[{"id":121204659,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://a.academia-assets.com/images/blank-paper.jpg","file_name":"Sustainability_2025.pdf","download_url":"https://www.academia.edu/attachments/121204659/download_file","bulk_download_file_name":"Sustainability2025.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/121204659/Sustainability_2025-libre.pdf?1738772188=\u0026response-content-disposition=attachment%3B+filename%3DSustainability2025.pdf\u0026Expires=1743209697\u0026Signature=HxedQM15-tjMKI4VBEc8oGxDEXLACFud5xoKTdFNZU9rnaRcvlf2OXxCwT889TxvSBtyAlnxPur0s3Py1pRRWDlZB6xNEh~vZIw~5qSlZrsI1-LtAnmJiHZhkwgDWKHaLpHazdnkUT9Wb4uXna-zydOmIspB-SIKfoFHgJm3Ylgl0Byq8QkqBk6pTsk12cl04gcJo6C9jLmdI6cDPKXqf~bm9ocnngD8bgkvKF7jtPfUrJgCf-K9Bj1AV6TRJrUJWqe~nEDEfY2c-uSLUMTAlrqeJsoNZ2qB63G9HeiQrbvCSy9Ve-bmcxzteapXwVpFjCK40edQETgzy~ZHsHDDxA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Sustainability2025","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"This study investigates uranium (U) and thorium (Th) levels in surface beach\r\nsediments from the Central Gulf of Gabes (SE Tunisia), aiming to identify concentration zones, geochemical behaviors, and enrichment factors. U concentrations ranged from 0.71 to 38.00 mg/kg, exceeding Th levels, which ranged from 1.00 to 10.60 mg/kg. A positive correlation between U and Th indicates a common source, which is most likely phosphogypsum wastes, and similar geochemical behaviors. The central sector near Gabes’ fertilizer factories showed the highest U and Th concentrations, with factors such as,proximity to industrial discharge, port structures’ influence, organic matter enrichment, low seawater pH, and high phosphorus levels affecting the spatial distribution of these elements. Thermochemical analysis suggests that U and Th exhibit parallel chemical behaviors in low-pH, phosphate-rich conditions. This is the first study to document U and Th presence in phosphogypsum-contaminated beach sediments in Gabes, underlining potential risks to the environment and human health. The findings of this work contribute to the international database of U and Th contamination in coastal sediments, providing essential data to support sustainable strategies aimed at safeguarding human health and preserving local environments affected by phosphate fertilizer industry pollution.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":121204659,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://a.academia-assets.com/images/blank-paper.jpg","file_name":"Sustainability_2025.pdf","download_url":"https://www.academia.edu/attachments/121204659/download_file","bulk_download_file_name":"Sustainability2025.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/121204659/Sustainability_2025-libre.pdf?1738772188=\u0026response-content-disposition=attachment%3B+filename%3DSustainability2025.pdf\u0026Expires=1743209697\u0026Signature=HxedQM15-tjMKI4VBEc8oGxDEXLACFud5xoKTdFNZU9rnaRcvlf2OXxCwT889TxvSBtyAlnxPur0s3Py1pRRWDlZB6xNEh~vZIw~5qSlZrsI1-LtAnmJiHZhkwgDWKHaLpHazdnkUT9Wb4uXna-zydOmIspB-SIKfoFHgJm3Ylgl0Byq8QkqBk6pTsk12cl04gcJo6C9jLmdI6cDPKXqf~bm9ocnngD8bgkvKF7jtPfUrJgCf-K9Bj1AV6TRJrUJWqe~nEDEfY2c-uSLUMTAlrqeJsoNZ2qB63G9HeiQrbvCSy9Ve-bmcxzteapXwVpFjCK40edQETgzy~ZHsHDDxA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":402,"name":"Environmental Science","url":"https://www.academia.edu/Documents/in/Environmental_Science"},{"id":3407,"name":"Environmental Studies","url":"https://www.academia.edu/Documents/in/Environmental_Studies"},{"id":3743,"name":"Environmental Geochemistry (Environmental Studies)","url":"https://www.academia.edu/Documents/in/Environmental_Geochemistry_Environmental_Studies_"},{"id":141315,"name":"Ecological Risk Assessment","url":"https://www.academia.edu/Documents/in/Ecological_Risk_Assessment"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-127478319-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="126842883"><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/126842883/JHM"><img alt="Research paper thumbnail of JHM" class="work-thumbnail" src="https://attachments.academia-assets.com/120661054/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/126842883/JHM">JHM</a></div><div class="wp-workCard_item"><span>Journal of Hazardous Materials</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE 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 foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a<br />spectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to<br />investigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine<br />the origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in<br />marine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,<br />and ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through<br />phosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)<br />destabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced<br />by wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific<br />organic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic<br />radiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated<br />with PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into<br />the coastal environment of Gabes.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="b41e19ad0e0a97373198b0a76a4cc028" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":120661054,"asset_id":126842883,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/120661054/download_file?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="126842883"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="126842883"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 126842883; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=126842883]").text(description); $(".js-view-count[data-work-id=126842883]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 126842883; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='126842883']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "b41e19ad0e0a97373198b0a76a4cc028" } } $('.js-work-strip[data-work-id=126842883]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":126842883,"title":"JHM","translated_title":"","metadata":{"doi":"10.1016/j.jhazmat.2024.135732","abstract":"The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a\nspectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to\ninvestigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine\nthe origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in\nmarine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,\nand ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through\nphosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)\ndestabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced\nby wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific\norganic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic\nradiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated\nwith PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into\nthe coastal environment of Gabes.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Journal of Hazardous Materials","grobid_abstract_attachment_id":120661054},"translated_abstract":"The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a\nspectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to\ninvestigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine\nthe origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in\nmarine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,\nand ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through\nphosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)\ndestabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced\nby wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific\norganic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic\nradiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated\nwith PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into\nthe coastal environment of Gabes.","internal_url":"https://www.academia.edu/126842883/JHM","translated_internal_url":"","created_at":"2025-01-06T05:22:31.319-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42927339,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":33462064,"co_author_invite_id":null,"email":"r***i@gmail.com","display_order":-3,"name":"Radhouane El Zrelli","title":"JHM"},{"id":42927340,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":38175029,"co_author_invite_id":null,"email":"s***e@irap.omp.eu","affiliation":"Observatoire Midi-Pyrénées, Université de Toulouse III Paul Sabatier","display_order":-2,"name":"Sébastien Fabre","title":"JHM"},{"id":42927341,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":66204658,"co_author_invite_id":null,"email":"s***t@get.omp.eu","display_order":-1,"name":"Sylvie castet","title":"JHM"},{"id":42927342,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":171331386,"co_author_invite_id":null,"email":"o***i@gmail.com","display_order":1,"name":"Oussema Fersi","title":"JHM"},{"id":42927343,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":163108689,"co_author_invite_id":null,"email":"c***e@ums-castaing.fr","display_order":2,"name":"Josse Claudie","title":"JHM"},{"id":42927344,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":11599272,"co_author_invite_id":null,"email":"p***e@orange.fr","display_order":3,"name":"Pierre Courjault-Radé","title":"JHM"},{"id":42927345,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":333067136,"co_author_invite_id":null,"email":"2***n@privaterelay.appleid.com","display_order":4,"name":"anne-marie cousin","title":"JHM"}],"downloadable_attachments":[{"id":120661054,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120661054/thumbnails/1.jpg","file_name":"JHM_2024.pdf","download_url":"https://www.academia.edu/attachments/120661054/download_file","bulk_download_file_name":"JHM.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120661054/JHM_2024-libre.pdf?1736172571=\u0026response-content-disposition=attachment%3B+filename%3DJHM.pdf\u0026Expires=1743209698\u0026Signature=WHXEzHx1vl4TmpsG-bvIbPZiurK7quGEhg7KJa7MKK-UzsiOupKDR~D0jcGxKgevIVYx~SjZAGlI11PpmUCkYexPrizyP04-l-2OLUbXlKwpm18J95~T543xspEphQTDAQzWg59q83m7LHlaf090ZlgvM8gIB0-h66LGarVvJ3O58jn686erXEwg6Daqcs~LB0VM1-4Z0fsF~AMM1QATvfx8MIEnWDeHJfvMO59Z~G9E1l6~O3QwWg9tCO7g7nyNq~afIQujbs8XYF6ruXT32qvFPyx~bdd-pcr82ymNpYvltr0azgXPlW9rqOJpgt4ki~ny-D67c5VyGppMo7RkLw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"JHM","translated_slug":"","page_count":13,"language":"en","content_type":"Work","summary":"The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a\nspectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to\ninvestigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine\nthe origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in\nmarine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,\nand ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through\nphosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)\ndestabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced\nby wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific\norganic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic\nradiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated\nwith PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into\nthe coastal environment of Gabes.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":120661054,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120661054/thumbnails/1.jpg","file_name":"JHM_2024.pdf","download_url":"https://www.academia.edu/attachments/120661054/download_file","bulk_download_file_name":"JHM.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120661054/JHM_2024-libre.pdf?1736172571=\u0026response-content-disposition=attachment%3B+filename%3DJHM.pdf\u0026Expires=1743209698\u0026Signature=WHXEzHx1vl4TmpsG-bvIbPZiurK7quGEhg7KJa7MKK-UzsiOupKDR~D0jcGxKgevIVYx~SjZAGlI11PpmUCkYexPrizyP04-l-2OLUbXlKwpm18J95~T543xspEphQTDAQzWg59q83m7LHlaf090ZlgvM8gIB0-h66LGarVvJ3O58jn686erXEwg6Daqcs~LB0VM1-4Z0fsF~AMM1QATvfx8MIEnWDeHJfvMO59Z~G9E1l6~O3QwWg9tCO7g7nyNq~afIQujbs8XYF6ruXT32qvFPyx~bdd-pcr82ymNpYvltr0azgXPlW9rqOJpgt4ki~ny-D67c5VyGppMo7RkLw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":402,"name":"Environmental Science","url":"https://www.academia.edu/Documents/in/Environmental_Science"},{"id":9513,"name":"MARINE POLLUTION","url":"https://www.academia.edu/Documents/in/MARINE_POLLUTION"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-126842883-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="126774625"><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/126774625/Lithos"><img alt="Research paper thumbnail of Lithos" class="work-thumbnail" src="https://attachments.academia-assets.com/120601592/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/126774625/Lithos">Lithos</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, 2025</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-...</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 granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-I low REE; Type-II high REE), leucotonalites, melatonalites and Qz-monzodiorites. These are I-type calc-alkaline granitoids, although classification of the newly identified melatonalites remains enigmatic, likely reflecting magma mixing between different sources for their formation. Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).<br />Fractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. Melatonalites and Type-II granodiorites appear to have been formed during the early evolution stages of subduction initiation, whereas leucotonalites represent the late-stage shallow crystallization granitoid phase.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="143ee8161517cd907c3d5e3f5a9308c4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":120601592,"asset_id":126774625,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/120601592/download_file?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="126774625"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="126774625"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 126774625; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=126774625]").text(description); $(".js-view-count[data-work-id=126774625]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 126774625; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='126774625']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "143ee8161517cd907c3d5e3f5a9308c4" } } $('.js-work-strip[data-work-id=126774625]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":126774625,"title":"Lithos","translated_title":"","metadata":{"doi":"10.1016/j.lithos.2024.107926","abstract":"The granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-I low REE; Type-II high REE), leucotonalites, melatonalites and Qz-monzodiorites. These are I-type calc-alkaline granitoids, although classification of the newly identified melatonalites remains enigmatic, likely reflecting magma mixing between different sources for their formation. Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).\nFractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. 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Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).\nFractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. Melatonalites and Type-II granodiorites appear to have been formed during the early evolution stages of subduction initiation, whereas leucotonalites represent the late-stage shallow crystallization granitoid phase.","internal_url":"https://www.academia.edu/126774625/Lithos","translated_internal_url":"","created_at":"2025-01-03T07:29:35.176-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42916769,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":374965,"co_author_invite_id":null,"email":"p***s@yahoo.com","affiliation":"National \u0026 Kapodistrian University of Athens","display_order":-4,"name":"Petros Koutsovitis","title":"Lithos"},{"id":42916770,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":58376876,"co_author_invite_id":null,"email":"m***n@gmail.com","display_order":-3,"name":"Michiel van der Meulen","title":"Lithos"},{"id":42916771,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":12114691,"co_author_invite_id":null,"email":"p***u@gmail.com","display_order":-2,"name":"Pavlos Tyrologou","title":"Lithos"},{"id":42916772,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":12369491,"co_author_invite_id":null,"email":"g***7@upatras.gr","affiliation":"University of Patras","display_order":-1,"name":"Alkiviades Sideridis","title":"Lithos"},{"id":42916773,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":465788,"email":"t***s@univie.ac.at","display_order":1,"name":"Theodoros Ntaflos","title":"Lithos"},{"id":42916774,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":244857696,"co_author_invite_id":null,"email":"l***s@gmail.com","display_order":2,"name":"konstantinos lentas","title":"Lithos"}],"downloadable_attachments":[{"id":120601592,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120601592/thumbnails/1.jpg","file_name":"Lithos_2025.pdf","download_url":"https://www.academia.edu/attachments/120601592/download_file","bulk_download_file_name":"Lithos.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120601592/Lithos_2025-libre.pdf?1735920364=\u0026response-content-disposition=attachment%3B+filename%3DLithos.pdf\u0026Expires=1743209698\u0026Signature=dhtRG5KcE8ROmY8faZCKyJLEW6LQvWV9HB5H9C9CsX4Q3sy1sIpm4DSMY62tn7VuVo9SrHqbuF5Om3ndLRThttKYkuU0o5g7MfblDpriGJ2~WrCq9H4DORbKVXsTU-Ows7TJ0R7miJe6rA7DInREODPdga35ZJYoSkzQoUw59POKu6BeOmWkYXMDPlxKKwvA7ZRB1lhYbz3s3sf6o4-lB2DETQrioDBRCDaj4bhe7MzgWpmTVL62J40blRK7RtHR6lqKdeXtH15YfTut6yv8vfT4y9PajGUt-UzKd3WdqUiYvIb~XWyFq7NFhVg4NkXslVaVvnxxFLNf8BRQaXtwNQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Lithos","translated_slug":"","page_count":19,"language":"en","content_type":"Work","summary":"The granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-I low REE; Type-II high REE), leucotonalites, melatonalites and Qz-monzodiorites. These are I-type calc-alkaline granitoids, although classification of the newly identified melatonalites remains enigmatic, likely reflecting magma mixing between different sources for their formation. Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).\nFractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. Melatonalites and Type-II granodiorites appear to have been formed during the early evolution stages of subduction initiation, whereas leucotonalites represent the late-stage shallow crystallization granitoid phase.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":120601592,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120601592/thumbnails/1.jpg","file_name":"Lithos_2025.pdf","download_url":"https://www.academia.edu/attachments/120601592/download_file","bulk_download_file_name":"Lithos.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120601592/Lithos_2025-libre.pdf?1735920364=\u0026response-content-disposition=attachment%3B+filename%3DLithos.pdf\u0026Expires=1743209698\u0026Signature=dhtRG5KcE8ROmY8faZCKyJLEW6LQvWV9HB5H9C9CsX4Q3sy1sIpm4DSMY62tn7VuVo9SrHqbuF5Om3ndLRThttKYkuU0o5g7MfblDpriGJ2~WrCq9H4DORbKVXsTU-Ows7TJ0R7miJe6rA7DInREODPdga35ZJYoSkzQoUw59POKu6BeOmWkYXMDPlxKKwvA7ZRB1lhYbz3s3sf6o4-lB2DETQrioDBRCDaj4bhe7MzgWpmTVL62J40blRK7RtHR6lqKdeXtH15YfTut6yv8vfT4y9PajGUt-UzKd3WdqUiYvIb~XWyFq7NFhVg4NkXslVaVvnxxFLNf8BRQaXtwNQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":28331,"name":"Granite (Earth Sciences)","url":"https://www.academia.edu/Documents/in/Granite_Earth_Sciences_"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-126774625-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="126769690"><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/126769690/CRGEOS"><img alt="Research paper thumbnail of CRGEOS" class="work-thumbnail" src="https://attachments.academia-assets.com/120597382/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/126769690/CRGEOS">CRGEOS</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/djerossemfelix">djerossem felix</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/Beno%C3%AEtJosephMbassa">Benoît Joseph Mbassa</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Comptes Rendus Géosciences</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones o...</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 poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="27a29c1011c3b7db2fbaf4838ba7c955" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":120597382,"asset_id":126769690,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/120597382/download_file?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="126769690"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="126769690"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 126769690; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=126769690]").text(description); $(".js-view-count[data-work-id=126769690]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 126769690; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='126769690']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "27a29c1011c3b7db2fbaf4838ba7c955" } } $('.js-work-strip[data-work-id=126769690]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":126769690,"title":"CRGEOS","translated_title":"","metadata":{"doi":"10.5802/crgeos.282","abstract":"The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.","ai_title_tag":"Geochemical Insights on Ouaddai Volcanics","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Comptes Rendus Géosciences","grobid_abstract_attachment_id":120597382},"translated_abstract":"The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.","internal_url":"https://www.academia.edu/126769690/CRGEOS","translated_internal_url":"","created_at":"2025-01-03T03:37:49.609-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42915748,"work_id":126769690,"tagging_user_id":10246740,"tagged_user_id":148209982,"co_author_invite_id":null,"email":"d***m@gmail.com","display_order":-3,"name":"djerossem felix","title":"CRGEOS"},{"id":42915749,"work_id":126769690,"tagging_user_id":10246740,"tagged_user_id":41335370,"co_author_invite_id":null,"email":"b***a@yahoo.fr","display_order":-2,"name":"Benoît Joseph Mbassa","title":"CRGEOS"},{"id":42915750,"work_id":126769690,"tagging_user_id":10246740,"tagged_user_id":2909958,"co_author_invite_id":null,"email":"o***e@get.omp.eu","affiliation":"Université Toulouse III","display_order":-1,"name":"Olivier Vanderhaeghe","title":"CRGEOS"}],"downloadable_attachments":[{"id":120597382,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120597382/thumbnails/1.jpg","file_name":"CRGEOS_2024.pdf","download_url":"https://www.academia.edu/attachments/120597382/download_file","bulk_download_file_name":"CRGEOS.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120597382/CRGEOS_2024-libre.pdf?1735904456=\u0026response-content-disposition=attachment%3B+filename%3DCRGEOS.pdf\u0026Expires=1743209698\u0026Signature=Pk2p0e7xWZOWw9LlqrtkD-qVS7eOSplx34yA0ATSoVg6K28LFpZVxrGHVE1xji4z3cyogDBIwbClvfRcjc68~5M4p8P10NDyUC8S03V5brZUP8Z6cLiiS12b5Te4PKA0U2Jxz7TS3ZJ~6mHUlBXbvsMHCBNh3EwLng7RxF~LMzcP79wJpxQpbi8ddyINJ8s7MEnkvnwQnF0RadhZu3V453~tvlX7FplF45PaAvoQS5Iws4NfT~l6qrG8UYUPcivsQcnj5yDz2wM1r6NQQJTvUQydyyHX9cMfFwXAbiNcp6Bxoxh3BZtukf4ztWu2iiLLHvewnK3vRiPMdLqdwEQIaA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"CRGEOS","translated_slug":"","page_count":19,"language":"en","content_type":"Work","summary":"The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":120597382,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120597382/thumbnails/1.jpg","file_name":"CRGEOS_2024.pdf","download_url":"https://www.academia.edu/attachments/120597382/download_file","bulk_download_file_name":"CRGEOS.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120597382/CRGEOS_2024-libre.pdf?1735904456=\u0026response-content-disposition=attachment%3B+filename%3DCRGEOS.pdf\u0026Expires=1743209698\u0026Signature=Pk2p0e7xWZOWw9LlqrtkD-qVS7eOSplx34yA0ATSoVg6K28LFpZVxrGHVE1xji4z3cyogDBIwbClvfRcjc68~5M4p8P10NDyUC8S03V5brZUP8Z6cLiiS12b5Te4PKA0U2Jxz7TS3ZJ~6mHUlBXbvsMHCBNh3EwLng7RxF~LMzcP79wJpxQpbi8ddyINJ8s7MEnkvnwQnF0RadhZu3V453~tvlX7FplF45PaAvoQS5Iws4NfT~l6qrG8UYUPcivsQcnj5yDz2wM1r6NQQJTvUQydyyHX9cMfFwXAbiNcp6Bxoxh3BZtukf4ztWu2iiLLHvewnK3vRiPMdLqdwEQIaA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"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") if (false) { Aedu.setUpFigureCarousel('profile-work-126769690-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="87011147"><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/87011147/Petrography_mineral_chemistry_and_geochemistry_of_hornblenditic_autholiths_and_hornblenditic_xenoliths_from_volcanic_alkaline_rocks_from_North_West_of_Marand_NW_Iran_"><img alt="Research paper thumbnail of Petrography, mineral chemistry and geochemistry of hornblenditic autholiths and hornblenditic xenoliths from volcanic alkaline rocks from North West of Marand (NW Iran)" class="work-thumbnail" src="https://attachments.academia-assets.com/91339933/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/87011147/Petrography_mineral_chemistry_and_geochemistry_of_hornblenditic_autholiths_and_hornblenditic_xenoliths_from_volcanic_alkaline_rocks_from_North_West_of_Marand_NW_Iran_">Petrography, mineral chemistry and geochemistry of hornblenditic autholiths and hornblenditic xenoliths from volcanic alkaline rocks from North West of Marand (NW Iran)</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://tabrizu.academia.edu/AhmadJahangiri">Ahmad Jahangiri</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Iranian Journal of Crystallography and Mineralogy</span><span>, 2018</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="538e9fe656c9fe2fd7ff931530c31c2c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":91339933,"asset_id":87011147,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/91339933/download_file?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="87011147"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="87011147"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 87011147; 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This study investigates hornblenditic autholiths and xenoliths found within trachy andesite and basaltic andesite rocks, classified into two groups based on plagioclase content: Group 1 with \u003c10% plagioclase, resembling the host volcanic magma, and Group 2 with \u003e20% plagioclase, indicating a different mantle-derived origin with less enrichment. The mineral chemistry and geochemical signatures reveal insights into the magmatic processes guiding these volcanic features.","publication_date":{"day":null,"month":null,"year":2018,"errors":{}},"publication_name":"Iranian Journal of Crystallography and Mineralogy"},"translated_abstract":null,"internal_url":"https://www.academia.edu/87011147/Petrography_mineral_chemistry_and_geochemistry_of_hornblenditic_autholiths_and_hornblenditic_xenoliths_from_volcanic_alkaline_rocks_from_North_West_of_Marand_NW_Iran_","translated_internal_url":"","created_at":"2022-09-21T03:56:44.095-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":4826161,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42605006,"work_id":87011147,"tagging_user_id":4826161,"tagged_user_id":10246740,"co_author_invite_id":null,"email":"m***e@get.omp.eu","affiliation":"Observatoire Midi-Pyrénées, Université de Toulouse III Paul 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dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-87011147-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124570903"><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/124570903/Insights_into_the_North_Patagonian_Massif_lower_crust_petrology_and_microstructure_of_granulite_xenoliths"><img alt="Research paper thumbnail of Insights into the North Patagonian Massif lower crust: petrology and microstructure of granulite xenoliths" class="work-thumbnail" src="https://attachments.academia-assets.com/118771293/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/124570903/Insights_into_the_North_Patagonian_Massif_lower_crust_petrology_and_microstructure_of_granulite_xenoliths">Insights into the North Patagonian Massif lower crust: petrology and microstructure of granulite xenoliths</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/NoeMuckensturm">Noé Muckensturm</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The continental lower crust constitutes a key zone for understanding the mantle-crust magmatic an...</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 continental lower crust constitutes a key zone for understanding the mantle-crust magmatic and mechanical transfers, but its study is hampered by the paucity of lower crust samples. Here, we characterise the petrological, geochemical and petrophysical processes structuring the lower crust of the North Patagonian Massif (NPM; Argentina) using a suite of representative mafic granulite and websterite xenoliths. These xenoliths were entrained by alkaline lavas from 5 volcanic centres that erupted between the Oligocene and Pleistocene. Electron microprobe and laser ablation inductively coupled plasma mass spectrometer (LA-ICPMS) were used to obtain in-situ geochemical data on the minerals, while microstructural data were obtained by Electron Backscatter Diffraction (EBSD). Both granulites and</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e6ceff20b4317884b1e14ad9bdc7f968" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118771293,"asset_id":124570903,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118771293/download_file?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="124570903"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124570903"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124570903; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124570903]").text(description); $(".js-view-count[data-work-id=124570903]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124570903; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124570903']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "e6ceff20b4317884b1e14ad9bdc7f968" } } $('.js-work-strip[data-work-id=124570903]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124570903,"title":"Insights into the North Patagonian Massif lower crust: petrology and microstructure of granulite xenoliths","translated_title":"","metadata":{"doi":"10.1093/petrology/egae100","ai_title_tag":"Granulite Xenoliths of North Patagonian Massif","grobid_abstract":"The continental lower crust constitutes a key zone for understanding the mantle-crust magmatic and mechanical transfers, but its study is hampered by the paucity of lower crust samples. Here, we characterise the petrological, geochemical and petrophysical processes structuring the lower crust of the North Patagonian Massif (NPM; Argentina) using a suite of representative mafic granulite and websterite xenoliths. These xenoliths were entrained by alkaline lavas from 5 volcanic centres that erupted between the Oligocene and Pleistocene. Electron microprobe and laser ablation inductively coupled plasma mass spectrometer (LA-ICPMS) were used to obtain in-situ geochemical data on the minerals, while microstructural data were obtained by Electron Backscatter Diffraction (EBSD). 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They constitute an important source of information about the melt migration mechanisms and related petrological processes in the shallowest part of the mantle beneath former oceanic spreading centres. In the field, these socalled 'melt migration structures' attract attention when they consist of mineral assemblages contrasting with that of their host peridotite. They therefore record a particular moment in the migration history: when the melt becomes out of equilibrium with the peridotite and causes a reaction impacting its modal composition, and/or when a temperature drop initiates the crystallization of the melt. The existence of cryptic effects of migration revealed by geochemical data shows that melts do not always leave a trail visible in the field. Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? What is the nature of the 'universal solvent' initiating infiltration melting and making channelized porous flow the most common mode of transport of magmas through a peridotite matrix regardless the tectonic setting? A fundamental message delivered by ophiolites is that the shallow mantle behaves as a particularly efficient reactive filter between the depths and the surface of the Earth. Unexpectedly, the reactions occurring there are enhanced by the hybridization between mafic melts and a hydrous component, whatever its origin (i.e. magmatic vs. hydrothermal). This hybridization triggers out of equilibrium reactions, leading to the formation of exotic lithologies, including metallic ores, and impacting the global geochemical cycle of a whole range of chemical elements.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e6bdb1f3e38b2929422c157faf3e847b" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118767046,"asset_id":124566052,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118767046/download_file?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="124566052"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124566052"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124566052; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124566052]").text(description); $(".js-view-count[data-work-id=124566052]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124566052; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124566052']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "e6bdb1f3e38b2929422c157faf3e847b" } } $('.js-work-strip[data-work-id=124566052]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124566052,"title":"The shallow mantle as a reactive filter: a hypothesis inspired and supported by field observations","translated_title":"","metadata":{"doi":"10.1180/EMU-notes.21.5","abstract":"The footprints of mafic melts travelling from the depths to the surface are abundant in the mantle section of ophiolites. They constitute an important source of information about the melt migration mechanisms and related petrological processes in the shallowest part of the mantle beneath former oceanic spreading centres. In the field, these socalled 'melt migration structures' attract attention when they consist of mineral assemblages contrasting with that of their host peridotite. They therefore record a particular moment in the migration history: when the melt becomes out of equilibrium with the peridotite and causes a reaction impacting its modal composition, and/or when a temperature drop initiates the crystallization of the melt. The existence of cryptic effects of migration revealed by geochemical data shows that melts do not always leave a trail visible in the field. Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? What is the nature of the 'universal solvent' initiating infiltration melting and making channelized porous flow the most common mode of transport of magmas through a peridotite matrix regardless the tectonic setting? A fundamental message delivered by ophiolites is that the shallow mantle behaves as a particularly efficient reactive filter between the depths and the surface of the Earth. 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They therefore record a particular moment in the migration history: when the melt becomes out of equilibrium with the peridotite and causes a reaction impacting its modal composition, and/or when a temperature drop initiates the crystallization of the melt. The existence of cryptic effects of migration revealed by geochemical data shows that melts do not always leave a trail visible in the field. Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? 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Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? What is the nature of the 'universal solvent' initiating infiltration melting and making channelized porous flow the most common mode of transport of magmas through a peridotite matrix regardless the tectonic setting? A fundamental message delivered by ophiolites is that the shallow mantle behaves as a particularly efficient reactive filter between the depths and the surface of the Earth. Unexpectedly, the reactions occurring there are enhanced by the hybridization between mafic melts and a hydrous component, whatever its origin (i.e. magmatic vs. hydrothermal). This hybridization triggers out of equilibrium reactions, leading to the formation of exotic lithologies, including metallic ores, and impacting the global geochemical cycle of a whole range of chemical elements.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118767046,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118767046/thumbnails/1.jpg","file_name":"EMU_21_Ch05.pdf","download_url":"https://www.academia.edu/attachments/118767046/download_file","bulk_download_file_name":"The_shallow_mantle_as_a_reactive_filter.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118767046/EMU_21_Ch05-libre.pdf?1728467451=\u0026response-content-disposition=attachment%3B+filename%3DThe_shallow_mantle_as_a_reactive_filter.pdf\u0026Expires=1743209698\u0026Signature=VhGKl-o11PXM58AAbyl4r5mIJ1JHv41lbbso~pFmLK2eph2LvUPn5PzWPydOosVmi0SmaUDxvXUCqViGIq1KkonXycNwQc5piB5Ni90288V8dTZcBy53~-bPRsUq74wudXtgYC8I1kF3-jPZVfKM51i45fOr8veoLxKR0U9xu-S4XflfThpDZddpiT7ZLo7B2HtQ9wFqfEhFFUzZ9tyx9sgiYuA3yaJpDIdbeQGWanZEnHaQF6jaWB4zE1ZO7kpiqbTF0dSbVRHksiidIWpocktDRYgv9VoR0BhEhz3Hv82PNPgnb3n7l7xkI8UtmHT6zEbdiNqSes1umYa-b6Nsrw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124566052-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565963"><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/124565963/Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us"><img alt="Research paper thumbnail of Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us" class="work-thumbnail" src="https://attachments.academia-assets.com/118766957/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/124565963/Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us">Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us</a></div><div class="wp-workCard_item"><span>EMU Notes in Mineralogy</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The present contribution synthesizes the main petrographic, mineralogical and chemical features o...</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 present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="881ab5a7262657f5cf20f35047fa5d9f" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766957,"asset_id":124565963,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766957/download_file?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="124565963"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565963"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565963; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565963]").text(description); $(".js-view-count[data-work-id=124565963]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565963; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565963']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "881ab5a7262657f5cf20f35047fa5d9f" } } $('.js-work-strip[data-work-id=124565963]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565963,"title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us","translated_title":"","metadata":{"doi":"10.1180/EMU-notes.21.3","abstract":"The present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"EMU Notes in Mineralogy"},"translated_abstract":"The present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.","internal_url":"https://www.academia.edu/124565963/Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us","translated_internal_url":"","created_at":"2024-10-09T02:26:37.534-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42517398,"work_id":124565963,"tagging_user_id":10246740,"tagged_user_id":32692857,"co_author_invite_id":null,"email":"g***h@u-psud.fr","affiliation":"Paris Sud XI University","display_order":1,"name":"Guillaume Delpech","title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us"},{"id":42517399,"work_id":124565963,"tagging_user_id":10246740,"tagged_user_id":25097216,"co_author_invite_id":null,"email":"m***b@univ-st-etienne.fr","affiliation":"Universite Jean Monnet - Saint-Etienne","display_order":2,"name":"Moine Bertrand","title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us"},{"id":42517400,"work_id":124565963,"tagging_user_id":10246740,"tagged_user_id":35541998,"co_author_invite_id":null,"email":"c***n@univ-st-etienne.fr","display_order":3,"name":"Jean-yves Cottin","title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us"}],"downloadable_attachments":[{"id":118766957,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766957/thumbnails/1.jpg","file_name":"EMU_21_Ch03.pdf","download_url":"https://www.academia.edu/attachments/118766957/download_file","bulk_download_file_name":"Nature_and_origin_of_heterogeneities_in.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766957/EMU_21_Ch03-libre.pdf?1728467439=\u0026response-content-disposition=attachment%3B+filename%3DNature_and_origin_of_heterogeneities_in.pdf\u0026Expires=1743209699\u0026Signature=EQtSkMr-N6IyhmGHnp2l0r~3snIqatNRUNykztSO55DdmUCw9EzBbLbAYEcmBJeB2vbCnUAnGk4zepA-gA6w34UMOXAQGe9x9CEy32g~yNEy9LwfE1PnAW4JsKHhEcH3hIzUWZXcWNiWA73XihGo599JxWCwcRkFpmhhMj7znLb6tHxoID3o1wGNJYg3LLL-5gTjFIUkuMLblsYJP5JQ8T~QtDckLAZAYfB0N0wxI9q2Ni3FIw00kNq2dimsa0im5ke2kiAuIlFsnnz6hiuGfMmnGgrxt0VJsAgyQkfnv36KRAVaagEhNhkfGMbwHslRMPHrbHfu10tXocru49IHiw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us","translated_slug":"","page_count":18,"language":"en","content_type":"Work","summary":"The present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766957,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766957/thumbnails/1.jpg","file_name":"EMU_21_Ch03.pdf","download_url":"https://www.academia.edu/attachments/118766957/download_file","bulk_download_file_name":"Nature_and_origin_of_heterogeneities_in.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766957/EMU_21_Ch03-libre.pdf?1728467439=\u0026response-content-disposition=attachment%3B+filename%3DNature_and_origin_of_heterogeneities_in.pdf\u0026Expires=1743209699\u0026Signature=EQtSkMr-N6IyhmGHnp2l0r~3snIqatNRUNykztSO55DdmUCw9EzBbLbAYEcmBJeB2vbCnUAnGk4zepA-gA6w34UMOXAQGe9x9CEy32g~yNEy9LwfE1PnAW4JsKHhEcH3hIzUWZXcWNiWA73XihGo599JxWCwcRkFpmhhMj7znLb6tHxoID3o1wGNJYg3LLL-5gTjFIUkuMLblsYJP5JQ8T~QtDckLAZAYfB0N0wxI9q2Ni3FIw00kNq2dimsa0im5ke2kiAuIlFsnnz6hiuGfMmnGgrxt0VJsAgyQkfnv36KRAVaagEhNhkfGMbwHslRMPHrbHfu10tXocru49IHiw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":123325,"name":"Mantle Geochemistry","url":"https://www.academia.edu/Documents/in/Mantle_Geochemistry"},{"id":134398,"name":"Mantle metasomatism","url":"https://www.academia.edu/Documents/in/Mantle_metasomatism"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565963-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565930"><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/124565930/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas"><img alt="Research paper thumbnail of Slab melting boosts the mantle wedge contribution to Li-rich magmas" 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">Slab melting boosts the mantle wedge contribution to Li-rich magmas</div><div class="wp-workCard_item"><span>Scientific reports</span><span>, Jul 2, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generat...</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 lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ &amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an &amp;quot;adakite&amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (&amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.</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="124565930"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565930"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565930; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565930]").text(description); $(".js-view-count[data-work-id=124565930]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565930; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565930']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565930]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565930,"title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas","translated_title":"","metadata":{"abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u0026amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \u0026amp;quot;adakite\u0026amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u0026amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","publication_date":{"day":2,"month":7,"year":2024,"errors":{}},"publication_name":"Scientific reports"},"translated_abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u0026amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \u0026amp;quot;adakite\u0026amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u0026amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","internal_url":"https://www.academia.edu/124565930/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_internal_url":"","created_at":"2024-10-09T02:24:25.517-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u0026amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \u0026amp;quot;adakite\u0026amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u0026amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":54668,"name":"Peridotite","url":"https://www.academia.edu/Documents/in/Peridotite"},{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism"},{"id":122773,"name":"Subduction","url":"https://www.academia.edu/Documents/in/Subduction"},{"id":123325,"name":"Mantle Geochemistry","url":"https://www.academia.edu/Documents/in/Mantle_Geochemistry"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":426446,"name":"Mantle Wedge","url":"https://www.academia.edu/Documents/in/Mantle_Wedge"},{"id":642278,"name":"Adakite","url":"https://www.academia.edu/Documents/in/Adakite"},{"id":3057331,"name":"Transition Zone","url":"https://www.academia.edu/Documents/in/Transition_Zone"}],"urls":[{"id":45061670,"url":"https://doi.org/10.1038/s41598-024-66174-y"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565930-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565929"><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/124565929/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite"><img alt="Research paper thumbnail of A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite" 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 geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite</div><div class="wp-workCard_item"><span>Chemical geology</span><span>, Jun 1, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpen...</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">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn&amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.</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="124565929"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565929"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565929; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565929]").text(description); $(".js-view-count[data-work-id=124565929]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565929; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565929']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565929]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565929,"title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite","translated_title":"","metadata":{"abstract":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn\u0026amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","publication_date":{"day":1,"month":6,"year":2024,"errors":{}},"publication_name":"Chemical geology"},"translated_abstract":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn\u0026amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","internal_url":"https://www.academia.edu/124565929/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_internal_url":"","created_at":"2024-10-09T02:24:24.836-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn\u0026amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16024,"name":"Chemical Geology","url":"https://www.academia.edu/Documents/in/Chemical_Geology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":75334,"name":"Fluid-rock interactions","url":"https://www.academia.edu/Documents/in/Fluid-rock_interactions"},{"id":521382,"name":"Gabbro","url":"https://www.academia.edu/Documents/in/Gabbro"},{"id":910472,"name":"Rodingites","url":"https://www.academia.edu/Documents/in/Rodingites"}],"urls":[{"id":45061669,"url":"https://doi.org/10.1016/j.chemgeo.2024.122237"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565929-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565926"><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/124565926/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_"><img alt="Research paper thumbnail of Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite - case study from the Kukes Massif (Mirdita ophiolite, Albania)" class="work-thumbnail" src="https://attachments.academia-assets.com/118766920/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/124565926/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_">Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite - case study from the Kukes Massif (Mirdita ophiolite, Albania)</a></div><div class="wp-workCard_item"><span>Journal of Geosciences</span><span>, May 20, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), ...</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 ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="b95aa46b2cd4f7cbbd7eec67fb24e6de" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766920,"asset_id":124565926,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766920/download_file?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="124565926"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565926"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565926; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565926]").text(description); $(".js-view-count[data-work-id=124565926]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565926; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565926']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "b95aa46b2cd4f7cbbd7eec67fb24e6de" } } $('.js-work-strip[data-work-id=124565926]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565926,"title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite - case study from the Kukes Massif (Mirdita ophiolite, Albania)","translated_title":"","metadata":{"ai_title_tag":"Melt-Rock Interaction in Kukes Massif Dunite","grobid_abstract":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","publication_date":{"day":20,"month":5,"year":2024,"errors":{}},"publication_name":"Journal of Geosciences","grobid_abstract_attachment_id":118766920},"translated_abstract":null,"internal_url":"https://www.academia.edu/124565926/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_","translated_internal_url":"","created_at":"2024-10-09T02:24:24.042-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118766920,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766920/thumbnails/1.jpg","file_name":"jgeosci_386_Mikrut.pdf","download_url":"https://www.academia.edu/attachments/118766920/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766920/jgeosci_386_Mikrut-libre.pdf?1728467477=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=Z3EnEDKUUmzu89ruA4MX1AxEb~8bm66bc8SEyo-IVi934PX7krZHkM7qy6Ykc6agDw38boMzt4FqbhJH6qW0sAse1CeIpGfX3WxmaRl8v3lozPI7fXztayNd7gczHNj3PrsEdHLq3Yuct1CUN37FTXwRcgOpVmwPKWE6uIo~67OW3urQWZ4mbR-q5sruGePVQQ16bEt9JfABHRKlsaHXwp6pFEH5AaOr9NYUK9P4KduTVkg4MnZI2zgzGJC2hqiNNoyUK86-g4SzXfMOzTlgjk0QhCbnX-tbHjP0Lr1OaRDdg1Z6pWNJWznOSjZ11huIsGVJ2NI5pWYAxGBvmZO3Bw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_","translated_slug":"","page_count":16,"language":"en","content_type":"Work","summary":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766920,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766920/thumbnails/1.jpg","file_name":"jgeosci_386_Mikrut.pdf","download_url":"https://www.academia.edu/attachments/118766920/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766920/jgeosci_386_Mikrut-libre.pdf?1728467477=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=Z3EnEDKUUmzu89ruA4MX1AxEb~8bm66bc8SEyo-IVi934PX7krZHkM7qy6Ykc6agDw38boMzt4FqbhJH6qW0sAse1CeIpGfX3WxmaRl8v3lozPI7fXztayNd7gczHNj3PrsEdHLq3Yuct1CUN37FTXwRcgOpVmwPKWE6uIo~67OW3urQWZ4mbR-q5sruGePVQQ16bEt9JfABHRKlsaHXwp6pFEH5AaOr9NYUK9P4KduTVkg4MnZI2zgzGJC2hqiNNoyUK86-g4SzXfMOzTlgjk0QhCbnX-tbHjP0Lr1OaRDdg1Z6pWNJWznOSjZ11huIsGVJ2NI5pWYAxGBvmZO3Bw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118766919,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766919/thumbnails/1.jpg","file_name":"jgeosci_386_Mikrut.pdf","download_url":"https://www.academia.edu/attachments/118766919/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766919/jgeosci_386_Mikrut-libre.pdf?1728467587=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=XipbAWT8IJV1HCFWdE0ceaWNDhKNt10zTE1HCZYYi5lPboY0i48bZ~PvRgAKeoKyju6uilvCJUciyjGMm9leqNtySHjchdzF1rL8632FaDSAvsdiN95TWNbp6IiFLon1Jl6T8TI87ZqWCpSwQVCcejk3No5EiZRMO0IiXrNiETwir4IL8WFxXwD97C5hVBMnreu64wsY7YsVwX~hwceTw~8XfxdQxzf4pVMAb~YWn~TTkI9~b-eqnMLvUL6FqnQNStPZyHrN7Q43K1F5PO5~aFUdvZfxz~2hs-8GCrXneH8fWmt-itqxC~RvYiR6e85tJ0Di~hfZgDmZWk2s6UwI4g__\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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":70524,"name":"Geosciences","url":"https://www.academia.edu/Documents/in/Geosciences"},{"id":281808,"name":"Olivine","url":"https://www.academia.edu/Documents/in/Olivine"},{"id":330036,"name":"Ophiolite","url":"https://www.academia.edu/Documents/in/Ophiolite"},{"id":895633,"name":"Chromite","url":"https://www.academia.edu/Documents/in/Chromite"},{"id":4348154,"name":"Massif","url":"https://www.academia.edu/Documents/in/Massif"}],"urls":[{"id":45061666,"url":"http://www.jgeosci.org/content/jgeosci_386_Mikrut.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565926-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565924"><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/124565924/Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift"><img alt="Research paper thumbnail of Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift" 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">Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift</div><div class="wp-workCard_item"><span>Gondwana research</span><span>, Jul 1, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and ph...</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 use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX</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="124565924"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565924"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565924; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565924]").text(description); $(".js-view-count[data-work-id=124565924]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565924; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565924']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565924]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565924,"title":"Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift","translated_title":"","metadata":{"abstract":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","publication_date":{"day":1,"month":7,"year":2024,"errors":{}},"publication_name":"Gondwana research"},"translated_abstract":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","internal_url":"https://www.academia.edu/124565924/Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift","translated_internal_url":"","created_at":"2024-10-09T02:24:23.679-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"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":2733,"name":"Petrophysics","url":"https://www.academia.edu/Documents/in/Petrophysics"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism"},{"id":78133,"name":"Gondwana","url":"https://www.academia.edu/Documents/in/Gondwana"},{"id":205582,"name":"Xenolith","url":"https://www.academia.edu/Documents/in/Xenolith"},{"id":281808,"name":"Olivine","url":"https://www.academia.edu/Documents/in/Olivine"},{"id":668253,"name":"Lithosphere","url":"https://www.academia.edu/Documents/in/Lithosphere"},{"id":2566417,"name":"Phlogopite","url":"https://www.academia.edu/Documents/in/Phlogopite"},{"id":3057331,"name":"Transition Zone","url":"https://www.academia.edu/Documents/in/Transition_Zone"}],"urls":[{"id":45061665,"url":"https://doi.org/10.1016/j.gr.2024.03.008"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565924-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565923"><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/124565923/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central"><img alt="Research paper thumbnail of Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central" class="work-thumbnail" src="https://attachments.academia-assets.com/118766917/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/124565923/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central">Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central</a></div><div class="wp-workCard_item"><span>Bulletin de la Société géologique de France</span><span>, Feb 15, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This paper presents and discusses new geochronological and petrological data on a suite of calc-a...</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">This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365À354 Ma (including uncertainties) for igneous crystallization. These calcalkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19À30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectono-metamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="01a873698302d9400d25d238901d1eb2" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766917,"asset_id":124565923,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766917/download_file?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="124565923"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565923"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565923; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565923]").text(description); $(".js-view-count[data-work-id=124565923]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565923; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565923']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "01a873698302d9400d25d238901d1eb2" } } $('.js-work-strip[data-work-id=124565923]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565923,"title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central","translated_title":"","metadata":{"grobid_abstract":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365À354 Ma (including uncertainties) for igneous crystallization. These calcalkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19À30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectono-metamorphic units of the Western French Massif Central were piled up after 354 Ma. 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In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19À30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectono-metamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766917,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766917/thumbnails/1.jpg","file_name":"bsgf230029.pdf","download_url":"https://www.academia.edu/attachments/118766917/download_file","bulk_download_file_name":"Short_lived_active_margin_magmatism_prec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766917/bsgf230029-libre.pdf?1728467486=\u0026response-content-disposition=attachment%3B+filename%3DShort_lived_active_margin_magmatism_prec.pdf\u0026Expires=1743209699\u0026Signature=fsoCUglqfkyab3XL3ivMogdcjEm5ZuCHIuRjJ6QGO~z-LuxPuIbLMJpKJjYJl6nCxauOWr0ez47qJref7~WDjq~AX54W~7y5y7H0LsZvZQv4YkDfLQ7x3HtstAU57GEiwtmBgUCPItO-jSrUU5SPAVbdZs~gBTs6i~0QTkv1tijOTr4uf2x7Vb~hmGMmIB8QML6e-bxDjuBDkgvtfRyjIhSClPiKsko2mut6iF06bdFarE4SLW5JEaxASZTSeEWTXrGTe8-cJVWMe0EdIStq2KOfi0i4EFzxvSRnN0Et5QsMsZknu9wK2ur3o5k36KnYSdJcVcs3NV2v~HHJ8sXIKQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118766918,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766918/thumbnails/1.jpg","file_name":"bsgf230029.pdf","download_url":"https://www.academia.edu/attachments/118766918/download_file","bulk_download_file_name":"Short_lived_active_margin_magmatism_prec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766918/bsgf230029-libre.pdf?1728467487=\u0026response-content-disposition=attachment%3B+filename%3DShort_lived_active_margin_magmatism_prec.pdf\u0026Expires=1743209699\u0026Signature=NwRO43lbHyozGLiWlm3l~UhATK5nKIYg5caxa2TuHA1wC6iWXzZD2wR08HRrKWq6zT~lGN5HcrP4qjfhjtFmR-bG2CPhkjtq~Tbd22RN8knZFlVcjeGPdrLFGODLVyzFZvjmogyp8z56k8yYQR8XHghJnlOIFLCAXEPFqR~PTaU61FdnrJB20cfZq7BhI9MqtRUh7gFnB6YQmnBLdk6LVYZiMuJtZuRp6DvZmz~vJwTqq0G5WwRz2j6Tbre6B-vo6HVvJM5vu3tXq6jk9pogpNw6zIvN~~LL7qo3LB7VtrZ~pm3GR1EcSdRF6RDXSkCb9jLcyXvgl823p9zEZcz1WQ__\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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology"},{"id":319872,"name":"Continental-arc","url":"https://www.academia.edu/Documents/in/Continental-arc"},{"id":422167,"name":"Massif Central","url":"https://www.academia.edu/Documents/in/Massif_Central"},{"id":755655,"name":"Variscan Orogeny","url":"https://www.academia.edu/Documents/in/Variscan_Orogeny"},{"id":4348154,"name":"Massif","url":"https://www.academia.edu/Documents/in/Massif"}],"urls":[{"id":45061664,"url":"https://www.bsgf.fr/articles/bsgf/pdf/forth/bsgf230029.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565923-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565922"><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/124565922/New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_E%C4%9Firdir_area_West_Anatolia_Turkey"><img alt="Research paper thumbnail of New insights into the ultrapotassic magmatism through xenoliths from the Eğirdir area, West Anatolia, Turkey" class="work-thumbnail" src="https://attachments.academia-assets.com/118766915/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/124565922/New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_E%C4%9Firdir_area_West_Anatolia_Turkey">New insights into the ultrapotassic magmatism through xenoliths from the Eğirdir area, West Anatolia, Turkey</a></div><div class="wp-workCard_item"><span>Arabian Journal of Geosciences</span><span>, Dec 7, 2023</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit ...</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">Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit in the Eğirdir lake area, belonging to the Potassic-Ultrapotassic Afyon volcanic Province, West Anatolia. They consist of kamafugite-type, feldsparbearing syenite, pyroxenite, leucitolite, some small-sized melilitolite and garnet-rich xenoliths, and a carbonatite. A new occurrence of kalsilite is described as either homogeneous acicular crystals or tabular two phases-exsolved crystals in the kamafugite-type and melilitolite xenoliths. Rock textures and compositions indicate cumulates and near-liquid composition rocks corresponding to relatively evolved magmas. All the rocks are strongly silica-undersaturated, Ca-, Mg-, and K-rich, and Al-poor. The fractional crystallization model includes clinopyroxene, apatite, phlogopite, melilite and leucite. Fe-Ti oxides and garnet may be also concerned. The P H2O during crystallization and differentiation is not more than 0.8 GPa. Major elements, trace elements, and REE patterns for xenoliths, which indicate near-liquid compositions, are typical of ultrapotassic series in a post-collisional geodynamic context, as it is the case for the Roman and Central ultrapotassic Italian provinces. The stable isotope 13 C and 18 O values of the calcio-carbonatite plot close to the primary carbonatite field, whereas the carbonates of the feldspar-bearing syenite and the peperite matrix suggest a low-T extensive contamination process. The origin of the carbonatite from kamafugite-type magmas by immiscibility or by fractional crystallization remains questionable; an origin by fractionation-melting of a metasomatized mantle source should be tested in the future.