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$(".js-view-count[data-work-id=25974988]").text(description); $(".js-view-count-work_25974988").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_25974988").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="25974988"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">8</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="407" rel="nofollow" href="https://www.academia.edu/Documents/in/Geochemistry">Geochemistry</a>, <script data-card-contents-for-ri="407" type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2404" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology">Petrology</a>, <script data-card-contents-for-ri="2404" type="text/json">{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2635" rel="nofollow" href="https://www.academia.edu/Documents/in/Metamorphic_Petrology">Metamorphic Petrology</a><script data-card-contents-for-ri="2635" type="text/json">{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=25974988]'), work: {"id":25974988,"title":"Igneous Rocks and Processes","created_at":"2016-06-07T18:22:32.535-07:00","url":"https://www.academia.edu/25974988/Igneous_Rocks_and_Processes?f_ri=15989","dom_id":"work_25974988","summary":"A practical guide","downloadable_attachments":[{"id":46324816,"asset_id":25974988,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":3963215,"first_name":"Juan Julio","last_name":"Julian","domain_name":"unmsm","page_name":"JuanJulioJulian","display_name":"Juan Julio Julian","profile_url":"https://unmsm.academia.edu/JuanJulioJulian?f_ri=15989","photo":"https://0.academia-photos.com/3963215/1489146/14279506/s65_juan_julio_julian.rosado.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989"},{"id":20615,"name":"Petroleum geology","url":"https://www.academia.edu/Documents/in/Petroleum_geology?f_ri=15989"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_29297536" data-work_id="29297536" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/29297536/Igneous_Rocks_A_Classification_and_Glossary_of_Terms_2nd_Le_Maitre">Igneous Rocks A Classification and Glossary of Terms 2nd Le Maitre</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Decades of field and microscope studies and more recent quantitative geochemical analyses have resulted in a vast, and sometimes overwhelming, array of nomenclature and terminology associated with igneous rocks. Under the auspices of the... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_29297536" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Decades of field and microscope studies and more recent quantitative geochemical analyses have resulted in a vast, and sometimes overwhelming, array of nomenclature and terminology associated with igneous rocks. Under the auspices of the International Union of Geological Sciences (IUGS), a group of petrologists from around the world has laboured for more than 30 years to collate these terms, gain international agreement on their usage, and reassess the methods by which we categorize and name igneous rocks.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/29297536" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="8f5192e45e206966b08ad7f1b75cc70f" rel="nofollow" data-download="{"attachment_id":49739887,"asset_id":29297536,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/49739887/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="55330152" href="https://ufes.academia.edu/GuilhermeMarques">Guilherme Marques Martins</a><script data-card-contents-for-user="55330152" type="text/json">{"id":55330152,"first_name":"Guilherme","last_name":"Marques Martins","domain_name":"ufes","page_name":"GuilhermeMarques","display_name":"Guilherme Marques Martins","profile_url":"https://ufes.academia.edu/GuilhermeMarques?f_ri=15989","photo":"https://0.academia-photos.com/55330152/14582821/15443595/s65_guilherme.marques.jpg"}</script></span></span></li><li class="js-paper-rank-work_29297536 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="29297536"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 29297536, container: ".js-paper-rank-work_29297536", }); 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$(".js-view-count[data-work-id=29297536]").text(description); $(".js-view-count-work_29297536").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_29297536").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="29297536"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">9</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2404" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology">Petrology</a>, <script data-card-contents-for-ri="2404" type="text/json">{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="65805" rel="nofollow" href="https://www.academia.edu/Documents/in/Nomenclature">Nomenclature</a><script data-card-contents-for-ri="65805" type="text/json">{"id":65805,"name":"Nomenclature","url":"https://www.academia.edu/Documents/in/Nomenclature?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=29297536]'), work: {"id":29297536,"title":"Igneous Rocks A Classification and Glossary of Terms 2nd Le Maitre","created_at":"2016-10-20T06:10:51.317-07:00","url":"https://www.academia.edu/29297536/Igneous_Rocks_A_Classification_and_Glossary_of_Terms_2nd_Le_Maitre?f_ri=15989","dom_id":"work_29297536","summary":"Decades of field and microscope studies and more recent quantitative geochemical analyses have resulted in a vast, and sometimes overwhelming, array of nomenclature and terminology associated with igneous rocks. Under the auspices of the International Union of Geological Sciences (IUGS), a group of petrologists from around the world has laboured for more than 30 years to collate these terms, gain international agreement on their usage, and reassess the methods by which we categorize and name igneous rocks.","downloadable_attachments":[{"id":49739887,"asset_id":29297536,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":55330152,"first_name":"Guilherme","last_name":"Marques Martins","domain_name":"ufes","page_name":"GuilhermeMarques","display_name":"Guilherme Marques Martins","profile_url":"https://ufes.academia.edu/GuilhermeMarques?f_ri=15989","photo":"https://0.academia-photos.com/55330152/14582821/15443595/s65_guilherme.marques.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":65805,"name":"Nomenclature","url":"https://www.academia.edu/Documents/in/Nomenclature?f_ri=15989","nofollow":true},{"id":66471,"name":"Mafic Alkaline Igneous Rocks","url":"https://www.academia.edu/Documents/in/Mafic_Alkaline_Igneous_Rocks?f_ri=15989"},{"id":147519,"name":"Geologia","url":"https://www.academia.edu/Documents/in/Geologia?f_ri=15989"},{"id":163307,"name":"Facilitation","url":"https://www.academia.edu/Documents/in/Facilitation?f_ri=15989"},{"id":242974,"name":"Ultramafic","url":"https://www.academia.edu/Documents/in/Ultramafic?f_ri=15989"},{"id":951061,"name":"Nomenclatura","url":"https://www.academia.edu/Documents/in/Nomenclatura?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_8376802" data-work_id="8376802" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/8376802/THE_OPERATION_OF_PORTABLE_PETROGRAPHIC_THIN_SECTION_LABORATORY_FOR_FIELD_STUDIES">THE OPERATION OF PORTABLE PETROGRAPHIC THIN-SECTION LABORATORY FOR FIELD STUDIES</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">A procedure for petrographic and micromorphological thin sections preparation and examination in extra-laboratory and field conditions is presented. With use of basic, often improvised off the shelf equipment, standard petrographic thin... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_8376802" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">A procedure for petrographic and micromorphological thin sections preparation and examination in extra-laboratory and field conditions is presented. With use of basic, often improvised off the shelf equipment, standard petrographic thin sections of rocks, sediments, ceramics, mortars and plasters can be produced and examined. The use of newly-introduced Goren portable microscope enables laboratory-grade examination and recording of such materials during field expeditions. Examples from the field of material analysis in art and archaeology are demonstrated.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/8376802" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2476fddddd30c6e68dfbcc9c66cc45c8" rel="nofollow" data-download="{"attachment_id":34775517,"asset_id":8376802,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/34775517/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="204598" href="https://bgu.academia.edu/YuvalGoren">Yuval Goren</a><script data-card-contents-for-user="204598" type="text/json">{"id":204598,"first_name":"Yuval","last_name":"Goren","domain_name":"bgu","page_name":"YuvalGoren","display_name":"Yuval Goren","profile_url":"https://bgu.academia.edu/YuvalGoren?f_ri=15989","photo":"https://0.academia-photos.com/204598/47853/5390976/s65_yuval.goren.jpg"}</script></span></span></li><li class="js-paper-rank-work_8376802 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="8376802"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 8376802, container: ".js-paper-rank-work_8376802", }); 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$(".js-view-count[data-work-id=8376802]").text(description); $(".js-view-count-work_8376802").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_8376802").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="8376802"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">40</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="261" rel="nofollow" href="https://www.academia.edu/Documents/in/Geography">Geography</a>, <script data-card-contents-for-ri="261" type="text/json">{"id":261,"name":"Geography","url":"https://www.academia.edu/Documents/in/Geography?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="392" rel="nofollow" href="https://www.academia.edu/Documents/in/Archaeology">Archaeology</a>, <script data-card-contents-for-ri="392" type="text/json">{"id":392,"name":"Archaeology","url":"https://www.academia.edu/Documents/in/Archaeology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="408" rel="nofollow" href="https://www.academia.edu/Documents/in/Geomorphology">Geomorphology</a><script data-card-contents-for-ri="408" type="text/json">{"id":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=8376802]'), work: {"id":8376802,"title":"THE OPERATION OF PORTABLE PETROGRAPHIC THIN-SECTION LABORATORY FOR FIELD STUDIES","created_at":"2014-09-17T22:25:41.095-07:00","url":"https://www.academia.edu/8376802/THE_OPERATION_OF_PORTABLE_PETROGRAPHIC_THIN_SECTION_LABORATORY_FOR_FIELD_STUDIES?f_ri=15989","dom_id":"work_8376802","summary":"A procedure for petrographic and micromorphological thin sections preparation and examination in extra-laboratory and field conditions is presented. With use of basic, often improvised off the shelf equipment, standard petrographic thin sections of rocks, sediments, ceramics, mortars and plasters can be produced and examined. The use of newly-introduced Goren portable microscope enables laboratory-grade examination and recording of such materials during field expeditions. Examples from the field of material analysis in art and archaeology are demonstrated.","downloadable_attachments":[{"id":34775517,"asset_id":8376802,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":204598,"first_name":"Yuval","last_name":"Goren","domain_name":"bgu","page_name":"YuvalGoren","display_name":"Yuval 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Science","url":"https://www.academia.edu/Documents/in/Soil_Science?f_ri=15989"},{"id":760,"name":"Microeconomics","url":"https://www.academia.edu/Documents/in/Microeconomics?f_ri=15989"},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989"},{"id":1444,"name":"Environmental microbiology","url":"https://www.academia.edu/Documents/in/Environmental_microbiology?f_ri=15989"},{"id":1588,"name":"Forensic Science","url":"https://www.academia.edu/Documents/in/Forensic_Science?f_ri=15989"},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989"},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989"},{"id":3091,"name":"Microscopy","url":"https://www.academia.edu/Documents/in/Microscopy?f_ri=15989"},{"id":3316,"name":"Archaeological Science","url":"https://www.academia.edu/Documents/in/Archaeological_Science?f_ri=15989"},{"id":5346,"name":"Archaeological Method \u0026 Theory","url":"https://www.academia.edu/Documents/in/Archaeological_Method_and_Theory?f_ri=15989"},{"id":6735,"name":"Heritage Conservation","url":"https://www.academia.edu/Documents/in/Heritage_Conservation?f_ri=15989"},{"id":7325,"name":"Archaeological Soil Micromorphology","url":"https://www.academia.edu/Documents/in/Archaeological_Soil_Micromorphology?f_ri=15989"},{"id":7710,"name":"Biology","url":"https://www.academia.edu/Documents/in/Biology?f_ri=15989"},{"id":12069,"name":"Histology","url":"https://www.academia.edu/Documents/in/Histology?f_ri=15989"},{"id":12807,"name":"Archaeometry","url":"https://www.academia.edu/Documents/in/Archaeometry?f_ri=15989"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":16068,"name":"Forensic Archaeology","url":"https://www.academia.edu/Documents/in/Forensic_Archaeology?f_ri=15989"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989"},{"id":20615,"name":"Petroleum geology","url":"https://www.academia.edu/Documents/in/Petroleum_geology?f_ri=15989"},{"id":23209,"name":"Environmental Soil Science","url":"https://www.academia.edu/Documents/in/Environmental_Soil_Science?f_ri=15989"},{"id":25050,"name":"Archaeomineralogy","url":"https://www.academia.edu/Documents/in/Archaeomineralogy?f_ri=15989"},{"id":25566,"name":"Archaeological Fieldwork","url":"https://www.academia.edu/Documents/in/Archaeological_Fieldwork?f_ri=15989"},{"id":43091,"name":"Ceramic Petrography","url":"https://www.academia.edu/Documents/in/Ceramic_Petrography?f_ri=15989"},{"id":48807,"name":"Sedimentary geology and stratigraphy","url":"https://www.academia.edu/Documents/in/Sedimentary_geology_and_stratigraphy?f_ri=15989"},{"id":60446,"name":"Quaternary Sedimentology and Geomorphology","url":"https://www.academia.edu/Documents/in/Quaternary_Sedimentology_and_Geomorphology?f_ri=15989"},{"id":63945,"name":"Microarchaeology","url":"https://www.academia.edu/Documents/in/Microarchaeology?f_ri=15989"},{"id":92271,"name":"Micromorphology","url":"https://www.academia.edu/Documents/in/Micromorphology?f_ri=15989"},{"id":106409,"name":"Archaeometallurgy, Mineralogy, Archaeometry","url":"https://www.academia.edu/Documents/in/Archaeometallurgy_Mineralogy_Archaeometry?f_ri=15989"},{"id":107625,"name":"Optical microscopy","url":"https://www.academia.edu/Documents/in/Optical_microscopy?f_ri=15989"},{"id":266093,"name":"GEOLOGIA Y PETROLEO","url":"https://www.academia.edu/Documents/in/GEOLOGIA_Y_PETROLEO?f_ri=15989"},{"id":280382,"name":"Optical Mineralogy","url":"https://www.academia.edu/Documents/in/Optical_Mineralogy?f_ri=15989"},{"id":517313,"name":"Mineral Prospecting/Mineral Exploration/Field Geology/Ore mineralogy/Petrography/Ore Deposits Modeling","url":"https://www.academia.edu/Documents/in/Mineral_Prospecting_Mineral_Exploration_Field_Geology_Ore_mineralogy_Petrography_Ore_Deposits_Modeli?f_ri=15989"},{"id":648442,"name":"Soil micromorphology","url":"https://www.academia.edu/Documents/in/Soil_micromorphology?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_11985505" data-work_id="11985505" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/11985505/Encyclopedia_of_Volcanoes">Encyclopedia of Volcanoes</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/11985505" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="cd5c537960a3ecdad357ab22b093b841" rel="nofollow" data-download="{"attachment_id":37332652,"asset_id":11985505,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/37332652/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="2821091" href="https://nitrr.academia.edu/NAIYARIMAM">NAIYAR IMAM</a><script data-card-contents-for-user="2821091" type="text/json">{"id":2821091,"first_name":"NAIYAR","last_name":"IMAM","domain_name":"nitrr","page_name":"NAIYARIMAM","display_name":"NAIYAR IMAM","profile_url":"https://nitrr.academia.edu/NAIYARIMAM?f_ri=15989","photo":"https://0.academia-photos.com/2821091/1278153/11112087/s65_naiyar.imam.jpg"}</script></span></span></li><li class="js-paper-rank-work_11985505 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" 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InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="11985505"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 11985505; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=11985505]").text(description); $(".js-view-count-work_11985505").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_11985505").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="11985505"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">2</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="1370" rel="nofollow" href="https://www.academia.edu/Documents/in/Volcanology">Volcanology</a>, <script data-card-contents-for-ri="1370" type="text/json">{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=11985505]'), work: {"id":11985505,"title":"Encyclopedia of Volcanoes","created_at":"2015-04-17T03:33:03.171-07:00","url":"https://www.academia.edu/11985505/Encyclopedia_of_Volcanoes?f_ri=15989","dom_id":"work_11985505","summary":null,"downloadable_attachments":[{"id":37332652,"asset_id":11985505,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":2821091,"first_name":"NAIYAR","last_name":"IMAM","domain_name":"nitrr","page_name":"NAIYARIMAM","display_name":"NAIYAR IMAM","profile_url":"https://nitrr.academia.edu/NAIYARIMAM?f_ri=15989","photo":"https://0.academia-photos.com/2821091/1278153/11112087/s65_naiyar.imam.jpg"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_35858536" data-work_id="35858536" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/35858536/Magma_plumbing_beneath_collapse_caldera_volcanic_systems">Magma plumbing beneath collapse caldera volcanic systems</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Advancing our knowledge of caldera volcanoes enables better assessment of hazard and more efficient harnessing of resources. In this paper we review developments in concepts of magma storage and transport during the life cycle of caldera... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_35858536" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Advancing our knowledge of caldera volcanoes enables better assessment of hazard and more efficient harnessing of resources. In this paper we review developments in concepts of magma storage and transport during the life cycle of caldera plumbing systems. We draw together: a) geological, geochemical and petrological data from intrusions and eruption deposits; b) geophysical and geochemical data from modern restless calderas; and c) geological and structural evidence from ancient calderas as well as insights from numerical and analogue models. <br /><br />Overall, magma plumbing systems beneath calderas develop incrementally as magma rises, intrudes and rejuvenates. Eventually accumulation and eruption of a sufficient magma volume drives subsidence of the plumbing system roof to form a caldera. The magma plumbing system may then reside relatively unchanged or continue to re-intrude on a variety of scales. Consequences include continued eruptions, crustal resurgence, or new cycles of caldera formation. Large magma volumes characteristic of calderas may evolve as a single progressively-enlarging reservoir or through the rapid amalgamation of small, initially-independent magma pockets. Eruptible magmas may reside at depths of up to 17 km, but typically lie at shallower depths as a caldera system evolves. Timescales of subcaldera magma residence reveal two remarkable concepts: (1) portions of melt within a magma may remain molten for> 106 years, and (2) melt can be created and mobilized in a few thousand years or less.<br /><br />Geophysical and geochemical data illustrate the present state of active sub-caldera plumbing systems and their development on timescales of hours to years. These studies commonly reveal aseismic, low-velocity zones at depths> 6 km with spatial extents that can be larger than the caldera. The seismic attributes are consistent with rock hosting magma bodies of variable volume and melt content. These are commonly overlain by shallower low-velocity zones linked with ground deformation. The exact nature of these shallower zones is unclear, but interpretations often include shallow sills and laccoliths, and hydrothermal circulation is likely a key process as well.<br /><br />Seismicity and geodetic data record the interplay between magma movement and crustal deformation at calderas. Together with evidence from field studies, numerical simulations and analogue models, such data show that magma migration at calderas may involve considerable lateral transport through dykes or sills to a site of eruption. While caldera-related magma intrusions commonly exploit structures produced by caldera subsidence, they may also follow regional tectonic structures that extend well beyond the border of the caldera. The increased structural complexity that occurs as a caldera evolves increases the permeability of the crust. This may promote small volume eruptions and shallow storage of magma in the post-collapse phase.<br /><br />Our review highlights the significant progress made in understanding the range of intrusion styles and timescales that define the magma plumbing beneath calderas. Yet there are still key questions that limit the application of this understanding to directly benefit humanity: (1) What are the limits to the detection of shallow magma bodies, and can we assess the eruption risks associated with magma bodies of different sizes, depths, compositions and crystal contents? (2) Is it viable to generate electricity by extracting heat directly from magma through the sub-caldera plumbing system?<br /><br />Geophysical and drillhole data from Krafla caldera, Iceland, show that rhyolite can exist undetected at shallow levels within the caldera and may not represent a hazard even when intersected by a borehole. Current work at Krafla is assessing the possibility of extracting geothermal energy from shallow magma bodies and/or superheated steam zones directly above. However, the extent and connectivity of this magma to larger volumes in time and space, as well as its applicability to other systems, may only be answered with continued focused magma drilling, geophysical experimentation and geological exploration.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/35858536" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="51baa44ad66021d8b2a1da4ee29c29b4" rel="nofollow" data-download="{"attachment_id":55737383,"asset_id":35858536,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/55737383/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="76268" href="https://ucd.academia.edu/EoghanHolohan">Eoghan P Holohan</a><script data-card-contents-for-user="76268" type="text/json">{"id":76268,"first_name":"Eoghan","last_name":"Holohan","domain_name":"ucd","page_name":"EoghanHolohan","display_name":"Eoghan P Holohan","profile_url":"https://ucd.academia.edu/EoghanHolohan?f_ri=15989","photo":"https://0.academia-photos.com/76268/21098/14897902/s65_eoghan.holohan.jpg"}</script></span></span></li><li class="js-paper-rank-work_35858536 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="35858536"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 35858536, container: ".js-paper-rank-work_35858536", }); });</script></li><li class="js-percentile-work_35858536 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 35858536; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_35858536"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_35858536 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="35858536"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 35858536; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=35858536]").text(description); $(".js-view-count-work_35858536").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_35858536").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="35858536"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">14</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="409" rel="nofollow" href="https://www.academia.edu/Documents/in/Geophysics">Geophysics</a>, <script data-card-contents-for-ri="409" type="text/json">{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1370" rel="nofollow" href="https://www.academia.edu/Documents/in/Volcanology">Volcanology</a>, <script data-card-contents-for-ri="1370" type="text/json">{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="3860" rel="nofollow" href="https://www.academia.edu/Documents/in/Volcanic_Geology">Volcanic Geology</a>, <script data-card-contents-for-ri="3860" type="text/json">{"id":3860,"name":"Volcanic Geology","url":"https://www.academia.edu/Documents/in/Volcanic_Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=35858536]'), work: {"id":35858536,"title":"Magma plumbing beneath collapse caldera volcanic systems","created_at":"2018-02-07T01:41:15.261-08:00","url":"https://www.academia.edu/35858536/Magma_plumbing_beneath_collapse_caldera_volcanic_systems?f_ri=15989","dom_id":"work_35858536","summary":"Advancing our knowledge of caldera volcanoes enables better assessment of hazard and more efficient harnessing of resources. In this paper we review developments in concepts of magma storage and transport during the life cycle of caldera plumbing systems. We draw together: a) geological, geochemical and petrological data from intrusions and eruption deposits; b) geophysical and geochemical data from modern restless calderas; and c) geological and structural evidence from ancient calderas as well as insights from numerical and analogue models. \n\nOverall, magma plumbing systems beneath calderas develop incrementally as magma rises, intrudes and rejuvenates. Eventually accumulation and eruption of a sufficient magma volume drives subsidence of the plumbing system roof to form a caldera. The magma plumbing system may then reside relatively unchanged or continue to re-intrude on a variety of scales. Consequences include continued eruptions, crustal resurgence, or new cycles of caldera formation. Large magma volumes characteristic of calderas may evolve as a single progressively-enlarging reservoir or through the rapid amalgamation of small, initially-independent magma pockets. Eruptible magmas may reside at depths of up to 17 km, but typically lie at shallower depths as a caldera system evolves. Timescales of subcaldera magma residence reveal two remarkable concepts: (1) portions of melt within a magma may remain molten for\u003e 106 years, and (2) melt can be created and mobilized in a few thousand years or less.