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="63b518dc0bb0dc3a8a7a25ffbbd18062" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766915,"asset_id":124565922,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766915/download_file?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="124565922"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565922"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565922; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565922]").text(description); $(".js-view-count[data-work-id=124565922]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565922; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565922']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "63b518dc0bb0dc3a8a7a25ffbbd18062" } } $('.js-work-strip[data-work-id=124565922]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565922,"title":"New insights into the ultrapotassic magmatism through xenoliths from the Eğirdir area, West Anatolia, Turkey","translated_title":"","metadata":{"publisher":"Springer Science+Business Media","grobid_abstract":"Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit in the Eğirdir lake area, belonging to the Potassic-Ultrapotassic Afyon volcanic Province, West Anatolia. They consist of kamafugite-type, feldsparbearing syenite, pyroxenite, leucitolite, some small-sized melilitolite and garnet-rich xenoliths, and a carbonatite. A new occurrence of kalsilite is described as either homogeneous acicular crystals or tabular two phases-exsolved crystals in the kamafugite-type and melilitolite xenoliths. Rock textures and compositions indicate cumulates and near-liquid composition rocks corresponding to relatively evolved magmas. All the rocks are strongly silica-undersaturated, Ca-, Mg-, and K-rich, and Al-poor. The fractional crystallization model includes clinopyroxene, apatite, phlogopite, melilite and leucite. Fe-Ti oxides and garnet may be also concerned. The P H2O during crystallization and differentiation is not more than 0.8 GPa. Major elements, trace elements, and REE patterns for xenoliths, which indicate near-liquid compositions, are typical of ultrapotassic series in a post-collisional geodynamic context, as it is the case for the Roman and Central ultrapotassic Italian provinces. The stable isotope 13 C and 18 O values of the calcio-carbonatite plot close to the primary carbonatite field, whereas the carbonates of the feldspar-bearing syenite and the peperite matrix suggest a low-T extensive contamination process. The origin of the carbonatite from kamafugite-type magmas by immiscibility or by fractional crystallization remains questionable; an origin by fractionation-melting of a metasomatized mantle source should be tested in the future.","publication_date":{"day":7,"month":12,"year":2023,"errors":{}},"publication_name":"Arabian Journal of Geosciences","grobid_abstract_attachment_id":118766915},"translated_abstract":null,"internal_url":"https://www.academia.edu/124565922/New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_E%C4%9Firdir_area_West_Anatolia_Turkey","translated_internal_url":"","created_at":"2024-10-09T02:24:23.036-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118766915,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766915/thumbnails/1.jpg","file_name":"document.pdf","download_url":"https://www.academia.edu/attachments/118766915/download_file","bulk_download_file_name":"New_insights_into_the_ultrapotassic_magm.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766915/document-libre.pdf?1728467458=\u0026response-content-disposition=attachment%3B+filename%3DNew_insights_into_the_ultrapotassic_magm.pdf\u0026Expires=1743209699\u0026Signature=UOzwPplcKY4zR-9WTIkFGX4hgFcmM~STnJWFKe7Xr2TPDRC6hngRFWG9AnUbc-cwWPv3GRBKtJN4ROVUBF3TfFGYWgzZ~bxUSQHqjV8lTQqPTuMHZ7eZfi-GlNITQ8JB9BXKgu1okCVvSrJijswcLv8DWMFp7X2Yl~waQHBvIC6XfWjRBggvoHOWsaOf01Ckd-huumXQ68EaLwGOJ1M7pbqESIzPe32wm3RtzCLZXjCMn0vNq4cqqC2X2vt1VUesQDYqAKzvdaidiu2UhNBP1b1Vzws1bVcwqC8RgAht3x2DV2cXJuSGqb1mYVJUMG4cCprRVPHpmCnt1~WBrd0ZDQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_Eğirdir_area_West_Anatolia_Turkey","translated_slug":"","page_count":27,"language":"en","content_type":"Work","summary":"Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit in the Eğirdir lake area, belonging to the Potassic-Ultrapotassic Afyon volcanic Province, West Anatolia. They consist of kamafugite-type, feldsparbearing syenite, pyroxenite, leucitolite, some small-sized melilitolite and garnet-rich xenoliths, and a carbonatite. A new occurrence of kalsilite is described as either homogeneous acicular crystals or tabular two phases-exsolved crystals in the kamafugite-type and melilitolite xenoliths. Rock textures and compositions indicate cumulates and near-liquid composition rocks corresponding to relatively evolved magmas. All the rocks are strongly silica-undersaturated, Ca-, Mg-, and K-rich, and Al-poor. The fractional crystallization model includes clinopyroxene, apatite, phlogopite, melilite and leucite. Fe-Ti oxides and garnet may be also concerned. The P H2O during crystallization and differentiation is not more than 0.8 GPa. Major elements, trace elements, and REE patterns for xenoliths, which indicate near-liquid compositions, are typical of ultrapotassic series in a post-collisional geodynamic context, as it is the case for the Roman and Central ultrapotassic Italian provinces. The stable isotope 13 C and 18 O values of the calcio-carbonatite plot close to the primary carbonatite field, whereas the carbonates of the feldspar-bearing syenite and the peperite matrix suggest a low-T extensive contamination process. The origin of the carbonatite from kamafugite-type magmas by immiscibility or by fractional crystallization remains questionable; an origin by fractionation-melting of a metasomatized mantle source should be tested in the future.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766915,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766915/thumbnails/1.jpg","file_name":"document.pdf","download_url":"https://www.academia.edu/attachments/118766915/download_file","bulk_download_file_name":"New_insights_into_the_ultrapotassic_magm.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766915/document-libre.pdf?1728467458=\u0026response-content-disposition=attachment%3B+filename%3DNew_insights_into_the_ultrapotassic_magm.pdf\u0026Expires=1743209699\u0026Signature=UOzwPplcKY4zR-9WTIkFGX4hgFcmM~STnJWFKe7Xr2TPDRC6hngRFWG9AnUbc-cwWPv3GRBKtJN4ROVUBF3TfFGYWgzZ~bxUSQHqjV8lTQqPTuMHZ7eZfi-GlNITQ8JB9BXKgu1okCVvSrJijswcLv8DWMFp7X2Yl~waQHBvIC6XfWjRBggvoHOWsaOf01Ckd-huumXQ68EaLwGOJ1M7pbqESIzPe32wm3RtzCLZXjCMn0vNq4cqqC2X2vt1VUesQDYqAKzvdaidiu2UhNBP1b1Vzws1bVcwqC8RgAht3x2DV2cXJuSGqb1mYVJUMG4cCprRVPHpmCnt1~WBrd0ZDQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118766916,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766916/thumbnails/1.jpg","file_name":"document.pdf","download_url":"https://www.academia.edu/attachments/118766916/download_file","bulk_download_file_name":"New_insights_into_the_ultrapotassic_magm.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766916/document-libre.pdf?1728467459=\u0026response-content-disposition=attachment%3B+filename%3DNew_insights_into_the_ultrapotassic_magm.pdf\u0026Expires=1743209699\u0026Signature=OHs3BabI~R9nZj3VrsyiD3dR2iVlcCLAMBe9uB9W5Blvvkpt6~G2kGEhdXXkG2z2gPT5V0f5gkmcN5xXGY3HydBo1hmZEG~66W2zooFsIjy1pVlxAk5Utsb8~kaURdd1VupaqeeljAI3yVdeFnoyYtuck9kCFANOb~3jQ5wUXsZZSkW83Fs3snQe~dK4MBPSg9Cg~UZR-5Yudq6fEzqDUflNrHyy4cZwl2RGpRxwPGLtBVi6qFOw6iw5lqYqGUOkRH4QPWuYOhe0gqZSdYkK3NKRVtzImUNUFCj2jouxYdLXlFlhFzRM7vHNE0~U0WYcrHmugakFRJkEq7mBtNpQ1w__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry"},{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism"},{"id":66471,"name":"Mafic Alkaline Igneous Rocks","url":"https://www.academia.edu/Documents/in/Mafic_Alkaline_Igneous_Rocks"},{"id":108863,"name":"Volcano","url":"https://www.academia.edu/Documents/in/Volcano"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"},{"id":197588,"name":"Kimberlite","url":"https://www.academia.edu/Documents/in/Kimberlite"},{"id":205576,"name":"Basalt","url":"https://www.academia.edu/Documents/in/Basalt"},{"id":205582,"name":"Xenolith","url":"https://www.academia.edu/Documents/in/Xenolith"},{"id":403641,"name":"Spinel","url":"https://www.academia.edu/Documents/in/Spinel"},{"id":568585,"name":"Trachyte","url":"https://www.academia.edu/Documents/in/Trachyte"},{"id":688910,"name":"Volcanic Rock","url":"https://www.academia.edu/Documents/in/Volcanic_Rock"},{"id":1168540,"name":"Eology","url":"https://www.academia.edu/Documents/in/Eology"},{"id":1186734,"name":"Allanite","url":"https://www.academia.edu/Documents/in/Allanite"},{"id":1464622,"name":"Carbonatite","url":"https://www.academia.edu/Documents/in/Carbonatite"},{"id":1590367,"name":"Monazite","url":"https://www.academia.edu/Documents/in/Monazite"},{"id":2566417,"name":"Phlogopite","url":"https://www.academia.edu/Documents/in/Phlogopite"}],"urls":[{"id":45061663,"url":"https://hal.science/hal-04337266/document"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565922-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565921"><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/124565921/Use_of_porphyry_indicator_zircons_PIZs_in_the_sedimentary_record_as_an_exploration_tool_for_covered_porphyry_copper_deposits_in_the_Atacama_Desert_Chile"><img alt="Research paper thumbnail of Use of porphyry indicator zircons (PIZs) in the sedimentary record as an exploration tool for covered porphyry copper deposits in the Atacama Desert, Chile" 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">Use of porphyry indicator zircons (PIZs) in the sedimentary record as an exploration tool for covered porphyry copper deposits in the Atacama Desert, Chile</div><div class="wp-workCard_item"><span>Journal of Geochemical Exploration</span><span>, Dec 31, 2023</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This work explores the potential of geochemical and petrographic characteristics of detrital zirc...</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">This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf &amp;gt;8,750 (ppm), Ce/Nd &amp;gt;1, Eu/Eu* &amp;gt;0.4, 10,000×(Eu/Eu*)/Y &amp;gt;1, (Ce/Nd)/Y &amp;gt;0.01, Dy/Yb &amp;lt;0.3 and 0.1 &amp;lt; Th/U &amp;lt; 1. These zircons also have Ti &amp;lt;9 ppm and Ce/Ce* &amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.</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="124565921"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565921"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565921; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565921]").text(description); $(".js-view-count[data-work-id=124565921]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565921; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565921']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565921]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565921,"title":"Use of porphyry indicator zircons (PIZs) in the sedimentary record as an exploration tool for covered porphyry copper deposits in the Atacama Desert, Chile","translated_title":"","metadata":{"abstract":"This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf \u0026amp;gt;8,750 (ppm), Ce/Nd \u0026amp;gt;1, Eu/Eu* \u0026amp;gt;0.4, 10,000×(Eu/Eu*)/Y \u0026amp;gt;1, (Ce/Nd)/Y \u0026amp;gt;0.01, Dy/Yb \u0026amp;lt;0.3 and 0.1 \u0026amp;lt; Th/U \u0026amp;lt; 1. These zircons also have Ti \u0026amp;lt;9 ppm and Ce/Ce* \u0026amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.","publisher":"Elsevier BV","publication_date":{"day":31,"month":12,"year":2023,"errors":{}},"publication_name":"Journal of Geochemical Exploration"},"translated_abstract":"This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf \u0026amp;gt;8,750 (ppm), Ce/Nd \u0026amp;gt;1, Eu/Eu* \u0026amp;gt;0.4, 10,000×(Eu/Eu*)/Y \u0026amp;gt;1, (Ce/Nd)/Y \u0026amp;gt;0.01, Dy/Yb \u0026amp;lt;0.3 and 0.1 \u0026amp;lt; Th/U \u0026amp;lt; 1. These zircons also have Ti \u0026amp;lt;9 ppm and Ce/Ce* \u0026amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.","internal_url":"https://www.academia.edu/124565921/Use_of_porphyry_indicator_zircons_PIZs_in_the_sedimentary_record_as_an_exploration_tool_for_covered_porphyry_copper_deposits_in_the_Atacama_Desert_Chile","translated_internal_url":"","created_at":"2024-10-09T02:24:22.770-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Use_of_porphyry_indicator_zircons_PIZs_in_the_sedimentary_record_as_an_exploration_tool_for_covered_porphyry_copper_deposits_in_the_Atacama_Desert_Chile","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf \u0026amp;gt;8,750 (ppm), Ce/Nd \u0026amp;gt;1, Eu/Eu* \u0026amp;gt;0.4, 10,000×(Eu/Eu*)/Y \u0026amp;gt;1, (Ce/Nd)/Y \u0026amp;gt;0.01, Dy/Yb \u0026amp;lt;0.3 and 0.1 \u0026amp;lt; Th/U \u0026amp;lt; 1. These zircons also have Ti \u0026amp;lt;9 ppm and Ce/Ce* \u0026amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[],"research_interests":[{"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":417,"name":"Paleontology","url":"https://www.academia.edu/Documents/in/Paleontology"},{"id":70416,"name":"Mineral exploration","url":"https://www.academia.edu/Documents/in/Mineral_exploration"},{"id":74607,"name":"Quartz","url":"https://www.academia.edu/Documents/in/Quartz"},{"id":82911,"name":"fluid Inclusions","url":"https://www.academia.edu/Documents/in/fluid_Inclusions"},{"id":103767,"name":"Petrography","url":"https://www.academia.edu/Documents/in/Petrography"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":282633,"name":"Geochemical exploration","url":"https://www.academia.edu/Documents/in/Geochemical_exploration"},{"id":1146625,"name":"Porphyry Copper Deposit","url":"https://www.academia.edu/Documents/in/Porphyry_Copper_Deposit"},{"id":1168540,"name":"Eology","url":"https://www.academia.edu/Documents/in/Eology"}],"urls":[{"id":45061662,"url":"https://doi.org/10.1016/j.gexplo.2023.107351"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565921-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="121796661"><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/121796661/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas"><img alt="Research paper thumbnail of Slab melting boosts the mantle wedge contribution to Li-rich magmas" class="work-thumbnail" src="https://attachments.academia-assets.com/116593888/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/121796661/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas">Slab melting boosts the mantle wedge contribution to Li-rich magmas</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/ErwinSchettino">Erwin Schettino</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Scientific Reports</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generat...</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 lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ > + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an "adakite"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (< 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="04a765de19929f52c678e8e65cbe678a" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":116593888,"asset_id":121796661,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/116593888/download_file?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="121796661"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="121796661"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 121796661; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=121796661]").text(description); $(".js-view-count[data-work-id=121796661]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 121796661; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='121796661']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "04a765de19929f52c678e8e65cbe678a" } } $('.js-work-strip[data-work-id=121796661]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":121796661,"title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas","translated_title":"","metadata":{"doi":"10.1038/s41598-024-66174-y","abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u003e + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \"adakite\"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u003c 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","publication_name":"Scientific Reports"},"translated_abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u003e + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \"adakite\"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u003c 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","internal_url":"https://www.academia.edu/121796661/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_internal_url":"","created_at":"2024-07-05T04:57:50.421-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42007492,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":319160819,"co_author_invite_id":8190613,"email":"e***8@gmail.com","display_order":-3,"name":"Erwin Schettino","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007493,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":50570743,"co_author_invite_id":null,"email":"c***o@iact.ugr-csic.es","display_order":-2,"name":"Claudio Marchesi","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007494,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":9883919,"co_author_invite_id":null,"email":"j***z@mq.edu.au","display_order":-1,"name":"Jose Gonzalez-Jimenez","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007495,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":28395431,"co_author_invite_id":null,"email":"r***c@gmail.com","affiliation":"CSIC (Consejo Superior de Investigaciones Científicas-Spanish National Research Council)","display_order":1,"name":"Romain Tilhac","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007496,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":112580305,"co_author_invite_id":null,"email":"a***e@gmail.com","display_order":2,"name":"Alexandre Corgne","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007497,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":27868342,"co_author_invite_id":null,"email":"m***d@gmail.com","affiliation":"Universidad Austral de Chile","display_order":3,"name":"Manuel Schilling","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"}],"downloadable_attachments":[{"id":116593888,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116593888/thumbnails/1.jpg","file_name":"SciRep_2024.pdf","download_url":"https://www.academia.edu/attachments/116593888/download_file","bulk_download_file_name":"Slab_melting_boosts_the_mantle_wedge_con.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116593888/SciRep_2024-libre.pdf?1720184002=\u0026response-content-disposition=attachment%3B+filename%3DSlab_melting_boosts_the_mantle_wedge_con.pdf\u0026Expires=1743209699\u0026Signature=euxvAd-8Q5zwJZkibKrl0BEaI6ACg-yufmbfOvAhs0UKuFMdIa3mpNA7R5FKJygYfIg5O34po6Gilvtpgb1gia2LGJJIrANO2dj1qTz3w19rFmWinO1ukiUrIxQlgsvA0RYcN~KOhsxB0w~l8~oKYR25YyWh4CElu0QowxbsAoKnIHHziSzekfKquXVHnw4Xn0ho7O~Kw0fDEL2zZG5qsoe1DISTnjboZeiTHOILzm492k1AUj4RWaUNFRhdRgkpu2fttRfjZkK8Hap31uG6iDHOReAYGSPEprRsDofAFIW5p9f3ViFaRE-uUsvhptVyJZrW8Fvx9wTstSUijLjKJQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_slug":"","page_count":14,"language":"en","content_type":"Work","summary":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. 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However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \"adakite\"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u003c 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":116593888,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116593888/thumbnails/1.jpg","file_name":"SciRep_2024.pdf","download_url":"https://www.academia.edu/attachments/116593888/download_file","bulk_download_file_name":"Slab_melting_boosts_the_mantle_wedge_con.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116593888/SciRep_2024-libre.pdf?1720184002=\u0026response-content-disposition=attachment%3B+filename%3DSlab_melting_boosts_the_mantle_wedge_con.pdf\u0026Expires=1743209699\u0026Signature=euxvAd-8Q5zwJZkibKrl0BEaI6ACg-yufmbfOvAhs0UKuFMdIa3mpNA7R5FKJygYfIg5O34po6Gilvtpgb1gia2LGJJIrANO2dj1qTz3w19rFmWinO1ukiUrIxQlgsvA0RYcN~KOhsxB0w~l8~oKYR25YyWh4CElu0QowxbsAoKnIHHziSzekfKquXVHnw4Xn0ho7O~Kw0fDEL2zZG5qsoe1DISTnjboZeiTHOILzm492k1AUj4RWaUNFRhdRgkpu2fttRfjZkK8Hap31uG6iDHOReAYGSPEprRsDofAFIW5p9f3ViFaRE-uUsvhptVyJZrW8Fvx9wTstSUijLjKJQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":123325,"name":"Mantle Geochemistry","url":"https://www.academia.edu/Documents/in/Mantle_Geochemistry"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-121796661-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="121533209"><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/121533209/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite"><img alt="Research paper thumbnail of A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite" class="work-thumbnail" src="https://attachments.academia-assets.com/116422208/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/121533209/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite">A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite</a></div><div class="wp-workCard_item"><span>Chemical Geology</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpen...</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">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.</span></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-121533209-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-121533209-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361218/figure-3-calculated-mineral-composition-depending-on-fluid"><img alt="Figure 3 Calculated mineral composition depending on fluid amount from the reaction of gabbro with the Seyfried’s solution (model E) at 300°C. Ab: albite, Adr: andradite, Ann: annite, Clc: clinochlore, Di: diopside, Hd: hedenbergite, Mtc: monticellite, Phl: Na-phlogopite, Prh: prehnite, Ves: vesuvianite, Wo: wollastonite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361210/figure-2-modal-composition-predicted-from-alteration-of"><img alt="Figure 2 Modal composition predicted from alteration of gabbro (1 kg) at 300°C depending on fluid amount and fluid composition: a) low fluid amount (10 kg) b) high fluid amount (1000 kg). Capital letters denote different fluid compositions as presented in Table 1. Modal proportions of minerals were calculated from molal amounts based on average density for each mineral published at www.webmineral.com (densities are available in Table SX). Ab: albite, Adr: andradite, Anh: anhydrite, Clc: clinochlore, Cld: chloritoid, Czo: clinozoisite, Di: diopside, Dph: daphnite, Ep: epidote, Hd: hedenbergite, Hem: hematite, MHSH: magnesium-hydroxide-sulphate-hydrate, Mtc: monticellite, Prh: prehnite, Qz: quartz, Stp: stilpnomelane, Tlc: talc, Tr: tremolite, Ves: vesuvianite, Wo: wollastonite, Wrk: wairakite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361197/figure-1-geochemical-model-for-the-transformation-of-gabbro"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361227/figure-4-element-amounts-in-the-modeled-solid-phase"><img alt="Figure 4 Element amounts in the modeled solid phase depending on fluid amount from the reaction of 1 kg of gabbro with the Seyfried’s solution (model E) at 300°C. Values were manually quantified from mineral amounts (and their respective compositions) calculated in the model. Note the progressive and significant Ca-enrichment with increasing fluid amount in the system. Ca-enrichment is also responsible for the increase of total mass of the solid phase. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361240/figure-5-graphical-representation-of-the-recalculated-whole"><img alt="Figure 5 Graphical representation of the recalculated whole rock composition (Table 2) of the altered rock resulting from the interaction of 1 kg of gabbro with variable amount of the Seyfried’s solution (model E) at 300°C. Note the decreasing SiOz and increasing CaO demonstrating the most typical changes in whole-rock chemistry during the rodingitization. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361253/figure-6-influence-of-changes-in-fluid-composition-on-the"><img alt="Figure 6 Influence of changes in fluid composition on the predicted mineralogy explored by one-factor-at-a-time method applied on experimental serpentinization fluid from Klein et al. (2015) (model D), 300°C, fluid amount 1000 kg. a) variable Ca concentration. b) variable Mg concentration. c) variable Si concentration. d) variable initial pH. Ab: albite, Adr: andradite, Ame: amesite, Br: brucite, Clc: clinochlore, Czo: clinozoisite, Di: diopside, Dph: daphnite, Ep: epidote, Hd: hedenbergite, Mtc: monticellite, Prh: prehnite, Qz: quartz, Rnk: rankinite, Ves: vesuvianite, Wo: wollastonite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_006.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361260/figure-7-influence-of-changes-in-fluid-composition-on-the"><img alt="Figure 7 Influence of changes in fluid composition on the predicted mineralogy explored by one-factor-at-a-time method applied on experimental serpentinization fluid from Seyfried et al. (2007) (model E), 300°C, fluid amount 1000 kg. a) variable Ca concentration. b) variable Mg concentration. d) variable initial pH. Ab: albite, Adr. andradite, Atg: antigorite, Br: brucite, Clc: clinochlore, Di: diopside, Hd: hedenbergite, Lrn: larnite, Mtc: monticellite, Phl: Na-phlogopite, Rnk: rankinite, Tro: troilite, Ves: vesuvianite, Wo: wollastonite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_007.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361268/figure-8-diagram-of-si-ca-molal-ratio-in-the-solid-phase-vs"><img alt="Figure 8 Diagram of Si/Ca (molal ratio) in the solid phase vs fluid amount in the system. It compares the calculated chemical composition (brown line, model E, section 3.2) with natural samples. Blue area represents gabbro compositions (n = 201) from a present seafloor, oxide-rich samples excluded (MacLeod et al., 2017). Green area represents vesuvianite-bearing rodingite compositions (n = 49) from the literature (Li et al., 2004, 2007, 2017; Kobayashi and Kaneda, 2010; Koutsovitis et al., 2013; Fukuyama et al., 2014; Dai et al., 2016; Salvioli-Mariani et Our calculations consistently show that increasing fluid amount results in an increasing quantity of vesuvianite (Figs. 2 and 3). This finding is also in good agreement with the thermodynamic model presented by Palandri and Reed (2004), where the interaction of a pyroxene-rich gabbro with a serpentinization fluid predicts vesuvianite only at a water-rock ratio above 200. Such high water-rock ratio can be hard to imagine considering the constraints from O isotopes studies suggesting a relatively low fluid-rock ratio (< 10) during serpentinization (Rouméjon et al., 2015; Zhao et al., 2023). However, these studies often focus on only partially serpentinized ultramafic rocks very probably forming at the beginning of the alteration (at lower fluid-rock ratio). Rodingites occur almost exclusively in completely serpentinized rocks (Katoh and Niida, 1983), which suggests a higher fluid amount participating in the process (Rouméjon et al., 2015, 2018). A high fluid amount can be achieved in nature either by a small to moderate fluid influx continuing for a long time, or by a very high fluid volume in contact with the rock during a short time. We assume the former option more plausible since it allows to advance the mineral reactions to the chemical equilibrium more easily. In any case, we conclude that vesuvianite formation requires an open system with a significant input of a fresh hydrothermal fluid. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_008.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361274/table-1-adjusted-to-charge-balance-the-solution-fluid"><img alt="* adjusted to charge balance the solution Table 1 Fluid compositions investigated in the models. A) pure water. B) average seawater (Nordstrom et al., 1979). C) evolved seawater composition measured ina vent at Logatchev (Charlou et al, 2002). D) experimental serpentinization fluid (Klein et al., 2015). E) experimental serpentinization fluid (Seyfried et al.,2007). Element concentrations are in mmol/kg. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/table_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361280/table-2-recalculated-whole-rock-composition-in-wt-normalized"><img alt="Table 2 Recalculated whole rock composition (in wt.%, normalized on 100 %) of the altered rock resulting fron the interaction of 1 kg of gabbro with variable amount of the Seyfried’s solution (model E) at 300°C. Values wer manually quantified from mineral amounts (and their respective compositions) calculated in the model. Thes values are shown in a graphical form in figure 5. 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This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Chemical Geology"},"translated_abstract":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","internal_url":"https://www.academia.edu/121533209/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_internal_url":"","created_at":"2024-06-26T07:51:35.032-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":41965331,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":291703187,"co_author_invite_id":null,"email":"j***k@umb.sk","display_order":-3,"name":"Juraj Butek","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"},{"id":41965332,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":97759662,"co_author_invite_id":null,"email":"f***n@wanadoo.fr","affiliation":"Université Toulouse II Jean Jaurès","display_order":-2,"name":"Sébastien Fabre","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"},{"id":41965333,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":7611257,"email":"s***e@get.omp.eu","display_order":-1,"name":"Stephanie Duchene","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"},{"id":41965334,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":7945934,"email":"j***k@umb.sk","display_order":1,"name":"Jan Spisiak","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"}],"downloadable_attachments":[{"id":116422208,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116422208/thumbnails/1.jpg","file_name":"Chem_Geol_2024.pdf","download_url":"https://www.academia.edu/attachments/116422208/download_file","bulk_download_file_name":"A_geochemical_model_for_the_transformati.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116422208/Chem_Geol_2024-libre.pdf?1719566012=\u0026response-content-disposition=attachment%3B+filename%3DA_geochemical_model_for_the_transformati.pdf\u0026Expires=1743209699\u0026Signature=gaCoLaPulMCea0zGc8ST13gKF0-z543EWMI1GX9S8Sc4800JDwdYm43rak88~3YB-M2hhAe0N7WLX~E8HOtj~azd3Q31v847X0LmIy4zB86i9LSqwa6xQ94~5rYFNtGCj4MLqCLDviX1iTTeAcYg4HpOeWl2Qz4Hjzf8a~3junQBehbT3C714M08-J9lAsfEWnFx3l5BDRTFBJr8kxPaROJZUelMOb4bT41srG4rt2BHMzqG5PPiQQHentisy~kJP2pbDcyn5yFAvSfsvv43ksjAA8bfIA0pNQdKfDgIaQAdr56Ccv1ELiagCHwBQEaGC5wIb0V-VLlznSAUrMDW3g__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_slug":"","page_count":25,"language":"en","content_type":"Work","summary":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":116422208,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116422208/thumbnails/1.jpg","file_name":"Chem_Geol_2024.pdf","download_url":"https://www.academia.edu/attachments/116422208/download_file","bulk_download_file_name":"A_geochemical_model_for_the_transformati.