\n\nGeophysical and geochemical data illustrate the present state of active sub-caldera plumbing systems and their development on timescales of hours to years. These studies commonly reveal aseismic, low-velocity zones at depths\u003e 6 km with spatial extents that can be larger than the caldera. The seismic attributes are consistent with rock hosting magma bodies of variable volume and melt content. These are commonly overlain by shallower low-velocity zones linked with ground deformation. The exact nature of these shallower zones is unclear, but interpretations often include shallow sills and laccoliths, and hydrothermal circulation is likely a key process as well.\n\nSeismicity and geodetic data record the interplay between magma movement and crustal deformation at calderas. Together with evidence from field studies, numerical simulations and analogue models, such data show that magma migration at calderas may involve considerable lateral transport through dykes or sills to a site of eruption. While caldera-related magma intrusions commonly exploit structures produced by caldera subsidence, they may also follow regional tectonic structures that extend well beyond the border of the caldera. The increased structural complexity that occurs as a caldera evolves increases the permeability of the crust. This may promote small volume eruptions and shallow storage of magma in the post-collapse phase.\n\nOur review highlights the significant progress made in understanding the range of intrusion styles and timescales that define the magma plumbing beneath calderas. Yet there are still key questions that limit the application of this understanding to directly benefit humanity: (1) What are the limits to the detection of shallow magma bodies, and can we assess the eruption risks associated with magma bodies of different sizes, depths, compositions and crystal contents? (2) Is it viable to generate electricity by extracting heat directly from magma through the sub-caldera plumbing system?\n\nGeophysical and drillhole data from Krafla caldera, Iceland, show that rhyolite can exist undetected at shallow levels within the caldera and may not represent a hazard even when intersected by a borehole. Current work at Krafla is assessing the possibility of extracting geothermal energy from shallow magma bodies and/or superheated steam zones directly above. However, the extent and connectivity of this magma to larger volumes in time and space, as well as its applicability to other systems, may only be answered with continued focused magma drilling, geophysical experimentation and geological exploration.","downloadable_attachments":[{"id":55737383,"asset_id":35858536,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":76268,"first_name":"Eoghan","last_name":"Holohan","domain_name":"ucd","page_name":"EoghanHolohan","display_name":"Eoghan P Holohan","profile_url":"https://ucd.academia.edu/EoghanHolohan?f_ri=15989","photo":"https://0.academia-photos.com/76268/21098/14897902/s65_eoghan.holohan.jpg"}],"research_interests":[{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=15989","nofollow":true},{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true},{"id":3860,"name":"Volcanic Geology","url":"https://www.academia.edu/Documents/in/Volcanic_Geology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16067,"name":"Caldera Volcanoes","url":"https://www.academia.edu/Documents/in/Caldera_Volcanoes?f_ri=15989"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989"},{"id":32424,"name":"Hydrothermal systems","url":"https://www.academia.edu/Documents/in/Hydrothermal_systems?f_ri=15989"},{"id":51810,"name":"Experimental petrology and volcanology","url":"https://www.academia.edu/Documents/in/Experimental_petrology_and_volcanology?f_ri=15989"},{"id":67273,"name":"Physical Volcanology","url":"https://www.academia.edu/Documents/in/Physical_Volcanology?f_ri=15989"},{"id":102861,"name":"Volcanoes","url":"https://www.academia.edu/Documents/in/Volcanoes?f_ri=15989"},{"id":153149,"name":"Volcanic hazards","url":"https://www.academia.edu/Documents/in/Volcanic_hazards?f_ri=15989"},{"id":197592,"name":"Magma","url":"https://www.academia.edu/Documents/in/Magma?f_ri=15989"},{"id":257012,"name":"Geology and Geophysics","url":"https://www.academia.edu/Documents/in/Geology_and_Geophysics?f_ri=15989"},{"id":637087,"name":"Petrology and Geochemistry of Igneous Rocks","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry_of_Igneous_Rocks?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_32138998" data-work_id="32138998" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/32138998/Fracture_Characterization_Through_Rate_Correlation_Analysis">Fracture Characterization Through Rate Correlation Analysis</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Statistical correlations in flowrate fluctuations between wells from many fields appear to bear out the expectation that the hydraulic conductivities of faults and fractures in reservoirs can be influenced by geomechanical perturbations... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_32138998" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Statistical correlations in flowrate fluctuations between wells from many fields appear to bear out the expectation that the hydraulic conductivities of faults and fractures in reservoirs can be influenced by geomechanical perturbations due to production operations: the fluctuations are characterised by high correlations over very large separation distances between wells; and those correlations appear to be stress-related and fault-related. An entirely separate relationship derived from observations in multiple fields is a strong bias of directionalities shown by injected fluids towards the local orientation of modern-day major principal horizontal principal stress axis (S Hmax ). These two sets of independent field observations provide mutually supporting observational evidences for the general geomechanical sensitivity of faults and fractures. However, whilst peaks in flowrate correlations are observed at about 30 o to S Hmax , the preferred flooding directionalities are at smaller angles to S Hmax . A recently proposed machanism is able to explain the orientational relationships in both sets of data. It involves interacting, stress-aligned, compliant micro-cracks near a critical density; there is a large background of observations of shear-wave splitting in many types of formations that supports the prevalence of such micro-cracks. As a practical low-cost tool, analysis of flowrate correlations can provide valuable information about the major reservoir pathways as an adjunct to reservoir characterisation studies. This information can aid history-matching of reservoir models, particularly those involving fractures. The technique is also well-suited to monitoring reservoir behaviour in time-lapse fashion.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/32138998" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="3a67325908f831995dc5b4074725ceb4" rel="nofollow" data-download="{"attachment_id":52380960,"asset_id":32138998,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/52380960/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="76442" href="https://hw.academia.edu/KesHeffer">Kes Heffer</a><script data-card-contents-for-user="76442" type="text/json">{"id":76442,"first_name":"Kes","last_name":"Heffer","domain_name":"hw","page_name":"KesHeffer","display_name":"Kes Heffer","profile_url":"https://hw.academia.edu/KesHeffer?f_ri=15989","photo":"https://0.academia-photos.com/76442/1765605/2109727/s65_kes.heffer.jpg"}</script></span></span></li><li class="js-paper-rank-work_32138998 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="32138998"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 32138998, container: ".js-paper-rank-work_32138998", }); 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$(".js-view-count[data-work-id=32138998]").text(description); $(".js-view-count-work_32138998").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_32138998").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="32138998"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">22</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="403" rel="nofollow" href="https://www.academia.edu/Documents/in/Gemology">Gemology</a>, <script data-card-contents-for-ri="403" type="text/json">{"id":403,"name":"Gemology","url":"https://www.academia.edu/Documents/in/Gemology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="407" rel="nofollow" href="https://www.academia.edu/Documents/in/Geochemistry">Geochemistry</a>, <script data-card-contents-for-ri="407" type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="408" rel="nofollow" href="https://www.academia.edu/Documents/in/Geomorphology">Geomorphology</a><script data-card-contents-for-ri="408" type="text/json">{"id":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=32138998]'), work: {"id":32138998,"title":"Fracture Characterization Through Rate Correlation Analysis","created_at":"2017-03-30T03:33:12.834-07:00","url":"https://www.academia.edu/32138998/Fracture_Characterization_Through_Rate_Correlation_Analysis?f_ri=15989","dom_id":"work_32138998","summary":"Statistical correlations in flowrate fluctuations between wells from many fields appear to bear out the expectation that the hydraulic conductivities of faults and fractures in reservoirs can be influenced by geomechanical perturbations due to production operations: the fluctuations are characterised by high correlations over very large separation distances between wells; and those correlations appear to be stress-related and fault-related. An entirely separate relationship derived from observations in multiple fields is a strong bias of directionalities shown by injected fluids towards the local orientation of modern-day major principal horizontal principal stress axis (S Hmax ). These two sets of independent field observations provide mutually supporting observational evidences for the general geomechanical sensitivity of faults and fractures. However, whilst peaks in flowrate correlations are observed at about 30 o to S Hmax , the preferred flooding directionalities are at smaller angles to S Hmax . A recently proposed machanism is able to explain the orientational relationships in both sets of data. It involves interacting, stress-aligned, compliant micro-cracks near a critical density; there is a large background of observations of shear-wave splitting in many types of formations that supports the prevalence of such micro-cracks. As a practical low-cost tool, analysis of flowrate correlations can provide valuable information about the major reservoir pathways as an adjunct to reservoir characterisation studies. This information can aid history-matching of reservoir models, particularly those involving fractures. The technique is also well-suited to monitoring reservoir behaviour in time-lapse fashion.","downloadable_attachments":[{"id":52380960,"asset_id":32138998,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":76442,"first_name":"Kes","last_name":"Heffer","domain_name":"hw","page_name":"KesHeffer","display_name":"Kes Heffer","profile_url":"https://hw.academia.edu/KesHeffer?f_ri=15989","photo":"https://0.academia-photos.com/76442/1765605/2109727/s65_kes.heffer.jpg"}],"research_interests":[{"id":403,"name":"Gemology","url":"https://www.academia.edu/Documents/in/Gemology?f_ri=15989","nofollow":true},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology?f_ri=15989","nofollow":true},{"id":410,"name":"Glaciology","url":"https://www.academia.edu/Documents/in/Glaciology?f_ri=15989"},{"id":411,"name":"Hydrogeology","url":"https://www.academia.edu/Documents/in/Hydrogeology?f_ri=15989"},{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989"},{"id":417,"name":"Paleontology","url":"https://www.academia.edu/Documents/in/Paleontology?f_ri=15989"},{"id":421,"name":"Soil 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href="https://www.academia.edu/9702225/Rocks_and_Minerals">Rocks and Minerals</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest">Monica Price<br />Kevin Walsh<br /><br />What are Minerals?<br />What are Rocks?<br />Rock Identification<br />Mineral Identification</div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/9702225" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="d11185409f186d8b513b3e5cc9ac44a4" rel="nofollow" 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Minerals","url":"https://www.academia.edu/Documents/in/Research_Related_to_Metallic_and_Minerals?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_33209013" data-work_id="33209013" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/33209013/S_type_granite_generation_and_emplacement_during_a_regional_switch_from_extensional_to_contractional_deformation_Central_Iberian_Zone_Iberian_autochthonous_domain_Variscan_Orogeny_">S‑type granite generation and emplacement during a regional switch from extensional to contractional deformation (Central Iberian Zone, Iberian autochthonous domain, Variscan Orogeny)</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Zircon grains extracted from S-type granites of the Mêda-Escalhão-Penedono Massif (Central Iberian Zone, Variscan Orogen) constrain the timing of emplacement and provide information about potential magma sources. Simple and composite... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_33209013" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Zircon grains extracted from S-type granites of the Mêda-Escalhão-Penedono Massif (Central Iberian Zone, Variscan Orogen) constrain the timing of emplacement and provide information about potential magma sources. Simple and composite zircon grains from three samples of S-type granite were analyzed by LA-ICP-MS. New U–Pb data indicate that granites crystallized in the Bashkirian (318.7 ± 4.8 Ma) overlapping the proposed age range of ca. 321–317 Ma of the nearby S-type granitic rocks of the Carrazeda de Anciães, Lamego and Ucanha-Vilar massifs. The timing of emplacement of such S-type granites seems to coincide with the waning stages of activity of a D2 extensional shear zone (i.e. Pinhel shear zone) developed in metamorphic conditions that reached partial melting and anatexis (ca. 321–317 Ma). Dykes of two-mica granites (resembling diatexite migmatite) are concordant and discordant to the compositional layering and S2 (main) foliation of the high-grade metamorphic rocks of the Pinhel shear zone. Much of the planar fabric in these dykes was formed during magmatic crystallization and subsequent solid-state deformation. Field relationships suggest contemporaneity between the ca. 319–317 Ma old magmatism of the study area and the switch from late D2 extensional deformation to early D3 contractional deformation. Inherited zircon cores are well preserved in these late D2-early D3 S-type granite plutons. U–Pb ages of inherited zircon cores range from ca. 2576 to ca. 421 Ma. The spectra of inherited cores overlap closely the range of detrital and magmatic zircon grains displayed by the Ediacaran to Silurian metasedimentary and metaigneous rocks of the Iberian autochthonous and parautochthonous domains. This is evidence of a genetic relationship between S-type granites and the host metamorphic rocks. There is no substantial evidence for the addition of mantle-derived material in the genesis of these late D2–early D3 S-type granitic rocks. The εNd arrays of heterogeneous crustal anatectic melts may be just inherited from the source, probably reflecting mixing of a range of crustal materials with different ages and primary isotopic signatures. The generation of the Bashkirian S-type granites has been dominated by continental crust recycling, rather than the addition of new material from mantle sources.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/33209013" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="0ec82dfabd0fb1608387e9a540c0d789" rel="nofollow" data-download="{"attachment_id":55475825,"asset_id":33209013,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/55475825/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="491020" href="https://igme-es.academia.edu/RubenDiezFernandez">Ruben Diez Fernandez</a><script data-card-contents-for-user="491020" type="text/json">{"id":491020,"first_name":"Ruben","last_name":"Diez Fernandez","domain_name":"igme-es","page_name":"RubenDiezFernandez","display_name":"Ruben Diez Fernandez","profile_url":"https://igme-es.academia.edu/RubenDiezFernandez?f_ri=15989","photo":"https://0.academia-photos.com/491020/240056/18668447/s65_ruben.diez_fernandez.jpg"}</script></span></span></li><li class="js-paper-rank-work_33209013 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="33209013"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 33209013, container: ".js-paper-rank-work_33209013", }); 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Simple and composite zircon grains from three samples of S-type granite were analyzed by LA-ICP-MS. New U–Pb data indicate that granites crystallized in the Bashkirian (318.7 ± 4.8 Ma) overlapping the proposed age range of ca. 321–317 Ma of the nearby S-type granitic rocks of the Carrazeda de Anciães, Lamego and Ucanha-Vilar massifs. The timing of emplacement of such S-type granites seems to coincide with the waning stages of activity of a D2 extensional shear zone (i.e. Pinhel shear zone) developed in metamorphic conditions that reached partial melting and anatexis (ca. 321–317 Ma). Dykes of two-mica granites (resembling diatexite migmatite) are concordant and discordant to the compositional layering and S2 (main) foliation of the high-grade metamorphic rocks of the Pinhel shear zone. Much of the planar fabric in these dykes was formed during magmatic crystallization and subsequent solid-state deformation. Field relationships suggest contemporaneity between the ca. 319–317 Ma old magmatism of the study area and the switch from late D2 extensional deformation to early D3 contractional deformation. Inherited zircon cores are well preserved in these late D2-early D3 S-type granite plutons. U–Pb ages of inherited zircon cores range from ca. 2576 to ca. 421 Ma. The spectra of inherited cores overlap closely the range of detrital and magmatic zircon grains displayed by the Ediacaran to Silurian metasedimentary and metaigneous rocks of the Iberian autochthonous and parautochthonous domains. This is evidence of a genetic relationship between S-type granites and the host metamorphic rocks. There is no substantial evidence for the addition of mantle-derived material in the genesis of these late D2–early D3 S-type granitic rocks. The εNd arrays of heterogeneous crustal anatectic melts may be just inherited from the source, probably reflecting mixing of a range of crustal materials with different ages and primary isotopic signatures. The generation of the Bashkirian S-type granites has been dominated by continental crust recycling, rather than the addition of new material from mantle sources.","downloadable_attachments":[{"id":55475825,"asset_id":33209013,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":491020,"first_name":"Ruben","last_name":"Diez Fernandez","domain_name":"igme-es","page_name":"RubenDiezFernandez","display_name":"Ruben Diez Fernandez","profile_url":"https://igme-es.academia.edu/RubenDiezFernandez?f_ri=15989","photo":"https://0.academia-photos.com/491020/240056/18668447/s65_ruben.diez_fernandez.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989","nofollow":true},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989","nofollow":true},{"id":14228,"name":"Geochronology","url":"https://www.academia.edu/Documents/in/Geochronology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":28331,"name":"Granite (Earth Sciences)","url":"https://www.academia.edu/Documents/in/Granite_Earth_Sciences_?f_ri=15989"},{"id":89567,"name":"Tectonics and Structural Geology, Metamorphic Petrology, Tectonic Geomorphology","url":"https://www.academia.edu/Documents/in/Tectonics_and_Structural_Geology_Metamorphic_Petrology_Tectonic_Geomorphology?f_ri=15989"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism?f_ri=15989"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology?f_ri=15989"},{"id":755655,"name":"Variscan Orogeny","url":"https://www.academia.edu/Documents/in/Variscan_Orogeny?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_9790276" data-work_id="9790276" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/9790276/Trajectory_analysis_concepts_and_applications">Trajectory analysis: concepts and applications</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Shoreline and shelf-edge trajectories describe the migration through time of sedimentary systems, using geomorphological breaks-in-slope that are associated with key changes in depositional processes and products. Analysis of these... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_9790276" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Shoreline and shelf-edge trajectories describe the migration through time of sedimentary systems, using geomorphological breaks-in-slope that are associated with key changes in depositional processes and products. Analysis of these trajectories provides a simple descriptive tool that complements and extends conventional sequence stratigraphic methods and models. Trajectory analysis offers four advantages over a sequence stratigraphic interpretation based on systems tracts: (1) each genetically related advance or retreat of a shoreline or shelf edge is viewed in the context of a continuously evolving depositional system, rather than as several discrete systems tracts; (2) subtle changes in depositional response (e.g. within systems tracts) can be identified and honoured; (3) trajectory analysis does not anticipate the succession of depositional events implied by systems-tract models; and (4) the descriptive emphasis of trajectory analysis does not involve any a priori assumptions about the type or nature of the mechanisms that drive sequence development. These four points allow the level of detail in a trajectory-based interpretation to be directly tailored to the available data, such that the interpretation may be qualitative or quantitative in two or three dimensions. Four classes of shoreline trajectory are recognized: ascending regressive, descending regressive, transgressive and stationary (i.e. nonmigratory). Ascending regressive and high-angle (accretionary) transgressive trajectories are associated with expanded facies belt thicknesses, the absence of laterally extensive erosional surfaces, and relatively high preservation of the shoreline depositional system. In contrast, descending regressive and low-angle (nonaccretionary) transgressive trajectories are associated with foreshortened and/or missing facies belts, the presence of laterally extensive erosional surfaces, and relatively low preservation of the shoreline depositional system. Stationary trajectories record shorelines positioned at a steeply sloping shelf edge, with accompanying bypass of sediment to the basin floor. Shelf-edge trajectories represent larger spatial and temporal scales than shoreline trajectories, and they can be subdivided into ascending, descending and stationary (i.e. nonmigratory) classes. Ascending trajectories are associated with a relatively large number and thickness of shoreline tongues (parasequences), the absence of laterally extensive erosional surfaces on the shelf, and relatively low sediment supply to the basin floor. Descending trajectories are associated with a few, thin shoreline tongues, the presence of laterally extensive erosional surfaces on the shelf, and high sediment supply to basin-floor fan systems. Stationary trajectories record near-total bypass of sediment across the shelf and mass transfer to the basin floor.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/9790276" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="91cd2bc98f354eb0e86be581b3f03eff" rel="nofollow" data-download="{"attachment_id":47645933,"asset_id":9790276,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/47645933/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="23587447" href="https://uib.academia.edu/WilliamHellandHansen">William Helland-Hansen</a><script data-card-contents-for-user="23587447" type="text/json">{"id":23587447,"first_name":"William","last_name":"Helland-Hansen","domain_name":"uib","page_name":"WilliamHellandHansen","display_name":"William Helland-Hansen","profile_url":"https://uib.academia.edu/WilliamHellandHansen?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_9790276 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="9790276"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 9790276, container: ".js-paper-rank-work_9790276", }); 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$(".js-view-count[data-work-id=9790276]").text(description); $(".js-view-count-work_9790276").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_9790276").