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116422208/Chem_Geol_2024-libre.pdf?1719566012=\u0026response-content-disposition=attachment%3B+filename%3DA_geochemical_model_for_the_transformati.pdf\u0026Expires=1743209699\u0026Signature=gaCoLaPulMCea0zGc8ST13gKF0-z543EWMI1GX9S8Sc4800JDwdYm43rak88~3YB-M2hhAe0N7WLX~E8HOtj~azd3Q31v847X0LmIy4zB86i9LSqwa6xQ94~5rYFNtGCj4MLqCLDviX1iTTeAcYg4HpOeWl2Qz4Hjzf8a~3junQBehbT3C714M08-J9lAsfEWnFx3l5BDRTFBJr8kxPaROJZUelMOb4bT41srG4rt2BHMzqG5PPiQQHentisy~kJP2pbDcyn5yFAvSfsvv43ksjAA8bfIA0pNQdKfDgIaQAdr56Ccv1ELiagCHwBQEaGC5wIb0V-VLlznSAUrMDW3g__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":75334,"name":"Fluid-rock interactions","url":"https://www.academia.edu/Documents/in/Fluid-rock_interactions"},{"id":910472,"name":"Rodingites","url":"https://www.academia.edu/Documents/in/Rodingites"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (true) { Aedu.setUpFigureCarousel('profile-work-121533209-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="119814581"><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/119814581/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania"><img alt="Research paper thumbnail of Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania" class="work-thumbnail" src="https://attachments.academia-assets.com/115151005/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/119814581/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania">Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania</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/MikrutJ">Jakub Mikrut</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Journal of Geosciences</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), ...</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 ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2fa394de18fb00c5e719e05379ea22d0" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":115151005,"asset_id":119814581,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/115151005/download_file?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="119814581"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="119814581"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 119814581; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=119814581]").text(description); $(".js-view-count[data-work-id=119814581]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 119814581; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='119814581']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "2fa394de18fb00c5e719e05379ea22d0" } } $('.js-work-strip[data-work-id=119814581]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":119814581,"title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania","translated_title":"","metadata":{"doi":"10.3190/jgeosci.386","abstract":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Journal of Geosciences"},"translated_abstract":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","internal_url":"https://www.academia.edu/119814581/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania","translated_internal_url":"","created_at":"2024-05-22T06:23:35.947-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":41731140,"work_id":119814581,"tagging_user_id":10246740,"tagged_user_id":315624277,"co_author_invite_id":8154103,"email":"j***t@uwr.edu.pl","display_order":-2,"name":"Jakub Mikrut","title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania"},{"id":41731141,"work_id":119814581,"tagging_user_id":10246740,"tagged_user_id":32572477,"co_author_invite_id":null,"email":"m***k@ing.uni.wroc.pl","display_order":-1,"name":"Magdalena Matusiak-małek","title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania"}],"downloadable_attachments":[{"id":115151005,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115151005/thumbnails/1.jpg","file_name":"JGeosciences_2024.pdf","download_url":"https://www.academia.edu/attachments/115151005/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115151005/JGeosciences_2024-libre.pdf?1716386647=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=f3gqN66AkzsIOzlGAj1Pl4OKKs3wMhFdFTbuEp3gQk91rQzBJW0Gxzjo7oTPFGVdtpzO-DuXBQ2Yrw7vdhcoh8JYgDEUAYLM3S7eLM2iiSIchCbO7c9G396-3cywn4xAkVOk1NHwpxpEx7nEx36ZHIrw7e6z7NCDBYOZuJ0fRfZYPNyvyn0h9ZyzDYnskR61gjkFd4dCqTrfqM4JurmvKYdOI1GEg2196wLvzHc6uUj4Ma0KujWCc1q6YMs-KgQhV6rT3T8uG~Sj~R~dCBpOLByHnReD9hJX4jzPLyYMNMqXoUt2Ii4mcqYtg3Vbfc7DFZMiKH3dIxCrbhhcPo3btw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania","translated_slug":"","page_count":16,"language":"en","content_type":"Work","summary":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":115151005,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115151005/thumbnails/1.jpg","file_name":"JGeosciences_2024.pdf","download_url":"https://www.academia.edu/attachments/115151005/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115151005/JGeosciences_2024-libre.pdf?1716386647=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=f3gqN66AkzsIOzlGAj1Pl4OKKs3wMhFdFTbuEp3gQk91rQzBJW0Gxzjo7oTPFGVdtpzO-DuXBQ2Yrw7vdhcoh8JYgDEUAYLM3S7eLM2iiSIchCbO7c9G396-3cywn4xAkVOk1NHwpxpEx7nEx36ZHIrw7e6z7NCDBYOZuJ0fRfZYPNyvyn0h9ZyzDYnskR61gjkFd4dCqTrfqM4JurmvKYdOI1GEg2196wLvzHc6uUj4Ma0KujWCc1q6YMs-KgQhV6rT3T8uG~Sj~R~dCBpOLByHnReD9hJX4jzPLyYMNMqXoUt2Ii4mcqYtg3Vbfc7DFZMiKH3dIxCrbhhcPo3btw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-119814581-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="117396662"><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/117396662/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central"><img alt="Research paper thumbnail of Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central" class="work-thumbnail" src="https://attachments.academia-assets.com/115237174/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/117396662/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central">Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central</a></div><div class="wp-workCard_item"><span>BSGF - Earth Science Bulletin</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This paper presents and discusses new geochronological and petrological data on a suite of calc-a...</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">This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365-354 Ma (including uncertainties) for igneous crystallization. These calc-alkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="82f26dbccf4286d29aab8d0cb9983378" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":115237174,"asset_id":117396662,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/115237174/download_file?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="117396662"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="117396662"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 117396662; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=117396662]").text(description); $(".js-view-count[data-work-id=117396662]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 117396662; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='117396662']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "82f26dbccf4286d29aab8d0cb9983378" } } $('.js-work-strip[data-work-id=117396662]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":117396662,"title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central","translated_title":"","metadata":{"doi":"10.1051/bsgf/2024003","abstract":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365-354 Ma (including uncertainties) for igneous crystallization. These calc-alkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.","ai_title_tag":"Active Margin Magmatism in Western Massif Central","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"BSGF - Earth Science Bulletin"},"translated_abstract":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365-354 Ma (including uncertainties) for igneous crystallization. These calc-alkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.","internal_url":"https://www.academia.edu/117396662/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central","translated_internal_url":"","created_at":"2024-04-12T06:28:48.785-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":41476148,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117174,"email":"j***r@get.omp.eu","display_order":-4,"name":"Julien Berger","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476149,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117175,"email":"b***4@yahoo.fr","display_order":-3,"name":"Lea Beau","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476150,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117176,"email":"j***4@gmail.com","display_order":-2,"name":"Julien Serrano","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476151,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":6104564,"email":"m***t@get.omp.eu","display_order":-1,"name":"Mathieu Benoit","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476152,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117177,"email":"b***a@gmail.com","display_order":1,"name":"Anissa Benmammar","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476153,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":7611257,"email":"s***e@get.omp.eu","display_order":2,"name":"Stephanie Duchene","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476154,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":26472103,"co_author_invite_id":null,"email":"o***r@gm.univ-montp2.fr","affiliation":"Université de Montpellier","display_order":3,"name":"Olivier Bruguier","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476155,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":32694530,"co_author_invite_id":null,"email":"j***e@umons.ac.be","affiliation":"Université de Mons","display_order":4,"name":"Jean-marc Baele","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"}],"downloadable_attachments":[{"id":115237174,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115237174/thumbnails/1.jpg","file_name":"BSGF_2024.pdf","download_url":"https://www.academia.edu/attachments/115237174/download_file","bulk_download_file_name":"Short_lived_active_margin_magmatism_prec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115237174/BSGF_2024-libre.pdf?1716563779=\u0026response-content-disposition=attachment%3B+filename%3DShort_lived_active_margin_magmatism_prec.pdf\u0026Expires=1743209699\u0026Signature=NP6kmHOPMAxi6onE72OZY~6OsgoSmP5b8McnhCf5QBvJyMTb55nykB6xddixmuyJBEVhW7KWJO8jDtvBiHfKWodSkEERnOqu8pN6gQVPUu1zJjjPS4nysQp9rxmn8JKrF1KG1aweHcJotNBccG-p54y7ZKoE3HG~KyNBc12B6W6HuvjKdoeYKpl5IEuLvad2X389kJLkP~DZF1NnVumFAaZEw97gyhtCBVAjlcEscjEidCwpCQlI5OZV3d899nkYcxMtsLk9cr05trEJSe1tw4YrgWwQty83rTu1iKFIfR5fyTcL8OSM4DB470n~pSeUkmNMo3P3ePW61mRwApwZBw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central","translated_slug":"","page_count":18,"language":"en","content_type":"Work","summary":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. 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In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. 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Presented at the 2014 Geological Society of America (GSA) Annual Meeting (Vancouver, Canada)</span></div><div class="wp-workCard_item wp-workCard--actions"><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-video-id="jZvDMj"><a class="js-profile-work-strip-edit-button" href="https://omp.academia.edu/video/edit/jZvDMj" rel="nofollow" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-video-id="jZvDMj">12 views</span></span></span></div></div></div></div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="1264219" id="papers"><div class="js-work-strip profile--work_container" data-work-id="127478319"><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/127478319/Sustainability2025"><img alt="Research paper thumbnail of Sustainability2025" 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/127478319/Sustainability2025">Sustainability2025</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://omp.academia.edu/MichelGregoire">Michel Gregoire</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/JessicaKlar1">Jessica Klar</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/PCourjaultRad%C3%A9">Pierre Courjault-Radé</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/SebastienFabre1">Sébastien Fabre</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This study investigates uranium (U) and thorium (Th) levels in surface beach sediments from the ...</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">This study investigates uranium (U) and thorium (Th) levels in surface beach <br />sediments from the Central Gulf of Gabes (SE Tunisia), aiming to identify concentration zones, geochemical behaviors, and enrichment factors. U concentrations ranged from 0.71 to 38.00 mg/kg, exceeding Th levels, which ranged from 1.00 to 10.60 mg/kg. A positive correlation between U and Th indicates a common source, which is most likely phosphogypsum wastes, and similar geochemical behaviors. The central sector near Gabes’ fertilizer factories showed the highest U and Th concentrations, with factors such as,proximity to industrial discharge, port structures’ influence, organic matter enrichment, low seawater pH, and high phosphorus levels affecting the spatial distribution of these elements. Thermochemical analysis suggests that U and Th exhibit parallel chemical behaviors in low-pH, phosphate-rich conditions. This is the first study to document U and Th presence in phosphogypsum-contaminated beach sediments in Gabes, underlining potential risks to the environment and human health. The findings of this work contribute to the international database of U and Th contamination in coastal sediments, providing essential data to support sustainable strategies aimed at safeguarding human health and preserving local environments affected by phosphate fertilizer industry pollution.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="7895ea4cbffc1c09e4c01474bbcec4c6" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":121204659,"asset_id":127478319,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/121204659/download_file?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="127478319"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="127478319"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 127478319; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=127478319]").text(description); $(".js-view-count[data-work-id=127478319]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 127478319; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='127478319']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "7895ea4cbffc1c09e4c01474bbcec4c6" } } $('.js-work-strip[data-work-id=127478319]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":127478319,"title":"Sustainability2025","translated_title":"","metadata":{"abstract":"This study investigates uranium (U) and thorium (Th) levels in surface beach\r\nsediments from the Central Gulf of Gabes (SE Tunisia), aiming to identify concentration zones, geochemical behaviors, and enrichment factors. 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The central sector near Gabes' fertilizer factories showed the highest U and Th concentrations, with factors such as proximity to industrial discharge, port structures' influence, organic matter enrichment, low seawater pH, and high phosphorus levels affecting the spatial distribution of these elements. Thermochemical analysis suggests that U and Th exhibit parallel chemical behaviors in low-pH, phosphate-rich conditions. This is the first study to document U and Th presence in phosphogypsum-contaminated beach sediments in Gabes, underlining potential risks to the environment and human health. The findings of this work contribute to the international database of U and Th contamination in coastal sediments, providing essential data to support sustainable strategies aimed at safeguarding human health and preserving local environments affected by phosphate fertilizer industry pollution.","grobid_abstract_attachment_id":121204659},"translated_abstract":"This study investigates uranium (U) and thorium (Th) levels in surface beach\r\nsediments from the Central Gulf of Gabes (SE Tunisia), aiming to identify concentration zones, geochemical behaviors, and enrichment factors. U concentrations ranged from 0.71 to 38.00 mg/kg, exceeding Th levels, which ranged from 1.00 to 10.60 mg/kg. A positive correlation between U and Th indicates a common source, which is most likely phosphogypsum wastes, and similar geochemical behaviors. The central sector near Gabes’ fertilizer factories showed the highest U and Th concentrations, with factors such as,proximity to industrial discharge, port structures’ influence, organic matter enrichment, low seawater pH, and high phosphorus levels affecting the spatial distribution of these elements. Thermochemical analysis suggests that U and Th exhibit parallel chemical behaviors in low-pH, phosphate-rich conditions. This is the first study to document U and Th presence in phosphogypsum-contaminated beach sediments in Gabes, underlining potential risks to the environment and human health. The findings of this work contribute to the international database of U and Th contamination in coastal sediments, providing essential data to support sustainable strategies aimed at safeguarding human health and preserving local environments affected by phosphate fertilizer industry pollution.","internal_url":"https://www.academia.edu/127478319/Sustainability2025","translated_internal_url":"","created_at":"2025-02-05T05:49:28.415-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":43079435,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":339069122,"co_author_invite_id":8334967,"email":"j***r@gmail.com","display_order":1,"name":"Jessica Klar","title":"Sustainability2025"},{"id":43079436,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":66204658,"co_author_invite_id":null,"email":"s***t@get.omp.eu","display_order":2,"name":"Sylvie castet","title":"Sustainability2025"},{"id":43079437,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":187138830,"co_author_invite_id":null,"email":"c***e@gmail.com","display_order":4,"name":"Pierre Courjault-Radé","title":"Sustainability2025"},{"id":43079438,"work_id":127478319,"tagging_user_id":10246740,"tagged_user_id":339018268,"co_author_invite_id":8334968,"email":"s***e@irap.omp.eu","display_order":5,"name":"Sébastien Fabre","title":"Sustainability2025"}],"downloadable_attachments":[{"id":121204659,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://a.academia-assets.com/images/blank-paper.jpg","file_name":"Sustainability_2025.pdf","download_url":"https://www.academia.edu/attachments/121204659/download_file","bulk_download_file_name":"Sustainability2025.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/121204659/Sustainability_2025-libre.pdf?1738772188=\u0026response-content-disposition=attachment%3B+filename%3DSustainability2025.pdf\u0026Expires=1743209697\u0026Signature=HxedQM15-tjMKI4VBEc8oGxDEXLACFud5xoKTdFNZU9rnaRcvlf2OXxCwT889TxvSBtyAlnxPur0s3Py1pRRWDlZB6xNEh~vZIw~5qSlZrsI1-LtAnmJiHZhkwgDWKHaLpHazdnkUT9Wb4uXna-zydOmIspB-SIKfoFHgJm3Ylgl0Byq8QkqBk6pTsk12cl04gcJo6C9jLmdI6cDPKXqf~bm9ocnngD8bgkvKF7jtPfUrJgCf-K9Bj1AV6TRJrUJWqe~nEDEfY2c-uSLUMTAlrqeJsoNZ2qB63G9HeiQrbvCSy9Ve-bmcxzteapXwVpFjCK40edQETgzy~ZHsHDDxA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Sustainability2025","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"This study investigates uranium (U) and thorium (Th) levels in surface beach\r\nsediments from the Central Gulf of Gabes (SE Tunisia), aiming to identify concentration zones, geochemical behaviors, and enrichment factors. U concentrations ranged from 0.71 to 38.00 mg/kg, exceeding Th levels, which ranged from 1.00 to 10.60 mg/kg. A positive correlation between U and Th indicates a common source, which is most likely phosphogypsum wastes, and similar geochemical behaviors. The central sector near Gabes’ fertilizer factories showed the highest U and Th concentrations, with factors such as,proximity to industrial discharge, port structures’ influence, organic matter enrichment, low seawater pH, and high phosphorus levels affecting the spatial distribution of these elements. Thermochemical analysis suggests that U and Th exhibit parallel chemical behaviors in low-pH, phosphate-rich conditions. This is the first study to document U and Th presence in phosphogypsum-contaminated beach sediments in Gabes, underlining potential risks to the environment and human health. The findings of this work contribute to the international database of U and Th contamination in coastal sediments, providing essential data to support sustainable strategies aimed at safeguarding human health and preserving local environments affected by phosphate fertilizer industry pollution.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":121204659,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://a.academia-assets.com/images/blank-paper.jpg","file_name":"Sustainability_2025.pdf","download_url":"https://www.academia.edu/attachments/121204659/download_file","bulk_download_file_name":"Sustainability2025.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/121204659/Sustainability_2025-libre.pdf?1738772188=\u0026response-content-disposition=attachment%3B+filename%3DSustainability2025.pdf\u0026Expires=1743209697\u0026Signature=HxedQM15-tjMKI4VBEc8oGxDEXLACFud5xoKTdFNZU9rnaRcvlf2OXxCwT889TxvSBtyAlnxPur0s3Py1pRRWDlZB6xNEh~vZIw~5qSlZrsI1-LtAnmJiHZhkwgDWKHaLpHazdnkUT9Wb4uXna-zydOmIspB-SIKfoFHgJm3Ylgl0Byq8QkqBk6pTsk12cl04gcJo6C9jLmdI6cDPKXqf~bm9ocnngD8bgkvKF7jtPfUrJgCf-K9Bj1AV6TRJrUJWqe~nEDEfY2c-uSLUMTAlrqeJsoNZ2qB63G9HeiQrbvCSy9Ve-bmcxzteapXwVpFjCK40edQETgzy~ZHsHDDxA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":402,"name":"Environmental Science","url":"https://www.academia.edu/Documents/in/Environmental_Science"},{"id":3407,"name":"Environmental Studies","url":"https://www.academia.edu/Documents/in/Environmental_Studies"},{"id":3743,"name":"Environmental Geochemistry (Environmental Studies)","url":"https://www.academia.edu/Documents/in/Environmental_Geochemistry_Environmental_Studies_"},{"id":141315,"name":"Ecological Risk Assessment","url":"https://www.academia.edu/Documents/in/Ecological_Risk_Assessment"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-127478319-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="126842883"><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/126842883/JHM"><img alt="Research paper thumbnail of JHM" class="work-thumbnail" src="https://attachments.academia-assets.com/120661054/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/126842883/JHM">JHM</a></div><div class="wp-workCard_item"><span>Journal of Hazardous Materials</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE 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 foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a<br />spectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to<br />investigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine<br />the origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in<br />marine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,<br />and ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through<br />phosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)<br />destabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced<br />by wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific<br />organic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic<br />radiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated<br />with PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into<br />the coastal environment of Gabes.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="b41e19ad0e0a97373198b0a76a4cc028" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":120661054,"asset_id":126842883,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/120661054/download_file?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="126842883"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="126842883"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 126842883; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=126842883]").text(description); $(".js-view-count[data-work-id=126842883]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 126842883; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='126842883']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "b41e19ad0e0a97373198b0a76a4cc028" } } $('.js-work-strip[data-work-id=126842883]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":126842883,"title":"JHM","translated_title":"","metadata":{"doi":"10.1016/j.jhazmat.2024.135732","abstract":"The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a\nspectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to\ninvestigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine\nthe origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in\nmarine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,\nand ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through\nphosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)\ndestabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced\nby wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific\norganic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic\nradiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated\nwith PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into\nthe coastal environment of Gabes.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Journal of Hazardous Materials","grobid_abstract_attachment_id":120661054},"translated_abstract":"The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a\nspectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to\ninvestigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine\nthe origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in\nmarine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,\nand ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through\nphosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)\ndestabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced\nby wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific\norganic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic\nradiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated\nwith PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into\nthe coastal environment of Gabes.","internal_url":"https://www.academia.edu/126842883/JHM","translated_internal_url":"","created_at":"2025-01-06T05:22:31.319-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42927339,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":33462064,"co_author_invite_id":null,"email":"r***i@gmail.com","display_order":-3,"name":"Radhouane El Zrelli","title":"JHM"},{"id":42927340,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":38175029,"co_author_invite_id":null,"email":"s***e@irap.omp.eu","affiliation":"Observatoire Midi-Pyrénées, Université de Toulouse III Paul Sabatier","display_order":-2,"name":"Sébastien Fabre","title":"JHM"},{"id":42927341,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":66204658,"co_author_invite_id":null,"email":"s***t@get.omp.eu","display_order":-1,"name":"Sylvie castet","title":"JHM"},{"id":42927342,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":171331386,"co_author_invite_id":null,"email":"o***i@gmail.com","display_order":1,"name":"Oussema Fersi","title":"JHM"},{"id":42927343,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":163108689,"co_author_invite_id":null,"email":"c***e@ums-castaing.fr","display_order":2,"name":"Josse Claudie","title":"JHM"},{"id":42927344,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":11599272,"co_author_invite_id":null,"email":"p***e@orange.fr","display_order":3,"name":"Pierre Courjault-Radé","title":"JHM"},{"id":42927345,"work_id":126842883,"tagging_user_id":10246740,"tagged_user_id":333067136,"co_author_invite_id":null,"email":"2***n@privaterelay.appleid.com","display_order":4,"name":"anne-marie cousin","title":"JHM"}],"downloadable_attachments":[{"id":120661054,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120661054/thumbnails/1.jpg","file_name":"JHM_2024.pdf","download_url":"https://www.academia.edu/attachments/120661054/download_file","bulk_download_file_name":"JHM.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120661054/JHM_2024-libre.pdf?1736172571=\u0026response-content-disposition=attachment%3B+filename%3DJHM.pdf\u0026Expires=1743209698\u0026Signature=WHXEzHx1vl4TmpsG-bvIbPZiurK7quGEhg7KJa7MKK-UzsiOupKDR~D0jcGxKgevIVYx~SjZAGlI11PpmUCkYexPrizyP04-l-2OLUbXlKwpm18J95~T543xspEphQTDAQzWg59q83m7LHlaf090ZlgvM8gIB0-h66LGarVvJ3O58jn686erXEwg6Daqcs~LB0VM1-4Z0fsF~AMM1QATvfx8MIEnWDeHJfvMO59Z~G9E1l6~O3QwWg9tCO7g7nyNq~afIQujbs8XYF6ruXT32qvFPyx~bdd-pcr82ymNpYvltr0azgXPlW9rqOJpgt4ki~ny-D67c5VyGppMo7RkLw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"JHM","translated_slug":"","page_count":13,"language":"en","content_type":"Work","summary":"The foamability of dissolved phosphogypsum from the phosphate fertilizer factories of Gabes (SE Tunisia) is a\nspectacular phenomenon that has not yet been thoroughly studied. The main objective of this research was to\ninvestigate the organic properties of phosphogypsum foam (PGF) to understand its formation process, determine\nthe origin of its enhanced radiochemical contaminants load, and identify its role in pollutants dispersion in\nmarine environment of the Southern Mediterranean Sea. This study identified PGF as an unnatural, surfactantstabilized,\nand ephemeral aqueous foam. PGF-forming process comprises three main steps: (i) formation (through\nphosphogypsum dissolution), (ii) stabilization (facilitated by organic surfactants and gypsum crystals), and (iii)\ndestabilization (geochemical (involving the dissolution of the PGF skeleton gypsum) and/or mechanical (influenced\nby wind and wave action)). The amphiphilic nature of PGF organic matter and the presence of specific\norganic groups are responsible for its high toxic contaminants load. PGF contributes, through its elevated pollutants content and its ability to migrate far from its source, to the marine dispersion of industrial toxic\nradiochemical contaminants. It is therefore recommended to mitigate the environmental and health risks associated\nwith PGF, including banning the discharge of untreated phosphogypsum and other industrial wastes into\nthe coastal environment of Gabes.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":120661054,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120661054/thumbnails/1.jpg","file_name":"JHM_2024.pdf","download_url":"https://www.academia.edu/attachments/120661054/download_file","bulk_download_file_name":"JHM.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120661054/JHM_2024-libre.pdf?1736172571=\u0026response-content-disposition=attachment%3B+filename%3DJHM.pdf\u0026Expires=1743209698\u0026Signature=WHXEzHx1vl4TmpsG-bvIbPZiurK7quGEhg7KJa7MKK-UzsiOupKDR~D0jcGxKgevIVYx~SjZAGlI11PpmUCkYexPrizyP04-l-2OLUbXlKwpm18J95~T543xspEphQTDAQzWg59q83m7LHlaf090ZlgvM8gIB0-h66LGarVvJ3O58jn686erXEwg6Daqcs~LB0VM1-4Z0fsF~AMM1QATvfx8MIEnWDeHJfvMO59Z~G9E1l6~O3QwWg9tCO7g7nyNq~afIQujbs8XYF6ruXT32qvFPyx~bdd-pcr82ymNpYvltr0azgXPlW9rqOJpgt4ki~ny-D67c5VyGppMo7RkLw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":402,"name":"Environmental Science","url":"https://www.academia.edu/Documents/in/Environmental_Science"},{"id":9513,"name":"MARINE POLLUTION","url":"https://www.academia.edu/Documents/in/MARINE_POLLUTION"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-126842883-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="126774625"><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/126774625/Lithos"><img alt="Research paper thumbnail of Lithos" class="work-thumbnail" src="https://attachments.academia-assets.com/120601592/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/126774625/Lithos">Lithos</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, 2025</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-...</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 granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-I low REE; Type-II high REE), leucotonalites, melatonalites and Qz-monzodiorites. These are I-type calc-alkaline granitoids, although classification of the newly identified melatonalites remains enigmatic, likely reflecting magma mixing between different sources for their formation. Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).<br />Fractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. Melatonalites and Type-II granodiorites appear to have been formed during the early evolution stages of subduction initiation, whereas leucotonalites represent the late-stage shallow crystallization granitoid phase.