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="9790276"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">24</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="400" rel="nofollow" href="https://www.academia.edu/Documents/in/Earth_Sciences">Earth Sciences</a>, <script data-card-contents-for-ri="400" type="text/json">{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="403" rel="nofollow" href="https://www.academia.edu/Documents/in/Gemology">Gemology</a>, <script data-card-contents-for-ri="403" type="text/json">{"id":403,"name":"Gemology","url":"https://www.academia.edu/Documents/in/Gemology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="407" rel="nofollow" href="https://www.academia.edu/Documents/in/Geochemistry">Geochemistry</a><script data-card-contents-for-ri="407" type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=9790276]'), work: {"id":9790276,"title":"Trajectory analysis: concepts and applications","created_at":"2014-12-16T00:42:45.951-08:00","url":"https://www.academia.edu/9790276/Trajectory_analysis_concepts_and_applications?f_ri=15989","dom_id":"work_9790276","summary":"Shoreline and shelf-edge trajectories describe the migration through time of sedimentary systems, using geomorphological breaks-in-slope that are associated with key changes in depositional processes and products. Analysis of these trajectories provides a simple descriptive tool that complements and extends conventional sequence stratigraphic methods and models. Trajectory analysis offers four advantages over a sequence stratigraphic interpretation based on systems tracts: (1) each genetically related advance or retreat of a shoreline or shelf edge is viewed in the context of a continuously evolving depositional system, rather than as several discrete systems tracts; (2) subtle changes in depositional response (e.g. within systems tracts) can be identified and honoured; (3) trajectory analysis does not anticipate the succession of depositional events implied by systems-tract models; and (4) the descriptive emphasis of trajectory analysis does not involve any a priori assumptions about the type or nature of the mechanisms that drive sequence development. These four points allow the level of detail in a trajectory-based interpretation to be directly tailored to the available data, such that the interpretation may be qualitative or quantitative in two or three dimensions. Four classes of shoreline trajectory are recognized: ascending regressive, descending regressive, transgressive and stationary (i.e. nonmigratory). Ascending regressive and high-angle (accretionary) transgressive trajectories are associated with expanded facies belt thicknesses, the absence of laterally extensive erosional surfaces, and relatively high preservation of the shoreline depositional system. In contrast, descending regressive and low-angle (nonaccretionary) transgressive trajectories are associated with foreshortened and/or missing facies belts, the presence of laterally extensive erosional surfaces, and relatively low preservation of the shoreline depositional system. Stationary trajectories record shorelines positioned at a steeply sloping shelf edge, with accompanying bypass of sediment to the basin floor. Shelf-edge trajectories represent larger spatial and temporal scales than shoreline trajectories, and they can be subdivided into ascending, descending and stationary (i.e. nonmigratory) classes. Ascending trajectories are associated with a relatively large number and thickness of shoreline tongues (parasequences), the absence of laterally extensive erosional surfaces on the shelf, and relatively low sediment supply to the basin floor. Descending trajectories are associated with a few, thin shoreline tongues, the presence of laterally extensive erosional surfaces on the shelf, and high sediment supply to basin-floor fan systems. Stationary trajectories record near-total bypass of sediment across the shelf and mass transfer to the basin floor.","downloadable_attachments":[{"id":47645933,"asset_id":9790276,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":23587447,"first_name":"William","last_name":"Helland-Hansen","domain_name":"uib","page_name":"WilliamHellandHansen","display_name":"William Helland-Hansen","profile_url":"https://uib.academia.edu/WilliamHellandHansen?f_ri=15989","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=15989","nofollow":true},{"id":403,"name":"Gemology","url":"https://www.academia.edu/Documents/in/Gemology?f_ri=15989","nofollow":true},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology?f_ri=15989"},{"id":410,"name":"Glaciology","url":"https://www.academia.edu/Documents/in/Glaciology?f_ri=15989"},{"id":411,"name":"Hydrogeology","url":"https://www.academia.edu/Documents/in/Hydrogeology?f_ri=15989"},{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989"},{"id":417,"name":"Paleontology","url":"https://www.academia.edu/Documents/in/Paleontology?f_ri=15989"},{"id":421,"name":"Soil Science","url":"https://www.academia.edu/Documents/in/Soil_Science?f_ri=15989"},{"id":1034,"name":"Stratigraphy","url":"https://www.academia.edu/Documents/in/Stratigraphy?f_ri=15989"},{"id":2403,"name":"Environmental Geology","url":"https://www.academia.edu/Documents/in/Environmental_Geology?f_ri=15989"},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989"},{"id":2406,"name":"Economic Geology","url":"https://www.academia.edu/Documents/in/Economic_Geology?f_ri=15989"},{"id":3869,"name":"Geobiology","url":"https://www.academia.edu/Documents/in/Geobiology?f_ri=15989"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":20564,"name":"Engineering Geology","url":"https://www.academia.edu/Documents/in/Engineering_Geology?f_ri=15989"},{"id":64108,"name":"Paleogeography","url":"https://www.academia.edu/Documents/in/Paleogeography?f_ri=15989"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism?f_ri=15989"},{"id":281011,"name":"Basin","url":"https://www.academia.edu/Documents/in/Basin?f_ri=15989"},{"id":417165,"name":"Volcanism","url":"https://www.academia.edu/Documents/in/Volcanism?f_ri=15989"},{"id":505937,"name":"Regional Geology","url":"https://www.academia.edu/Documents/in/Regional_Geology?f_ri=15989"},{"id":581258,"name":"Hazards","url":"https://www.academia.edu/Documents/in/Hazards?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_28757362" data-work_id="28757362" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/28757362/Referat_Gangguan_Depresi_Berat_dengan_Gejala_Psikotik">Referat Gangguan Depresi Berat dengan Gejala Psikotik</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">PENDAHULUAN Depresi bisa berdiri sendiri maupun bersamaan dengan penyakit organik. Depresi akan sulit di diagnosis jika depresi ditemukan bersamaan dengan penyakit lain. Banyak gangguan medis dan neurologis serta agen farmakologis dapat... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_28757362" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">PENDAHULUAN Depresi bisa berdiri sendiri maupun bersamaan dengan penyakit organik. Depresi akan sulit di diagnosis jika depresi ditemukan bersamaan dengan penyakit lain. Banyak gangguan medis dan neurologis serta agen farmakologis dapat menghasilkan gejala depresi. Biasanya pasien datang dengan gangguan depresi pertama kali pergi ke dokter umum dengan keluhan somatik, mereka mengeluh gangguan sistem endokrin, gangguan infeksi dan peradangan, serta penyakit medis lain seperti kanker dan penyakit kardiopulmonal. Baik depresi yang berdiri sendiri maupun yang bersamaan dengan penyakit lain harus diobati dengan sungguh-sungguh, karena depresi dapat mempengaruhi dan memperburuk penyakit organik yang sudah ada. Pemilihan obat anti depresan yang tepat sangat diperlukan agar mendapatkan efek terapi yang optimal dan menghindari efek samping yang mungkin timbul. DEFINISI Gangguan depresif merupakan suatu masa terganggunya fungsi manusia yang berkaitan dengan alam perasaan yang sedih dengan gejala penyerta termasuk perubahan pola tidur, nafsu makan, psikomotor, konsentrasi, anhedonia, kelelahan, rasa putus asa, tak berdaya dan gagasan bunuh diri. Depresi adalah penyakit yang menyerang "keseluruhan hidup seseorang", meliputi seluruh tubuh, suasana perasaan dan pikiran. ia juga mempengaruhi pola makan dan tidur. Gangguan ini tidak sama dengan seorang yang dalam keadaan kelelahan atau malas. Seorang yang mengalami gangguan depresi tidak dapat "menguasai diri" dan keadaaannya untuk dapat kembali pada keadaannya seperti semula. Tanpa penanganan yang baik maka gejala-gejala tersebut mengakibatkan terganggunya fungsi sosial, pekerjaan atau fungsi penting lainnya dari seseorang dan gejala tersebut berlangsungnya jadi lebih lama. Penatalaksanaan yang sesuai dapat menolong seseorang yang mengalami depresi untuk cepat kembali seperti semula lebih baik. Definisi gangguan depresi adalah gangguan mental yang dikarakteristikan dengan rasa sedih yang dalam dan berkepanjangan. Penderita hilang minat (interest) pada sesuatu yang sebelumnya menyenangkan baginya. Biasanya disertai dengan perubahan-perubahan lain pada dirinya misalnya berkurangnya energi, mudah lelah dan berkurangnya</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/28757362" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="3fa62f157df46e7e615ee639e82cb38e" rel="nofollow" data-download="{"attachment_id":49173705,"asset_id":28757362,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/49173705/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="32817600" href="https://independent.academia.edu/DepaPeow">El Luma</a><script data-card-contents-for-user="32817600" type="text/json">{"id":32817600,"first_name":"El","last_name":"Luma","domain_name":"independent","page_name":"DepaPeow","display_name":"El Luma","profile_url":"https://independent.academia.edu/DepaPeow?f_ri=15989","photo":"https://0.academia-photos.com/32817600/9975355/15230687/s65_depa.peow.jpg"}</script></span></span></li><li class="js-paper-rank-work_28757362 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="28757362"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 28757362, container: ".js-paper-rank-work_28757362", }); });</script></li><li class="js-percentile-work_28757362 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 28757362; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_28757362"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_28757362 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="28757362"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 28757362; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=28757362]").text(description); $(".js-view-count-work_28757362").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_28757362").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="28757362"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i></div><span class="InlineList-item-text u-textTruncate u-pl6x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (false) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=28757362]'), work: {"id":28757362,"title":"Referat Gangguan Depresi Berat dengan Gejala Psikotik","created_at":"2016-09-28T00:00:03.417-07:00","url":"https://www.academia.edu/28757362/Referat_Gangguan_Depresi_Berat_dengan_Gejala_Psikotik?f_ri=15989","dom_id":"work_28757362","summary":"PENDAHULUAN Depresi bisa berdiri sendiri maupun bersamaan dengan penyakit organik. Depresi akan sulit di diagnosis jika depresi ditemukan bersamaan dengan penyakit lain. Banyak gangguan medis dan neurologis serta agen farmakologis dapat menghasilkan gejala depresi. Biasanya pasien datang dengan gangguan depresi pertama kali pergi ke dokter umum dengan keluhan somatik, mereka mengeluh gangguan sistem endokrin, gangguan infeksi dan peradangan, serta penyakit medis lain seperti kanker dan penyakit kardiopulmonal. Baik depresi yang berdiri sendiri maupun yang bersamaan dengan penyakit lain harus diobati dengan sungguh-sungguh, karena depresi dapat mempengaruhi dan memperburuk penyakit organik yang sudah ada. Pemilihan obat anti depresan yang tepat sangat diperlukan agar mendapatkan efek terapi yang optimal dan menghindari efek samping yang mungkin timbul. DEFINISI Gangguan depresif merupakan suatu masa terganggunya fungsi manusia yang berkaitan dengan alam perasaan yang sedih dengan gejala penyerta termasuk perubahan pola tidur, nafsu makan, psikomotor, konsentrasi, anhedonia, kelelahan, rasa putus asa, tak berdaya dan gagasan bunuh diri. Depresi adalah penyakit yang menyerang \"keseluruhan hidup seseorang\", meliputi seluruh tubuh, suasana perasaan dan pikiran. ia juga mempengaruhi pola makan dan tidur. Gangguan ini tidak sama dengan seorang yang dalam keadaan kelelahan atau malas. Seorang yang mengalami gangguan depresi tidak dapat \"menguasai diri\" dan keadaaannya untuk dapat kembali pada keadaannya seperti semula. Tanpa penanganan yang baik maka gejala-gejala tersebut mengakibatkan terganggunya fungsi sosial, pekerjaan atau fungsi penting lainnya dari seseorang dan gejala tersebut berlangsungnya jadi lebih lama. Penatalaksanaan yang sesuai dapat menolong seseorang yang mengalami depresi untuk cepat kembali seperti semula lebih baik. Definisi gangguan depresi adalah gangguan mental yang dikarakteristikan dengan rasa sedih yang dalam dan berkepanjangan. Penderita hilang minat (interest) pada sesuatu yang sebelumnya menyenangkan baginya. Biasanya disertai dengan perubahan-perubahan lain pada dirinya misalnya berkurangnya energi, mudah lelah dan berkurangnya","downloadable_attachments":[{"id":49173705,"asset_id":28757362,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":32817600,"first_name":"El","last_name":"Luma","domain_name":"independent","page_name":"DepaPeow","display_name":"El Luma","profile_url":"https://independent.academia.edu/DepaPeow?f_ri=15989","photo":"https://0.academia-photos.com/32817600/9975355/15230687/s65_depa.peow.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_36058773 coauthored" data-work_id="36058773" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/36058773/Carbonatitic_dykes_during_Pangaea_transtension_Pelagonian_Zone_Greece_">Carbonatitic dykes during Pangaea transtension (Pelagonian Zone, Greece)</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Carbonatitic dykes surrounded by K-Na-fenites were discovered in the Pelagonian Zone in Greece. Their carbon-ate portions have an isotopic mantle signature of δ 13 C and δ 18 O ranging from −5.18 to −5.56 (‰ vs. VPDB) and from 10.68 to... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_36058773" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Carbonatitic dykes surrounded by K-Na-fenites were discovered in the Pelagonian Zone in Greece. Their carbon-ate portions have an isotopic mantle signature of δ 13 C and δ 18 O ranging from −5.18 to −5.56 (‰ vs. VPDB) and from 10.68 to 11.59 (‰ vs. VSMOW) respectively, whereas their mafic silicate portions have high Nb, Ta and ɛ Nd values, typical of alkaline basalts. Textural relationships hint at a cogenetic intrusion of silicate and carbonate liquids that according to antithetic REE profiles segregated at shallow depths (b0.6 GPa) from a parental melt sourced deeper in the mantle. Fenites bear similar REE abundances to mafic rocks but with high Rb-Ba and low Nb-Ta values. SHRIMP II U-Pb analyses of magmatic zircon cores (δ 18 O = 7.21–7.51) from a carbonate-bearing syenitic amphibolite yielded a Permian intrusion age at 278 ± 2 Ma, considerably older than a Cretaceous (118 ± 4 Ma) greenschist overprint obtained from metamorphic zircon rims (δ 18 O = 6.78–7.02). From 300 to 175 Ma the ɛ Nd of the Pelagonian magmatism rose irregularly to more primitive values attesting to a higher increment of asthenosphere-derived melts. In this context, the carbonatite formed within a transtensional regime of an intra-Pangaea dextral transform fault that signalled the forthcoming penetrating breakoff of the su-percontinent, manifested in the Permo-Triassic.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/36058773" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="9e019897e6c4412717f0a9226fca2fb6" rel="nofollow" data-download="{"attachment_id":55944285,"asset_id":36058773,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/55944285/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="77293" href="https://uoa.academia.edu/DimitriosKostopoulos">Dimitrios Kostopoulos</a><script data-card-contents-for-user="77293" type="text/json">{"id":77293,"first_name":"Dimitrios","last_name":"Kostopoulos","domain_name":"uoa","page_name":"DimitriosKostopoulos","display_name":"Dimitrios Kostopoulos","profile_url":"https://uoa.academia.edu/DimitriosKostopoulos?f_ri=15989","photo":"https://0.academia-photos.com/77293/21425/19557489/s65_dimitrios.kostopoulos.png"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-36058773">+1</span><div class="hidden js-additional-users-36058773"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://independent.academia.edu/FilippoSchenker">Filippo Luca Schenker</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-36058773'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-36058773').html(); 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container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_36058773 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="36058773"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 36058773; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=36058773]").text(description); $(".js-view-count-work_36058773").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_36058773").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="36058773"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">14</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="407" rel="nofollow" href="https://www.academia.edu/Documents/in/Geochemistry">Geochemistry</a>, <script data-card-contents-for-ri="407" type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2404" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology">Petrology</a>, <script data-card-contents-for-ri="2404" type="text/json">{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2635" rel="nofollow" href="https://www.academia.edu/Documents/in/Metamorphic_Petrology">Metamorphic Petrology</a><script data-card-contents-for-ri="2635" type="text/json">{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=36058773]'), work: {"id":36058773,"title":"Carbonatitic dykes during Pangaea transtension (Pelagonian Zone, Greece)","created_at":"2018-03-02T03:33:39.039-08:00","url":"https://www.academia.edu/36058773/Carbonatitic_dykes_during_Pangaea_transtension_Pelagonian_Zone_Greece_?f_ri=15989","dom_id":"work_36058773","summary":"Carbonatitic dykes surrounded by K-Na-fenites were discovered in the Pelagonian Zone in Greece. Their carbon-ate portions have an isotopic mantle signature of δ 13 C and δ 18 O ranging from −5.18 to −5.56 (‰ vs. VPDB) and from 10.68 to 11.59 (‰ vs. VSMOW) respectively, whereas their mafic silicate portions have high Nb, Ta and ɛ Nd values, typical of alkaline basalts. Textural relationships hint at a cogenetic intrusion of silicate and carbonate liquids that according to antithetic REE profiles segregated at shallow depths (b0.6 GPa) from a parental melt sourced deeper in the mantle. Fenites bear similar REE abundances to mafic rocks but with high Rb-Ba and low Nb-Ta values. SHRIMP II U-Pb analyses of magmatic zircon cores (δ 18 O = 7.21–7.51) from a carbonate-bearing syenitic amphibolite yielded a Permian intrusion age at 278 ± 2 Ma, considerably older than a Cretaceous (118 ± 4 Ma) greenschist overprint obtained from metamorphic zircon rims (δ 18 O = 6.78–7.02). From 300 to 175 Ma the ɛ Nd of the Pelagonian magmatism rose irregularly to more primitive values attesting to a higher increment of asthenosphere-derived melts. In this context, the carbonatite formed within a transtensional regime of an intra-Pangaea dextral transform fault that signalled the forthcoming penetrating breakoff of the su-percontinent, manifested in the Permo-Triassic.","downloadable_attachments":[{"id":55944285,"asset_id":36058773,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":77293,"first_name":"Dimitrios","last_name":"Kostopoulos","domain_name":"uoa","page_name":"DimitriosKostopoulos","display_name":"Dimitrios Kostopoulos","profile_url":"https://uoa.academia.edu/DimitriosKostopoulos?f_ri=15989","photo":"https://0.academia-photos.com/77293/21425/19557489/s65_dimitrios.kostopoulos.png"},{"id":61116883,"first_name":"Filippo Luca","last_name":"Schenker","domain_name":"independent","page_name":"FilippoSchenker","display_name":"Filippo Luca Schenker","profile_url":"https://independent.academia.edu/FilippoSchenker?f_ri=15989","photo":"https://0.academia-photos.com/61116883/18728919/18689736/s65_filippo_luca.schenker.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989","nofollow":true},{"id":7959,"name":"Stable Isotope Geochemistry","url":"https://www.academia.edu/Documents/in/Stable_Isotope_Geochemistry?f_ri=15989"},{"id":8116,"name":"Trace element Geochemistry","url":"https://www.academia.edu/Documents/in/Trace_element_Geochemistry?f_ri=15989"},{"id":15947,"name":"Geodynamics","url":"https://www.academia.edu/Documents/in/Geodynamics?f_ri=15989"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989"},{"id":20000,"name":"Radiogenic Isotope Geochemistry","url":"https://www.academia.edu/Documents/in/Radiogenic_Isotope_Geochemistry?f_ri=15989"},{"id":29674,"name":"Isotope Geochemistry","url":"https://www.academia.edu/Documents/in/Isotope_Geochemistry?f_ri=15989"},{"id":48044,"name":"Greece","url":"https://www.academia.edu/Documents/in/Greece?f_ri=15989"},{"id":99318,"name":"Geotectonics and Geodynamics","url":"https://www.academia.edu/Documents/in/Geotectonics_and_Geodynamics?f_ri=15989"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_17355707" data-work_id="17355707" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/17355707/Karakteristik_Kekar_Tiang_pada_Lava_Andesit_Daerah_Randubang_Kabupaten_Wonogiri_Provinsi_Jawa_Tengah">Karakteristik Kekar Tiang pada Lava Andesit Daerah Randubang, Kabupaten Wonogiri, Provinsi Jawa Tengah</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Kekar tiang merupakan salah satu bentukan morfologi yang sangat berkaitan dengan aktivitas vulkanik maupun intrusi. Bentukan kekar tiang ini merupakan hasil dari pendinginan yang cepat dari suatu batuan yang bersifat panas seperti lava,... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_17355707" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Kekar tiang merupakan salah satu bentukan morfologi yang sangat berkaitan dengan aktivitas vulkanik maupun intrusi. Bentukan kekar tiang ini merupakan hasil dari pendinginan yang cepat dari suatu batuan yang bersifat panas seperti lava, intrusi, maupun batuan piroklastik. Daerah penelitian terletak di daerah Randubang,Wonogiri, Jawa Tengah yang termasuk dalam Formasi Mandalika yang berumur Oligosen Akhir -Miosen Awal. Batuan yang terdapat pada daerah penelitian adalah lava andesit dan aglomerat. Struktur geologi yang ada di daerah penelitian berupa sesar geser mengiri dengan bidang sesar berarah N35 o E/76 o dan sesar turun dengan bidang sesar berarah N150 o E/80 o . Kekar tiang di daerah penelitian terbentuk dari suatu tubuh lava andesit bervolume besar yang terbentuk secara bertahap dan berulang-ulang. Secara umum, kekar tiang memiliki kemiringan yang tegak lurus (90 o ) dengan bidang pendinginan. Pada daerah penelitian ditemukan bahwa kekar tiang memiliki orientasi kemiringan yang tidak vertikal yaitu berkisarantara 5-75 o dengan arah yang bervariasi. Kekar tiang di daerah penelitian memiliki morfologi yang khas berjenis colonnade dengan bentukan segi 3, 4, 5 dan 6 dengan diameter antara 15 sentimeter hingga 1 meter. Kekar tiang di daerah penelitian memiliki dimensi panjang kolom berkisar antara 4 meter hingga 25 meter. Berdasarkan kenampakan di lapangan, struktur geologi tersebut tidak berpengaruh dominan terhadap morfologi kekar tiang tersebut. Peneliti menyimpulkan bahwa kekar tiang di daerah penelitian merupakan kekar tiang hasil pendinginan suatu masa lava andesit bervolume besar yang terbentuk secara bertahap pada paleoslope yang cukup curam. Kemiringan yang beragam dari kekar tiang pada daerah penelitian lebih dikontrol oleh aspek paleoslope. Berdasarkan interpretasi arah aliran lava dan paleslope, diperkirakan daerah penelitian merupakan pusat erupsi dari suatu gunungapi purba berbentuk dome dengan paleoslope yang curam.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/17355707" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="80b229b9f4efa0e79bedb3d1ce153e88" rel="nofollow" data-download="{"attachment_id":39464037,"asset_id":17355707,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/39464037/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="20706574" href="https://ugm.academia.edu/adityapratama">Aditya Pratama</a><script data-card-contents-for-user="20706574" type="text/json">{"id":20706574,"first_name":"Aditya","last_name":"Pratama","domain_name":"ugm","page_name":"adityapratama","display_name":"Aditya Pratama","profile_url":"https://ugm.academia.edu/adityapratama?f_ri=15989","photo":"https://0.academia-photos.com/20706574/10548393/11772542/s65_aditya.pratama.jpg"}</script></span></span></li><li class="js-paper-rank-work_17355707 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="17355707"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 17355707, container: ".js-paper-rank-work_17355707", }); });</script></li><li class="js-percentile-work_17355707 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 17355707; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_17355707"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_17355707 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="17355707"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 17355707; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=17355707]").text(description); $(".js-view-count-work_17355707").