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="143ee8161517cd907c3d5e3f5a9308c4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":120601592,"asset_id":126774625,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/120601592/download_file?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="126774625"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="126774625"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 126774625; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=126774625]").text(description); $(".js-view-count[data-work-id=126774625]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 126774625; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='126774625']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "143ee8161517cd907c3d5e3f5a9308c4" } } $('.js-work-strip[data-work-id=126774625]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":126774625,"title":"Lithos","translated_title":"","metadata":{"doi":"10.1016/j.lithos.2024.107926","abstract":"The granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-I low REE; Type-II high REE), leucotonalites, melatonalites and Qz-monzodiorites. These are I-type calc-alkaline granitoids, although classification of the newly identified melatonalites remains enigmatic, likely reflecting magma mixing between different sources for their formation. Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).\nFractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. 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Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).\nFractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. Melatonalites and Type-II granodiorites appear to have been formed during the early evolution stages of subduction initiation, whereas leucotonalites represent the late-stage shallow crystallization granitoid phase.","internal_url":"https://www.academia.edu/126774625/Lithos","translated_internal_url":"","created_at":"2025-01-03T07:29:35.176-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42916769,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":374965,"co_author_invite_id":null,"email":"p***s@yahoo.com","affiliation":"National \u0026 Kapodistrian University of Athens","display_order":-4,"name":"Petros Koutsovitis","title":"Lithos"},{"id":42916770,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":58376876,"co_author_invite_id":null,"email":"m***n@gmail.com","display_order":-3,"name":"Michiel van der Meulen","title":"Lithos"},{"id":42916771,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":12114691,"co_author_invite_id":null,"email":"p***u@gmail.com","display_order":-2,"name":"Pavlos Tyrologou","title":"Lithos"},{"id":42916772,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":12369491,"co_author_invite_id":null,"email":"g***7@upatras.gr","affiliation":"University of Patras","display_order":-1,"name":"Alkiviades Sideridis","title":"Lithos"},{"id":42916773,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":465788,"email":"t***s@univie.ac.at","display_order":1,"name":"Theodoros Ntaflos","title":"Lithos"},{"id":42916774,"work_id":126774625,"tagging_user_id":10246740,"tagged_user_id":244857696,"co_author_invite_id":null,"email":"l***s@gmail.com","display_order":2,"name":"konstantinos lentas","title":"Lithos"}],"downloadable_attachments":[{"id":120601592,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120601592/thumbnails/1.jpg","file_name":"Lithos_2025.pdf","download_url":"https://www.academia.edu/attachments/120601592/download_file","bulk_download_file_name":"Lithos.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120601592/Lithos_2025-libre.pdf?1735920364=\u0026response-content-disposition=attachment%3B+filename%3DLithos.pdf\u0026Expires=1743209698\u0026Signature=dhtRG5KcE8ROmY8faZCKyJLEW6LQvWV9HB5H9C9CsX4Q3sy1sIpm4DSMY62tn7VuVo9SrHqbuF5Om3ndLRThttKYkuU0o5g7MfblDpriGJ2~WrCq9H4DORbKVXsTU-Ows7TJ0R7miJe6rA7DInREODPdga35ZJYoSkzQoUw59POKu6BeOmWkYXMDPlxKKwvA7ZRB1lhYbz3s3sf6o4-lB2DETQrioDBRCDaj4bhe7MzgWpmTVL62J40blRK7RtHR6lqKdeXtH15YfTut6yv8vfT4y9PajGUt-UzKd3WdqUiYvIb~XWyFq7NFhVg4NkXslVaVvnxxFLNf8BRQaXtwNQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Lithos","translated_slug":"","page_count":19,"language":"en","content_type":"Work","summary":"The granitoids in St. Martin Island, Lesser Antilles – Caribbean, consist of granodiorites (Type-I low REE; Type-II high REE), leucotonalites, melatonalites and Qz-monzodiorites. These are I-type calc-alkaline granitoids, although classification of the newly identified melatonalites remains enigmatic, likely reflecting magma mixing between different sources for their formation. Geothermometry applications yield high formation temperatures for the melatonalites and the Type-II granodiorites exceeding by ∼100 °C those calculated for the other granitoids. Pressure conditions were relatively high for the melatonalites and granodiorites (∼4.2 and ∼ 4.0 kbar respectively), with the lowest assigned to the leucotonalites (∼1.8 kbar). Magnesiohornblende crystallized at the final crystallization stages (∼740 °C; ∼2.5 km depth), under hydrous (H2O = ∼3.5 wt%) and highly oxidizing conditions (ΔNNO up to +2.7).\nFractional crystallization significantly contributed to the compositional variability of the evolved granitoid lithotypes, with plagioclase being preferably fractionated in the Type-I granodiorites, relative to the Type-II granodiorites that mostly involved K-feldspar removal. Additionally, fluctuation of the hydrous and slab-derived fluid fluxes further promoted granitoid differentiation. Geochemical and Sr-Nd isotopic data reveal restricted sediment contamination of the mantle wedge. Melatonalites and Type-II granodiorites appear to have been formed during the early evolution stages of subduction initiation, whereas leucotonalites represent the late-stage shallow crystallization granitoid phase.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":120601592,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120601592/thumbnails/1.jpg","file_name":"Lithos_2025.pdf","download_url":"https://www.academia.edu/attachments/120601592/download_file","bulk_download_file_name":"Lithos.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120601592/Lithos_2025-libre.pdf?1735920364=\u0026response-content-disposition=attachment%3B+filename%3DLithos.pdf\u0026Expires=1743209698\u0026Signature=dhtRG5KcE8ROmY8faZCKyJLEW6LQvWV9HB5H9C9CsX4Q3sy1sIpm4DSMY62tn7VuVo9SrHqbuF5Om3ndLRThttKYkuU0o5g7MfblDpriGJ2~WrCq9H4DORbKVXsTU-Ows7TJ0R7miJe6rA7DInREODPdga35ZJYoSkzQoUw59POKu6BeOmWkYXMDPlxKKwvA7ZRB1lhYbz3s3sf6o4-lB2DETQrioDBRCDaj4bhe7MzgWpmTVL62J40blRK7RtHR6lqKdeXtH15YfTut6yv8vfT4y9PajGUt-UzKd3WdqUiYvIb~XWyFq7NFhVg4NkXslVaVvnxxFLNf8BRQaXtwNQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":28331,"name":"Granite (Earth Sciences)","url":"https://www.academia.edu/Documents/in/Granite_Earth_Sciences_"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-126774625-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="126769690"><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/126769690/CRGEOS"><img alt="Research paper thumbnail of CRGEOS" class="work-thumbnail" src="https://attachments.academia-assets.com/120597382/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/126769690/CRGEOS">CRGEOS</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/djerossemfelix">djerossem felix</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/Beno%C3%AEtJosephMbassa">Benoît Joseph Mbassa</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Comptes Rendus Géosciences</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones o...</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 poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="27a29c1011c3b7db2fbaf4838ba7c955" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":120597382,"asset_id":126769690,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/120597382/download_file?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="126769690"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="126769690"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 126769690; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=126769690]").text(description); $(".js-view-count[data-work-id=126769690]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 126769690; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='126769690']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "27a29c1011c3b7db2fbaf4838ba7c955" } } $('.js-work-strip[data-work-id=126769690]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":126769690,"title":"CRGEOS","translated_title":"","metadata":{"doi":"10.5802/crgeos.282","abstract":"The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.","ai_title_tag":"Geochemical Insights on Ouaddai Volcanics","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Comptes Rendus Géosciences","grobid_abstract_attachment_id":120597382},"translated_abstract":"The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.","internal_url":"https://www.academia.edu/126769690/CRGEOS","translated_internal_url":"","created_at":"2025-01-03T03:37:49.609-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42915748,"work_id":126769690,"tagging_user_id":10246740,"tagged_user_id":148209982,"co_author_invite_id":null,"email":"d***m@gmail.com","display_order":-3,"name":"djerossem felix","title":"CRGEOS"},{"id":42915749,"work_id":126769690,"tagging_user_id":10246740,"tagged_user_id":41335370,"co_author_invite_id":null,"email":"b***a@yahoo.fr","display_order":-2,"name":"Benoît Joseph Mbassa","title":"CRGEOS"},{"id":42915750,"work_id":126769690,"tagging_user_id":10246740,"tagged_user_id":2909958,"co_author_invite_id":null,"email":"o***e@get.omp.eu","affiliation":"Université Toulouse III","display_order":-1,"name":"Olivier Vanderhaeghe","title":"CRGEOS"}],"downloadable_attachments":[{"id":120597382,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120597382/thumbnails/1.jpg","file_name":"CRGEOS_2024.pdf","download_url":"https://www.academia.edu/attachments/120597382/download_file","bulk_download_file_name":"CRGEOS.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120597382/CRGEOS_2024-libre.pdf?1735904456=\u0026response-content-disposition=attachment%3B+filename%3DCRGEOS.pdf\u0026Expires=1743209698\u0026Signature=Pk2p0e7xWZOWw9LlqrtkD-qVS7eOSplx34yA0ATSoVg6K28LFpZVxrGHVE1xji4z3cyogDBIwbClvfRcjc68~5M4p8P10NDyUC8S03V5brZUP8Z6cLiiS12b5Te4PKA0U2Jxz7TS3ZJ~6mHUlBXbvsMHCBNh3EwLng7RxF~LMzcP79wJpxQpbi8ddyINJ8s7MEnkvnwQnF0RadhZu3V453~tvlX7FplF45PaAvoQS5Iws4NfT~l6qrG8UYUPcivsQcnj5yDz2wM1r6NQQJTvUQydyyHX9cMfFwXAbiNcp6Bxoxh3BZtukf4ztWu2iiLLHvewnK3vRiPMdLqdwEQIaA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"CRGEOS","translated_slug":"","page_count":19,"language":"en","content_type":"Work","summary":"The poorly documented volcanic rocks of the Ouaddai massif in Chad are a continuity of the ones of the Cameroon Volcanic Line further to the SE, located within the Central African rift system. New mineralogical and geochemical data from the Iriba basanites (SiO2: 41–45 wt%) show depletion in HREE, slight negative Sm anomaly and high LREE/HREE ratios, which is typical of OIB. The main differentiation process is fractional crystallization with a complete lack of crustal contamination. These features, similar to basanites exposed in southern Cameroon, reflect the partial melting of a metasomatized subcontinental lithospheric root reworked during the formation of the Cenozoic Central Africa Rift System. We propose to define by Cameroon-Chad Volcanic Line this continental scale structure controlling the emplacement of alkaline magmas.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":120597382,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/120597382/thumbnails/1.jpg","file_name":"CRGEOS_2024.pdf","download_url":"https://www.academia.edu/attachments/120597382/download_file","bulk_download_file_name":"CRGEOS.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/120597382/CRGEOS_2024-libre.pdf?1735904456=\u0026response-content-disposition=attachment%3B+filename%3DCRGEOS.pdf\u0026Expires=1743209698\u0026Signature=Pk2p0e7xWZOWw9LlqrtkD-qVS7eOSplx34yA0ATSoVg6K28LFpZVxrGHVE1xji4z3cyogDBIwbClvfRcjc68~5M4p8P10NDyUC8S03V5brZUP8Z6cLiiS12b5Te4PKA0U2Jxz7TS3ZJ~6mHUlBXbvsMHCBNh3EwLng7RxF~LMzcP79wJpxQpbi8ddyINJ8s7MEnkvnwQnF0RadhZu3V453~tvlX7FplF45PaAvoQS5Iws4NfT~l6qrG8UYUPcivsQcnj5yDz2wM1r6NQQJTvUQydyyHX9cMfFwXAbiNcp6Bxoxh3BZtukf4ztWu2iiLLHvewnK3vRiPMdLqdwEQIaA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"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") if (false) { Aedu.setUpFigureCarousel('profile-work-126769690-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="87011147"><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/87011147/Petrography_mineral_chemistry_and_geochemistry_of_hornblenditic_autholiths_and_hornblenditic_xenoliths_from_volcanic_alkaline_rocks_from_North_West_of_Marand_NW_Iran_"><img alt="Research paper thumbnail of Petrography, mineral chemistry and geochemistry of hornblenditic autholiths and hornblenditic xenoliths from volcanic alkaline rocks from North West of Marand (NW Iran)" class="work-thumbnail" src="https://attachments.academia-assets.com/91339933/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/87011147/Petrography_mineral_chemistry_and_geochemistry_of_hornblenditic_autholiths_and_hornblenditic_xenoliths_from_volcanic_alkaline_rocks_from_North_West_of_Marand_NW_Iran_">Petrography, mineral chemistry and geochemistry of hornblenditic autholiths and hornblenditic xenoliths from volcanic alkaline rocks from North West of Marand (NW Iran)</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://tabrizu.academia.edu/AhmadJahangiri">Ahmad Jahangiri</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Iranian Journal of Crystallography and Mineralogy</span><span>, 2018</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="538e9fe656c9fe2fd7ff931530c31c2c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":91339933,"asset_id":87011147,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/91339933/download_file?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="87011147"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="87011147"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 87011147; 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This study investigates hornblenditic autholiths and xenoliths found within trachy andesite and basaltic andesite rocks, classified into two groups based on plagioclase content: Group 1 with \u003c10% plagioclase, resembling the host volcanic magma, and Group 2 with \u003e20% plagioclase, indicating a different mantle-derived origin with less enrichment. The mineral chemistry and geochemical signatures reveal insights into the magmatic processes guiding these volcanic features.","publication_date":{"day":null,"month":null,"year":2018,"errors":{}},"publication_name":"Iranian Journal of Crystallography and Mineralogy"},"translated_abstract":null,"internal_url":"https://www.academia.edu/87011147/Petrography_mineral_chemistry_and_geochemistry_of_hornblenditic_autholiths_and_hornblenditic_xenoliths_from_volcanic_alkaline_rocks_from_North_West_of_Marand_NW_Iran_","translated_internal_url":"","created_at":"2022-09-21T03:56:44.095-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":4826161,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42605006,"work_id":87011147,"tagging_user_id":4826161,"tagged_user_id":10246740,"co_author_invite_id":null,"email":"m***e@get.omp.eu","affiliation":"Observatoire Midi-Pyrénées, Université de Toulouse III Paul 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dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-87011147-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124570903"><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/124570903/Insights_into_the_North_Patagonian_Massif_lower_crust_petrology_and_microstructure_of_granulite_xenoliths"><img alt="Research paper thumbnail of Insights into the North Patagonian Massif lower crust: petrology and microstructure of granulite xenoliths" class="work-thumbnail" src="https://attachments.academia-assets.com/118771293/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/124570903/Insights_into_the_North_Patagonian_Massif_lower_crust_petrology_and_microstructure_of_granulite_xenoliths">Insights into the North Patagonian Massif lower crust: petrology and microstructure of granulite xenoliths</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/NoeMuckensturm">Noé Muckensturm</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The continental lower crust constitutes a key zone for understanding the mantle-crust magmatic an...</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 continental lower crust constitutes a key zone for understanding the mantle-crust magmatic and mechanical transfers, but its study is hampered by the paucity of lower crust samples. Here, we characterise the petrological, geochemical and petrophysical processes structuring the lower crust of the North Patagonian Massif (NPM; Argentina) using a suite of representative mafic granulite and websterite xenoliths. These xenoliths were entrained by alkaline lavas from 5 volcanic centres that erupted between the Oligocene and Pleistocene. Electron microprobe and laser ablation inductively coupled plasma mass spectrometer (LA-ICPMS) were used to obtain in-situ geochemical data on the minerals, while microstructural data were obtained by Electron Backscatter Diffraction (EBSD). Both granulites and</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e6ceff20b4317884b1e14ad9bdc7f968" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118771293,"asset_id":124570903,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118771293/download_file?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="124570903"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124570903"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124570903; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124570903]").text(description); $(".js-view-count[data-work-id=124570903]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124570903; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124570903']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "e6ceff20b4317884b1e14ad9bdc7f968" } } $('.js-work-strip[data-work-id=124570903]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124570903,"title":"Insights into the North Patagonian Massif lower crust: petrology and microstructure of granulite xenoliths","translated_title":"","metadata":{"doi":"10.1093/petrology/egae100","ai_title_tag":"Granulite Xenoliths of North Patagonian Massif","grobid_abstract":"The continental lower crust constitutes a key zone for understanding the mantle-crust magmatic and mechanical transfers, but its study is hampered by the paucity of lower crust samples. Here, we characterise the petrological, geochemical and petrophysical processes structuring the lower crust of the North Patagonian Massif (NPM; Argentina) using a suite of representative mafic granulite and websterite xenoliths. These xenoliths were entrained by alkaline lavas from 5 volcanic centres that erupted between the Oligocene and Pleistocene. Electron microprobe and laser ablation inductively coupled plasma mass spectrometer (LA-ICPMS) were used to obtain in-situ geochemical data on the minerals, while microstructural data were obtained by Electron Backscatter Diffraction (EBSD). 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They constitute an important source of information about the melt migration mechanisms and related petrological processes in the shallowest part of the mantle beneath former oceanic spreading centres. In the field, these socalled 'melt migration structures' attract attention when they consist of mineral assemblages contrasting with that of their host peridotite. They therefore record a particular moment in the migration history: when the melt becomes out of equilibrium with the peridotite and causes a reaction impacting its modal composition, and/or when a temperature drop initiates the crystallization of the melt. The existence of cryptic effects of migration revealed by geochemical data shows that melts do not always leave a trail visible in the field. Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? What is the nature of the 'universal solvent' initiating infiltration melting and making channelized porous flow the most common mode of transport of magmas through a peridotite matrix regardless the tectonic setting? A fundamental message delivered by ophiolites is that the shallow mantle behaves as a particularly efficient reactive filter between the depths and the surface of the Earth. Unexpectedly, the reactions occurring there are enhanced by the hybridization between mafic melts and a hydrous component, whatever its origin (i.e. magmatic vs. hydrothermal). This hybridization triggers out of equilibrium reactions, leading to the formation of exotic lithologies, including metallic ores, and impacting the global geochemical cycle of a whole range of chemical elements.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e6bdb1f3e38b2929422c157faf3e847b" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118767046,"asset_id":124566052,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118767046/download_file?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="124566052"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124566052"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124566052; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124566052]").text(description); $(".js-view-count[data-work-id=124566052]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124566052; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124566052']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "e6bdb1f3e38b2929422c157faf3e847b" } } $('.js-work-strip[data-work-id=124566052]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124566052,"title":"The shallow mantle as a reactive filter: a hypothesis inspired and supported by field observations","translated_title":"","metadata":{"doi":"10.1180/EMU-notes.21.5","abstract":"The footprints of mafic melts travelling from the depths to the surface are abundant in the mantle section of ophiolites. They constitute an important source of information about the melt migration mechanisms and related petrological processes in the shallowest part of the mantle beneath former oceanic spreading centres. In the field, these socalled 'melt migration structures' attract attention when they consist of mineral assemblages contrasting with that of their host peridotite. They therefore record a particular moment in the migration history: when the melt becomes out of equilibrium with the peridotite and causes a reaction impacting its modal composition, and/or when a temperature drop initiates the crystallization of the melt. The existence of cryptic effects of migration revealed by geochemical data shows that melts do not always leave a trail visible in the field. Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? What is the nature of the 'universal solvent' initiating infiltration melting and making channelized porous flow the most common mode of transport of magmas through a peridotite matrix regardless the tectonic setting? A fundamental message delivered by ophiolites is that the shallow mantle behaves as a particularly efficient reactive filter between the depths and the surface of the Earth. 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They therefore record a particular moment in the migration history: when the melt becomes out of equilibrium with the peridotite and causes a reaction impacting its modal composition, and/or when a temperature drop initiates the crystallization of the melt. The existence of cryptic effects of migration revealed by geochemical data shows that melts do not always leave a trail visible in the field. Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? 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Although incomplete and patchy, the melt migration structures preserved in ophiolites are witnesses of processes that do actually occur in nature, which constitutes an invaluable support to the interpretation of geophysical data and inescapable constraints for numerical simulations and models of chemical geodynamics. Here we show how field observations and related petrological and geochemical studies allow us to propose answers to fundamental questions such as these: At which temperature is porous flow superseded by dyking? What are the factors governing melt trajectories? What is the nature of the 'universal solvent' initiating infiltration melting and making channelized porous flow the most common mode of transport of magmas through a peridotite matrix regardless the tectonic setting? A fundamental message delivered by ophiolites is that the shallow mantle behaves as a particularly efficient reactive filter between the depths and the surface of the Earth. Unexpectedly, the reactions occurring there are enhanced by the hybridization between mafic melts and a hydrous component, whatever its origin (i.e. magmatic vs. hydrothermal). This hybridization triggers out of equilibrium reactions, leading to the formation of exotic lithologies, including metallic ores, and impacting the global geochemical cycle of a whole range of chemical elements.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118767046,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118767046/thumbnails/1.jpg","file_name":"EMU_21_Ch05.pdf","download_url":"https://www.academia.edu/attachments/118767046/download_file","bulk_download_file_name":"The_shallow_mantle_as_a_reactive_filter.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118767046/EMU_21_Ch05-libre.pdf?1728467451=\u0026response-content-disposition=attachment%3B+filename%3DThe_shallow_mantle_as_a_reactive_filter.pdf\u0026Expires=1743209698\u0026Signature=VhGKl-o11PXM58AAbyl4r5mIJ1JHv41lbbso~pFmLK2eph2LvUPn5PzWPydOosVmi0SmaUDxvXUCqViGIq1KkonXycNwQc5piB5Ni90288V8dTZcBy53~-bPRsUq74wudXtgYC8I1kF3-jPZVfKM51i45fOr8veoLxKR0U9xu-S4XflfThpDZddpiT7ZLo7B2HtQ9wFqfEhFFUzZ9tyx9sgiYuA3yaJpDIdbeQGWanZEnHaQF6jaWB4zE1ZO7kpiqbTF0dSbVRHksiidIWpocktDRYgv9VoR0BhEhz3Hv82PNPgnb3n7l7xkI8UtmHT6zEbdiNqSes1umYa-b6Nsrw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124566052-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565963"><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/124565963/Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us"><img alt="Research paper thumbnail of Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us" class="work-thumbnail" src="https://attachments.academia-assets.com/118766957/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/124565963/Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us">Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us</a></div><div class="wp-workCard_item"><span>EMU Notes in Mineralogy</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The present contribution synthesizes the main petrographic, mineralogical and chemical features o...</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 present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="881ab5a7262657f5cf20f35047fa5d9f" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766957,"asset_id":124565963,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766957/download_file?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="124565963"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565963"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565963; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565963]").text(description); $(".js-view-count[data-work-id=124565963]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565963; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565963']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "881ab5a7262657f5cf20f35047fa5d9f" } } $('.js-work-strip[data-work-id=124565963]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565963,"title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us","translated_title":"","metadata":{"doi":"10.1180/EMU-notes.21.3","abstract":"The present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"EMU Notes in Mineralogy"},"translated_abstract":"The present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.","internal_url":"https://www.academia.edu/124565963/Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us","translated_internal_url":"","created_at":"2024-10-09T02:26:37.534-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42517398,"work_id":124565963,"tagging_user_id":10246740,"tagged_user_id":32692857,"co_author_invite_id":null,"email":"g***h@u-psud.fr","affiliation":"Paris Sud XI University","display_order":1,"name":"Guillaume Delpech","title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us"},{"id":42517399,"work_id":124565963,"tagging_user_id":10246740,"tagged_user_id":25097216,"co_author_invite_id":null,"email":"m***b@univ-st-etienne.fr","affiliation":"Universite Jean Monnet - Saint-Etienne","display_order":2,"name":"Moine Bertrand","title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us"},{"id":42517400,"work_id":124565963,"tagging_user_id":10246740,"tagged_user_id":35541998,"co_author_invite_id":null,"email":"c***n@univ-st-etienne.fr","display_order":3,"name":"Jean-yves Cottin","title":"Nature and origin of heterogeneities in the lithospheric mantle in the context of asthenospheric upwelling and mantle wedge zones: What do mantle xenoliths tell us"}],"downloadable_attachments":[{"id":118766957,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766957/thumbnails/1.jpg","file_name":"EMU_21_Ch03.pdf","download_url":"https://www.academia.edu/attachments/118766957/download_file","bulk_download_file_name":"Nature_and_origin_of_heterogeneities_in.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766957/EMU_21_Ch03-libre.pdf?1728467439=\u0026response-content-disposition=attachment%3B+filename%3DNature_and_origin_of_heterogeneities_in.pdf\u0026Expires=1743209699\u0026Signature=EQtSkMr-N6IyhmGHnp2l0r~3snIqatNRUNykztSO55DdmUCw9EzBbLbAYEcmBJeB2vbCnUAnGk4zepA-gA6w34UMOXAQGe9x9CEy32g~yNEy9LwfE1PnAW4JsKHhEcH3hIzUWZXcWNiWA73XihGo599JxWCwcRkFpmhhMj7znLb6tHxoID3o1wGNJYg3LLL-5gTjFIUkuMLblsYJP5JQ8T~QtDckLAZAYfB0N0wxI9q2Ni3FIw00kNq2dimsa0im5ke2kiAuIlFsnnz6hiuGfMmnGgrxt0VJsAgyQkfnv36KRAVaagEhNhkfGMbwHslRMPHrbHfu10tXocru49IHiw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Nature_and_origin_of_heterogeneities_in_the_lithospheric_mantle_in_the_context_of_asthenospheric_upwelling_and_mantle_wedge_zones_What_do_mantle_xenoliths_tell_us","translated_slug":"","page_count":18,"language":"en","content_type":"Work","summary":"The present contribution synthesizes the main petrographic, mineralogical and chemical features of mantle xenoliths uplifted by Phanerozoic lavas. The collections of mantle xenoliths consist predominantly of peridotites but minor pyroxenites are commonly associated. Two main petrogenetic processes are responsible for the features of mantle xenoliths: partial melting and circulation of melts/fluids and associated metasomatic and magmatic processes. Partial melting processes lead to the formation of residual pieces of upper mantle while two main types of mantle metasomatism could be recognized such as LILE enrichment, the first referring to asthenosphere upwelling settings (essentially mantle plumes, rifting zones and asthenosphere window zones) and the second to mantle wedge settings. The AUZ (asthenospheric upwelling zones) metasomatism is essentially related to the migration of more or less CO 2-rich alkaline silicate melts and associated fluids while the MWZ (mantle wedge zones) metasomatism is associated with the activity of hydrated liquids (fluids) commonly SiO 2-rich.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766957,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766957/thumbnails/1.jpg","file_name":"EMU_21_Ch03.pdf","download_url":"https://www.academia.edu/attachments/118766957/download_file","bulk_download_file_name":"Nature_and_origin_of_heterogeneities_in.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766957/EMU_21_Ch03-libre.pdf?1728467439=\u0026response-content-disposition=attachment%3B+filename%3DNature_and_origin_of_heterogeneities_in.pdf\u0026Expires=1743209699\u0026Signature=EQtSkMr-N6IyhmGHnp2l0r~3snIqatNRUNykztSO55DdmUCw9EzBbLbAYEcmBJeB2vbCnUAnGk4zepA-gA6w34UMOXAQGe9x9CEy32g~yNEy9LwfE1PnAW4JsKHhEcH3hIzUWZXcWNiWA73XihGo599JxWCwcRkFpmhhMj7znLb6tHxoID3o1wGNJYg3LLL-5gTjFIUkuMLblsYJP5JQ8T~QtDckLAZAYfB0N0wxI9q2Ni3FIw00kNq2dimsa0im5ke2kiAuIlFsnnz6hiuGfMmnGgrxt0VJsAgyQkfnv36KRAVaagEhNhkfGMbwHslRMPHrbHfu10tXocru49IHiw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":123325,"name":"Mantle Geochemistry","url":"https://www.academia.edu/Documents/in/Mantle_Geochemistry"},{"id":134398,"name":"Mantle metasomatism","url":"https://www.academia.edu/Documents/in/Mantle_metasomatism"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565963-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565930"><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/124565930/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas"><img alt="Research paper thumbnail of Slab melting boosts the mantle wedge contribution to Li-rich magmas" 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">Slab melting boosts the mantle wedge contribution to Li-rich magmas</div><div class="wp-workCard_item"><span>Scientific reports</span><span>, Jul 2, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generat...</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 lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ &amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an &amp;quot;adakite&amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (&amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.</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="124565930"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565930"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565930; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565930]").text(description); $(".js-view-count[data-work-id=124565930]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565930; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565930']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565930]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565930,"title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas","translated_title":"","metadata":{"abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u0026amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \u0026amp;quot;adakite\u0026amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u0026amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","publication_date":{"day":2,"month":7,"year":2024,"errors":{}},"publication_name":"Scientific reports"},"translated_abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u0026amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \u0026amp;quot;adakite\u0026amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u0026amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","internal_url":"https://www.academia.edu/124565930/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_internal_url":"","created_at":"2024-10-09T02:24:25.517-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u0026amp;gt; + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \u0026amp;quot;adakite\u0026amp;quot;-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u0026amp;lt; 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":54668,"name":"Peridotite","url":"https://www.academia.edu/Documents/in/Peridotite"},{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism"},{"id":122773,"name":"Subduction","url":"https://www.academia.edu/Documents/in/Subduction"},{"id":123325,"name":"Mantle Geochemistry","url":"https://www.academia.edu/Documents/in/Mantle_Geochemistry"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":426446,"name":"Mantle Wedge","url":"https://www.academia.edu/Documents/in/Mantle_Wedge"},{"id":642278,"name":"Adakite","url":"https://www.academia.edu/Documents/in/Adakite"},{"id":3057331,"name":"Transition Zone","url":"https://www.academia.edu/Documents/in/Transition_Zone"}],"urls":[{"id":45061670,"url":"https://doi.org/10.1038/s41598-024-66174-y"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565930-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565929"><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/124565929/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite"><img alt="Research paper thumbnail of A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite" 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 geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite</div><div class="wp-workCard_item"><span>Chemical geology</span><span>, Jun 1, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpen...</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">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn&amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.</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="124565929"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565929"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565929; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565929]").text(description); $(".js-view-count[data-work-id=124565929]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565929; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565929']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565929]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565929,"title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite","translated_title":"","metadata":{"abstract":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn\u0026amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","publication_date":{"day":1,"month":6,"year":2024,"errors":{}},"publication_name":"Chemical geology"},"translated_abstract":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn\u0026amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","internal_url":"https://www.academia.edu/124565929/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_internal_url":"","created_at":"2024-10-09T02:24:24.836-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn\u0026amp;#39;t need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16024,"name":"Chemical Geology","url":"https://www.academia.edu/Documents/in/Chemical_Geology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":75334,"name":"Fluid-rock interactions","url":"https://www.academia.edu/Documents/in/Fluid-rock_interactions"},{"id":521382,"name":"Gabbro","url":"https://www.academia.edu/Documents/in/Gabbro"},{"id":910472,"name":"Rodingites","url":"https://www.academia.edu/Documents/in/Rodingites"}],"urls":[{"id":45061669,"url":"https://doi.org/10.1016/j.chemgeo.2024.122237"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565929-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565926"><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/124565926/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_"><img alt="Research paper thumbnail of Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite - case study from the Kukes Massif (Mirdita ophiolite, Albania)" class="work-thumbnail" src="https://attachments.academia-assets.com/118766920/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/124565926/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_">Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite - case study from the Kukes Massif (Mirdita ophiolite, Albania)</a></div><div class="wp-workCard_item"><span>Journal of Geosciences</span><span>, May 20, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), ...</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 ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="b95aa46b2cd4f7cbbd7eec67fb24e6de" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766920,"asset_id":124565926,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766920/download_file?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="124565926"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565926"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565926; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565926]").text(description); $(".js-view-count[data-work-id=124565926]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565926; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565926']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "b95aa46b2cd4f7cbbd7eec67fb24e6de" } } $('.js-work-strip[data-work-id=124565926]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565926,"title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite - case study from the Kukes Massif (Mirdita ophiolite, Albania)","translated_title":"","metadata":{"ai_title_tag":"Melt-Rock Interaction in Kukes Massif Dunite","grobid_abstract":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","publication_date":{"day":20,"month":5,"year":2024,"errors":{}},"publication_name":"Journal of Geosciences","grobid_abstract_attachment_id":118766920},"translated_abstract":null,"internal_url":"https://www.academia.edu/124565926/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_","translated_internal_url":"","created_at":"2024-10-09T02:24:24.042-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118766920,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766920/thumbnails/1.jpg","file_name":"jgeosci_386_Mikrut.pdf","download_url":"https://www.academia.edu/attachments/118766920/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766920/jgeosci_386_Mikrut-libre.pdf?1728467477=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=Z3EnEDKUUmzu89ruA4MX1AxEb~8bm66bc8SEyo-IVi934PX7krZHkM7qy6Ykc6agDw38boMzt4FqbhJH6qW0sAse1CeIpGfX3WxmaRl8v3lozPI7fXztayNd7gczHNj3PrsEdHLq3Yuct1CUN37FTXwRcgOpVmwPKWE6uIo~67OW3urQWZ4mbR-q5sruGePVQQ16bEt9JfABHRKlsaHXwp6pFEH5AaOr9NYUK9P4KduTVkg4MnZI2zgzGJC2hqiNNoyUK86-g4SzXfMOzTlgjk0QhCbnX-tbHjP0Lr1OaRDdg1Z6pWNJWznOSjZ11huIsGVJ2NI5pWYAxGBvmZO3Bw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania_","translated_slug":"","page_count":16,"language":"en","content_type":"Work","summary":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766920,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766920/thumbnails/1.jpg","file_name":"jgeosci_386_Mikrut.pdf","download_url":"https://www.academia.edu/attachments/118766920/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766920/jgeosci_386_Mikrut-libre.pdf?1728467477=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=Z3EnEDKUUmzu89ruA4MX1AxEb~8bm66bc8SEyo-IVi934PX7krZHkM7qy6Ykc6agDw38boMzt4FqbhJH6qW0sAse1CeIpGfX3WxmaRl8v3lozPI7fXztayNd7gczHNj3PrsEdHLq3Yuct1CUN37FTXwRcgOpVmwPKWE6uIo~67OW3urQWZ4mbR-q5sruGePVQQ16bEt9JfABHRKlsaHXwp6pFEH5AaOr9NYUK9P4KduTVkg4MnZI2zgzGJC2hqiNNoyUK86-g4SzXfMOzTlgjk0QhCbnX-tbHjP0Lr1OaRDdg1Z6pWNJWznOSjZ11huIsGVJ2NI5pWYAxGBvmZO3Bw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118766919,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766919/thumbnails/1.jpg","file_name":"jgeosci_386_Mikrut.pdf","download_url":"https://www.academia.edu/attachments/118766919/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766919/jgeosci_386_Mikrut-libre.pdf?1728467587=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=XipbAWT8IJV1HCFWdE0ceaWNDhKNt10zTE1HCZYYi5lPboY0i48bZ~PvRgAKeoKyju6uilvCJUciyjGMm9leqNtySHjchdzF1rL8632FaDSAvsdiN95TWNbp6IiFLon1Jl6T8TI87ZqWCpSwQVCcejk3No5EiZRMO0IiXrNiETwir4IL8WFxXwD97C5hVBMnreu64wsY7YsVwX~hwceTw~8XfxdQxzf4pVMAb~YWn~TTkI9~b-eqnMLvUL6FqnQNStPZyHrN7Q43K1F5PO5~aFUdvZfxz~2hs-8GCrXneH8fWmt-itqxC~RvYiR6e85tJ0Di~hfZgDmZWk2s6UwI4g__\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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":70524,"name":"Geosciences","url":"https://www.academia.edu/Documents/in/Geosciences"},{"id":281808,"name":"Olivine","url":"https://www.academia.edu/Documents/in/Olivine"},{"id":330036,"name":"Ophiolite","url":"https://www.academia.edu/Documents/in/Ophiolite"},{"id":895633,"name":"Chromite","url":"https://www.academia.edu/Documents/in/Chromite"},{"id":4348154,"name":"Massif","url":"https://www.academia.edu/Documents/in/Massif"}],"urls":[{"id":45061666,"url":"http://www.jgeosci.org/content/jgeosci_386_Mikrut.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565926-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565924"><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/124565924/Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift"><img alt="Research paper thumbnail of Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift" 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">Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift</div><div class="wp-workCard_item"><span>Gondwana research</span><span>, Jul 1, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and ph...</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 use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX</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="124565924"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565924"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565924; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565924]").text(description); $(".js-view-count[data-work-id=124565924]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565924; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565924']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565924]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565924,"title":"Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift","translated_title":"","metadata":{"abstract":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","publication_date":{"day":1,"month":7,"year":2024,"errors":{}},"publication_name":"Gondwana research"},"translated_abstract":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","internal_url":"https://www.academia.edu/124565924/Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift","translated_internal_url":"","created_at":"2024-10-09T02:24:23.679-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"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":2733,"name":"Petrophysics","url":"https://www.academia.edu/Documents/in/Petrophysics"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism"},{"id":78133,"name":"Gondwana","url":"https://www.academia.edu/Documents/in/Gondwana"},{"id":205582,"name":"Xenolith","url":"https://www.academia.edu/Documents/in/Xenolith"},{"id":281808,"name":"Olivine","url":"https://www.academia.edu/Documents/in/Olivine"},{"id":668253,"name":"Lithosphere","url":"https://www.academia.edu/Documents/in/Lithosphere"},{"id":2566417,"name":"Phlogopite","url":"https://www.academia.edu/Documents/in/Phlogopite"},{"id":3057331,"name":"Transition Zone","url":"https://www.academia.edu/Documents/in/Transition_Zone"}],"urls":[{"id":45061665,"url":"https://doi.org/10.1016/j.gr.2024.03.008"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565924-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565923"><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/124565923/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central"><img alt="Research paper thumbnail of Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central" class="work-thumbnail" src="https://attachments.academia-assets.com/118766917/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/124565923/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central">Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central</a></div><div class="wp-workCard_item"><span>Bulletin de la Société géologique de France</span><span>, Feb 15, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This paper presents and discusses new geochronological and petrological data on a suite of calc-a...</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">This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365À354 Ma (including uncertainties) for igneous crystallization. These calcalkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19À30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectono-metamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="01a873698302d9400d25d238901d1eb2" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766917,"asset_id":124565923,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766917/download_file?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="124565923"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565923"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565923; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565923]").text(description); $(".js-view-count[data-work-id=124565923]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565923; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565923']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "01a873698302d9400d25d238901d1eb2" } } $('.js-work-strip[data-work-id=124565923]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565923,"title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central","translated_title":"","metadata":{"grobid_abstract":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365À354 Ma (including uncertainties) for igneous crystallization. These calcalkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19À30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectono-metamorphic units of the Western French Massif Central were piled up after 354 Ma. 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In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19À30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectono-metamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766917,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766917/thumbnails/1.jpg","file_name":"bsgf230029.pdf","download_url":"https://www.academia.edu/attachments/118766917/download_file","bulk_download_file_name":"Short_lived_active_margin_magmatism_prec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766917/bsgf230029-libre.pdf?1728467486=\u0026response-content-disposition=attachment%3B+filename%3DShort_lived_active_margin_magmatism_prec.pdf\u0026Expires=1743209699\u0026Signature=fsoCUglqfkyab3XL3ivMogdcjEm5ZuCHIuRjJ6QGO~z-LuxPuIbLMJpKJjYJl6nCxauOWr0ez47qJref7~WDjq~AX54W~7y5y7H0LsZvZQv4YkDfLQ7x3HtstAU57GEiwtmBgUCPItO-jSrUU5SPAVbdZs~gBTs6i~0QTkv1tijOTr4uf2x7Vb~hmGMmIB8QML6e-bxDjuBDkgvtfRyjIhSClPiKsko2mut6iF06bdFarE4SLW5JEaxASZTSeEWTXrGTe8-cJVWMe0EdIStq2KOfi0i4EFzxvSRnN0Et5QsMsZknu9wK2ur3o5k36KnYSdJcVcs3NV2v~HHJ8sXIKQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118766918,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766918/thumbnails/1.jpg","file_name":"bsgf230029.pdf","download_url":"https://www.academia.edu/attachments/118766918/download_file","bulk_download_file_name":"Short_lived_active_margin_magmatism_prec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766918/bsgf230029-libre.pdf?1728467487=\u0026response-content-disposition=attachment%3B+filename%3DShort_lived_active_margin_magmatism_prec.pdf\u0026Expires=1743209699\u0026Signature=NwRO43lbHyozGLiWlm3l~UhATK5nKIYg5caxa2TuHA1wC6iWXzZD2wR08HRrKWq6zT~lGN5HcrP4qjfhjtFmR-bG2CPhkjtq~Tbd22RN8knZFlVcjeGPdrLFGODLVyzFZvjmogyp8z56k8yYQR8XHghJnlOIFLCAXEPFqR~PTaU61FdnrJB20cfZq7BhI9MqtRUh7gFnB6YQmnBLdk6LVYZiMuJtZuRp6DvZmz~vJwTqq0G5WwRz2j6Tbre6B-vo6HVvJM5vu3tXq6jk9pogpNw6zIvN~~LL7qo3LB7VtrZ~pm3GR1EcSdRF6RDXSkCb9jLcyXvgl823p9zEZcz1WQ__\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":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology"},{"id":319872,"name":"Continental-arc","url":"https://www.academia.edu/Documents/in/Continental-arc"},{"id":422167,"name":"Massif Central","url":"https://www.academia.edu/Documents/in/Massif_Central"},{"id":755655,"name":"Variscan Orogeny","url":"https://www.academia.edu/Documents/in/Variscan_Orogeny"},{"id":4348154,"name":"Massif","url":"https://www.academia.edu/Documents/in/Massif"}],"urls":[{"id":45061664,"url":"https://www.bsgf.fr/articles/bsgf/pdf/forth/bsgf230029.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565923-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565922"><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/124565922/New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_E%C4%9Firdir_area_West_Anatolia_Turkey"><img alt="Research paper thumbnail of New insights into the ultrapotassic magmatism through xenoliths from the Eğirdir area, West Anatolia, Turkey" class="work-thumbnail" src="https://attachments.academia-assets.com/118766915/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/124565922/New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_E%C4%9Firdir_area_West_Anatolia_Turkey">New insights into the ultrapotassic magmatism through xenoliths from the Eğirdir area, West Anatolia, Turkey</a></div><div class="wp-workCard_item"><span>Arabian Journal of Geosciences</span><span>, Dec 7, 2023</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit ...</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">Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit in the Eğirdir lake area, belonging to the Potassic-Ultrapotassic Afyon volcanic Province, West Anatolia. They consist of kamafugite-type, feldsparbearing syenite, pyroxenite, leucitolite, some small-sized melilitolite and garnet-rich xenoliths, and a carbonatite. A new occurrence of kalsilite is described as either homogeneous acicular crystals or tabular two phases-exsolved crystals in the kamafugite-type and melilitolite xenoliths. Rock textures and compositions indicate cumulates and near-liquid composition rocks corresponding to relatively evolved magmas. All the rocks are strongly silica-undersaturated, Ca-, Mg-, and K-rich, and Al-poor. The fractional crystallization model includes clinopyroxene, apatite, phlogopite, melilite and leucite. Fe-Ti oxides and garnet may be also concerned. The P H2O during crystallization and differentiation is not more than 0.8 GPa. Major elements, trace elements, and REE patterns for xenoliths, which indicate near-liquid compositions, are typical of ultrapotassic series in a post-collisional geodynamic context, as it is the case for the Roman and Central ultrapotassic Italian provinces. The stable isotope 13 C and 18 O values of the calcio-carbonatite plot close to the primary carbonatite field, whereas the carbonates of the feldspar-bearing syenite and the peperite matrix suggest a low-T extensive contamination process. The origin of the carbonatite from kamafugite-type magmas by immiscibility or by fractional crystallization remains questionable; an origin by fractionation-melting of a metasomatized mantle source should be tested in the future.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="63b518dc0bb0dc3a8a7a25ffbbd18062" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118766915,"asset_id":124565922,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118766915/download_file?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="124565922"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565922"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565922; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565922]").text(description); $(".js-view-count[data-work-id=124565922]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565922; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565922']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "63b518dc0bb0dc3a8a7a25ffbbd18062" } } $('.js-work-strip[data-work-id=124565922]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565922,"title":"New insights into the ultrapotassic magmatism through xenoliths from the Eğirdir area, West Anatolia, Turkey","translated_title":"","metadata":{"publisher":"Springer Science+Business Media","grobid_abstract":"Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit in the Eğirdir lake area, belonging to the Potassic-Ultrapotassic Afyon volcanic Province, West Anatolia. They consist of kamafugite-type, feldsparbearing syenite, pyroxenite, leucitolite, some small-sized melilitolite and garnet-rich xenoliths, and a carbonatite. A new occurrence of kalsilite is described as either homogeneous acicular crystals or tabular two phases-exsolved crystals in the kamafugite-type and melilitolite xenoliths. Rock textures and compositions indicate cumulates and near-liquid composition rocks corresponding to relatively evolved magmas. All the rocks are strongly silica-undersaturated, Ca-, Mg-, and K-rich, and Al-poor. The fractional crystallization model includes clinopyroxene, apatite, phlogopite, melilite and leucite. Fe-Ti oxides and garnet may be also concerned. The P H2O during crystallization and differentiation is not more than 0.8 GPa. Major elements, trace elements, and REE patterns for xenoliths, which indicate near-liquid compositions, are typical of ultrapotassic series in a post-collisional geodynamic context, as it is the case for the Roman and Central ultrapotassic Italian provinces. The stable isotope 13 C and 18 O values of the calcio-carbonatite plot close to the primary carbonatite field, whereas the carbonates of the feldspar-bearing syenite and the peperite matrix suggest a low-T extensive contamination process. The origin of the carbonatite from kamafugite-type magmas by immiscibility or by fractional crystallization remains questionable; an origin by fractionation-melting of a metasomatized mantle source should be tested in the future.","publication_date":{"day":7,"month":12,"year":2023,"errors":{}},"publication_name":"Arabian Journal of Geosciences","grobid_abstract_attachment_id":118766915},"translated_abstract":null,"internal_url":"https://www.academia.edu/124565922/New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_E%C4%9Firdir_area_West_Anatolia_Turkey","translated_internal_url":"","created_at":"2024-10-09T02:24:23.036-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118766915,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766915/thumbnails/1.jpg","file_name":"document.pdf","download_url":"https://www.academia.edu/attachments/118766915/download_file","bulk_download_file_name":"New_insights_into_the_ultrapotassic_magm.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766915/document-libre.pdf?1728467458=\u0026response-content-disposition=attachment%3B+filename%3DNew_insights_into_the_ultrapotassic_magm.pdf\u0026Expires=1743209699\u0026Signature=UOzwPplcKY4zR-9WTIkFGX4hgFcmM~STnJWFKe7Xr2TPDRC6hngRFWG9AnUbc-cwWPv3GRBKtJN4ROVUBF3TfFGYWgzZ~bxUSQHqjV8lTQqPTuMHZ7eZfi-GlNITQ8JB9BXKgu1okCVvSrJijswcLv8DWMFp7X2Yl~waQHBvIC6XfWjRBggvoHOWsaOf01Ckd-huumXQ68EaLwGOJ1M7pbqESIzPe32wm3RtzCLZXjCMn0vNq4cqqC2X2vt1VUesQDYqAKzvdaidiu2UhNBP1b1Vzws1bVcwqC8RgAht3x2DV2cXJuSGqb1mYVJUMG4cCprRVPHpmCnt1~WBrd0ZDQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"New_insights_into_the_ultrapotassic_magmatism_through_xenoliths_from_the_Eğirdir_area_West_Anatolia_Turkey","translated_slug":"","page_count":27,"language":"en","content_type":"Work","summary":"Plutonic xenoliths have been found within a pipe and a related phreatomagmatic leucitite deposit in the Eğirdir lake area, belonging to the Potassic-Ultrapotassic Afyon volcanic Province, West Anatolia. They consist of kamafugite-type, feldsparbearing syenite, pyroxenite, leucitolite, some small-sized melilitolite and garnet-rich xenoliths, and a carbonatite. A new occurrence of kalsilite is described as either homogeneous acicular crystals or tabular two phases-exsolved crystals in the kamafugite-type and melilitolite xenoliths. Rock textures and compositions indicate cumulates and near-liquid composition rocks corresponding to relatively evolved magmas. All the rocks are strongly silica-undersaturated, Ca-, Mg-, and K-rich, and Al-poor. The fractional crystallization model includes clinopyroxene, apatite, phlogopite, melilite and leucite. Fe-Ti oxides and garnet may be also concerned. The P H2O during crystallization and differentiation is not more than 0.8 GPa. Major elements, trace elements, and REE patterns for xenoliths, which indicate near-liquid compositions, are typical of ultrapotassic series in a post-collisional geodynamic context, as it is the case for the Roman and Central ultrapotassic Italian provinces. The stable isotope 13 C and 18 O values of the calcio-carbonatite plot close to the primary carbonatite field, whereas the carbonates of the feldspar-bearing syenite and the peperite matrix suggest a low-T extensive contamination process. The origin of the carbonatite from kamafugite-type magmas by immiscibility or by fractional crystallization remains questionable; an origin by fractionation-melting of a metasomatized mantle source should be tested in the future.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":118766915,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766915/thumbnails/1.jpg","file_name":"document.pdf","download_url":"https://www.academia.edu/attachments/118766915/download_file","bulk_download_file_name":"New_insights_into_the_ultrapotassic_magm.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766915/document-libre.pdf?1728467458=\u0026response-content-disposition=attachment%3B+filename%3DNew_insights_into_the_ultrapotassic_magm.pdf\u0026Expires=1743209699\u0026Signature=UOzwPplcKY4zR-9WTIkFGX4hgFcmM~STnJWFKe7Xr2TPDRC6hngRFWG9AnUbc-cwWPv3GRBKtJN4ROVUBF3TfFGYWgzZ~bxUSQHqjV8lTQqPTuMHZ7eZfi-GlNITQ8JB9BXKgu1okCVvSrJijswcLv8DWMFp7X2Yl~waQHBvIC6XfWjRBggvoHOWsaOf01Ckd-huumXQ68EaLwGOJ1M7pbqESIzPe32wm3RtzCLZXjCMn0vNq4cqqC2X2vt1VUesQDYqAKzvdaidiu2UhNBP1b1Vzws1bVcwqC8RgAht3x2DV2cXJuSGqb1mYVJUMG4cCprRVPHpmCnt1~WBrd0ZDQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118766916,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118766916/thumbnails/1.jpg","file_name":"document.pdf","download_url":"https://www.academia.edu/attachments/118766916/download_file","bulk_download_file_name":"New_insights_into_the_ultrapotassic_magm.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118766916/document-libre.pdf?1728467459=\u0026response-content-disposition=attachment%3B+filename%3DNew_insights_into_the_ultrapotassic_magm.pdf\u0026Expires=1743209699\u0026Signature=OHs3BabI~R9nZj3VrsyiD3dR2iVlcCLAMBe9uB9W5Blvvkpt6~G2kGEhdXXkG2z2gPT5V0f5gkmcN5xXGY3HydBo1hmZEG~66W2zooFsIjy1pVlxAk5Utsb8~kaURdd1VupaqeeljAI3yVdeFnoyYtuck9kCFANOb~3jQ5wUXsZZSkW83Fs3snQe~dK4MBPSg9Cg~UZR-5Yudq6fEzqDUflNrHyy4cZwl2RGpRxwPGLtBVi6qFOw6iw5lqYqGUOkRH4QPWuYOhe0gqZSdYkK3NKRVtzImUNUFCj2jouxYdLXlFlhFzRM7vHNE0~U0WYcrHmugakFRJkEq7mBtNpQ1w__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry"},{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism"},{"id":66471,"name":"Mafic Alkaline Igneous Rocks","url":"https://www.academia.edu/Documents/in/Mafic_Alkaline_Igneous_Rocks"},{"id":108863,"name":"Volcano","url":"https://www.academia.edu/Documents/in/Volcano"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"},{"id":197588,"name":"Kimberlite","url":"https://www.academia.edu/Documents/in/Kimberlite"},{"id":205576,"name":"Basalt","url":"https://www.academia.edu/Documents/in/Basalt"},{"id":205582,"name":"Xenolith","url":"https://www.academia.edu/Documents/in/Xenolith"},{"id":403641,"name":"Spinel","url":"https://www.academia.edu/Documents/in/Spinel"},{"id":568585,"name":"Trachyte","url":"https://www.academia.edu/Documents/in/Trachyte"},{"id":688910,"name":"Volcanic Rock","url":"https://www.academia.edu/Documents/in/Volcanic_Rock"},{"id":1168540,"name":"Eology","url":"https://www.academia.edu/Documents/in/Eology"},{"id":1186734,"name":"Allanite","url":"https://www.academia.edu/Documents/in/Allanite"},{"id":1464622,"name":"Carbonatite","url":"https://www.academia.edu/Documents/in/Carbonatite"},{"id":1590367,"name":"Monazite","url":"https://www.academia.edu/Documents/in/Monazite"},{"id":2566417,"name":"Phlogopite","url":"https://www.academia.edu/Documents/in/Phlogopite"}],"urls":[{"id":45061663,"url":"https://hal.science/hal-04337266/document"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565922-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="124565921"><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/124565921/Use_of_porphyry_indicator_zircons_PIZs_in_the_sedimentary_record_as_an_exploration_tool_for_covered_porphyry_copper_deposits_in_the_Atacama_Desert_Chile"><img alt="Research paper thumbnail of Use of porphyry indicator zircons (PIZs) in the sedimentary record as an exploration tool for covered porphyry copper deposits in the Atacama Desert, Chile" 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">Use of porphyry indicator zircons (PIZs) in the sedimentary record as an exploration tool for covered porphyry copper deposits in the Atacama Desert, Chile</div><div class="wp-workCard_item"><span>Journal of Geochemical Exploration</span><span>, Dec 31, 2023</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This work explores the potential of geochemical and petrographic characteristics of detrital zirc...