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_17355707").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="17355707"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">3</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="199072" rel="nofollow" href="https://www.academia.edu/Documents/in/Vulcanology">Vulcanology</a><script data-card-contents-for-ri="199072" type="text/json">{"id":199072,"name":"Vulcanology","url":"https://www.academia.edu/Documents/in/Vulcanology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=17355707]'), work: {"id":17355707,"title":"Karakteristik Kekar Tiang pada Lava Andesit Daerah Randubang, Kabupaten Wonogiri, Provinsi Jawa Tengah","created_at":"2015-10-27T10:41:58.496-07:00","url":"https://www.academia.edu/17355707/Karakteristik_Kekar_Tiang_pada_Lava_Andesit_Daerah_Randubang_Kabupaten_Wonogiri_Provinsi_Jawa_Tengah?f_ri=15989","dom_id":"work_17355707","summary":"Kekar tiang merupakan salah satu bentukan morfologi yang sangat berkaitan dengan aktivitas vulkanik maupun intrusi. Bentukan kekar tiang ini merupakan hasil dari pendinginan yang cepat dari suatu batuan yang bersifat panas seperti lava, intrusi, maupun batuan piroklastik. Daerah penelitian terletak di daerah Randubang,Wonogiri, Jawa Tengah yang termasuk dalam Formasi Mandalika yang berumur Oligosen Akhir -Miosen Awal. Batuan yang terdapat pada daerah penelitian adalah lava andesit dan aglomerat. Struktur geologi yang ada di daerah penelitian berupa sesar geser mengiri dengan bidang sesar berarah N35 o E/76 o dan sesar turun dengan bidang sesar berarah N150 o E/80 o . Kekar tiang di daerah penelitian terbentuk dari suatu tubuh lava andesit bervolume besar yang terbentuk secara bertahap dan berulang-ulang. Secara umum, kekar tiang memiliki kemiringan yang tegak lurus (90 o ) dengan bidang pendinginan. Pada daerah penelitian ditemukan bahwa kekar tiang memiliki orientasi kemiringan yang tidak vertikal yaitu berkisarantara 5-75 o dengan arah yang bervariasi. Kekar tiang di daerah penelitian memiliki morfologi yang khas berjenis colonnade dengan bentukan segi 3, 4, 5 dan 6 dengan diameter antara 15 sentimeter hingga 1 meter. Kekar tiang di daerah penelitian memiliki dimensi panjang kolom berkisar antara 4 meter hingga 25 meter. Berdasarkan kenampakan di lapangan, struktur geologi tersebut tidak berpengaruh dominan terhadap morfologi kekar tiang tersebut. Peneliti menyimpulkan bahwa kekar tiang di daerah penelitian merupakan kekar tiang hasil pendinginan suatu masa lava andesit bervolume besar yang terbentuk secara bertahap pada paleoslope yang cukup curam. Kemiringan yang beragam dari kekar tiang pada daerah penelitian lebih dikontrol oleh aspek paleoslope. Berdasarkan interpretasi arah aliran lava dan paleslope, diperkirakan daerah penelitian merupakan pusat erupsi dari suatu gunungapi purba berbentuk dome dengan paleoslope yang curam.","downloadable_attachments":[{"id":39464037,"asset_id":17355707,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":20706574,"first_name":"Aditya","last_name":"Pratama","domain_name":"ugm","page_name":"adityapratama","display_name":"Aditya Pratama","profile_url":"https://ugm.academia.edu/adityapratama?f_ri=15989","photo":"https://0.academia-photos.com/20706574/10548393/11772542/s65_aditya.pratama.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":199072,"name":"Vulcanology","url":"https://www.academia.edu/Documents/in/Vulcanology?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_29345476 coauthored" data-work_id="29345476" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/29345476/Slab_rollback_ignimbrite_flareups_in_the_southern_Great_Basin_and_other_Cenozoic_American_arcs_A_distinct_style_of_arc_volcanism">Slab-rollback ignimbrite flareups in the southern Great Basin and other Cenozoic American arcs: A distinct style of arc volcanism</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">In continental-margin subduction zones, basalt magmas spawned in the mantle interact with the crust to produce a broad spectrum of volcanic arc associations. A distinct style of very voluminous arc volcanism develops far inland on thick... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_29345476" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">In continental-margin subduction zones, basalt magmas spawned in the mantle interact with the crust to produce a broad spectrum of volcanic arc associations. A distinct style of very voluminous arc volcanism develops far inland on thick crust over periods of 10–20 m.y. and involves relatively infrequent caldera-forming explosive eruptions of dominantly calc-alkaline rhyo-lite, dacite, and trachydacite with repose times of 10 4 –10 6 yr. Volumes of individual eruptions are large (10 2 –10 3 km 3), and nested super-eruptions of thousands of cubic kilometers are common. Calderas are as much as 60–75 km in diameter , and surrounding individual ignimbrite outflow sheets extend outward as much as 150 km, blanketing upwards of 10 5 km 2. Little or no basalt is extruded, whereas andesitic differentiates coeval with silicic ignimbrites range from minor to dominant in relative volume. A common feature in these flareups is essentially nonextending, thick, inland crust overlying a subducting oceanic plate with transverse tears that rolled back to a steeper dip from a previously flat configuration. Lithospheric delamination is locally possible. Large volumes of basalt that provide heat and mass for silicic magma generation in the crust form by fluid fluxing of the growing mantle wedge overlying the steep-ening dehydrating slab and from asthenospheric decompression. Variations in the mantle input, together with variations in crustal thickness, temperature, and composition, modulate the expression of the flareups. As a consequence of the high flux of mantle-derived magma into the thick crust, geotherms become elevated, and the brittle-ductile transition can rise to depths as shallow as 7 km. At this transition, diapirically rising magmas from a melting, assimilation , storage, and homogenization (MASH) zone are blocked and spread laterally into discoid chambers that grow until a thermomechanical threshold is attained, triggering climactic eruption and caldera collapse. This ignimbrite flareup style of continental arc volcanism is exemplified by the mid-Cenozoic southern Great Basin ignimbrite province; other examples include the contemporaneous Southern Rocky Mountain, Mogollon-Datil, vast Sierra Madre Occidental volcanic fields, and the late Cenozoic Altiplano-Puna volcanic complex in the Central Andes. Rhyolitic and trachydacitic ignimbrites typically have erupted, but where the crust was predominantly felsic, prewarmed, and orogenically thickened, well-developed MASH zones have spawned multiple super-eruptions of phenocryst-rich dacite, or monotonous intermediates, and smaller volumes of calc-alkaline rhyolite ignimbrite. In the Great Basin, eruptions of dry, hot trachydacite magma followed the monotonous intermediates. Partial melting in thinner crust with a major mafic component yielded more alkalic rhyolite and related trachydacite.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/29345476" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="30648e6efe625cffa7e77159d9edb8e4" rel="nofollow" data-download="{"attachment_id":49787443,"asset_id":29345476,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/49787443/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="76756" href="https://byu.academia.edu/EricChristiansen">Eric H Christiansen</a><script data-card-contents-for-user="76756" type="text/json">{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H Christiansen","profile_url":"https://byu.academia.edu/EricChristiansen?f_ri=15989","photo":"https://0.academia-photos.com/76756/84665/284057/s65_eric.christiansen.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-29345476">+2</span><div class="hidden js-additional-users-29345476"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://unitedstatesgeologicalsurvey.academia.edu/PeterLipman">Peter Lipman</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://oregonstate.academia.edu/ShandeSilva">Shan de Silva</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-29345476'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-29345476').html(); 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container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_29345476 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="29345476"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 29345476; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=29345476]").text(description); $(".js-view-count-work_29345476").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_29345476").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="29345476"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">4</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="16067" rel="nofollow" href="https://www.academia.edu/Documents/in/Caldera_Volcanoes">Caldera Volcanoes</a>, <script data-card-contents-for-ri="16067" type="text/json">{"id":16067,"name":"Caldera Volcanoes","url":"https://www.academia.edu/Documents/in/Caldera_Volcanoes?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="45278" rel="nofollow" href="https://www.academia.edu/Documents/in/Large_Igneous_Provinces">Large Igneous Provinces</a>, <script data-card-contents-for-ri="45278" type="text/json">{"id":45278,"name":"Large Igneous Provinces","url":"https://www.academia.edu/Documents/in/Large_Igneous_Provinces?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="275969" rel="nofollow" href="https://www.academia.edu/Documents/in/Ignimbrite">Ignimbrite</a><script data-card-contents-for-ri="275969" type="text/json">{"id":275969,"name":"Ignimbrite","url":"https://www.academia.edu/Documents/in/Ignimbrite?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=29345476]'), work: {"id":29345476,"title":"Slab-rollback ignimbrite flareups in the southern Great Basin and other Cenozoic American arcs: A distinct style of arc volcanism","created_at":"2016-10-22T07:12:05.411-07:00","url":"https://www.academia.edu/29345476/Slab_rollback_ignimbrite_flareups_in_the_southern_Great_Basin_and_other_Cenozoic_American_arcs_A_distinct_style_of_arc_volcanism?f_ri=15989","dom_id":"work_29345476","summary":"In continental-margin subduction zones, basalt magmas spawned in the mantle interact with the crust to produce a broad spectrum of volcanic arc associations. A distinct style of very voluminous arc volcanism develops far inland on thick crust over periods of 10–20 m.y. and involves relatively infrequent caldera-forming explosive eruptions of dominantly calc-alkaline rhyo-lite, dacite, and trachydacite with repose times of 10 4 –10 6 yr. Volumes of individual eruptions are large (10 2 –10 3 km 3), and nested super-eruptions of thousands of cubic kilometers are common. Calderas are as much as 60–75 km in diameter , and surrounding individual ignimbrite outflow sheets extend outward as much as 150 km, blanketing upwards of 10 5 km 2. Little or no basalt is extruded, whereas andesitic differentiates coeval with silicic ignimbrites range from minor to dominant in relative volume. A common feature in these flareups is essentially nonextending, thick, inland crust overlying a subducting oceanic plate with transverse tears that rolled back to a steeper dip from a previously flat configuration. Lithospheric delamination is locally possible. Large volumes of basalt that provide heat and mass for silicic magma generation in the crust form by fluid fluxing of the growing mantle wedge overlying the steep-ening dehydrating slab and from asthenospheric decompression. Variations in the mantle input, together with variations in crustal thickness, temperature, and composition, modulate the expression of the flareups. As a consequence of the high flux of mantle-derived magma into the thick crust, geotherms become elevated, and the brittle-ductile transition can rise to depths as shallow as 7 km. At this transition, diapirically rising magmas from a melting, assimilation , storage, and homogenization (MASH) zone are blocked and spread laterally into discoid chambers that grow until a thermomechanical threshold is attained, triggering climactic eruption and caldera collapse. This ignimbrite flareup style of continental arc volcanism is exemplified by the mid-Cenozoic southern Great Basin ignimbrite province; other examples include the contemporaneous Southern Rocky Mountain, Mogollon-Datil, vast Sierra Madre Occidental volcanic fields, and the late Cenozoic Altiplano-Puna volcanic complex in the Central Andes. Rhyolitic and trachydacitic ignimbrites typically have erupted, but where the crust was predominantly felsic, prewarmed, and orogenically thickened, well-developed MASH zones have spawned multiple super-eruptions of phenocryst-rich dacite, or monotonous intermediates, and smaller volumes of calc-alkaline rhyolite ignimbrite. In the Great Basin, eruptions of dry, hot trachydacite magma followed the monotonous intermediates. Partial melting in thinner crust with a major mafic component yielded more alkalic rhyolite and related trachydacite.","downloadable_attachments":[{"id":49787443,"asset_id":29345476,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H Christiansen","profile_url":"https://byu.academia.edu/EricChristiansen?f_ri=15989","photo":"https://0.academia-photos.com/76756/84665/284057/s65_eric.christiansen.jpg"},{"id":40919085,"first_name":"Peter","last_name":"Lipman","domain_name":"unitedstatesgeologicalsurvey","page_name":"PeterLipman","display_name":"Peter Lipman","profile_url":"https://unitedstatesgeologicalsurvey.academia.edu/PeterLipman?f_ri=15989","photo":"/images/s65_no_pic.png"},{"id":19120620,"first_name":"Shan","last_name":"de Silva","domain_name":"oregonstate","page_name":"ShandeSilva","display_name":"Shan de Silva","profile_url":"https://oregonstate.academia.edu/ShandeSilva?f_ri=15989","photo":"https://0.academia-photos.com/19120620/10906235/12171077/s65_shan.de_silva.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16067,"name":"Caldera Volcanoes","url":"https://www.academia.edu/Documents/in/Caldera_Volcanoes?f_ri=15989","nofollow":true},{"id":45278,"name":"Large Igneous Provinces","url":"https://www.academia.edu/Documents/in/Large_Igneous_Provinces?f_ri=15989","nofollow":true},{"id":275969,"name":"Ignimbrite","url":"https://www.academia.edu/Documents/in/Ignimbrite?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_12097213" data-work_id="12097213" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/12097213/FRAMBOIDS_FROM_THEIR_ORIGIN_TO_APPLICATION">FRAMBOIDS: FROM THEIR ORIGIN TO APPLICATION</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Framboids, spherical aggregates of minute, usually pyrite, grains are the commonest texture of sulfides in sedimentary rocks. They also occur in many other environments, ranging from magmatic rocks to antiquarian books. Framboidal... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_12097213" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Framboids, spherical aggregates of minute, usually pyrite, grains are the commonest texture of sulfides in sedimentary rocks. They also occur in many other environments, ranging from magmatic rocks to antiquarian books. Framboidal textures are formed by several minerals including copper and zinc sulfides, greigite, magnetite, magnesioferrite or hematite, as the products of both primary deposition and replacement. Special attention is paid to pyrite framboids in this paper, with detailed descriptions of different framboid-related forms: annular framboids, sunflower framboids, micro- and polyframboids. Framboidal forms are often hierarchically structured over three size scales, with complexities ranging from microframboids, to framboids, and to polyframboids. Pyrite in framboids results from inorganic reactions between dissolved iron and sulfide, with a greigite intermediary. The sulfur is usually biogenic in origin. Simple pyrite framboids are formed during aggregation, possibly enhanced by the magnetic properties of the monosulfide precursor. Further processes, including particulation and organically controlled aggregation, result in more complicated forms such as polyframboids. Pyrite framboids can grow to euhedral grains provided the supply of iron and sulfide is not limited. Pyrite framboids often occur in close spatial relationship with organic matter, silica or carbonates, which influence their formation and growth. Replacement of iron sulfide framboid-related forms by other minerals can be indicative of sediment diagenetic conditions, or additional processes such as mineralization in ore deposits. Framboids influence the distribution of many trace elements. Due to their high specific surface areas, framboids can accumulate these trace elements during growth. Recrystallization of framboids can redistribute many trace elements. An overview of the common association between pyrite framboids and fossils is given, stressing both the importance of organic matter in framboid formation, and of the framboids in the processes of mineralization and preservation of fossils. Iron sulfide framboids may have influenced the earliest stages of life formation on the Earth as a source of energy and catalytic action, by accumulating organic compounds, and by acting as reaction chambers and templates which facilitated reproduction and information transfer. Applications from framboid studies are presented, ranging from determination of the redox conditions in water and sediment columns using size and distribution of framboids, to evaluation of deterioration processes in museum specimens.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/12097213" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="f8c87c58f940daa572cfe41f43a93429" rel="nofollow" data-download="{"attachment_id":37414368,"asset_id":12097213,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/37414368/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="3354303" href="https://jagiellonian.academia.edu/ZbigniewSawlowicz">Zbigniew Sawlowicz</a><script data-card-contents-for-user="3354303" type="text/json">{"id":3354303,"first_name":"Zbigniew","last_name":"Sawlowicz","domain_name":"jagiellonian","page_name":"ZbigniewSawlowicz","display_name":"Zbigniew Sawlowicz","profile_url":"https://jagiellonian.academia.edu/ZbigniewSawlowicz?f_ri=15989","photo":"https://0.academia-photos.com/3354303/18209105/18189028/s65_zbigniew.sawlowicz.jpg"}</script></span></span></li><li class="js-paper-rank-work_12097213 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="12097213"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 12097213, container: ".js-paper-rank-work_12097213", }); 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$(".js-view-count[data-work-id=12097213]").text(description); $(".js-view-count-work_12097213").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_12097213").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="12097213"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">14</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="414" rel="nofollow" href="https://www.academia.edu/Documents/in/Mineralogy">Mineralogy</a>, <script data-card-contents-for-ri="414" type="text/json">{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="20092" rel="nofollow" href="https://www.academia.edu/Documents/in/Sedimentary_Petrology">Sedimentary Petrology</a>, <script data-card-contents-for-ri="20092" type="text/json">{"id":20092,"name":"Sedimentary Petrology","url":"https://www.academia.edu/Documents/in/Sedimentary_Petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="46378" rel="nofollow" href="https://www.academia.edu/Documents/in/Ore_Geology">Ore Geology</a><script data-card-contents-for-ri="46378" type="text/json">{"id":46378,"name":"Ore Geology","url":"https://www.academia.edu/Documents/in/Ore_Geology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=12097213]'), work: {"id":12097213,"title":"FRAMBOIDS: FROM THEIR ORIGIN TO APPLICATION","created_at":"2015-04-24T16:26:12.658-07:00","url":"https://www.academia.edu/12097213/FRAMBOIDS_FROM_THEIR_ORIGIN_TO_APPLICATION?f_ri=15989","dom_id":"work_12097213","summary":"Framboids, spherical aggregates of minute, usually pyrite, grains are the commonest texture of sulfides in sedimentary rocks. They also occur in many other environments, ranging from magmatic rocks to antiquarian books. Framboidal textures are formed by several minerals including copper and zinc sulfides, greigite, magnetite, magnesioferrite or hematite, as the products of both primary deposition and replacement. Special attention is paid to pyrite framboids in this paper, with detailed descriptions of different framboid-related forms: annular framboids, sunflower framboids, micro- and polyframboids. Framboidal forms are often hierarchically structured over three size scales, with complexities ranging from microframboids, to framboids, and to polyframboids. Pyrite in framboids results from inorganic reactions between dissolved iron and sulfide, with a greigite intermediary. The sulfur is usually biogenic in origin. Simple pyrite framboids are formed during aggregation, possibly enhanced by the magnetic properties of the monosulfide precursor. Further processes, including particulation and organically controlled aggregation, result in more complicated forms such as polyframboids. Pyrite framboids can grow to euhedral grains provided the supply of iron and sulfide is not limited. Pyrite framboids often occur in close spatial relationship with organic matter, silica or carbonates, which influence their formation and growth. Replacement of iron sulfide framboid-related forms by other minerals can be indicative of sediment diagenetic conditions, or additional processes such as mineralization in ore deposits. Framboids influence the distribution of many trace elements. Due to their high specific surface areas, framboids can accumulate these trace elements during growth. Recrystallization of framboids can redistribute many trace elements. An overview of the common association between pyrite framboids and fossils is given, stressing both the importance of organic matter in framboid formation, and of the framboids in the processes of mineralization and preservation of fossils. Iron sulfide framboids may have influenced the earliest stages of life formation on the Earth as a source of energy and catalytic action, by accumulating organic compounds, and by acting as reaction chambers and templates which facilitated reproduction and information transfer. Applications from framboid studies are presented, ranging from determination of the redox conditions in water and sediment columns using size and distribution of framboids, to evaluation of deterioration processes in museum specimens.","downloadable_attachments":[{"id":37414368,"asset_id":12097213,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":3354303,"first_name":"Zbigniew","last_name":"Sawlowicz","domain_name":"jagiellonian","page_name":"ZbigniewSawlowicz","display_name":"Zbigniew Sawlowicz","profile_url":"https://jagiellonian.academia.edu/ZbigniewSawlowicz?f_ri=15989","photo":"https://0.academia-photos.com/3354303/18209105/18189028/s65_zbigniew.sawlowicz.jpg"}],"research_interests":[{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":20092,"name":"Sedimentary Petrology","url":"https://www.academia.edu/Documents/in/Sedimentary_Petrology?f_ri=15989","nofollow":true},{"id":46378,"name":"Ore Geology","url":"https://www.academia.edu/Documents/in/Ore_Geology?f_ri=15989","nofollow":true},{"id":77334,"name":"Ore deposits","url":"https://www.academia.edu/Documents/in/Ore_deposits?f_ri=15989"},{"id":156636,"name":"Pyrite","url":"https://www.academia.edu/Documents/in/Pyrite?f_ri=15989"},{"id":205552,"name":"Pyrite Oxidation","url":"https://www.academia.edu/Documents/in/Pyrite_Oxidation?f_ri=15989"},{"id":214347,"name":"Pyrite Formation","url":"https://www.academia.edu/Documents/in/Pyrite_Formation?f_ri=15989"},{"id":350912,"name":"Genesis of ore deposits","url":"https://www.academia.edu/Documents/in/Genesis_of_ore_deposits?f_ri=15989"},{"id":403211,"name":"Ore Geochmistry","url":"https://www.academia.edu/Documents/in/Ore_Geochmistry?f_ri=15989"},{"id":474988,"name":"Black shale + Pyrite","url":"https://www.academia.edu/Documents/in/Black_shale_Pyrite?f_ri=15989"},{"id":517313,"name":"Mineral Prospecting/Mineral Exploration/Field Geology/Ore mineralogy/Petrography/Ore Deposits Modeling","url":"https://www.academia.edu/Documents/in/Mineral_Prospecting_Mineral_Exploration_Field_Geology_Ore_mineralogy_Petrography_Ore_Deposits_Modeli?f_ri=15989"},{"id":727346,"name":"Ore Textures","url":"https://www.academia.edu/Documents/in/Ore_Textures?f_ri=15989"},{"id":902071,"name":"Ore Forming","url":"https://www.academia.edu/Documents/in/Ore_Forming?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_37358317 coauthored" data-work_id="37358317" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/37358317/International_Geology_Review_The_Eastern_Makran_Ophiolite_SE_Iran_evidence_for_a_Late_Cretaceous_fore_arc_oceanic_crust">International Geology Review The Eastern Makran Ophiolite (SE Iran): evidence for a Late Cretaceous fore-arc oceanic crust</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The nature, magmatic evolution, and geodynamic setting of both inner and outer Makran ophiolites, in SE Iran, are enigmatic. Here, we report mineral chemistry, whole-rock geochemistry, and Sr–Nd–Pb isotope composition of mantle... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_37358317" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The nature, magmatic evolution, and geodynamic setting of both inner and outer Makran ophiolites, in SE Iran, are enigmatic. Here, we report mineral chemistry, whole-rock geochemistry, and Sr–Nd–Pb isotope composition of mantle peridotites and igneous rocks from the Eastern Makran Ophiolite (EMO) to assess the origin and tectono-magmatic evolution of the Makran oceanic realm. The EMO includes mantle peridotites (both harzburgites and impregnated lherzolites), isotropic gabbros, diabase dikes, and basaltic to andesitic pillow and massive lava flows. The Late Cretaceous pelagic limestones are found as covers of lava flows and/or interlayers between them. All ophiolite components<br />are somehow sheared and fragmented, probably in Cenozoic time, during the emplacement of ophiolite. This event has produced a considerable extent of tectonic melange. Tectonic slices of trachy-basaltic lavas with oceanic island basalt (OIB)-like signature seal the tectonic melange. Our new geochemical data indicate a magmatic evolution from fore-arc basalt (FAB) to island-arc tholeiite (IAT)-like signatures for the Late Cretaceous EMO lavas. EMO extrusive rocks have high εNd(t) (+8 to +8.9) and isotopically are similar to the Oman lavas. This isotopic signature indicates a depleted mid-ocean ridge basalt (MORB) mantle source for the genesis of these rocks, except isotopic gabbros containing lower εNd(t) (+5.1 to +5.7) and thus show higher contribution of subducted slab components in their mantle source. High 207Pb/204Pb and 208Pb/204Pb isotopic ratios for the EMO igneous rocks also suggest considerable involvement of slab-derived components into the mantle source of these rocks. The variable geochemical signatures of the EMO lavas are mostly similar to Zagros and Oman ophiolite magmatic rocks, although the Pb isotopic composition shows similarity to the isotopic characteristic of inner Zagros ophiolite belt. This study postulates that the EMO formed during the early stages of Neo-Tethyan subduction initiation beneath the Lut block in a proto-forearc basin. We suggest subduction initiation caused asthenospheric upwelling and thereafter melting to generate<br />the MORB-like melts. This event left the harzburgitic residues and the MORB-like melts interacted with the surrounding peridotites to generate the impregnated lherzolites, which are quite abundant in the EMO. Therefore, these lherzolites formed due to the refertilization of mantle rocks through porous flows of MORB-like melts. The inception of subduction caused mantle wedge to be enriched slightly by the slab components. Melting of these metasomatized mantle generated isotropic gabbros and basaltic to andesitic lavas with FAB-like signature. At the later stage, higher contribution of the slab derived components into the overlying mantle wedge causes formation of diabase dikes with suprasubduction zone – or IAT-like signatures. Trachy-basalts were probably the result of late-stage magmatism fed by the melts originated from an OIB source asthenospheric mantle due to slab break-off. This occurred after emplacement of EMO and the formation of tectonic melange</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/37358317" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="f5084d791c7da7174b44080ae2a6b377" rel="nofollow" data-download="{"attachment_id":57319121,"asset_id":37358317,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/57319121/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="22204163" href="https://iasbs.academia.edu/ImanMonsef">Iman Monsef</a><script data-card-contents-for-user="22204163" type="text/json">{"id":22204163,"first_name":"Iman","last_name":"Monsef","domain_name":"iasbs","page_name":"ImanMonsef","display_name":"Iman Monsef","profile_url":"https://iasbs.academia.edu/ImanMonsef?f_ri=15989","photo":"https://0.academia-photos.com/22204163/24164537/23123290/s65_iman.monsef.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-37358317">+1</span><div class="hidden js-additional-users-37358317"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-37358317'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-37358317').html(); 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Here, we report mineral chemistry, whole-rock geochemistry, and Sr–Nd–Pb isotope composition of mantle peridotites and igneous rocks from the Eastern Makran Ophiolite (EMO) to assess the origin and tectono-magmatic evolution of the Makran oceanic realm. The EMO includes mantle peridotites (both harzburgites and impregnated lherzolites), isotropic gabbros, diabase dikes, and basaltic to andesitic pillow and massive lava flows. The Late Cretaceous pelagic limestones are found as covers of lava flows and/or interlayers between them. All ophiolite components\nare somehow sheared and fragmented, probably in Cenozoic time, during the emplacement of ophiolite. This event has produced a considerable extent of tectonic melange. Tectonic slices of trachy-basaltic lavas with oceanic island basalt (OIB)-like signature seal the tectonic melange. Our new geochemical data indicate a magmatic evolution from fore-arc basalt (FAB) to island-arc tholeiite (IAT)-like signatures for the Late Cretaceous EMO lavas. EMO extrusive rocks have high εNd(t) (+8 to +8.9) and isotopically are similar to the Oman lavas. This isotopic signature indicates a depleted mid-ocean ridge basalt (MORB) mantle source for the genesis of these rocks, except isotopic gabbros containing lower εNd(t) (+5.1 to +5.7) and thus show higher contribution of subducted slab components in their mantle source. High 207Pb/204Pb and 208Pb/204Pb isotopic ratios for the EMO igneous rocks also suggest considerable involvement of slab-derived components into the mantle source of these rocks. The variable geochemical signatures of the EMO lavas are mostly similar to Zagros and Oman ophiolite magmatic rocks, although the Pb isotopic composition shows similarity to the isotopic characteristic of inner Zagros ophiolite belt. This study postulates that the EMO formed during the early stages of Neo-Tethyan subduction initiation beneath the Lut block in a proto-forearc basin. We suggest subduction initiation caused asthenospheric upwelling and thereafter melting to generate\nthe MORB-like melts. This event left the harzburgitic residues and the MORB-like melts interacted with the surrounding peridotites to generate the impregnated lherzolites, which are quite abundant in the EMO. Therefore, these lherzolites formed due to the refertilization of mantle rocks through porous flows of MORB-like melts. The inception of subduction caused mantle wedge to be enriched slightly by the slab components. Melting of these metasomatized mantle generated isotropic gabbros and basaltic to andesitic lavas with FAB-like signature. At the later stage, higher contribution of the slab derived components into the overlying mantle wedge causes formation of diabase dikes with suprasubduction zone – or IAT-like signatures. Trachy-basalts were probably the result of late-stage magmatism fed by the melts originated from an OIB source asthenospheric mantle due to slab break-off. This occurred after emplacement of EMO and the formation of tectonic melange","downloadable_attachments":[{"id":57319121,"asset_id":37358317,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":22204163,"first_name":"Iman","last_name":"Monsef","domain_name":"iasbs","page_name":"ImanMonsef","display_name":"Iman Monsef","profile_url":"https://iasbs.academia.edu/ImanMonsef?f_ri=15989","photo":"https://0.academia-photos.com/22204163/24164537/23123290/s65_iman.monsef.jpg"},{"id":10246740,"first_name":"Michel","last_name":"Gregoire","domain_name":"omp","page_name":"MichelGregoire","display_name":"Michel Gregoire","profile_url":"https://omp.academia.edu/MichelGregoire?f_ri=15989","photo":"https://0.academia-photos.com/10246740/3143594/153643901/s65_michel.gregoire.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites?f_ri=15989","nofollow":true},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_34239282" data-work_id="34239282" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/34239282/GEOLOGI_DAN_ALTERASI_HIDROTERMAL_PADA_DAERAH_KEBONAGUNG_DAN_SEKITARNYA_KECAMATAN_KEBONAGUNG_KABUPATEN_PACITAN_PROVINSI_JAWATIMUR">GEOLOGI DAN ALTERASI HIDROTERMAL PADA DAERAH KEBONAGUNG DAN SEKITARNYA KECAMATAN KEBONAGUNG, KABUPATEN PACITAN, PROVINSI JAWATIMUR</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Batuan di daerah penelitian terdiri atas 5 satuan, yaitu intrusi batuan andesit yang secara umum berwarna abu-abu dan telah mengalami proses alterasi hidrothermal yang berumur oligosen akhir hingga miosen awal yang mana batuan beku inilah... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_34239282" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Batuan di daerah penelitian terdiri atas 5 satuan, yaitu intrusi batuan andesit yang secara umum berwarna abu-abu dan telah mengalami proses alterasi hidrothermal yang berumur oligosen akhir hingga miosen awal yang mana batuan beku inilah yang menjadi sumber panas pada daerah penelitian. Satuan batugamping kristalin yang berwarna putih-coklatmuda dengan umur miosen awal yang mengendap secara lokal di daerah penelitian. Setelah itu dilanjutkan dengan pengendapan satuan breksi vulkanik dengan komposisi fragmen yang umumnya terdiri dari batuan andesit berumur miosen tengah. Dan diikuti oleh pengendapan satuan batugamping terumbu yang berwarna putih pada daerah utara dan selatan daerah penelitian, berumur miosen akhir. Dan pada kuarter mulai terendapkan kembali endapan aluvial disekitar sungai Karanganyar. Berdasarkan analisa sayatan tipis, mineragrafi dan analisa XRD pada sampel batuan, hadir dua zona alterasi di daerah penelitian yaitu zona alterasi klorit-albit-epidot-pyrite dengan kisaran suhu sekitar ± 250°-320°C, dengan pH 6-7 dan zona alterasi kuarsa-karbonat-lempung-pyrite dengan kisaran temperatur ± 200°-300°C, dengan pH 4-6. Selanjutnya, mengacu kepada kesebandingan oleh Corbett dan Leach (1997), zona-zona alterasi tersebut disebandingkan menjadi zona propilitik dan zona filik. Dan dari hasil pengamatan analisa petrografi diinterpretasikan zonasi klorit-albit-epidot-pyrite hadir pertama dan diikuti dengan zonasi kuarsa-karbonat-lempung-pyrite muncul diakhir karena terlihat adanya overprinting dari mineral kuarsa dan mineral karbonat pada beberapa mineral klorit.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/34239282" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="ca7820c86fee3e2a4bc14180054f8d33" rel="nofollow" data-download="{"attachment_id":54153247,"asset_id":34239282,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/54153247/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="61892884" href="https://independent.academia.edu/MardikaHari">Hari Mardika</a><script data-card-contents-for-user="61892884" type="text/json">{"id":61892884,"first_name":"Hari","last_name":"Mardika","domain_name":"independent","page_name":"MardikaHari","display_name":"Hari Mardika","profile_url":"https://independent.academia.edu/MardikaHari?f_ri=15989","photo":"https://0.academia-photos.com/61892884/16072164/16537672/s65_hari.mardika.jpg"}</script></span></span></li><li class="js-paper-rank-work_34239282 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="34239282"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 34239282, container: ".js-paper-rank-work_34239282", }); 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$(".js-view-count[data-work-id=34239282]").text(description); $(".js-view-count-work_34239282").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_34239282").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="34239282"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">6</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="414" rel="nofollow" href="https://www.academia.edu/Documents/in/Mineralogy">Mineralogy</a>, <script data-card-contents-for-ri="414" type="text/json">{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2404" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology">Petrology</a>, <script data-card-contents-for-ri="2404" type="text/json">{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=34239282]'), work: {"id":34239282,"title":"GEOLOGI DAN ALTERASI HIDROTERMAL PADA DAERAH KEBONAGUNG DAN SEKITARNYA KECAMATAN KEBONAGUNG, KABUPATEN PACITAN, PROVINSI JAWATIMUR","created_at":"2017-08-16T02:51:04.124-07:00","url":"https://www.academia.edu/34239282/GEOLOGI_DAN_ALTERASI_HIDROTERMAL_PADA_DAERAH_KEBONAGUNG_DAN_SEKITARNYA_KECAMATAN_KEBONAGUNG_KABUPATEN_PACITAN_PROVINSI_JAWATIMUR?f_ri=15989","dom_id":"work_34239282","summary":"Batuan di daerah penelitian terdiri atas 5 satuan, yaitu intrusi batuan andesit yang secara umum berwarna abu-abu dan telah mengalami proses alterasi hidrothermal yang berumur oligosen akhir hingga miosen awal yang mana batuan beku inilah yang menjadi sumber panas pada daerah penelitian. Satuan batugamping kristalin yang berwarna putih-coklatmuda dengan umur miosen awal yang mengendap secara lokal di daerah penelitian. Setelah itu dilanjutkan dengan pengendapan satuan breksi vulkanik dengan komposisi fragmen yang umumnya terdiri dari batuan andesit berumur miosen tengah. Dan diikuti oleh pengendapan satuan batugamping terumbu yang berwarna putih pada daerah utara dan selatan daerah penelitian, berumur miosen akhir. Dan pada kuarter mulai terendapkan kembali endapan aluvial disekitar sungai Karanganyar. Berdasarkan analisa sayatan tipis, mineragrafi dan analisa XRD pada sampel batuan, hadir dua zona alterasi di daerah penelitian yaitu zona alterasi klorit-albit-epidot-pyrite dengan kisaran suhu sekitar ± 250°-320°C, dengan pH 6-7 dan zona alterasi kuarsa-karbonat-lempung-pyrite dengan kisaran temperatur ± 200°-300°C, dengan pH 4-6. Selanjutnya, mengacu kepada kesebandingan oleh Corbett dan Leach (1997), zona-zona alterasi tersebut disebandingkan menjadi zona propilitik dan zona filik. Dan dari hasil pengamatan analisa petrografi diinterpretasikan zonasi klorit-albit-epidot-pyrite hadir pertama dan diikuti dengan zonasi kuarsa-karbonat-lempung-pyrite muncul diakhir karena terlihat adanya overprinting dari mineral kuarsa dan mineral karbonat pada beberapa mineral klorit.","downloadable_attachments":[{"id":54153247,"asset_id":34239282,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":61892884,"first_name":"Hari","last_name":"Mardika","domain_name":"independent","page_name":"MardikaHari","display_name":"Hari Mardika","profile_url":"https://independent.academia.edu/MardikaHari?f_ri=15989","photo":"https://0.academia-photos.com/61892884/16072164/16537672/s65_hari.mardika.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989","nofollow":true},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":17285,"name":"Field Geology","url":"https://www.academia.edu/Documents/in/Field_Geology?f_ri=15989"},{"id":200896,"name":"Hydrothermal Alteration","url":"https://www.academia.edu/Documents/in/Hydrothermal_Alteration?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_11679344" data-work_id="11679344" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/11679344/Spatial_association_of_Neoproterozoic_continental_arc_I_type_and_post_collision_A_type_granitoids_in_the_Arabian_Nubian_Shield_The_Wadi_Al_Baroud_Older_and_Younger_Granites_North_Eastern_Desert_Egypt">Spatial association of Neoproterozoic continental arc I-type and post-collision A-type granitoids in the Arabian–Nubian Shield: The Wadi Al-Baroud Older and Younger Granites, North Eastern Desert, Egypt</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Neoproterozoic basement of Wadi Al-Baroud area located at the northern Eastern Desert (ED) of Egypt, at the northernmost segment of the Arabian–Nubian Shield (ANS), is comprised of two different granite suites. A large batholith... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_11679344" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Neoproterozoic basement of Wadi Al-Baroud area located at the northern Eastern Desert (ED) of<br />Egypt, at the northernmost segment of the Arabian–Nubian Shield (ANS), is comprised of two different<br />granite suites. A large batholith ascribed to the Older Granite suite, extends across the boundary between<br />the northern and central ED, and is intruded by two isolated plutons of the Younger Granite suite. The<br />Older Granite suite includes gray-colored, massive to gneissose, granodiorites to tonalites typically containing<br />microgranular mafic enclaves. These are calc-alkaline, magensian, metaluminous I-type granitoids,<br />with high Sr contents, and depleted in Rb, Nb, Y and REE. The Younger Granite suite plutons are<br />pink to red, biotite and two-mica monzogranites. These are peraluminous A-type granites exhibiting a<br />high-K calc-alkaline nature, and varying between ferroan and magnesian type granites. The A-type granites<br />of the Younger Granite suite are enriched in Ga, Y, HFSE and REE elements, and depleted in the LILE<br />elements Ba, Sr and Rb and transition metals Cr, Ni, Co, Sc and V. Magmatic saturation temperatures indicate<br />early crystallization of apatite at high temperature in the metaluminous I-type Older Granite suite,<br />while in the peraluminous A-type Younger Granites its crystallization occurs later after separation of zircon<br />and monazite. The plutons of the Younger Granite suite were generated during the post-collisional<br />stage of the northern ANS, following collision between the juvenile ANS crust and the pre-Neoproterozoic<br />continental blocks of west Gondwana. The emplacement of the Older Granite suite took place earlier,<br />within a normally mature continental arc prior to the collision. These pre-collision granitoids evolved<br />through assimilation-fractional crystallization processes from mantle-derived parental magmas, which<br />have interacted with crustal materials during ascent and storage. The post-collisional Younger Granite<br />suite seems to have been derived by high degree, partial melting of metasedimentary sources, particularly<br />psammitic and pelitic metasediments.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/11679344" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="0a67a23d1f49101662f911310ef2258a" rel="nofollow" data-download="{"attachment_id":37128594,"asset_id":11679344,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/37128594/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="678897" href="https://independent.academia.edu/MohammedElBialy">Mohammed El-Bialy</a><script data-card-contents-for-user="678897" type="text/json">{"id":678897,"first_name":"Mohammed","last_name":"El-Bialy","domain_name":"independent","page_name":"MohammedElBialy","display_name":"Mohammed El-Bialy","profile_url":"https://independent.academia.edu/MohammedElBialy?f_ri=15989","photo":"https://0.academia-photos.com/678897/4170617/9055636/s65_mohammed.el-bialy.jpg"}</script></span></span></li><li class="js-paper-rank-work_11679344 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="11679344"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 11679344, container: ".js-paper-rank-work_11679344", }); 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$(".js-view-count[data-work-id=11679344]").text(description); $(".js-view-count-work_11679344").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_11679344").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="11679344"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="407" rel="nofollow" href="https://www.academia.edu/Documents/in/Geochemistry">Geochemistry</a>, <script data-card-contents-for-ri="407" type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="56109" rel="nofollow" href="https://www.academia.edu/Documents/in/Precambrian_Geology">Precambrian Geology</a>, <script data-card-contents-for-ri="56109" type="text/json">{"id":56109,"name":"Precambrian Geology","url":"https://www.academia.edu/Documents/in/Precambrian_Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="319882" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrogenesis">Petrogenesis</a><script data-card-contents-for-ri="319882" type="text/json">{"id":319882,"name":"Petrogenesis","url":"https://www.academia.edu/Documents/in/Petrogenesis?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=11679344]'), work: {"id":11679344,"title":"Spatial association of Neoproterozoic continental arc I-type and post-collision A-type granitoids in the Arabian–Nubian Shield: The Wadi Al-Baroud Older and Younger Granites, North Eastern Desert, Egypt","created_at":"2015-03-26T23:19:02.728-07:00","url":"https://www.academia.edu/11679344/Spatial_association_of_Neoproterozoic_continental_arc_I_type_and_post_collision_A_type_granitoids_in_the_Arabian_Nubian_Shield_The_Wadi_Al_Baroud_Older_and_Younger_Granites_North_Eastern_Desert_Egypt?f_ri=15989","dom_id":"work_11679344","summary":"The Neoproterozoic basement of Wadi Al-Baroud area located at the northern Eastern Desert (ED) of\nEgypt, at the northernmost segment of the Arabian–Nubian Shield (ANS), is comprised of two different\ngranite suites. A large batholith ascribed to the Older Granite suite, extends across the boundary between\nthe northern and central ED, and is intruded by two isolated plutons of the Younger Granite suite. The\nOlder Granite suite includes gray-colored, massive to gneissose, granodiorites to tonalites typically containing\nmicrogranular mafic enclaves. These are calc-alkaline, magensian, metaluminous I-type granitoids,\nwith high Sr contents, and depleted in Rb, Nb, Y and REE. The Younger Granite suite plutons are\npink to red, biotite and two-mica monzogranites. These are peraluminous A-type granites exhibiting a\nhigh-K calc-alkaline nature, and varying between ferroan and magnesian type granites. The A-type granites\nof the Younger Granite suite are enriched in Ga, Y, HFSE and REE elements, and depleted in the LILE\nelements Ba, Sr and Rb and transition metals Cr, Ni, Co, Sc and V. Magmatic saturation temperatures indicate\nearly crystallization of apatite at high temperature in the metaluminous I-type Older Granite suite,\nwhile in the peraluminous A-type Younger Granites its crystallization occurs later after separation of zircon\nand monazite. The plutons of the Younger Granite suite were generated during the post-collisional\nstage of the northern ANS, following collision between the juvenile ANS crust and the pre-Neoproterozoic\ncontinental blocks of west Gondwana. The emplacement of the Older Granite suite took place earlier,\nwithin a normally mature continental arc prior to the collision. These pre-collision granitoids evolved\nthrough assimilation-fractional crystallization processes from mantle-derived parental magmas, which\nhave interacted with crustal materials during ascent and storage. The post-collisional Younger Granite\nsuite seems to have been derived by high degree, partial melting of metasedimentary sources, particularly\npsammitic and pelitic metasediments.","downloadable_attachments":[{"id":37128594,"asset_id":11679344,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":678897,"first_name":"Mohammed","last_name":"El-Bialy","domain_name":"independent","page_name":"MohammedElBialy","display_name":"Mohammed El-Bialy","profile_url":"https://independent.academia.edu/MohammedElBialy?f_ri=15989","photo":"https://0.academia-photos.com/678897/4170617/9055636/s65_mohammed.el-bialy.jpg"}],"research_interests":[{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":56109,"name":"Precambrian Geology","url":"https://www.academia.edu/Documents/in/Precambrian_Geology?f_ri=15989","nofollow":true},{"id":319882,"name":"Petrogenesis","url":"https://www.academia.edu/Documents/in/Petrogenesis?f_ri=15989","nofollow":true},{"id":431312,"name":"Crustal evolution","url":"https://www.academia.edu/Documents/in/Crustal_evolution?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_2519768" data-work_id="2519768" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/2519768/Phanerozoic_volcanism">Phanerozoic volcanism</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/2519768" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="54cb3c743b511b2e3b3b03786ef46c0b" rel="nofollow" data-download="{"attachment_id":30535823,"asset_id":2519768,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/30535823/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="1278771" href="https://cardiff.academia.edu/AndrewKerr">Andrew Kerr</a><script data-card-contents-for-user="1278771" type="text/json">{"id":1278771,"first_name":"Andrew","last_name":"Kerr","domain_name":"cardiff","page_name":"AndrewKerr","display_name":"Andrew Kerr","profile_url":"https://cardiff.academia.edu/AndrewKerr?f_ri=15989","photo":"https://0.academia-photos.com/1278771/469059/590910/s65_andrew.kerr.jpg"}</script></span></span></li><li class="js-paper-rank-work_2519768 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="2519768"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 2519768, container: ".js-paper-rank-work_2519768", }); 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$(".js-view-count[data-work-id=2519768]").text(description); $(".js-view-count-work_2519768").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_2519768").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="2519768"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="16937" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry">Petrology and Geochemistry</a>, <script data-card-contents-for-ri="16937" type="text/json">{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="44748" rel="nofollow" href="https://www.academia.edu/Documents/in/Subduction_Zone_Processes">Subduction Zone Processes</a>, <script data-card-contents-for-ri="44748" type="text/json">{"id":44748,"name":"Subduction Zone Processes","url":"https://www.academia.edu/Documents/in/Subduction_Zone_Processes?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="45278" rel="nofollow" href="https://www.academia.edu/Documents/in/Large_Igneous_Provinces">Large Igneous Provinces</a><script data-card-contents-for-ri="45278" type="text/json">{"id":45278,"name":"Large Igneous Provinces","url":"https://www.academia.edu/Documents/in/Large_Igneous_Provinces?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=2519768]'), work: {"id":2519768,"title":"Phanerozoic volcanism","created_at":"2013-02-05T06:10:49.584-08:00","url":"https://www.academia.edu/2519768/Phanerozoic_volcanism?f_ri=15989","dom_id":"work_2519768","summary":null,"downloadable_attachments":[{"id":30535823,"asset_id":2519768,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":1278771,"first_name":"Andrew","last_name":"Kerr","domain_name":"cardiff","page_name":"AndrewKerr","display_name":"Andrew Kerr","profile_url":"https://cardiff.academia.edu/AndrewKerr?f_ri=15989","photo":"https://0.academia-photos.com/1278771/469059/590910/s65_andrew.kerr.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true},{"id":44748,"name":"Subduction Zone Processes","url":"https://www.academia.edu/Documents/in/Subduction_Zone_Processes?f_ri=15989","nofollow":true},{"id":45278,"name":"Large Igneous Provinces","url":"https://www.academia.edu/Documents/in/Large_Igneous_Provinces?f_ri=15989","nofollow":true},{"id":70919,"name":"Mid Ocean Ridge","url":"https://www.academia.edu/Documents/in/Mid_Ocean_Ridge?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_8703572" data-work_id="8703572" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/8703572/The_timescales_of_magmatic_processes_prior_to_a_caldera_forming_eruption">The timescales of magmatic processes prior to a caldera-forming eruption</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Large, explosive, caldera-forming eruptions are amongst the most destructive phenomena on the planet, but the processes that allow the large bodies of crystal-poor silicic magma that feed them to assemble in the shallow crust are still... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_8703572" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Large, explosive, caldera-forming eruptions are amongst the most destructive phenomena on the planet, but the processes that allow the large bodies of crystal-poor silicic magma that feed them to assemble in the shallow crust are still poorly understood. Of particular interest is the timescales over which these reservoirs exist prior to eruption. Long storage times—up to 10^5 y—have previously been estimated using the repose times between eruptions and radiometric dating of crystals found within the eruptive products. However, more recent work modelling diffusion within single crystals has been used to argue that the reservoirs that feed even the largest eruptions are assembled over much shorter periods—10^1–10^2 y. <br /> <br />In order to address this question, I studied the >10 km3, 22-ka, dacitic Cape Riva eruption of Santorini, Greece. Over the ~18 ky preceding the Cape Riva eruption a series of dacitic lava dome and coulées were erupted, and these lavas are interspersed with occasional dacitic pumice fall deposits (the Therasia dome complex). These dacites have similar major element contents to the dacite that was erupted during the Cape Riva eruption, and have previously been described as “precursory leaks” from the growing Cape Riva magma reservoir. However, the Cape Riva magma is depleted in incompatible elements (such as K, Zr, La, Ce) relative to the Therasia magma, as are the plagioclase crystals in the respective magmas. This difference cannot be explained using shallow processes such as fractional crystallisation or crustal assimilation, which suggests that the Cape Riva and Therasia magmas are separate batches. Furthermore, there is evidence that the Therasia dacites were not fed from a long-lived, melt-dominated reservoir. There are non-systematic variations in melt composition, plagioclase rim compositions, and plagioclase textures throughout the sequence. In addition, high-temperature residence times of plagioclase and orthopyroxene crystals from the Therasia dacites estimated using diffusion chronometry are 10^1–10^2 y. This is short compared to the average time between eruptions (~1,500 y), which suggests the crystals in each lava grew only shortly before eruption. The different incompatible element contents of the Cape Riva and Therasia magmas and plagioclase crystals suggest that a new batch of incompatible-depleted silicic magma arrived in the shallow volcanic plumbing system shortly before the Cape Riva eruption. This influx must have taken place after the last Therasia eruption, which 40Ar/39Ar dates show occurred less than 2,800 ± 1,400 years before the Cape Riva eruption. <br /> <br />The rims of the plagioclase crystals found in the Cape Riva dacite are in equilibrium with a rhyodacite, with a similar composition to the Cape Riva glass. However, the major and trace element zoning patterns of the crystals record variations in the melt composition during their growth. The compositions at the centre of most crystals are the same as the rims; however, these crystals are often partially resorbed and overgrown by more calcic plagioclase. The plagioclase then grades normally back to rim compositions. This cycle is repeated up to three times. The tight relationships between the anorthite, Sr and Ti contents of the different zones suggests that the composition of the plagioclase crystals correlates with the composition of the melt from which they grew. The different plagioclase compositions correspond to dacitic and rhyodacitic melt compositions. The orthopyroxene crystals reveal a similar sequence, although they only record one cycle. These zoning patterns are interpreted to document the assembly of the Cape Riva reservoir in the shallow crust through the amalgamation of multiple batches of compositionally diverse magma. Models of magnesium diffusion in plagioclase and Fe–Mg interdiffusion in orthopyroxene suggest that this amalgamation took place within 10^1–10^2 y of the Cape Riva eruption.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/8703572" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="fe45c030629b24288f492aeef2ca102f" rel="nofollow" data-download="{"attachment_id":35055422,"asset_id":8703572,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/35055422/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="2568459" href="https://nanyang.academia.edu/GarethFabbro">Gareth Fabbro</a><script data-card-contents-for-user="2568459" type="text/json">{"id":2568459,"first_name":"Gareth","last_name":"Fabbro","domain_name":"nanyang","page_name":"GarethFabbro","display_name":"Gareth Fabbro","profile_url":"https://nanyang.academia.edu/GarethFabbro?f_ri=15989","photo":"https://0.academia-photos.com/2568459/2542284/2950939/s65_gareth.fabbro.jpg"}</script></span></span></li><li class="js-paper-rank-work_8703572 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="8703572"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 8703572, container: ".js-paper-rank-work_8703572", }); 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Of particular interest is the timescales over which these reservoirs exist prior to eruption. Long storage times—up to 10^5 y—have previously been estimated using the repose times between eruptions and radiometric dating of crystals found within the eruptive products. However, more recent work modelling diffusion within single crystals has been used to argue that the reservoirs that feed even the largest eruptions are assembled over much shorter periods—10^1–10^2 y.\r\n\r\nIn order to address this question, I studied the \u003e10 km3, 22-ka, dacitic Cape Riva eruption of Santorini, Greece. Over the ~18 ky preceding the Cape Riva eruption a series of dacitic lava dome and coulées were erupted, and these lavas are interspersed with occasional dacitic pumice fall deposits (the Therasia dome complex). These dacites have similar major element contents to the dacite that was erupted during the Cape Riva eruption, and have previously been described as “precursory leaks” from the growing Cape Riva magma reservoir. However, the Cape Riva magma is depleted in incompatible elements (such as K, Zr, La, Ce) relative to the Therasia magma, as are the plagioclase crystals in the respective magmas. This difference cannot be explained using shallow processes such as fractional crystallisation or crustal assimilation, which suggests that the Cape Riva and Therasia magmas are separate batches. Furthermore, there is evidence that the Therasia dacites were not fed from a long-lived, melt-dominated reservoir. There are non-systematic variations in melt composition, plagioclase rim compositions, and plagioclase textures throughout the sequence. In addition, high-temperature residence times of plagioclase and orthopyroxene crystals from the Therasia dacites estimated using diffusion chronometry are 10^1–10^2 y. This is short compared to the average time between eruptions (~1,500 y), which suggests the crystals in each lava grew only shortly before eruption. The different incompatible element contents of the Cape Riva and Therasia magmas and plagioclase crystals suggest that a new batch of incompatible-depleted silicic magma arrived in the shallow volcanic plumbing system shortly before the Cape Riva eruption. This influx must have taken place after the last Therasia eruption, which 40Ar/39Ar dates show occurred less than 2,800 ± 1,400 years before the Cape Riva eruption.\r\n\r\nThe rims of the plagioclase crystals found in the Cape Riva dacite are in equilibrium with a rhyodacite, with a similar composition to the Cape Riva glass. However, the major and trace element zoning patterns of the crystals record variations in the melt composition during their growth. The compositions at the centre of most crystals are the same as the rims; however, these crystals are often partially resorbed and overgrown by more calcic plagioclase. The plagioclase then grades normally back to rim compositions. This cycle is repeated up to three times. The tight relationships between the anorthite, Sr and Ti contents of the different zones suggests that the composition of the plagioclase crystals correlates with the composition of the melt from which they grew. The different plagioclase compositions correspond to dacitic and rhyodacitic melt compositions. The orthopyroxene crystals reveal a similar sequence, although they only record one cycle. These zoning patterns are interpreted to document the assembly of the Cape Riva reservoir in the shallow crust through the amalgamation of multiple batches of compositionally diverse magma. Models of magnesium diffusion in plagioclase and Fe–Mg interdiffusion in orthopyroxene suggest that this amalgamation took place within 10^1–10^2 y of the Cape Riva eruption.","downloadable_attachments":[{"id":35055422,"asset_id":8703572,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":2568459,"first_name":"Gareth","last_name":"Fabbro","domain_name":"nanyang","page_name":"GarethFabbro","display_name":"Gareth Fabbro","profile_url":"https://nanyang.academia.edu/GarethFabbro?f_ri=15989","photo":"https://0.academia-photos.com/2568459/2542284/2950939/s65_gareth.fabbro.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989"},{"id":83315,"name":"Diffusion","url":"https://www.academia.edu/Documents/in/Diffusion?f_ri=15989"},{"id":138261,"name":"Magma Chambers","url":"https://www.academia.edu/Documents/in/Magma_Chambers?f_ri=15989"},{"id":185650,"name":"Santorini eruption dates","url":"https://www.academia.edu/Documents/in/Santorini_eruption_dates?f_ri=15989"},{"id":200887,"name":"Explosive volcanic eruptions","url":"https://www.academia.edu/Documents/in/Explosive_volcanic_eruptions?f_ri=15989"},{"id":269328,"name":"Santorini","url":"https://www.academia.edu/Documents/in/Santorini?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_37535484" data-work_id="37535484" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/37535484/Roll_Back_Extension_and_Mantle_Upwelling_Triggered_Eocene_Potassic_Magmatism_in_NW_Iran">Roll-Back, Extension and Mantle Upwelling Triggered Eocene Potassic Magmatism in NW Iran</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Igneous activity in the rear-arc of the Paleogene Urumieh–Dokhtar Magmatic Belt of Iran has to date been poorly studied. An example of such activity, Late Eocene potassic mafic to intermediate magmatic rocks in the Lahrud area of NW Iran,... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_37535484" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Igneous activity in the rear-arc of the Paleogene Urumieh–Dokhtar Magmatic Belt of Iran has to date been poorly studied. An example of such activity, Late Eocene potassic mafic to intermediate magmatic rocks in the Lahrud area of NW Iran, is the focus of this work. These lavas include olivine-bearing clinopyroxene-phyric basalts, analcime-bearing leucite–clinopyroxene-phyric basalts, andesites, and trachytes, and Paleocene–Early Eocene pyroclastic rocks. Monzo-syenite plugs (dated here at $37 Ma), clinopyroxene-phyric basaltic dikes, and leucite-bearing clinopyrox-ene-phyric basaltic dikes intrude older lavas and pyroclastic rocks. Olivine-bearing clinopyroxene-phyric basalts and analcime-bearing leucite–clinopyroxene-phyric basalts are characterized by large phenocrysts of olivine, clinopyroxene, leucite, and analcime. Clinopyroxene-rich enclaves and partially resorbed mantle xenoliths also occur. Olivine phenocrysts are zoned from high-Mg# cores (Mg# ¼ 90) to Fe-rich rims (Mg# ¼ 66). Clinopyroxene phenocrysts from the olivine-bearing clinopyroxene-phyric basalts, analcime-bearing leucite–clinopyroxene-phyric basalts and clinopyr-oxene crystals in the enclaves show complex oscillatory zoning, sieve textures, and resorption textures , but with systematic core–rim compositional trends. Their 87 Sr/ 86 Sr isotopic compositions measured in situ range from 0Á7037 to 0Á7068 (mean ¼ 0Á7052 6 0Á0004), suggesting negligible crustal assimilation during fractional crystallization. The Lahrud lavas are potassic and are enriched in light rare earth elements and large ion lithophile elements such as Th, Rb, K and U. High field strength elements (HFSE), such as Nb, are depleted in the olivine-bearing clinopyroxene-phyric basalts and analcime-bearing leucite–clinopyroxene-phyric basalts, but enriched in the trachytes and trachytic ignimbrites. The isotopic compositions vary: 87 Sr/ 86 Sr t from 0Á7045 to 0Á7052, eNd(t) from þ2Á8 to þ3Á3, and eHf(t) from þ7Á2 to þ7Á7. The rocks have radiogenic lead 206 Pb/ 204 Pb from 18Á66 to 18Á76, 207 Pb/ 204 Pb from 15Á58 to 15Á62, and 208 Pb/ 204 Pb from 38Á73 to 38Á81. Modeling of</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/37535484" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="ed63124b4ed7591596fd4c9b163682bc" rel="nofollow" data-download="{"attachment_id":57509398,"asset_id":37535484,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/57509398/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="40932563" href="https://kfs.academia.edu/DrMohamedKhedr">DrMohamed Khedr</a><script data-card-contents-for-user="40932563" type="text/json">{"id":40932563,"first_name":"DrMohamed","last_name":"Khedr","domain_name":"kfs","page_name":"DrMohamedKhedr","display_name":"DrMohamed Khedr","profile_url":"https://kfs.academia.edu/DrMohamedKhedr?f_ri=15989","photo":"https://0.academia-photos.com/40932563/12744216/14174549/s65_drmohamed.khedr.jpg_oh_645cb2662ba11d040a88cc8044dc879c_oe_57e18c11"}</script></span></span></li><li class="js-paper-rank-work_37535484 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="37535484"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 37535484, container: ".js-paper-rank-work_37535484", }); 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$(".js-view-count[data-work-id=37535484]").text(description); $(".js-view-count-work_37535484").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_37535484").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="37535484"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="16937" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry">Petrology and Geochemistry</a>, <script data-card-contents-for-ri="16937" type="text/json">{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="22595" rel="nofollow" href="https://www.academia.edu/Documents/in/Geochronology_and_isotope_Geology">Geochronology & isotope Geology</a><script data-card-contents-for-ri="22595" type="text/json">{"id":22595,"name":"Geochronology \u0026 isotope Geology","url":"https://www.academia.edu/Documents/in/Geochronology_and_isotope_Geology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=37535484]'), work: {"id":37535484,"title":"Roll-Back, Extension and Mantle Upwelling Triggered Eocene Potassic Magmatism in NW Iran","created_at":"2018-10-05T05:51:36.712-07:00","url":"https://www.academia.edu/37535484/Roll_Back_Extension_and_Mantle_Upwelling_Triggered_Eocene_Potassic_Magmatism_in_NW_Iran?f_ri=15989","dom_id":"work_37535484","summary":"Igneous activity in the rear-arc of the Paleogene Urumieh–Dokhtar Magmatic Belt of Iran has to date been poorly studied. An example of such activity, Late Eocene potassic mafic to intermediate magmatic rocks in the Lahrud area of NW Iran, is the focus of this work. These lavas include olivine-bearing clinopyroxene-phyric basalts, analcime-bearing leucite–clinopyroxene-phyric basalts, andesites, and trachytes, and Paleocene–Early Eocene pyroclastic rocks. Monzo-syenite plugs (dated here at $37 Ma), clinopyroxene-phyric basaltic dikes, and leucite-bearing clinopyrox-ene-phyric basaltic dikes intrude older lavas and pyroclastic rocks. Olivine-bearing clinopyroxene-phyric basalts and analcime-bearing leucite–clinopyroxene-phyric basalts are characterized by large phenocrysts of olivine, clinopyroxene, leucite, and analcime. Clinopyroxene-rich enclaves and partially resorbed mantle xenoliths also occur. Olivine phenocrysts are zoned from high-Mg# cores (Mg# ¼ 90) to Fe-rich rims (Mg# ¼ 66). Clinopyroxene phenocrysts from the olivine-bearing clinopyroxene-phyric basalts, analcime-bearing leucite–clinopyroxene-phyric basalts and clinopyr-oxene crystals in the enclaves show complex oscillatory zoning, sieve textures, and resorption textures , but with systematic core–rim compositional trends. Their 87 Sr/ 86 Sr isotopic compositions measured in situ range from 0Á7037 to 0Á7068 (mean ¼ 0Á7052 6 0Á0004), suggesting negligible crustal assimilation during fractional crystallization. The Lahrud lavas are potassic and are enriched in light rare earth elements and large ion lithophile elements such as Th, Rb, K and U. High field strength elements (HFSE), such as Nb, are depleted in the olivine-bearing clinopyroxene-phyric basalts and analcime-bearing leucite–clinopyroxene-phyric basalts, but enriched in the trachytes and trachytic ignimbrites. The isotopic compositions vary: 87 Sr/ 86 Sr t from 0Á7045 to 0Á7052, eNd(t) from þ2Á8 to þ3Á3, and eHf(t) from þ7Á2 to þ7Á7. The rocks have radiogenic lead 206 Pb/ 204 Pb from 18Á66 to 18Á76, 207 Pb/ 204 Pb from 15Á58 to 15Á62, and 208 Pb/ 204 Pb from 38Á73 to 38Á81. Modeling of","downloadable_attachments":[{"id":57509398,"asset_id":37535484,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":40932563,"first_name":"DrMohamed","last_name":"Khedr","domain_name":"kfs","page_name":"DrMohamedKhedr","display_name":"DrMohamed Khedr","profile_url":"https://kfs.academia.edu/DrMohamedKhedr?f_ri=15989","photo":"https://0.academia-photos.com/40932563/12744216/14174549/s65_drmohamed.khedr.jpg_oh_645cb2662ba11d040a88cc8044dc879c_oe_57e18c11"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true},{"id":22595,"name":"Geochronology \u0026 isotope Geology","url":"https://www.academia.edu/Documents/in/Geochronology_and_isotope_Geology?f_ri=15989","nofollow":true},{"id":44747,"name":"Plate Tectonics","url":"https://www.academia.edu/Documents/in/Plate_Tectonics?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_32041793" data-work_id="32041793" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/32041793/Extensional_flow_produces_recumbent_folds_in_syn_orogenic_granitoids_Padr%C3%B3n_migmatitic_dome_NW_Iberian_Massif">Extensional flow produces recumbent folds in syn-orogenic granitoids (Padrón migmatitic dome, NW Iberian Massif</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">This contribution provides a case example on the generation of large-scale recumbent folds in syn-orogenic gran-itoids. We analyze the progressive reworking of extension-related structures into later ones after a period of crustal... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_32041793" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">This contribution provides a case example on the generation of large-scale recumbent folds in syn-orogenic gran-itoids. We analyze the progressive reworking of extension-related structures into later ones after a period of crustal thickening. The Padrón migmatitic dome formed after the climax of the Gondwana-Laurussia collision in the late Paleozoic. Petrostructural analysis carried out in the eastern flank of this dome reveals that extensional flow resulted in progressive exhumation of mainland Gondwana, which rested under peri-gondwanan alloch-thonous terranes and a suture zone during maximum crustal thickening. Exhumation proceeded up to upper crust levels (andalusite stability field) along with partial melting of the middle-lower crust and with the generation of granitoid laccoliths during an early extensional stage. Newly-formed lithological and mechanical anisot-ropies, such as the presence of variably-sized sheet-shaped bodies of syn-orogenic granitoids, provided a favorable rheological setting for fold nucleation during the intermediate stages of extension. In extending oro-genic crust, whether recumbent folds occur after significant melt production depends on the lateral/vertical flow ratio, and on the orientation of deforming bodies with regard to kinematic/strain axes. We suggest that subhorizontal extensional flow dominated over vertical flow during the early and intermediate stages of the evolution of the Padrón dome. A component of vertical (diapiric) flow caused progressive tilting of the sheet-like bodies and obliquity respect to strain axes. This resulted in the development of regional-scale folds at the expense of syn-orogenic granitoids, such as in the case of the Portomouro recumbent synform. Extensional ductile flow was oblique to the trend of the orogen during the whole process, and directed to the NNW during the formation of recumbent folds. Non-coaxial shearing favored an (NNW-SSE) elongate shape for the syn-kinematic granitic massifs as well as the subsequent nucleation of recumbent folds. Deformation concentrated along discrete detachments during the late stages of extension.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/32041793" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="c624319f20dd15aa7cce05f1e3eb2a1f" rel="nofollow" data-download="{"attachment_id":52303815,"asset_id":32041793,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/52303815/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="491020" href="https://igme-es.academia.edu/RubenDiezFernandez">Ruben Diez Fernandez</a><script data-card-contents-for-user="491020" type="text/json">{"id":491020,"first_name":"Ruben","last_name":"Diez Fernandez","domain_name":"igme-es","page_name":"RubenDiezFernandez","display_name":"Ruben Diez Fernandez","profile_url":"https://igme-es.academia.edu/RubenDiezFernandez?f_ri=15989","photo":"https://0.academia-photos.com/491020/240056/18668447/s65_ruben.diez_fernandez.jpg"}</script></span></span></li><li class="js-paper-rank-work_32041793 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="32041793"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 32041793, container: ".js-paper-rank-work_32041793", }); 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$(".js-view-count[data-work-id=32041793]").text(description); $(".js-view-count-work_32041793").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_32041793").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="32041793"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">18</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1419" rel="nofollow" href="https://www.academia.edu/Documents/in/Structural_Geology">Structural Geology</a>, <script data-card-contents-for-ri="1419" type="text/json">{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2635" rel="nofollow" href="https://www.academia.edu/Documents/in/Metamorphic_Petrology">Metamorphic Petrology</a>, <script data-card-contents-for-ri="2635" type="text/json">{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="3199" rel="nofollow" href="https://www.academia.edu/Documents/in/Folding_Structural_Geology_">Folding (Structural Geology)</a><script data-card-contents-for-ri="3199" type="text/json">{"id":3199,"name":"Folding (Structural Geology)","url":"https://www.academia.edu/Documents/in/Folding_Structural_Geology_?