</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">This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf &amp;gt;8,750 (ppm), Ce/Nd &amp;gt;1, Eu/Eu* &amp;gt;0.4, 10,000×(Eu/Eu*)/Y &amp;gt;1, (Ce/Nd)/Y &amp;gt;0.01, Dy/Yb &amp;lt;0.3 and 0.1 &amp;lt; Th/U &amp;lt; 1. These zircons also have Ti &amp;lt;9 ppm and Ce/Ce* &amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.</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="124565921"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="124565921"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 124565921; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=124565921]").text(description); $(".js-view-count[data-work-id=124565921]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 124565921; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='124565921']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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" } } $('.js-work-strip[data-work-id=124565921]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":124565921,"title":"Use of porphyry indicator zircons (PIZs) in the sedimentary record as an exploration tool for covered porphyry copper deposits in the Atacama Desert, Chile","translated_title":"","metadata":{"abstract":"This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf \u0026amp;gt;8,750 (ppm), Ce/Nd \u0026amp;gt;1, Eu/Eu* \u0026amp;gt;0.4, 10,000×(Eu/Eu*)/Y \u0026amp;gt;1, (Ce/Nd)/Y \u0026amp;gt;0.01, Dy/Yb \u0026amp;lt;0.3 and 0.1 \u0026amp;lt; Th/U \u0026amp;lt; 1. These zircons also have Ti \u0026amp;lt;9 ppm and Ce/Ce* \u0026amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.","publisher":"Elsevier BV","publication_date":{"day":31,"month":12,"year":2023,"errors":{}},"publication_name":"Journal of Geochemical Exploration"},"translated_abstract":"This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf \u0026amp;gt;8,750 (ppm), Ce/Nd \u0026amp;gt;1, Eu/Eu* \u0026amp;gt;0.4, 10,000×(Eu/Eu*)/Y \u0026amp;gt;1, (Ce/Nd)/Y \u0026amp;gt;0.01, Dy/Yb \u0026amp;lt;0.3 and 0.1 \u0026amp;lt; Th/U \u0026amp;lt; 1. These zircons also have Ti \u0026amp;lt;9 ppm and Ce/Ce* \u0026amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.","internal_url":"https://www.academia.edu/124565921/Use_of_porphyry_indicator_zircons_PIZs_in_the_sedimentary_record_as_an_exploration_tool_for_covered_porphyry_copper_deposits_in_the_Atacama_Desert_Chile","translated_internal_url":"","created_at":"2024-10-09T02:24:22.770-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Use_of_porphyry_indicator_zircons_PIZs_in_the_sedimentary_record_as_an_exploration_tool_for_covered_porphyry_copper_deposits_in_the_Atacama_Desert_Chile","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"This work explores the potential of geochemical and petrographic characteristics of detrital zircons coming from the sedimentary record of the Centinela District in Northern Chile to identify the presence of buried porphyry copper deposits under a transported gravel cover. The sampled sedimentary section was recovered from the pit of the exotic copper deposit of El Tesoro, located approximately 2 and 4 km west of the Esperanza and Mirador porphyries, respectively. The sedimentary cover comprises four units, Tesoro II, Tesoro III, Arrieros and Recent gravels, deposited since the late Cenozoic in an arid continental environment dominated by alluvial fans. Except for the Tesoro III gravels, all other units contain exotic-Cu mineralisation. In order to interpret the geochemical footprint of the investigated zircons, the Porphyry Indicator Zircon (PIZ) concept (Pizarro et al., 2020) is used. A PIZ need to comply with each of the following geochemical values: Hf \u0026amp;gt;8,750 (ppm), Ce/Nd \u0026amp;gt;1, Eu/Eu* \u0026amp;gt;0.4, 10,000×(Eu/Eu*)/Y \u0026amp;gt;1, (Ce/Nd)/Y \u0026amp;gt;0.01, Dy/Yb \u0026amp;lt;0.3 and 0.1 \u0026amp;lt; Th/U \u0026amp;lt; 1. These zircons also have Ti \u0026amp;lt;9 ppm and Ce/Ce* \u0026amp;lt;100 and usually show euhedral morphologies characterised by prismatic forms of type {110}. The geochemical andpetrographic characteristics of the PIZs collected in the gravels are similar to zircons from the nearby Mirador and Esperanza porphyries. The highest PIZ concentration coincides with the gravel horizons with exotic-Cu mineralisation. Therefore, the PIZs found in the sedimentary record are a potential tracer of adjacent copper porphyries and represent a promising exploration tool for this type of hidden ore deposits in challenging sediment-covered areas.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[],"research_interests":[{"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":417,"name":"Paleontology","url":"https://www.academia.edu/Documents/in/Paleontology"},{"id":70416,"name":"Mineral exploration","url":"https://www.academia.edu/Documents/in/Mineral_exploration"},{"id":74607,"name":"Quartz","url":"https://www.academia.edu/Documents/in/Quartz"},{"id":82911,"name":"fluid Inclusions","url":"https://www.academia.edu/Documents/in/fluid_Inclusions"},{"id":103767,"name":"Petrography","url":"https://www.academia.edu/Documents/in/Petrography"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":282633,"name":"Geochemical exploration","url":"https://www.academia.edu/Documents/in/Geochemical_exploration"},{"id":1146625,"name":"Porphyry Copper Deposit","url":"https://www.academia.edu/Documents/in/Porphyry_Copper_Deposit"},{"id":1168540,"name":"Eology","url":"https://www.academia.edu/Documents/in/Eology"}],"urls":[{"id":45061662,"url":"https://doi.org/10.1016/j.gexplo.2023.107351"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-124565921-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="121796661"><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/121796661/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas"><img alt="Research paper thumbnail of Slab melting boosts the mantle wedge contribution to Li-rich magmas" class="work-thumbnail" src="https://attachments.academia-assets.com/116593888/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/121796661/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas">Slab melting boosts the mantle wedge contribution to Li-rich magmas</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/ErwinSchettino">Erwin Schettino</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Scientific Reports</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generat...</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 lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ > + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an "adakite"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (< 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="04a765de19929f52c678e8e65cbe678a" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":116593888,"asset_id":121796661,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/116593888/download_file?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="121796661"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="121796661"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 121796661; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=121796661]").text(description); $(".js-view-count[data-work-id=121796661]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 121796661; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='121796661']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "04a765de19929f52c678e8e65cbe678a" } } $('.js-work-strip[data-work-id=121796661]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":121796661,"title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas","translated_title":"","metadata":{"doi":"10.1038/s41598-024-66174-y","abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u003e + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \"adakite\"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u003c 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","publication_name":"Scientific Reports"},"translated_abstract":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. Here, we look from the mantle source perspective at the geological processes controlling the Li mobility in convergent margins, by characterizing a set of sub-arc mantle xenoliths from the southern Andes (Coyhaique, western Patagonia). The mineral trace element signatures and oxygen fugacity estimates (FMQ \u003e + 3) in some of these peridotite xenoliths record the interaction with arc magmas enriched in fluid-mobile elements originally scavenged by slab dehydration. This subduction-related metasomatism was poorly effective on enhancing the Li inventory of the sub-arc lithospheric mantle, underpinning the inefficiency of slab-derived fluids on mobilizing Li through the mantle wedge. However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \"adakite\"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u003c 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","internal_url":"https://www.academia.edu/121796661/Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_internal_url":"","created_at":"2024-07-05T04:57:50.421-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":42007492,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":319160819,"co_author_invite_id":8190613,"email":"e***8@gmail.com","display_order":-3,"name":"Erwin Schettino","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007493,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":50570743,"co_author_invite_id":null,"email":"c***o@iact.ugr-csic.es","display_order":-2,"name":"Claudio Marchesi","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007494,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":9883919,"co_author_invite_id":null,"email":"j***z@mq.edu.au","display_order":-1,"name":"Jose Gonzalez-Jimenez","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007495,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":28395431,"co_author_invite_id":null,"email":"r***c@gmail.com","affiliation":"CSIC (Consejo Superior de Investigaciones Científicas-Spanish National Research Council)","display_order":1,"name":"Romain Tilhac","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007496,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":112580305,"co_author_invite_id":null,"email":"a***e@gmail.com","display_order":2,"name":"Alexandre Corgne","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"},{"id":42007497,"work_id":121796661,"tagging_user_id":10246740,"tagged_user_id":27868342,"co_author_invite_id":null,"email":"m***d@gmail.com","affiliation":"Universidad Austral de Chile","display_order":3,"name":"Manuel Schilling","title":"Slab melting boosts the mantle wedge contribution to Li-rich magmas"}],"downloadable_attachments":[{"id":116593888,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116593888/thumbnails/1.jpg","file_name":"SciRep_2024.pdf","download_url":"https://www.academia.edu/attachments/116593888/download_file","bulk_download_file_name":"Slab_melting_boosts_the_mantle_wedge_con.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116593888/SciRep_2024-libre.pdf?1720184002=\u0026response-content-disposition=attachment%3B+filename%3DSlab_melting_boosts_the_mantle_wedge_con.pdf\u0026Expires=1743209699\u0026Signature=euxvAd-8Q5zwJZkibKrl0BEaI6ACg-yufmbfOvAhs0UKuFMdIa3mpNA7R5FKJygYfIg5O34po6Gilvtpgb1gia2LGJJIrANO2dj1qTz3w19rFmWinO1ukiUrIxQlgsvA0RYcN~KOhsxB0w~l8~oKYR25YyWh4CElu0QowxbsAoKnIHHziSzekfKquXVHnw4Xn0ho7O~Kw0fDEL2zZG5qsoe1DISTnjboZeiTHOILzm492k1AUj4RWaUNFRhdRgkpu2fttRfjZkK8Hap31uG6iDHOReAYGSPEprRsDofAFIW5p9f3ViFaRE-uUsvhptVyJZrW8Fvx9wTstSUijLjKJQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Slab_melting_boosts_the_mantle_wedge_contribution_to_Li_rich_magmas","translated_slug":"","page_count":14,"language":"en","content_type":"Work","summary":"The lithium cycling in the supra-subduction mantle wedge is crucial for understanding the generation of Li-rich magmas that may potentially source ore deposition in continental arcs. 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However, major and trace element compositions of mantle minerals in other xenoliths also record transient thermal and chemical anomalies associated with the percolation of slab window-related magmas, which exhibit an \"adakite\"-type geochemical fingerprint inherited by slab-derived melts produced during ridge subduction and slab window opening event. As these melts percolated through the shallow (7.2-16.8 kbar) and hot (952-1054 °C) lithospheric mantle wedge, they promoted the crystallization of metasomatic clinopyroxene having exceptionally high Li abundances (6-15 ppm). Numerical modeling shows that low degrees (\u003c 10%) of partial melting of this Li-rich and fertile sub-arc lithospheric mantle generates primitive melts having twofold Li enrichment (~13 ppm) compared with average subduction-zone basalts. Prolonged fractional crystallization of these melts produces extremely Li-enriched silicic rocks, which may stoke the Li inventory of mineralizing fluids in the shallow crust.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":116593888,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116593888/thumbnails/1.jpg","file_name":"SciRep_2024.pdf","download_url":"https://www.academia.edu/attachments/116593888/download_file","bulk_download_file_name":"Slab_melting_boosts_the_mantle_wedge_con.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116593888/SciRep_2024-libre.pdf?1720184002=\u0026response-content-disposition=attachment%3B+filename%3DSlab_melting_boosts_the_mantle_wedge_con.pdf\u0026Expires=1743209699\u0026Signature=euxvAd-8Q5zwJZkibKrl0BEaI6ACg-yufmbfOvAhs0UKuFMdIa3mpNA7R5FKJygYfIg5O34po6Gilvtpgb1gia2LGJJIrANO2dj1qTz3w19rFmWinO1ukiUrIxQlgsvA0RYcN~KOhsxB0w~l8~oKYR25YyWh4CElu0QowxbsAoKnIHHziSzekfKquXVHnw4Xn0ho7O~Kw0fDEL2zZG5qsoe1DISTnjboZeiTHOILzm492k1AUj4RWaUNFRhdRgkpu2fttRfjZkK8Hap31uG6iDHOReAYGSPEprRsDofAFIW5p9f3ViFaRE-uUsvhptVyJZrW8Fvx9wTstSUijLjKJQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"},{"id":123325,"name":"Mantle Geochemistry","url":"https://www.academia.edu/Documents/in/Mantle_Geochemistry"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-121796661-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="121533209"><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/121533209/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite"><img alt="Research paper thumbnail of A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite" class="work-thumbnail" src="https://attachments.academia-assets.com/116422208/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/121533209/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite">A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite</a></div><div class="wp-workCard_item"><span>Chemical Geology</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpen...</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">Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.</span></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-121533209-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-121533209-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361218/figure-3-calculated-mineral-composition-depending-on-fluid"><img alt="Figure 3 Calculated mineral composition depending on fluid amount from the reaction of gabbro with the Seyfried’s solution (model E) at 300°C. Ab: albite, Adr: andradite, Ann: annite, Clc: clinochlore, Di: diopside, Hd: hedenbergite, Mtc: monticellite, Phl: Na-phlogopite, Prh: prehnite, Ves: vesuvianite, Wo: wollastonite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361210/figure-2-modal-composition-predicted-from-alteration-of"><img alt="Figure 2 Modal composition predicted from alteration of gabbro (1 kg) at 300°C depending on fluid amount and fluid composition: a) low fluid amount (10 kg) b) high fluid amount (1000 kg). Capital letters denote different fluid compositions as presented in Table 1. Modal proportions of minerals were calculated from molal amounts based on average density for each mineral published at www.webmineral.com (densities are available in Table SX). Ab: albite, Adr: andradite, Anh: anhydrite, Clc: clinochlore, Cld: chloritoid, Czo: clinozoisite, Di: diopside, Dph: daphnite, Ep: epidote, Hd: hedenbergite, Hem: hematite, MHSH: magnesium-hydroxide-sulphate-hydrate, Mtc: monticellite, Prh: prehnite, Qz: quartz, Stp: stilpnomelane, Tlc: talc, Tr: tremolite, Ves: vesuvianite, Wo: wollastonite, Wrk: wairakite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361197/figure-1-geochemical-model-for-the-transformation-of-gabbro"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361227/figure-4-element-amounts-in-the-modeled-solid-phase"><img alt="Figure 4 Element amounts in the modeled solid phase depending on fluid amount from the reaction of 1 kg of gabbro with the Seyfried’s solution (model E) at 300°C. Values were manually quantified from mineral amounts (and their respective compositions) calculated in the model. Note the progressive and significant Ca-enrichment with increasing fluid amount in the system. Ca-enrichment is also responsible for the increase of total mass of the solid phase. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361240/figure-5-graphical-representation-of-the-recalculated-whole"><img alt="Figure 5 Graphical representation of the recalculated whole rock composition (Table 2) of the altered rock resulting from the interaction of 1 kg of gabbro with variable amount of the Seyfried’s solution (model E) at 300°C. Note the decreasing SiOz and increasing CaO demonstrating the most typical changes in whole-rock chemistry during the rodingitization. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361253/figure-6-influence-of-changes-in-fluid-composition-on-the"><img alt="Figure 6 Influence of changes in fluid composition on the predicted mineralogy explored by one-factor-at-a-time method applied on experimental serpentinization fluid from Klein et al. (2015) (model D), 300°C, fluid amount 1000 kg. a) variable Ca concentration. b) variable Mg concentration. c) variable Si concentration. d) variable initial pH. Ab: albite, Adr: andradite, Ame: amesite, Br: brucite, Clc: clinochlore, Czo: clinozoisite, Di: diopside, Dph: daphnite, Ep: epidote, Hd: hedenbergite, Mtc: monticellite, Prh: prehnite, Qz: quartz, Rnk: rankinite, Ves: vesuvianite, Wo: wollastonite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_006.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361260/figure-7-influence-of-changes-in-fluid-composition-on-the"><img alt="Figure 7 Influence of changes in fluid composition on the predicted mineralogy explored by one-factor-at-a-time method applied on experimental serpentinization fluid from Seyfried et al. (2007) (model E), 300°C, fluid amount 1000 kg. a) variable Ca concentration. b) variable Mg concentration. d) variable initial pH. Ab: albite, Adr. andradite, Atg: antigorite, Br: brucite, Clc: clinochlore, Di: diopside, Hd: hedenbergite, Lrn: larnite, Mtc: monticellite, Phl: Na-phlogopite, Rnk: rankinite, Tro: troilite, Ves: vesuvianite, Wo: wollastonite. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_007.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361268/figure-8-diagram-of-si-ca-molal-ratio-in-the-solid-phase-vs"><img alt="Figure 8 Diagram of Si/Ca (molal ratio) in the solid phase vs fluid amount in the system. It compares the calculated chemical composition (brown line, model E, section 3.2) with natural samples. Blue area represents gabbro compositions (n = 201) from a present seafloor, oxide-rich samples excluded (MacLeod et al., 2017). Green area represents vesuvianite-bearing rodingite compositions (n = 49) from the literature (Li et al., 2004, 2007, 2017; Kobayashi and Kaneda, 2010; Koutsovitis et al., 2013; Fukuyama et al., 2014; Dai et al., 2016; Salvioli-Mariani et Our calculations consistently show that increasing fluid amount results in an increasing quantity of vesuvianite (Figs. 2 and 3). This finding is also in good agreement with the thermodynamic model presented by Palandri and Reed (2004), where the interaction of a pyroxene-rich gabbro with a serpentinization fluid predicts vesuvianite only at a water-rock ratio above 200. Such high water-rock ratio can be hard to imagine considering the constraints from O isotopes studies suggesting a relatively low fluid-rock ratio (< 10) during serpentinization (Rouméjon et al., 2015; Zhao et al., 2023). However, these studies often focus on only partially serpentinized ultramafic rocks very probably forming at the beginning of the alteration (at lower fluid-rock ratio). Rodingites occur almost exclusively in completely serpentinized rocks (Katoh and Niida, 1983), which suggests a higher fluid amount participating in the process (Rouméjon et al., 2015, 2018). A high fluid amount can be achieved in nature either by a small to moderate fluid influx continuing for a long time, or by a very high fluid volume in contact with the rock during a short time. We assume the former option more plausible since it allows to advance the mineral reactions to the chemical equilibrium more easily. In any case, we conclude that vesuvianite formation requires an open system with a significant input of a fresh hydrothermal fluid. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/figure_008.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361274/table-1-adjusted-to-charge-balance-the-solution-fluid"><img alt="* adjusted to charge balance the solution Table 1 Fluid compositions investigated in the models. A) pure water. B) average seawater (Nordstrom et al., 1979). C) evolved seawater composition measured ina vent at Logatchev (Charlou et al, 2002). D) experimental serpentinization fluid (Klein et al., 2015). E) experimental serpentinization fluid (Seyfried et al.,2007). Element concentrations are in mmol/kg. " class="figure-slide-image" src="https://figures.academia-assets.com/116422208/table_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/50361280/table-2-recalculated-whole-rock-composition-in-wt-normalized"><img alt="Table 2 Recalculated whole rock composition (in wt.%, normalized on 100 %) of the altered rock resulting fron the interaction of 1 kg of gabbro with variable amount of the Seyfried’s solution (model E) at 300°C. Values wer manually quantified from mineral amounts (and their respective compositions) calculated in the model. Thes values are shown in a graphical form in figure 5. 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This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Chemical Geology"},"translated_abstract":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","internal_url":"https://www.academia.edu/121533209/A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_internal_url":"","created_at":"2024-06-26T07:51:35.032-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":41965331,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":291703187,"co_author_invite_id":null,"email":"j***k@umb.sk","display_order":-3,"name":"Juraj Butek","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"},{"id":41965332,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":97759662,"co_author_invite_id":null,"email":"f***n@wanadoo.fr","affiliation":"Université Toulouse II Jean Jaurès","display_order":-2,"name":"Sébastien Fabre","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"},{"id":41965333,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":7611257,"email":"s***e@get.omp.eu","display_order":-1,"name":"Stephanie Duchene","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"},{"id":41965334,"work_id":121533209,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":7945934,"email":"j***k@umb.sk","display_order":1,"name":"Jan Spisiak","title":"A geochemical model for the transformation of gabbro into vesuvianite-bearing rodingite"}],"downloadable_attachments":[{"id":116422208,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116422208/thumbnails/1.jpg","file_name":"Chem_Geol_2024.pdf","download_url":"https://www.academia.edu/attachments/116422208/download_file","bulk_download_file_name":"A_geochemical_model_for_the_transformati.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116422208/Chem_Geol_2024-libre.pdf?1719566012=\u0026response-content-disposition=attachment%3B+filename%3DA_geochemical_model_for_the_transformati.pdf\u0026Expires=1743209699\u0026Signature=gaCoLaPulMCea0zGc8ST13gKF0-z543EWMI1GX9S8Sc4800JDwdYm43rak88~3YB-M2hhAe0N7WLX~E8HOtj~azd3Q31v847X0LmIy4zB86i9LSqwa6xQ94~5rYFNtGCj4MLqCLDviX1iTTeAcYg4HpOeWl2Qz4Hjzf8a~3junQBehbT3C714M08-J9lAsfEWnFx3l5BDRTFBJr8kxPaROJZUelMOb4bT41srG4rt2BHMzqG5PPiQQHentisy~kJP2pbDcyn5yFAvSfsvv43ksjAA8bfIA0pNQdKfDgIaQAdr56Ccv1ELiagCHwBQEaGC5wIb0V-VLlznSAUrMDW3g__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"A_geochemical_model_for_the_transformation_of_gabbro_into_vesuvianite_bearing_rodingite","translated_slug":"","page_count":25,"language":"en","content_type":"Work","summary":"Rodingite is a Ca-rich and Si-poor metasomatic rock commonly occurring in association with serpentinites. This rock is characterized by specific mineral assemblages consisting of hydrated garnet, diopside, vesuvianite, epidote-zoisite, chlorite, or prehnite. However, natural rodingites are significantly heterogeneous in mineral composition and vesuvianite occurs only in some extensively rodingitized rocks. Major factors controlling the mineral diversity as well as details on fluid-rock interactions leading to the evolution of mineral and chemical composition during rodingitization have not yet been fully constrained. In this work, we use PHREEQC software to present a geochemical model for the transformation of a mafic rock into vesuvianite-bearing rodingite at a temperature of 300 °C. Through these simulations, we investigate the effect of fluid composition and progress of the metasomatic process on rodingite formation. Our results show that rodingitization requires an open system with a high input of hydrothermal fluid. Additionally, a decrease in the Si/Ca ratio in the metasomatized rock is correlated to an increase in the volume of incoming fluid. Whole rock chemical and mineral composition in natural rodingites are well reproduced by the model. Furthermore, the diversity of mineral parageneses results mainly from different degrees of transformation and only to a lesser extent to the chemical composition of hydrothermal fluid or protolith. The hydrothermal fluid doesn't need to be especially rich in calcium to transform a mafic rock into rodingite, but it must be low in magnesium, silicon, and have a high pH, which is naturally controlled by serpentinization of surrounding ultramafic rocks.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":116422208,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116422208/thumbnails/1.jpg","file_name":"Chem_Geol_2024.pdf","download_url":"https://www.academia.edu/attachments/116422208/download_file","bulk_download_file_name":"A_geochemical_model_for_the_transformati.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116422208/Chem_Geol_2024-libre.pdf?1719566012=\u0026response-content-disposition=attachment%3B+filename%3DA_geochemical_model_for_the_transformati.pdf\u0026Expires=1743209699\u0026Signature=gaCoLaPulMCea0zGc8ST13gKF0-z543EWMI1GX9S8Sc4800JDwdYm43rak88~3YB-M2hhAe0N7WLX~E8HOtj~azd3Q31v847X0LmIy4zB86i9LSqwa6xQ94~5rYFNtGCj4MLqCLDviX1iTTeAcYg4HpOeWl2Qz4Hjzf8a~3junQBehbT3C714M08-J9lAsfEWnFx3l5BDRTFBJr8kxPaROJZUelMOb4bT41srG4rt2BHMzqG5PPiQQHentisy~kJP2pbDcyn5yFAvSfsvv43ksjAA8bfIA0pNQdKfDgIaQAdr56Ccv1ELiagCHwBQEaGC5wIb0V-VLlznSAUrMDW3g__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":75334,"name":"Fluid-rock interactions","url":"https://www.academia.edu/Documents/in/Fluid-rock_interactions"},{"id":910472,"name":"Rodingites","url":"https://www.academia.edu/Documents/in/Rodingites"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (true) { Aedu.setUpFigureCarousel('profile-work-121533209-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="119814581"><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/119814581/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania"><img alt="Research paper thumbnail of Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania" class="work-thumbnail" src="https://attachments.academia-assets.com/115151005/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/119814581/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania">Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania</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/MikrutJ">Jakub Mikrut</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div><div class="wp-workCard_item"><span>Journal of Geosciences</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), ...</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 ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2fa394de18fb00c5e719e05379ea22d0" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":115151005,"asset_id":119814581,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/115151005/download_file?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="119814581"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="119814581"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 119814581; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=119814581]").text(description); $(".js-view-count[data-work-id=119814581]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 119814581; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='119814581']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "2fa394de18fb00c5e719e05379ea22d0" } } $('.js-work-strip[data-work-id=119814581]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":119814581,"title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania","translated_title":"","metadata":{"doi":"10.3190/jgeosci.386","abstract":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Journal of Geosciences"},"translated_abstract":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","internal_url":"https://www.academia.edu/119814581/Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania","translated_internal_url":"","created_at":"2024-05-22T06:23:35.947-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":41731140,"work_id":119814581,"tagging_user_id":10246740,"tagged_user_id":315624277,"co_author_invite_id":8154103,"email":"j***t@uwr.edu.pl","display_order":-2,"name":"Jakub Mikrut","title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania"},{"id":41731141,"work_id":119814581,"tagging_user_id":10246740,"tagged_user_id":32572477,"co_author_invite_id":null,"email":"m***k@ing.uni.wroc.pl","display_order":-1,"name":"Magdalena Matusiak-małek","title":"Melt-rock interaction as a factor controlling evolution of chromite and olivine in dunite -case study from the Kukes Massif (Mirdita ophiolite, Albania"}],"downloadable_attachments":[{"id":115151005,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115151005/thumbnails/1.jpg","file_name":"JGeosciences_2024.pdf","download_url":"https://www.academia.edu/attachments/115151005/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115151005/JGeosciences_2024-libre.pdf?1716386647=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=f3gqN66AkzsIOzlGAj1Pl4OKKs3wMhFdFTbuEp3gQk91rQzBJW0Gxzjo7oTPFGVdtpzO-DuXBQ2Yrw7vdhcoh8JYgDEUAYLM3S7eLM2iiSIchCbO7c9G396-3cywn4xAkVOk1NHwpxpEx7nEx36ZHIrw7e6z7NCDBYOZuJ0fRfZYPNyvyn0h9ZyzDYnskR61gjkFd4dCqTrfqM4JurmvKYdOI1GEg2196wLvzHc6uUj4Ma0KujWCc1q6YMs-KgQhV6rT3T8uG~Sj~R~dCBpOLByHnReD9hJX4jzPLyYMNMqXoUt2Ii4mcqYtg3Vbfc7DFZMiKH3dIxCrbhhcPo3btw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Melt_rock_interaction_as_a_factor_controlling_evolution_of_chromite_and_olivine_in_dunite_case_study_from_the_Kukes_Massif_Mirdita_ophiolite_Albania","translated_slug":"","page_count":16,"language":"en","content_type":"Work","summary":"The ultramafic Kukes Massif is located in the eastern part of the Mirdita ophiolite (N Albania), which is recognised as representing Supra-Subduction lithosphere. It comprises a thick (0.8-2.5 km) dunite zone containing abundant occurrences of chromite ores and is cut by orthopyroxenitic and clinopyroxenitic veins. In this paper we focus on the genesis and evolution of olivine and chromite forming dunite in the northern part of the Kukes Massif. The chemical composition of minerals in dunites is highly variabile and apparent at outcrop scale. The most significant changes are recorded by olivine, which contains over 90 Fo in the host dunite but decreases to 87.5 in proximity of clinopyroxenitic veins. The composition of spinel is also sensitive to the presence of veins: in host dunite its Cr# is over 80 (chromite type I), whereas the presence of veins causes its decrease to 68 (type II). Clinopyroxene in vein-forming clinopyroxenite has Mg# from 86 to 92 and is Al-rich (Al 2 O 3 0.8-2.6 wt. %). Orthopyroxene forms orthopyroxenites (Mg# 90-93, Al 2 O 3 0.2-1.6 wt. %), but also screens (Mg# 83-91, Al 2 O 3 0.8-2.4 wt. %) at the contact between clinopyroxenite veins and the host dunite. The thick dunitic sequence at Kukes must have been formed as a result of intensive percolation of possibly boninitic melt through parental harzburgite. Another step in the evolution of the Kukes massif was related to intrusion of the pyroxenitic veins. These melts were not equilibrated with the host dunite and led to metasomatic modification of chromite and olivine, increasing Al 2 O 3 content in former (from 6-8 up to 18 wt. %) and decreasing Fo (extremely from 92 to 87.5) in the latter. The process is evident proximal to clinopyroxenite veins, but a subtle effect is also recorded in the chemical composition of dunite contacting orthopyroxenite, leading to increase in Fe 2 O 3 content. Metasomatism modified the composition of dunites in a zone of 0.5 m around pyroxenites. Our studies indicate a multistage evolution of the SSZ peridotites and show that its deciphering requires careful mineralogical examination.