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=32041793]'), work: {"id":32041793,"title":"Extensional flow produces recumbent folds in syn-orogenic granitoids (Padrón migmatitic dome, NW Iberian Massif","created_at":"2017-03-25T10:06:34.083-07:00","url":"https://www.academia.edu/32041793/Extensional_flow_produces_recumbent_folds_in_syn_orogenic_granitoids_Padr%C3%B3n_migmatitic_dome_NW_Iberian_Massif?f_ri=15989","dom_id":"work_32041793","summary":"This contribution provides a case example on the generation of large-scale recumbent folds in syn-orogenic gran-itoids. We analyze the progressive reworking of extension-related structures into later ones after a period of crustal thickening. The Padrón migmatitic dome formed after the climax of the Gondwana-Laurussia collision in the late Paleozoic. Petrostructural analysis carried out in the eastern flank of this dome reveals that extensional flow resulted in progressive exhumation of mainland Gondwana, which rested under peri-gondwanan alloch-thonous terranes and a suture zone during maximum crustal thickening. Exhumation proceeded up to upper crust levels (andalusite stability field) along with partial melting of the middle-lower crust and with the generation of granitoid laccoliths during an early extensional stage. Newly-formed lithological and mechanical anisot-ropies, such as the presence of variably-sized sheet-shaped bodies of syn-orogenic granitoids, provided a favorable rheological setting for fold nucleation during the intermediate stages of extension. In extending oro-genic crust, whether recumbent folds occur after significant melt production depends on the lateral/vertical flow ratio, and on the orientation of deforming bodies with regard to kinematic/strain axes. We suggest that subhorizontal extensional flow dominated over vertical flow during the early and intermediate stages of the evolution of the Padrón dome. A component of vertical (diapiric) flow caused progressive tilting of the sheet-like bodies and obliquity respect to strain axes. This resulted in the development of regional-scale folds at the expense of syn-orogenic granitoids, such as in the case of the Portomouro recumbent synform. Extensional ductile flow was oblique to the trend of the orogen during the whole process, and directed to the NNW during the formation of recumbent folds. Non-coaxial shearing favored an (NNW-SSE) elongate shape for the syn-kinematic granitic massifs as well as the subsequent nucleation of recumbent folds. Deformation concentrated along discrete detachments during the late stages of extension.","downloadable_attachments":[{"id":52303815,"asset_id":32041793,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":491020,"first_name":"Ruben","last_name":"Diez Fernandez","domain_name":"igme-es","page_name":"RubenDiezFernandez","display_name":"Ruben Diez Fernandez","profile_url":"https://igme-es.academia.edu/RubenDiezFernandez?f_ri=15989","photo":"https://0.academia-photos.com/491020/240056/18668447/s65_ruben.diez_fernandez.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989","nofollow":true},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989","nofollow":true},{"id":3199,"name":"Folding (Structural Geology)","url":"https://www.academia.edu/Documents/in/Folding_Structural_Geology_?f_ri=15989","nofollow":true},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":28331,"name":"Granite (Earth Sciences)","url":"https://www.academia.edu/Documents/in/Granite_Earth_Sciences_?f_ri=15989"},{"id":171492,"name":"Paleozoic","url":"https://www.academia.edu/Documents/in/Paleozoic?f_ri=15989"},{"id":173639,"name":"Late Variscan Granites","url":"https://www.academia.edu/Documents/in/Late_Variscan_Granites?f_ri=15989"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism?f_ri=15989"},{"id":215061,"name":"Orogenic Tectonics","url":"https://www.academia.edu/Documents/in/Orogenic_Tectonics?f_ri=15989"},{"id":238750,"name":"Structural Geology and Tectonics","url":"https://www.academia.edu/Documents/in/Structural_Geology_and_Tectonics?f_ri=15989"},{"id":239149,"name":"Variscan tectonic","url":"https://www.academia.edu/Documents/in/Variscan_tectonic?f_ri=15989"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology?f_ri=15989"},{"id":280136,"name":"Variscan belt","url":"https://www.academia.edu/Documents/in/Variscan_belt?f_ri=15989"},{"id":298329,"name":"Continental collision","url":"https://www.academia.edu/Documents/in/Continental_collision?f_ri=15989"},{"id":598753,"name":"Continental Lithosphere","url":"https://www.academia.edu/Documents/in/Continental_Lithosphere?f_ri=15989"},{"id":755655,"name":"Variscan Orogeny","url":"https://www.academia.edu/Documents/in/Variscan_Orogeny?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_38857376 coauthored" data-work_id="38857376" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/38857376/Article_Compositional_variations_of_chromian_spinels_from_peridotites_of_the_Spontang_ophiolite_complex_Ladakh_NW_Himalayas_India_petrogenetic_implications">Article Compositional variations of chromian spinels from peridotites of the Spontang ophiolite complex, Ladakh, NW Himalayas, India: petrogenetic implications</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Spontang ophiolite complex exposed along the Indus Tsangpo Suture Zone (ITSZ) represents a fragment of oce-anic lithosphere emplaced after the closure of the Neo-Tethyan Ocean. The complex lying south of the ITSZ forms the highest... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_38857376" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Spontang ophiolite complex exposed along the Indus Tsangpo Suture Zone (ITSZ) represents a fragment of oce-anic lithosphere emplaced after the closure of the Neo-Tethyan Ocean. The complex lying south of the ITSZ forms the highest tec-tonic thrust slice above the Mesozoic-Early Tertiary continental margin in the Ladakh-Zanskar Himalaya. The complex consists of a well-preserved ophiolite sequence dominated by peridotites, gabbros and ultramafic cumulates along with highly tectonized sheeted dykes and pillow lavas. The mantle suite of rocks is represented by minor lherzolites, harzburgites and dunites. Chromian spinel is brown to reddish, and its morphology and textural relationship with coexisting silicates varies with strain. Spinel occurs as blebs and vermicular exsolutions within orthopyroxene to spherical inclusions within olivine, characteristic of which is the elongate holly leaf shape. Chrome spinels are characterized by low TiO 2 and high Cr 2 O 3 indicative of their depleted nature. Cr# [= atomic ratio Cr/(Cr + Al)] in the studied spinels are characterized by a small decrease in TiO 2 for a larger increase in Cr# consistent with observations for spinels aligned along the Luobusa trend of the Yarlung Zangpo Suture Zone (YZSZ) ophiolites. Variations in Cr-spinel Cr# and Mg# observed in the investigated peridotites may have resulted from a wide range of degrees of mantle melting during their evolution. Mineral and whole-rock chemistry of the Spontang peridotites is characterized by interaction between depleted magma and pre-existing oceanic lithosphere, typical of supra-subduction zone settings. The Spontang peridotites have olivine, clinopyroxene and orthopyroxene compositions similar to those from both abyssal and fore-arc peridotites and display spoon shaped REE profiles characteristic of interaction between LREE-enriched melt, derived from the subducting slab and LREE-depleted mantle residues. Equilibration temperatures calculated for the above rocks indicate that the studied samples represent typical mantle peridotites formed within the spinel stability field.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/38857376" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="d6cded597d09fd54a97151fda61a1f13" rel="nofollow" data-download="{"attachment_id":58953118,"asset_id":38857376,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/58953118/download_file?st=MTczOTgyNjA5MSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="10246740" href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a><script data-card-contents-for-user="10246740" type="text/json">{"id":10246740,"first_name":"Michel","last_name":"Gregoire","domain_name":"omp","page_name":"MichelGregoire","display_name":"Michel Gregoire","profile_url":"https://omp.academia.edu/MichelGregoire?f_ri=15989","photo":"https://0.academia-photos.com/10246740/3143594/153643901/s65_michel.gregoire.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-38857376">+1</span><div class="hidden js-additional-users-38857376"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://unipune.academia.edu/ShivaniHarshe">Shivani Harshe</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-38857376'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-38857376').html(); 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container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_38857376 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="38857376"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 38857376; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=38857376]").text(description); $(".js-view-count-work_38857376").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_38857376").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="38857376"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">4</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="16248" rel="nofollow" href="https://www.academia.edu/Documents/in/Ophiolites">Ophiolites</a>, <script data-card-contents-for-ri="16248" type="text/json">{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="191873" rel="nofollow" href="https://www.academia.edu/Documents/in/Magmatism">Magmatism</a>, <script data-card-contents-for-ri="191873" type="text/json">{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="895633" rel="nofollow" href="https://www.academia.edu/Documents/in/Chromite">Chromite</a><script data-card-contents-for-ri="895633" type="text/json">{"id":895633,"name":"Chromite","url":"https://www.academia.edu/Documents/in/Chromite?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=38857376]'), work: {"id":38857376,"title":"Article Compositional variations of chromian spinels from peridotites of the Spontang ophiolite complex, Ladakh, NW Himalayas, India: petrogenetic implications","created_at":"2019-04-19T00:54:38.894-07:00","url":"https://www.academia.edu/38857376/Article_Compositional_variations_of_chromian_spinels_from_peridotites_of_the_Spontang_ophiolite_complex_Ladakh_NW_Himalayas_India_petrogenetic_implications?f_ri=15989","dom_id":"work_38857376","summary":"The Spontang ophiolite complex exposed along the Indus Tsangpo Suture Zone (ITSZ) represents a fragment of oce-anic lithosphere emplaced after the closure of the Neo-Tethyan Ocean. The complex lying south of the ITSZ forms the highest tec-tonic thrust slice above the Mesozoic-Early Tertiary continental margin in the Ladakh-Zanskar Himalaya. The complex consists of a well-preserved ophiolite sequence dominated by peridotites, gabbros and ultramafic cumulates along with highly tectonized sheeted dykes and pillow lavas. The mantle suite of rocks is represented by minor lherzolites, harzburgites and dunites. Chromian spinel is brown to reddish, and its morphology and textural relationship with coexisting silicates varies with strain. Spinel occurs as blebs and vermicular exsolutions within orthopyroxene to spherical inclusions within olivine, characteristic of which is the elongate holly leaf shape. Chrome spinels are characterized by low TiO 2 and high Cr 2 O 3 indicative of their depleted nature. Cr# [= atomic ratio Cr/(Cr + Al)] in the studied spinels are characterized by a small decrease in TiO 2 for a larger increase in Cr# consistent with observations for spinels aligned along the Luobusa trend of the Yarlung Zangpo Suture Zone (YZSZ) ophiolites. Variations in Cr-spinel Cr# and Mg# observed in the investigated peridotites may have resulted from a wide range of degrees of mantle melting during their evolution. Mineral and whole-rock chemistry of the Spontang peridotites is characterized by interaction between depleted magma and pre-existing oceanic lithosphere, typical of supra-subduction zone settings. The Spontang peridotites have olivine, clinopyroxene and orthopyroxene compositions similar to those from both abyssal and fore-arc peridotites and display spoon shaped REE profiles characteristic of interaction between LREE-enriched melt, derived from the subducting slab and LREE-depleted mantle residues. Equilibration temperatures calculated for the above rocks indicate that the studied samples represent typical mantle peridotites formed within the spinel stability field.","downloadable_attachments":[{"id":58953118,"asset_id":38857376,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":10246740,"first_name":"Michel","last_name":"Gregoire","domain_name":"omp","page_name":"MichelGregoire","display_name":"Michel Gregoire","profile_url":"https://omp.academia.edu/MichelGregoire?f_ri=15989","photo":"https://0.academia-photos.com/10246740/3143594/153643901/s65_michel.gregoire.jpg"},{"id":8729786,"first_name":"Shivani","last_name":"Harshe","domain_name":"unipune","page_name":"ShivaniHarshe","display_name":"Shivani Harshe","profile_url":"https://unipune.academia.edu/ShivaniHarshe?f_ri=15989","photo":"https://0.academia-photos.com/8729786/11635021/12973847/s65_shivani.harshe.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16248,"name":"Ophiolites","url":"https://www.academia.edu/Documents/in/Ophiolites?f_ri=15989","nofollow":true},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism?f_ri=15989","nofollow":true},{"id":895633,"name":"Chromite","url":"https://www.academia.edu/Documents/in/Chromite?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_37679086 coauthored" data-work_id="37679086" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/37679086/Transport_of_Volatile_rich_Melt_from_the_Mantle_Transition_Zone_via_Compaction_Pockets_Implications_for_Mantle_Metasomatism_and_the_Origin_of_Alkaline_Lavas_in_the_Turkish_Iranian_Plateau">Transport of Volatile-rich Melt from the Mantle Transition Zone via Compaction Pockets: Implications for Mantle Metasomatism and the Origin of Alkaline Lavas in the Turkish-Iranian Plateau</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">This study is based on an integrated approach combining results from petrology, geophysics and modeling to explain the origin of continental alkaline magmatism in the Turkish-Iranian plateau (TIP). Synthesis of the petrological and... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_37679086" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">This study is based on an integrated approach combining results from petrology, geophysics and modeling to explain the origin of continental alkaline magmatism in the Turkish-Iranian plateau (TIP). Synthesis of the petrological and chemical characteristics of the alkaline magmatism of the TIP, extending from 80 Ma to the present, shows that the alkaline lavas can be classified as ultrapotassic (UK), transitional potassic to sodic (TK) and sodic-high potassium (HK) and sodic-low potassium (LK) lavas, all derived from a heterogeneous mantle source. Synthesis of the most recent seismic tomography images for the region shows the presence of a large set of low velocity elliptical bodies, ~100 km in size, referred to as " Compaction Pockets " (CP), scattered from the top of the mantle Transition Zone (MTZ) to the base of the lithosphere beneath the TIP.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/37679086" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="cdad9ed7e9f4fed4ac849b50a5bf6f61" rel="nofollow" data-download="{"attachment_id":58021948,"asset_id":37679086,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/58021948/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="5634572" href="https://nrcan-gc.academia.edu/azamsoltanmohammadi">Azam Soltanmohammadi</a><script data-card-contents-for-user="5634572" type="text/json">{"id":5634572,"first_name":"Azam","last_name":"Soltanmohammadi","domain_name":"nrcan-gc","page_name":"azamsoltanmohammadi","display_name":"Azam Soltanmohammadi","profile_url":"https://nrcan-gc.academia.edu/azamsoltanmohammadi?f_ri=15989","photo":"https://0.academia-photos.com/5634572/4699602/34374074/s65_azam.soltanmohammadi.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-37679086">+1</span><div class="hidden js-additional-users-37679086"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-37679086'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-37679086').html(); 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Synthesis of the petrological and chemical characteristics of the alkaline magmatism of the TIP, extending from 80 Ma to the present, shows that the alkaline lavas can be classified as ultrapotassic (UK), transitional potassic to sodic (TK) and sodic-high potassium (HK) and sodic-low potassium (LK) lavas, all derived from a heterogeneous mantle source. Synthesis of the most recent seismic tomography images for the region shows the presence of a large set of low velocity elliptical bodies, ~100 km in size, referred to as \" Compaction Pockets \" (CP), scattered from the top of the mantle Transition Zone (MTZ) to the base of the lithosphere beneath the TIP.","downloadable_attachments":[{"id":58021948,"asset_id":37679086,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":5634572,"first_name":"Azam","last_name":"Soltanmohammadi","domain_name":"nrcan-gc","page_name":"azamsoltanmohammadi","display_name":"Azam Soltanmohammadi","profile_url":"https://nrcan-gc.academia.edu/azamsoltanmohammadi?f_ri=15989","photo":"https://0.academia-photos.com/5634572/4699602/34374074/s65_azam.soltanmohammadi.jpg"},{"id":10246740,"first_name":"Michel","last_name":"Gregoire","domain_name":"omp","page_name":"MichelGregoire","display_name":"Michel Gregoire","profile_url":"https://omp.academia.edu/MichelGregoire?f_ri=15989","photo":"https://0.academia-photos.com/10246740/3143594/153643901/s65_michel.gregoire.jpg"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=15989","nofollow":true},{"id":10251,"name":"Experimental Petrology","url":"https://www.academia.edu/Documents/in/Experimental_Petrology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":257012,"name":"Geology and Geophysics","url":"https://www.academia.edu/Documents/in/Geology_and_Geophysics?f_ri=15989","nofollow":true},{"id":637087,"name":"Petrology and Geochemistry of Igneous Rocks","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry_of_Igneous_Rocks?f_ri=15989"},{"id":1202397,"name":"Experimental Mineralogy","url":"https://www.academia.edu/Documents/in/Experimental_Mineralogy?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_34653630" data-work_id="34653630" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/34653630/Cuando_y_como_se_cre%C3%B3_la_corteza_continental_Cuando_el_presente_no_es_la_clave_del_pasado">Cuando y como se creó la corteza continental; Cuando el presente no es la clave del pasado</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Tanto en el Arcaico como hoy en día, los granitoides constituyen el núcleo de la corteza continental formada en las zonas de subducción. La corteza hadeana era máfica y sufrió una fusión parcial interna, esta fue interrumpida por un... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_34653630" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Tanto en el Arcaico como hoy en día, los granitoides constituyen el núcleo de la corteza continental formada en las zonas de subducción. La corteza hadeana era máfica y sufrió una fusión parcial interna, esta fue interrumpida por un bombardeo meteorítico. Después de esto, hace unos 3900 Ma, la tectónica de placas comenzó a funcionar. A final del Arcaico y hasta finales del Proterozoico, la corteza continental creció episódicamente por la convección acelerada del manto. El mayor volumen de corteza continental se dio con la llegada de superplumas mantélicas desplazando material de la parte superior del manto y acelerando la velocidad de subducción. <br /> <br />Prácticamente no hay afloramientos arcaicos, las suposiciones de los científicos se basan en datos geoquímicos, geofísicos y mineralógicos; pero todavía no se conocen cuáles fueron los procesos exactos que actuaron en la Tierra primitiva, y no siempre se debe suponer que lo que sucede en el presente puede ser clave para saber lo que pasó en el pasado.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/34653630" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="19b09d45832ce0b27dfae237d764dd92" rel="nofollow" data-download="{"attachment_id":56045175,"asset_id":34653630,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/56045175/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="10257960" href="https://uab.academia.edu/CristinaAA">Cristina Agüera Angel</a><script data-card-contents-for-user="10257960" type="text/json">{"id":10257960,"first_name":"Cristina","last_name":"Agüera Angel","domain_name":"uab","page_name":"CristinaAA","display_name":"Cristina Agüera Angel","profile_url":"https://uab.academia.edu/CristinaAA?f_ri=15989","photo":"https://0.academia-photos.com/10257960/3353283/17824330/s65_cristina.ag_era_angel.jpg"}</script></span></span></li><li class="js-paper-rank-work_34653630 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="34653630"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 34653630, container: ".js-paper-rank-work_34653630", }); 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Cuando el presente no es la clave del pasado","created_at":"2017-09-23T04:03:56.766-07:00","url":"https://www.academia.edu/34653630/Cuando_y_como_se_cre%C3%B3_la_corteza_continental_Cuando_el_presente_no_es_la_clave_del_pasado?f_ri=15989","dom_id":"work_34653630","summary":"Tanto en el Arcaico como hoy en día, los granitoides constituyen el núcleo de la corteza continental formada en las zonas de subducción. La corteza hadeana era máfica y sufrió una fusión parcial interna, esta fue interrumpida por un bombardeo meteorítico. Después de esto, hace unos 3900 Ma, la tectónica de placas comenzó a funcionar. A final del Arcaico y hasta finales del Proterozoico, la corteza continental creció episódicamente por la convección acelerada del manto. El mayor volumen de corteza continental se dio con la llegada de superplumas mantélicas desplazando material de la parte superior del manto y acelerando la velocidad de subducción. \r\n\r\nPrácticamente no hay afloramientos arcaicos, las suposiciones de los científicos se basan en datos geoquímicos, geofísicos y mineralógicos; pero todavía no se conocen cuáles fueron los procesos exactos que actuaron en la Tierra primitiva, y no siempre se debe suponer que lo que sucede en el presente puede ser clave para saber lo que pasó en el pasado.\r\n","downloadable_attachments":[{"id":56045175,"asset_id":34653630,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":10257960,"first_name":"Cristina","last_name":"Agüera Angel","domain_name":"uab","page_name":"CristinaAA","display_name":"Cristina Agüera Angel","profile_url":"https://uab.academia.edu/CristinaAA?f_ri=15989","photo":"https://0.academia-photos.com/10257960/3353283/17824330/s65_cristina.ag_era_angel.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":45449,"name":"Continental crust: origin and composition","url":"https://www.academia.edu/Documents/in/Continental_crust_origin_and_composition?f_ri=15989"},{"id":49400,"name":"Evolution of continental crust","url":"https://www.academia.edu/Documents/in/Evolution_of_continental_crust?f_ri=15989"},{"id":199072,"name":"Vulcanology","url":"https://www.academia.edu/Documents/in/Vulcanology?f_ri=15989"},{"id":298333,"name":"Origin of continental crust","url":"https://www.academia.edu/Documents/in/Origin_of_continental_crust?f_ri=15989"},{"id":421956,"name":"Continental Crust","url":"https://www.academia.edu/Documents/in/Continental_Crust?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_37153968" data-work_id="37153968" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/37153968/Petrology_and_geochemistry_of_the_Mesoproterozoic_Vattikod_lamproites_Eastern_Dharwar_Craton_southern_India_evidence_for_multiple_enrichment_of_sub_continental_lithospheric_mantle_and_links_with_amalgamation_and_break_up_of_the_Columbia_supercontinent">Petrology and geochemistry of the Mesoproterozoic Vattikod lamproites, Eastern Dharwar Craton, southern India: evidence for multiple enrichment of sub-continental lithospheric mantle and links with amalgamation and break-up of the Columbia supercontinent</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Numerous lamproite dykes are hosted by the Eastern Dharwar Craton, southern India, particularly towards the northwestern margin of the Cuddapah Basin. We present here a comprehensive mineralogical and geochemical (including Sr and Nd... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_37153968" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Numerous lamproite dykes are hosted by the Eastern Dharwar Craton, southern India, particularly towards the northwestern margin of the Cuddapah Basin. We present here a comprehensive mineralogical and geochemical (including Sr and Nd isotopic) study on the lamproites from the Vattikod Field, exposed in the vicinity of the well-studied Ramadugu lamproite field. The Vattikod lamproites trend WNW–ESE to NW–SE and reveal effects of low-temperature post-magmatic alteration. The studied lamproites show porphyritic texture with carbonated and serpentinized olivine, diopside, fluorine-rich phlo-gopite, amphibole, apatite, chromite, allanite, and calcite. The trace-element geochemistry (elevated Sr and HFSE) reveals their mixed affinity to orogenic as well as anorogenic lamproites. Higher fluorine content of the hydrous phases coupled with higher whole-rock K 2 O highlights the role of metasomatic phlogopite and apatite in the mantle source regions. Trace-element ratios such as Zr/Hf and Ti/Eu reveal carbonate metasomatism of mantle previously enriched by ancient subduction processes. The initial 87 Sr/ 86 Sr-isotopic ratios (calculated for an assumed emplacement age of 1350 Ma) vary from 0.7037 to 0.7087 and ɛNd range from − 10.6 to − 9.3, consistent with data on global lamproites and ultrapotassic rocks. We attribute the mixed orogenic–anorogenic character for the lamproites under study to multi-stage metasomatism. We relate the (1) earlier subduction-related enrichment to the Paleoproterozoic amalgamation of the Columbia supercontinent and the (2) second episode of carbonate metasomatism to the Mesoproterozoic rift-related asthenospheric upwelling associated with the Columbia breakup. This study highlights the association of lamproites with supercontinent amalgamation and fragmentation in the Earth history. Keywords Lamproites · Mesoproterozoic · Dharwar craton · Carbonate metasomatism · Columbia · Supercontinents</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/37153968" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="e45f0a2f0dc0601bf5ea39a9af845a43" rel="nofollow" data-download="{"attachment_id":57104224,"asset_id":37153968,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/57104224/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="11470681" href="https://bhu-in.academia.edu/NVChalapathiRao">N.V.Chalapathi Rao</a><script data-card-contents-for-user="11470681" type="text/json">{"id":11470681,"first_name":"N.V.Chalapathi","last_name":"Rao","domain_name":"bhu-in","page_name":"NVChalapathiRao","display_name":"N.V.Chalapathi Rao","profile_url":"https://bhu-in.academia.edu/NVChalapathiRao?f_ri=15989","photo":"https://0.academia-photos.com/11470681/3337993/12279091/s65_n.v.chalapathi.rao.jpg"}</script></span></span></li><li class="js-paper-rank-work_37153968 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="37153968"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 37153968, container: ".js-paper-rank-work_37153968", }); });</script></li><li class="js-percentile-work_37153968 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 37153968; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_37153968"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_37153968 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="37153968"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 37153968; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=37153968]").text(description); $(".js-view-count-work_37153968").