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":115151005,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115151005/thumbnails/1.jpg","file_name":"JGeosciences_2024.pdf","download_url":"https://www.academia.edu/attachments/115151005/download_file","bulk_download_file_name":"Melt_rock_interaction_as_a_factor_contro.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115151005/JGeosciences_2024-libre.pdf?1716386647=\u0026response-content-disposition=attachment%3B+filename%3DMelt_rock_interaction_as_a_factor_contro.pdf\u0026Expires=1743209699\u0026Signature=f3gqN66AkzsIOzlGAj1Pl4OKKs3wMhFdFTbuEp3gQk91rQzBJW0Gxzjo7oTPFGVdtpzO-DuXBQ2Yrw7vdhcoh8JYgDEUAYLM3S7eLM2iiSIchCbO7c9G396-3cywn4xAkVOk1NHwpxpEx7nEx36ZHIrw7e6z7NCDBYOZuJ0fRfZYPNyvyn0h9ZyzDYnskR61gjkFd4dCqTrfqM4JurmvKYdOI1GEg2196wLvzHc6uUj4Ma0KujWCc1q6YMs-KgQhV6rT3T8uG~Sj~R~dCBpOLByHnReD9hJX4jzPLyYMNMqXoUt2Ii4mcqYtg3Vbfc7DFZMiKH3dIxCrbhhcPo3btw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-119814581-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="117396662"><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/117396662/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central"><img alt="Research paper thumbnail of Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central" class="work-thumbnail" src="https://attachments.academia-assets.com/115237174/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/117396662/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central">Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central</a></div><div class="wp-workCard_item"><span>BSGF - Earth Science Bulletin</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">This paper presents and discusses new geochronological and petrological data on a suite of calc-a...</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">This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365-354 Ma (including uncertainties) for igneous crystallization. These calc-alkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="82f26dbccf4286d29aab8d0cb9983378" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":115237174,"asset_id":117396662,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/115237174/download_file?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="117396662"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="117396662"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 117396662; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=117396662]").text(description); $(".js-view-count[data-work-id=117396662]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 117396662; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='117396662']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "82f26dbccf4286d29aab8d0cb9983378" } } $('.js-work-strip[data-work-id=117396662]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":117396662,"title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central","translated_title":"","metadata":{"doi":"10.1051/bsgf/2024003","abstract":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365-354 Ma (including uncertainties) for igneous crystallization. These calc-alkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.","ai_title_tag":"Active Margin Magmatism in Western Massif Central","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"BSGF - Earth Science Bulletin"},"translated_abstract":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365-354 Ma (including uncertainties) for igneous crystallization. These calc-alkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.","internal_url":"https://www.academia.edu/117396662/Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central","translated_internal_url":"","created_at":"2024-04-12T06:28:48.785-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":41476148,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117174,"email":"j***r@get.omp.eu","display_order":-4,"name":"Julien Berger","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476149,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117175,"email":"b***4@yahoo.fr","display_order":-3,"name":"Lea Beau","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476150,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117176,"email":"j***4@gmail.com","display_order":-2,"name":"Julien Serrano","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476151,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":6104564,"email":"m***t@get.omp.eu","display_order":-1,"name":"Mathieu Benoit","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476152,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117177,"email":"b***a@gmail.com","display_order":1,"name":"Anissa Benmammar","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476153,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":7611257,"email":"s***e@get.omp.eu","display_order":2,"name":"Stephanie Duchene","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476154,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":26472103,"co_author_invite_id":null,"email":"o***r@gm.univ-montp2.fr","affiliation":"Université de Montpellier","display_order":3,"name":"Olivier Bruguier","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"},{"id":41476155,"work_id":117396662,"tagging_user_id":10246740,"tagged_user_id":32694530,"co_author_invite_id":null,"email":"j***e@umons.ac.be","affiliation":"Université de Mons","display_order":4,"name":"Jean-marc Baele","title":"Short-lived active margin magmatism preceding Variscan collision in the Western French Massif Central"}],"downloadable_attachments":[{"id":115237174,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115237174/thumbnails/1.jpg","file_name":"BSGF_2024.pdf","download_url":"https://www.academia.edu/attachments/115237174/download_file","bulk_download_file_name":"Short_lived_active_margin_magmatism_prec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115237174/BSGF_2024-libre.pdf?1716563779=\u0026response-content-disposition=attachment%3B+filename%3DShort_lived_active_margin_magmatism_prec.pdf\u0026Expires=1743209699\u0026Signature=NP6kmHOPMAxi6onE72OZY~6OsgoSmP5b8McnhCf5QBvJyMTb55nykB6xddixmuyJBEVhW7KWJO8jDtvBiHfKWodSkEERnOqu8pN6gQVPUu1zJjjPS4nysQp9rxmn8JKrF1KG1aweHcJotNBccG-p54y7ZKoE3HG~KyNBc12B6W6HuvjKdoeYKpl5IEuLvad2X389kJLkP~DZF1NnVumFAaZEw97gyhtCBVAjlcEscjEidCwpCQlI5OZV3d899nkYcxMtsLk9cr05trEJSe1tw4YrgWwQty83rTu1iKFIfR5fyTcL8OSM4DB470n~pSeUkmNMo3P3ePW61mRwApwZBw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Short_lived_active_margin_magmatism_preceding_Variscan_collision_in_the_Western_French_Massif_Central","translated_slug":"","page_count":18,"language":"en","content_type":"Work","summary":"This paper presents and discusses new geochronological and petrological data on a suite of calc-alkaline plutons composed predominantly of diorites and tonalites from the West Massif Central. Their petrochemical fingerprints are compatible with partial melting of a hydrous mantle wedge followed by fractional crystallization of amphibole and plagioclase before final emplacement between 5 and 8 kbar within the continental upper plate of a subduction system. In situ U-Pb zircon dating on tonalites yields a fairly narrow age range of 365-354 Ma (including uncertainties) for igneous crystallization. These calc-alkaline plutons imply active margin magmatism near the Devonian-Carboniferous boundary and are contemporaneous with the back-arc magmatism and HP metamorphism as dated by recent studies. However, such isolated igneous bodies do not form a transcrustal magmatic arc but rather represent dispersed plutons emplaced within less than 30 Myr when all data from the Variscan belt of France are considered. In Limousin, they intrude migmatitic paragneisses and retrogressed eclogites from the Upper Gneiss Unit (UGU), suggesting that the high pressure rocks were already exhumed at 19-30 km depth before 365 Ma. Moreover, the diorites and tonalites are never found within units below the UGU. It therefore suggests that these tectonometamorphic units of the Western French Massif Central were piled up after 354 Ma. Altogether these results support the monocyclic model for Variscan geodynamics in the French Massif Central, with the transition between oceanic subduction and continental collision taking place between Upper Devonian and Lower Carboniferous.","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":115237174,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115237174/thumbnails/1.jpg","file_name":"BSGF_2024.pdf","download_url":"https://www.academia.edu/attachments/115237174/download_file","bulk_download_file_name":"Short_lived_active_margin_magmatism_prec.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115237174/BSGF_2024-libre.pdf?1716563779=\u0026response-content-disposition=attachment%3B+filename%3DShort_lived_active_margin_magmatism_prec.pdf\u0026Expires=1743209699\u0026Signature=NP6kmHOPMAxi6onE72OZY~6OsgoSmP5b8McnhCf5QBvJyMTb55nykB6xddixmuyJBEVhW7KWJO8jDtvBiHfKWodSkEERnOqu8pN6gQVPUu1zJjjPS4nysQp9rxmn8JKrF1KG1aweHcJotNBccG-p54y7ZKoE3HG~KyNBc12B6W6HuvjKdoeYKpl5IEuLvad2X389kJLkP~DZF1NnVumFAaZEw97gyhtCBVAjlcEscjEidCwpCQlI5OZV3d899nkYcxMtsLk9cr05trEJSe1tw4YrgWwQty83rTu1iKFIfR5fyTcL8OSM4DB470n~pSeUkmNMo3P3ePW61mRwApwZBw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology"},{"id":422167,"name":"Massif Central","url":"https://www.academia.edu/Documents/in/Massif_Central"},{"id":755655,"name":"Variscan Orogeny","url":"https://www.academia.edu/Documents/in/Variscan_Orogeny"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-117396662-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="117395067"><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/117395067/Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift"><img alt="Research paper thumbnail of Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift" class="work-thumbnail" src="https://attachments.academia-assets.com/113262836/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/117395067/Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift">Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift</a></div><div class="wp-workCard_item"><span>Gondwana Research</span><span>, 2024</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and ph...</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 use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX</span></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-117395067-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-117395067-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975463/figure-1-tecto-volcanic-map-of-the-ntd-the-first-order"><img alt="Fig. 1. Tecto-volcanic map of the NTD. The first-order geological units are indicated (Dawson and Smith, 1988; Fritz et al., 2013; Smith and Mosley, 1993): orange for the Tanzanian Craton, blue and green for the Western and Eastern parts, respectively, of the Mozambique Belt. The inferred edges of the Masai block are repre- sented by the blue dashed line. The major normal faults are represented by the continuous black lines. EBF = Eyasi Border Faults, NBF = Natron Border Fault, MBF = Manyara Border Fault, OOF = Ol Doinyo Ogol Fault, PBF = Pangani Border Fault. Green triangles indicate the location of the main volcanoes. The red star indicates the sample area of this study (Pello Hill). The ages of the volcanism are written in italic next to the volcanic edifices (Dawson, 1992; Macintyre et al., 1974; Mana et al., 2015, 2012; Manega, 1993; Mollel, 2007; Nonnotte, 2007; Sherrod et al., 2013; Wilkinson et al., 1986). The two N-S and E-W chemical axes are repre- sented by the green and purple arrows, respectively. Volcanoes abbreviations. B = Burko, El = Eledoi, Em = Embakai, Es = Essimingor, G = Gelai, H = Hanang, Ke = Kerimasi, Ket = Ketumbeine, Ki = Kilimanjaro, Kw = Kwahara, Lab = Labait, La = Lashaine, M = Monduli, Me = Meru, Ng = Ngorongoro, OL = Ol Doinyo Lengai, Olm = Olmani, PH = Pello Hill, T = Tarosero. The East-West red dashed line represents the track of the P-wave tomographic vertical cross-section in Fig. 7. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975469/figure-2-photomicrographs-of-pello-hill-mantle-xenolith-thin"><img alt="Fig. 2. Photomicrographs of Pello Hill mantle xenolith thin sections in plane polarized light. a) orthopyroxene, with amphibole inclusion, and reaction rim with clinopyroxene (PH13); b) interstitial clinopyroxene, orthopyroxene and chromite in PH18 dunite; c) Typical multi-millimeter amphibole/phlogopite/clinopyroxene " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975477/figure-3-major-element-compositions-for-clinopyroxenes-and"><img alt="Fig. 3. Major element compositions for a) clinopyroxenes, b) and c) amphiboles, and d) phlogopites from the Pello Hill mantle xenoliths. Triangles are for in- vein minerals, circles for in-peridotite minerals and crosses for lava minerals. Mg# = Mg/(Mg + Fe”*) x 100. " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975483/figure-4-comparison-between-the-whole-sample-the-peridotite"><img alt="Fig. 4. Comparison between the whole sample, the peridotite (without vein), and the vein seismic properties (each one being computed in one step) for PH18, PH9, PH4, and PH27 xenoliths, at pressure 2 GPa and 1200 °C. The peridotite was computed directly with AnisEulerSC while the peridotite + vein and the vein were corrected from the temperature effect by applying a percentage decrease (Supplementary Material 3). The proportion of the vein in a sample is provided in brackets next to the sample name. All plots are lower hemisphere. Vein orientations are represented by the red lines on the olivine [100] axis pole figures. The " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975488/figure-4-locity-from-to-km-for-vp-and-from-to-km-for-vs-that"><img alt="locity from 8.5-7.4 to 7.6-6.5 km.s~! for Vp and from 4.6-4.1 to 4.1-3.7 km.s~! for Vs. That corresponds to a decrease by 10-12 % Vp and 9-10 % Vs compared to the peridotite (PH9, Fig. 4 and Table 2). This vein proportion initiates a shift of the velocity directions, and the " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975493/figure-5-seismic-property-calculations-with-different-lens"><img alt="Fig. 5. Seismic property calculations with different lens-shape inclusion orientations and fluid filling in PH9 22 % vein-bearing xenolith sample. Calculations are at pressure 2 GPa and temperature 1200 °C with AnisEulerSC. The first row shows a sketch of the orientation of the inclusions in the sample reference frame, where (X,Y) is the foliation plane and X the lineation (olivine [100] axis). Al and A3 are the longest and shortest ellipse axes, respectively. Al = A2 = 5 and A3 = 1. AZ stands for the azimuth (counter clockwise) of the ellipse axes and INC for their vertical inclination. The velocity plots are lower hemisphere, and the maximum and minimum velocities are marked by a black square and a white circle, respectively. " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_006.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975496/figure-6-calculated-temperature-and-pressure-for-pello-hill"><img alt="Fig. 6. Calculated temperature and pressure for Pello Hill xenoliths with Brey and Kohler (1990) and Kohler and Brey (1990) thermobarometers (orthopyrox- ene-clinopyroxene and olivine-clinopyroxene couples). Lashaine P-T conditions are from Rudnick et al. (1994) and Gibson et al. (2013). The Labait xenoliths P- T conditions are from Lee and Rudnick (1999) and Koornneef et al. (2009). The P-T conditions of the partial melting of the Labait nephelinite are calculated from Baudouin and Parat (2020). Additional data of vein-free xenoliths from Pello Hill (black crosses, Dawson and Smith, 1988) were used to calculate P-T con- ditions as a comparison. The Pello Hill and Labait Moho were determined with receiver functions from Plasman et al. (2017) and A. Clutier personal communi- cation, respectively. The LAB depth below the Labait and Pello Hill were estimated by Craig et al. (2011) with surface wave tomography (vertical resolution of + 25 km). Cratonic geotherm (44 mW.m~, Selway et al., 2014), plume modified geotherm (50 mW.m~, Gibson and McKenzie, 2023), Proterozoic and Cenozoic geotherms (Artemieva, 2009) are also reported. The two peridotite solidi and the modeled melt CO, isopleths (thin grey lines, with CO, wt.% in the melt) are from Dasgupta et al. (2013). " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_007.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975506/figure-8-seismic-properties-of-mantle-metasomatism-from"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_008.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975513/figure-8-maximum-square-minimum-triangle-and-mean-crosses"><img alt="Fig. 8. Maximum (square), minimum (triangle) and mean (crosses) P-wave velocity variations (AVp) computed for a) the crystallized vein-bearing mantle xenoliths with equation (3) and with temperature correction (1200 °C), and b-d) for lens-shaped fluid-filled inclusions in PH9 mantle xenoliths. b) vertical veins perpendicular to the foliation (1:5:5), c) vertical veins parallel to the foliation (5:5:1), d) horizontal veins perpendicular to the foliation (5:1:5). The red and orange straight lines delimit the range of the tomographic low velocity variations induced by the metasomatizing fluid circulation. In graph a), the variation of velocity between the dif. ferent samples for a common vein percentage is induced by the mineralogical assemblage. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_009.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975517/figure-9-simplified-structural-diagram-of-west-east-profile"><img alt="Fig. 9. Simplified structural diagram of a west-east profile in the North Tanzanian Divergence with representations (a-d) of possible relationship between fluid-filled veins (yellow planes) and the peridotites from natural xenoliths in the mantle. The orientation of the seismic velocities in the NTD are constrained by the vertical fo- liation and horizontal lineation in peridotite (with no veins) far from the rift axis (a), and by foliation, horizontal lineation and veins (perpendicular to the rift) in the rift axis (d), ie. with intermediate vertical velocity. Spinel-garnet boundary is from Lee et al. (2000). Diagram modified from Kendall et al. (2006). (For interpre- tation of the references to colour in this figure legend, the reader is referred to the web version of this article.) " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/figure_010.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975522/table-1-modal-composition-of-pello-hill-mantle-xenoliths"><img alt="Modal composition of Pello Hill mantle xenoliths determined by EBSD. " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/table_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975530/table-2-seismic-properties-computed-with-aniseulersc-at-gpa"><img alt="Seismic properties computed with AnisEulerSC at 2 GPa and 1200 °C. Velocity variations are relative to the IAPS91 Earth model (Kennett and Engdahl, 1991) for Pello Hill mantle xenolith samples, crystallized full aggregates. Supplementary Material 1). For all mineral equilibrium, we chose grains as close as possible to each other, and far from veins. By using the two-pyroxenes thermometer from Putirka (2008), we determined an a priori equilibrium temperature (Tippy). Then, an a priori pressure (Pinpus) is determined graphically from the geotherm modified by a plume thermal anomaly from Selway et al. (2014) and Tippy. Finally, Tinput ANd Pinpyr Were implemented in PTEXL3 spreadsheet (from T. Koehler and modified by A. Girnis; https://www.mineralogie.uni- frankfurt.de/index.html), where the final temperatures is determined with the orthopyroxene-clinopyroxene equilibrium from Brey and Kohler (1990). In the case of xenoliths without orthopyroxene, the par- titioning of Ca between the olivine and the clinopyroxene from Kohler and Brey (1990) was used. The final pressure was computed using Ca partitioning between the olivine and the clinopyroxene from Kohler and Brey (1990) for the garnet-free mantle xenoliths from Pello Hill. and carbonatitic intermediate compositions (Aulbach et al., 2011; Burton et al., 2000). In addition, isotopic signatures for Ol Doinyo Lengai and the Ngorongoro volcanic complex are evidence of even more diverse enriched mantle signatures (HIMU and EM1, Aulbach et al.. 2011: Bell and Simonetti. 1996: Mollel et al.. 2011. 2009). " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/table_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975532/table-3-seismic-properties-computed-with-aniseulersc-at-gpa"><img alt="Seismic properties computed with AnisEulerSC at 2 GPa and 1200 °C. Velocity variations are relative to the IAPS91 Earth model (Kennett and Engdahl, 1991) for Pello Hill mantle xenolith samples with vertical 5:5:1 fluid-filled inclusions. " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/table_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975537/figure-5-bulk-moduli-used-for-the-computation-of-velocities"><img alt="Bulk moduli used for the computation of velocities for the fluid-filled vein- bearing samples in Fig. 5, at 1-4 GPa. Our computation of seismic properties of natural mantle xenoliths from Pello Hill clearly indicates that the presence of melt and/or fluids in peridotitic rocks decreases both Vp and Vs (Fig. 4 vs Fig. 5 and Table 2 vs Table 3). The presence of anhydrous peridotitic melt in the crystal- lized peridotitic mantle would lower the P-velocity by 5 to 8 % and S- velocity by 4 to 10 % for 6 % of the melt fraction (peridotite + fluid/ melt velocities in Table 3 and peridotite velocity in Fig. 4). This agrees with the elastic properties of silicate melts which predict a P and S wave velocity decrease of up to 9 and 11 %, respectively, for 1-5 % of the an- hydrous melt between 70 and 150 km deep (Clark and Lesher, 2017). Table 4 " class="figure-slide-image" src="https://figures.academia-assets.com/113262836/table_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975538/table-5-seismic-properties-of-mantle-metasomatism-from"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/113262836/table_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/32975540/table-6-seismic-properties-of-mantle-metasomatism-from"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/113262836/table_006.jpg" /></a></figure></div><div class="next-slide-container js-next-button-container"><button aria-label="Next" class="carousel-navigation-button js-profile-work-117395067-figures-next"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_forward_ios</span></button></div></div></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2cab4b62e9540873aa5aac3348706cb2" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":113262836,"asset_id":117395067,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/113262836/download_file?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="117395067"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="117395067"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 117395067; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=117395067]").text(description); $(".js-view-count[data-work-id=117395067]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 117395067; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='117395067']"); 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></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.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: "2cab4b62e9540873aa5aac3348706cb2" } } $('.js-work-strip[data-work-id=117395067]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":117395067,"title":"Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift","translated_title":"","metadata":{"doi":"10.1016/j.gr.2024.03.008","abstract":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","ai_title_tag":"Seismic Properties of Mantle Metasomatism in Tanzania Rift","publication_date":{"day":null,"month":null,"year":2024,"errors":{}},"publication_name":"Gondwana Research"},"translated_abstract":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. Our results help to interpret the seismic tomographic images in terms of vein and inclusions proportions in the lithospheric mantle. We focus on mantle xenoliths from the in-rift Pello Hill volcano in the North Tanzanian Divergence (NTD). These xenoliths reveal the presence of refractory mantle harzburgites and dunites with coarse granular to porphyroclastic textures and 6-80 % of diopside, phlogopite and amphibole-bearing veins and phlogopite-rich hornblendite xenolith. The presence of calc-potassic and FeO, TiO 2-rich veins, and mineral equilibria of olivine and pyroxenes indicate that fluid/melt-rock interactions occurred at depth from 40 km to 80-90 km, and indicate the presence of a high-temperature isotherm beneath the NTD (T = 1040-1200°C). We computed the seismic properties of the mantle xenoliths with different proportions, compositions, and geometric distributions of crystallized and fluid-filled veins. Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","internal_url":"https://www.academia.edu/117395067/Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift","translated_internal_url":"","created_at":"2024-04-12T05:56:14.773-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":10246740,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":41475937,"work_id":117395067,"tagging_user_id":10246740,"tagged_user_id":131212699,"co_author_invite_id":null,"email":"a***r@umontpellier.fr","affiliation":"University of Montpellier","display_order":-3,"name":"Adeline Clutier","title":"Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift"},{"id":41475938,"work_id":117395067,"tagging_user_id":10246740,"tagged_user_id":39907626,"co_author_invite_id":null,"email":"F***t@gm.univ-montp2.fr","display_order":-2,"name":"Fleurice Parat","title":"Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift"},{"id":41475940,"work_id":117395067,"tagging_user_id":10246740,"tagged_user_id":214695258,"co_author_invite_id":null,"email":"c***i@umontpellier.fr","display_order":1,"name":"Tiberi Christel","title":"Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift"},{"id":41475941,"work_id":117395067,"tagging_user_id":10246740,"tagged_user_id":null,"co_author_invite_id":8117127,"email":"s***x@umontpellier.fr","display_order":2,"name":"Stéphanie Gautier","title":"Seismic properties of mantle metasomatism from mantle xenoliths beneath the North Tanzania Divergence, East African Rift"}],"downloadable_attachments":[{"id":113262836,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/113262836/thumbnails/1.jpg","file_name":"DraftProof_Clutier_et_al_2024.pdf","download_url":"https://www.academia.edu/attachments/113262836/download_file","bulk_download_file_name":"Seismic_properties_of_mantle_metasomatis.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/113262836/DraftProof_Clutier_et_al_2024-libre.pdf?1712926994=\u0026response-content-disposition=attachment%3B+filename%3DSeismic_properties_of_mantle_metasomatis.pdf\u0026Expires=1743209699\u0026Signature=HqSZLP5qvJJBTgrFlL0tkZd4DbiJXb9XqbEBo~MrOtxSPQWyX3syHHfm8Ascs77u-3Oe7NDMf~Ujwb5l3X3iy38E6FFE9zBtrwcihQA7f5BEuuWn2714u-LZ6u4gGVSXQhc3G~k2HL8YuToxY847kCX~HYFWW5MpSw9u1Gi808Ho8jbVUSPPHdhSt8gaDL60Sj2T6eteKUnc-6amGUVeZFbI5NKUcmVE2zFB2QWDUmHrjCRhaf93Qs2ubSyraquLJfFy0Tyty54ib0Y5EPRUYv470A4PMGdqU1nxTYc7lHCrpjs6SkxPz0FZxJbqRsxq527gHtgtF7tmqOH4ZH81vQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Seismic_properties_of_mantle_metasomatism_from_mantle_xenoliths_beneath_the_North_Tanzania_Divergence_East_African_Rift","translated_slug":"","page_count":22,"language":"en","content_type":"Work","summary":"We use mantle xenoliths brought to the surface by alkaline lavas to determine the chemical and physical properties of the metasomatized lithospheric mantle that contribute to the earliest rifting stage in East Africa. 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Compared to vein-free peridotites, for crystallized vein-bearing xenoliths, the velocity is lowered by 2-4 % to 28-37 % for Vp and by 2-3 % to 25-29 % for Vs for 6 % to 60 % veins, respectively. For fluid-filled inclusions, hydrous melt lens-shape inclusions are the most effective parameter to reduce P velocity, compared to dry or 2.5 %-CO 2 peridotitic melt. A comparison with seismic tomography velocities allows us to discuss the current state of the lithospheric mantle. The best agreement obtained between P teleseismic tomography (Vp anomalies between −9 % and −15 %) and vein-bearing peridotites (depth 40-90 km) corresponds to 12-25 % of crystallized veins or 8-15 % for fluid filled-veins for a vertical foliation and transtensional strain regime in the mantle lithosphere beneath the NTD. © 20XX","owner":{"id":10246740,"first_name":"Michel","middle_initials":null,"last_name":"Gregoire","page_name":"MichelGregoire","domain_name":"omp","created_at":"2014-03-18T20:51:29.892-07:00","display_name":"Michel Gregoire","url":"https://omp.academia.edu/MichelGregoire"},"attachments":[{"id":113262836,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/113262836/thumbnails/1.jpg","file_name":"DraftProof_Clutier_et_al_2024.pdf","download_url":"https://www.academia.edu/attachments/113262836/download_file","bulk_download_file_name":"Seismic_properties_of_mantle_metasomatis.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/113262836/DraftProof_Clutier_et_al_2024-libre.pdf?1712926994=\u0026response-content-disposition=attachment%3B+filename%3DSeismic_properties_of_mantle_metasomatis.pdf\u0026Expires=1743209699\u0026Signature=HqSZLP5qvJJBTgrFlL0tkZd4DbiJXb9XqbEBo~MrOtxSPQWyX3syHHfm8Ascs77u-3Oe7NDMf~Ujwb5l3X3iy38E6FFE9zBtrwcihQA7f5BEuuWn2714u-LZ6u4gGVSXQhc3G~k2HL8YuToxY847kCX~HYFWW5MpSw9u1Gi808Ho8jbVUSPPHdhSt8gaDL60Sj2T6eteKUnc-6amGUVeZFbI5NKUcmVE2zFB2QWDUmHrjCRhaf93Qs2ubSyraquLJfFy0Tyty54ib0Y5EPRUYv470A4PMGdqU1nxTYc7lHCrpjs6SkxPz0FZxJbqRsxq527gHtgtF7tmqOH4ZH81vQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":2733,"name":"Petrophysics","url":"https://www.academia.edu/Documents/in/Petrophysics"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology"},{"id":31049,"name":"Mantle Petrology","url":"https://www.academia.edu/Documents/in/Mantle_Petrology"}],"urls":[]}, dispatcherData: dispatcherData }); 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