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_37153968").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="37153968"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i></div><span class="InlineList-item-text u-textTruncate u-pl6x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (false) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=37153968]'), work: {"id":37153968,"title":"Petrology and geochemistry of the Mesoproterozoic Vattikod lamproites, Eastern Dharwar Craton, southern India: evidence for multiple enrichment of sub-continental lithospheric mantle and links with amalgamation and break-up of the Columbia supercontinent","created_at":"2018-07-30T20:55:17.812-07:00","url":"https://www.academia.edu/37153968/Petrology_and_geochemistry_of_the_Mesoproterozoic_Vattikod_lamproites_Eastern_Dharwar_Craton_southern_India_evidence_for_multiple_enrichment_of_sub_continental_lithospheric_mantle_and_links_with_amalgamation_and_break_up_of_the_Columbia_supercontinent?f_ri=15989","dom_id":"work_37153968","summary":"Numerous lamproite dykes are hosted by the Eastern Dharwar Craton, southern India, particularly towards the northwestern margin of the Cuddapah Basin. We present here a comprehensive mineralogical and geochemical (including Sr and Nd isotopic) study on the lamproites from the Vattikod Field, exposed in the vicinity of the well-studied Ramadugu lamproite field. The Vattikod lamproites trend WNW–ESE to NW–SE and reveal effects of low-temperature post-magmatic alteration. The studied lamproites show porphyritic texture with carbonated and serpentinized olivine, diopside, fluorine-rich phlo-gopite, amphibole, apatite, chromite, allanite, and calcite. The trace-element geochemistry (elevated Sr and HFSE) reveals their mixed affinity to orogenic as well as anorogenic lamproites. Higher fluorine content of the hydrous phases coupled with higher whole-rock K 2 O highlights the role of metasomatic phlogopite and apatite in the mantle source regions. Trace-element ratios such as Zr/Hf and Ti/Eu reveal carbonate metasomatism of mantle previously enriched by ancient subduction processes. The initial 87 Sr/ 86 Sr-isotopic ratios (calculated for an assumed emplacement age of 1350 Ma) vary from 0.7037 to 0.7087 and ɛNd range from − 10.6 to − 9.3, consistent with data on global lamproites and ultrapotassic rocks. We attribute the mixed orogenic–anorogenic character for the lamproites under study to multi-stage metasomatism. We relate the (1) earlier subduction-related enrichment to the Paleoproterozoic amalgamation of the Columbia supercontinent and the (2) second episode of carbonate metasomatism to the Mesoproterozoic rift-related asthenospheric upwelling associated with the Columbia breakup. This study highlights the association of lamproites with supercontinent amalgamation and fragmentation in the Earth history. Keywords Lamproites · Mesoproterozoic · Dharwar craton · Carbonate metasomatism · Columbia · Supercontinents","downloadable_attachments":[{"id":57104224,"asset_id":37153968,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":11470681,"first_name":"N.V.Chalapathi","last_name":"Rao","domain_name":"bhu-in","page_name":"NVChalapathiRao","display_name":"N.V.Chalapathi Rao","profile_url":"https://bhu-in.academia.edu/NVChalapathiRao?f_ri=15989","photo":"https://0.academia-photos.com/11470681/3337993/12279091/s65_n.v.chalapathi.rao.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_36368054 coauthored" data-work_id="36368054" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/36368054/Experimental_constraints_on_metasomatism_of_mantle_wedge_peridotites_by_hybridized_adakitic_melts">Experimental constraints on metasomatism of mantle wedge peridotites by hybridized adakitic melts</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">In this study, a series of high-pressure (1.5 GPa) and high-temperature (1000–1300 °C) experiments were performed to investigate the petrological imprints of adakitic metasomatism on mantle wedge peridotites. Reaction couples were... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_36368054" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">In this study, a series of high-pressure (1.5 GPa) and high-temperature (1000–1300 °C) experiments were performed to investigate the petrological imprints of adakitic metasomatism on mantle wedge peridotites. Reaction couples were prepared using a powdered adakite from Cerro Pampa, Argentina (Mg# ~0.7) placed in contact with a cored sample of medium-grained protogranular depleted spinel lherzolite from Pali Aike (Chile). Textural and chemical analyses of the run products allow us to identify key features of modal metasomatism by hybridized adakitic melts. The main changes in phase relations are associated with the following metasomatic reactions: incongruent dissolution of olivine and associated precipitation of secondary orthopyroxene, dissolution of primary spinel and subsequent replacement by secondary high-Cr spinel. In experiments with high water contents (9–12 wt%), precipitation of pargasitic amphibole also occurred, possibly at the expense of primary clinopyroxene. Neither phlogopite nor Ti-oxides were precipitated in any of these experiments. As expected, primary pyroxenes do not show evidence of being significantly altered following the interaction with the produced siliceous melts. Within the adakitic portion of the experimental charge, it was also observed the crystallization of secondary Ti-rich, Cr-and Na-poor diopsidic clinopyroxene, andesine plagioclase and, at low temperature , Fe-enriched secondary orthopyroxene. Considering textural criteria, we interpreted the formation of these minerals as crystallization products of the adakite component and not as true products of metasomatic reactions. The experimental results are used to discuss some of the petrological evidences presented to support modal metasomatism by slab-derived melts of mantle xenoliths extracted from several suprasubduction settings located around the Pacific Ring of Fire.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/36368054" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="6c1a9b9135877fa94f9f1c0fcb55d4b8" rel="nofollow" data-download="{"attachment_id":56277429,"asset_id":36368054,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/56277429/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="27868342" href="https://uach.academia.edu/ManuelSchilling">Manuel Schilling</a><script data-card-contents-for-user="27868342" type="text/json">{"id":27868342,"first_name":"Manuel","last_name":"Schilling","domain_name":"uach","page_name":"ManuelSchilling","display_name":"Manuel Schilling","profile_url":"https://uach.academia.edu/ManuelSchilling?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-36368054">+1</span><div class="hidden js-additional-users-36368054"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://omp.academia.edu/MichelGregoire">Michel Gregoire</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-36368054'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-36368054').html(); 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Reaction couples were prepared using a powdered adakite from Cerro Pampa, Argentina (Mg# ~0.7) placed in contact with a cored sample of medium-grained protogranular depleted spinel lherzolite from Pali Aike (Chile). Textural and chemical analyses of the run products allow us to identify key features of modal metasomatism by hybridized adakitic melts. The main changes in phase relations are associated with the following metasomatic reactions: incongruent dissolution of olivine and associated precipitation of secondary orthopyroxene, dissolution of primary spinel and subsequent replacement by secondary high-Cr spinel. In experiments with high water contents (9–12 wt%), precipitation of pargasitic amphibole also occurred, possibly at the expense of primary clinopyroxene. Neither phlogopite nor Ti-oxides were precipitated in any of these experiments. As expected, primary pyroxenes do not show evidence of being significantly altered following the interaction with the produced siliceous melts. Within the adakitic portion of the experimental charge, it was also observed the crystallization of secondary Ti-rich, Cr-and Na-poor diopsidic clinopyroxene, andesine plagioclase and, at low temperature , Fe-enriched secondary orthopyroxene. Considering textural criteria, we interpreted the formation of these minerals as crystallization products of the adakite component and not as true products of metasomatic reactions. The experimental results are used to discuss some of the petrological evidences presented to support modal metasomatism by slab-derived melts of mantle xenoliths extracted from several suprasubduction settings located around the Pacific Ring of Fire.","downloadable_attachments":[{"id":56277429,"asset_id":36368054,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":27868342,"first_name":"Manuel","last_name":"Schilling","domain_name":"uach","page_name":"ManuelSchilling","display_name":"Manuel Schilling","profile_url":"https://uach.academia.edu/ManuelSchilling?f_ri=15989","photo":"/images/s65_no_pic.png"},{"id":10246740,"first_name":"Michel","last_name":"Gregoire","domain_name":"omp","page_name":"MichelGregoire","display_name":"Michel Gregoire","profile_url":"https://omp.academia.edu/MichelGregoire?f_ri=15989","photo":"https://0.academia-photos.com/10246740/3143594/153643901/s65_michel.gregoire.jpg"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=15989","nofollow":true},{"id":10251,"name":"Experimental Petrology","url":"https://www.academia.edu/Documents/in/Experimental_Petrology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_12912402" data-work_id="12912402" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/12912402/PETROGRAPHY_AND_GEOCHEMISTRY_OF_MAFIC_ROCKS_IN_AND_AROUND_SATI_AND_SARASPADA_NORTH_OF_BISOI_MAYURBHANJ_DISTRICT_NORTHERN_PART_OF_STATE_ORISSA_EASTERN_INDIA">PETROGRAPHY AND GEOCHEMISTRY OF MAFIC ROCKS IN AND AROUND SATI AND SARASPADA, NORTH OF BISOI, MAYURBHANJ DISTRICT, NORTHERN PART OF STATE ORISSA, EASTERN INDIA</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">This Geological study has been carried out in and around Saraspada and Sati, Northern part of Bisoi in the Mayurbhanj district at the northern part of the state of Orissa. The principle objective of this study was to thoroughly study the... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_12912402" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">This Geological study has been carried out in and around Saraspada and Sati, Northern part of Bisoi in the Mayurbhanj district at the northern part of the state of Orissa. The principle objective of this study was to thoroughly study the mafic rocks of the area. Numerous outcrops of this type of rocks were observed in the study area. Various field measurements including trend, grain size, mutual distribution, association with granitic country rock and sampling were performed, which fall within the toposheet no: 73 J/8. The mesoarchean-Paleoproterozoic stratigraphic record of the Singbhum crustal province, eastern India, implies sedimentation and volcanism in a changing tectonic scenario and thus assumes geological significance. Mafic magmatism in the craton spreads from 3.3 Ga (Oldest enclaves of amphibolltes) to about 0.1 Ga (Newer dolerite dyke group). The present study is based on evolution of magmatic rocks in relation to tectonic setting in a region which is southern extension of Singbhum shear zone.These outcrops occur as chain of hillocks with low elevation. Trend wise they vary from two main orientations: NW-SE and NE-SW. The dykes show variable grain size, texture and mineralogy. These basic dykes are found exclusively associated with Singhbhum granite. The bodies range in width from 20m to over 60m and in length of around 100m. Grain size varies from medium to coarse, with some fine grained varieties restricted to contact zones. Mineralogically, the mafic rock is mainly composed of orthopyroxene, clinopyroxene and plagioclase feldspar. Clinopyroxene grains are most abundant. Orthopyroxene grains are stubby shaped and highly fractured. Solely consisted groundmass plagioclase grains are unusually large and trap the pyroxenes as inclusion. A true magmatic texture of minerals is observed. Alteration of mineral is found generally near the contact of granitic body, otherwise the rock is fresh. This work consists of detailed petrographic study with the aid of high power microscopes, geochemical analysis and plotting modal analysis data, major element compositions, normative calculations, AFM diagram along with variation diagrams. In this purpose three important parameters are used i.e. SiO2 content, Mg no. and Differential Index (D.I). From the plotting of modal analysis data the name of the rock is Mela-gabbronorite. High Mg no. indicates the primitive character of magma. Plotting of the samples in AFM diagram inferred iron enrichment trends of the magma.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/12912402" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="95372eb2e7cdb9df43c77f0538cf237f" rel="nofollow" data-download="{"attachment_id":42789785,"asset_id":12912402,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/42789785/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="31900147" href="https://nitk.academia.edu/KALYANBRATAHATUI">KALYANBRATA HATUI</a><script data-card-contents-for-user="31900147" type="text/json">{"id":31900147,"first_name":"KALYANBRATA","last_name":"HATUI","domain_name":"nitk","page_name":"KALYANBRATAHATUI","display_name":"KALYANBRATA HATUI","profile_url":"https://nitk.academia.edu/KALYANBRATAHATUI?f_ri=15989","photo":"https://0.academia-photos.com/31900147/9566067/10656093/s65_kalyanbrata.hatui.jpg"}</script></span></span></li><li class="js-paper-rank-work_12912402 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="12912402"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 12912402, container: ".js-paper-rank-work_12912402", }); 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$(".js-view-count[data-work-id=12912402]").text(description); $(".js-view-count-work_12912402").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_12912402").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="12912402"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">6</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="407" rel="nofollow" href="https://www.academia.edu/Documents/in/Geochemistry">Geochemistry</a>, <script data-card-contents-for-ri="407" type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="16937" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry">Petrology and Geochemistry</a>, <script data-card-contents-for-ri="16937" type="text/json">{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="93887" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology_geochemistry">Igneous petrology, geochemistry</a><script data-card-contents-for-ri="93887" type="text/json">{"id":93887,"name":"Igneous petrology, geochemistry","url":"https://www.academia.edu/Documents/in/Igneous_petrology_geochemistry?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=12912402]'), work: {"id":12912402,"title":"PETROGRAPHY AND GEOCHEMISTRY OF MAFIC ROCKS IN AND AROUND SATI AND SARASPADA, NORTH OF BISOI, MAYURBHANJ DISTRICT, NORTHERN PART OF STATE ORISSA, EASTERN INDIA","created_at":"2015-06-10T15:28:54.999-07:00","url":"https://www.academia.edu/12912402/PETROGRAPHY_AND_GEOCHEMISTRY_OF_MAFIC_ROCKS_IN_AND_AROUND_SATI_AND_SARASPADA_NORTH_OF_BISOI_MAYURBHANJ_DISTRICT_NORTHERN_PART_OF_STATE_ORISSA_EASTERN_INDIA?f_ri=15989","dom_id":"work_12912402","summary":"\nThis Geological study has been carried out in and around Saraspada and Sati, Northern part of Bisoi in the Mayurbhanj district at the northern part of the state of Orissa. The principle objective of this study was to thoroughly study the mafic rocks of the area. Numerous outcrops of this type of rocks were observed in the study area. Various field measurements including trend, grain size, mutual distribution, association with granitic country rock and sampling were performed, which fall within the toposheet no: 73 J/8. The mesoarchean-Paleoproterozoic stratigraphic record of the Singbhum crustal province, eastern India, implies sedimentation and volcanism in a changing tectonic scenario and thus assumes geological significance. Mafic magmatism in the craton spreads from 3.3 Ga (Oldest enclaves of amphibolltes) to about 0.1 Ga (Newer dolerite dyke group). The present study is based on evolution of magmatic rocks in relation to tectonic setting in a region which is southern extension of Singbhum shear zone.These outcrops occur as chain of hillocks with low elevation. Trend wise they vary from two main orientations: NW-SE and NE-SW. The dykes show variable grain size, texture and mineralogy. These basic dykes are found exclusively associated with Singhbhum granite. The bodies range in width from 20m to over 60m and in length of around 100m. Grain size varies from medium to coarse, with some fine grained varieties restricted to contact zones. Mineralogically, the mafic rock is mainly composed of orthopyroxene, clinopyroxene and plagioclase feldspar. Clinopyroxene grains are most abundant. Orthopyroxene grains are stubby shaped and highly fractured. Solely consisted groundmass plagioclase grains are unusually large and trap the pyroxenes as inclusion. A true magmatic texture of minerals is observed. Alteration of mineral is found generally near the contact of granitic body, otherwise the rock is fresh. This work consists of detailed petrographic study with the aid of high power microscopes, geochemical analysis and plotting modal analysis data, major element compositions, normative calculations, AFM diagram along with variation diagrams. In this purpose three important parameters are used i.e. SiO2 content, Mg no. and Differential Index (D.I). From the plotting of modal analysis data the name of the rock is Mela-gabbronorite. High Mg no. indicates the primitive character of magma. Plotting of the samples in AFM diagram inferred iron enrichment trends of the magma. \n","downloadable_attachments":[{"id":42789785,"asset_id":12912402,"asset_type":"Work","always_allow_download":false},{"id":37877663,"asset_id":12912402,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":31900147,"first_name":"KALYANBRATA","last_name":"HATUI","domain_name":"nitk","page_name":"KALYANBRATAHATUI","display_name":"KALYANBRATA HATUI","profile_url":"https://nitk.academia.edu/KALYANBRATAHATUI?f_ri=15989","photo":"https://0.academia-photos.com/31900147/9566067/10656093/s65_kalyanbrata.hatui.jpg"}],"research_interests":[{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true},{"id":93887,"name":"Igneous petrology, geochemistry","url":"https://www.academia.edu/Documents/in/Igneous_petrology_geochemistry?f_ri=15989","nofollow":true},{"id":637087,"name":"Petrology and Geochemistry of Igneous Rocks","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry_of_Igneous_Rocks?f_ri=15989"},{"id":764863,"name":"Mafic Dikes","url":"https://www.academia.edu/Documents/in/Mafic_Dikes?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_6416917" data-work_id="6416917" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/6416917/PetroGraph_A_new_software_to_visualize_model_and_present_geochemical_data_in_igneous_petrology">PetroGraph: A new software to visualize, model, and present geochemical data in igneous petrology</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">1] A new software, PetroGraph, has been developed to visualize, elaborate, and model geochemical data for igneous petrology purposes. The software is able to plot data on several different diagrams, including a large number of... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_6416917" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">1] A new software, PetroGraph, has been developed to visualize, elaborate, and model geochemical data for igneous petrology purposes. The software is able to plot data on several different diagrams, including a large number of classification and ''petrotectonic'' plots. PetroGraph gives the opportunity to handle large geochemical data sets in a single program without the need of passing from one software to the other as usually happens in petrologic data handling. Along with these basic functions, PetroGraph contains a wide choice of modeling possibilities, from major element mass balance calculations to the most common partial melting and magma evolution models based on trace element and isotopic data. Results and graphs can be exported as vector graphics in publication-quality form, or they can be copied and pasted within the most common graphics programs for further modifications. All these features make PetroGraph one of the most complete software presently available for igneous petrology research.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/6416917" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="926b2d96d25e13698295883d7e6e3c6c" rel="nofollow" data-download="{"attachment_id":48876628,"asset_id":6416917,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/48876628/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="10100034" href="https://unipg.academia.edu/MaurizioPetrelli">Maurizio Petrelli</a><script data-card-contents-for-user="10100034" type="text/json">{"id":10100034,"first_name":"Maurizio","last_name":"Petrelli","domain_name":"unipg","page_name":"MaurizioPetrelli","display_name":"Maurizio Petrelli","profile_url":"https://unipg.academia.edu/MaurizioPetrelli?f_ri=15989","photo":"https://0.academia-photos.com/10100034/4844059/5574661/s65_maurizio.petrelli.jpg"}</script></span></span></li><li class="js-paper-rank-work_6416917 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="6416917"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 6416917, container: ".js-paper-rank-work_6416917", }); 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The software is able to plot data on several different diagrams, including a large number of classification and ''petrotectonic'' plots. PetroGraph gives the opportunity to handle large geochemical data sets in a single program without the need of passing from one software to the other as usually happens in petrologic data handling. Along with these basic functions, PetroGraph contains a wide choice of modeling possibilities, from major element mass balance calculations to the most common partial melting and magma evolution models based on trace element and isotopic data. Results and graphs can be exported as vector graphics in publication-quality form, or they can be copied and pasted within the most common graphics programs for further modifications. All these features make PetroGraph one of the most complete software presently available for igneous petrology research.","downloadable_attachments":[{"id":48876628,"asset_id":6416917,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":10100034,"first_name":"Maurizio","last_name":"Petrelli","domain_name":"unipg","page_name":"MaurizioPetrelli","display_name":"Maurizio Petrelli","profile_url":"https://unipg.academia.edu/MaurizioPetrelli?f_ri=15989","photo":"https://0.academia-photos.com/10100034/4844059/5574661/s65_maurizio.petrelli.jpg"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=15989","nofollow":true},{"id":8131,"name":"Data Management","url":"https://www.academia.edu/Documents/in/Data_Management?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences?f_ri=15989","nofollow":true},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting?f_ri=15989"},{"id":406250,"name":"Data Handling","url":"https://www.academia.edu/Documents/in/Data_Handling?f_ri=15989"},{"id":608519,"name":"Graphical Programming","url":"https://www.academia.edu/Documents/in/Graphical_Programming?f_ri=15989"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element?f_ri=15989"},{"id":1707373,"name":"Mass Balance","url":"https://www.academia.edu/Documents/in/Mass_Balance?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_30096014 coauthored" data-work_id="30096014" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/30096014/Geological_setting_and_geochemical_signatures_of_the_mafic_rocks_from_the_Intra_Pontide_Suture_Zone_implications_for_the_geodynamic_reconstruction_of_the_Mesozoic_Neotethys">Geological setting and geochemical signatures of the mafic rocks from the Intra‑Pontide Suture Zone: implications for the geodynamic reconstruction of the Mesozoic Neotethys</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">blueschist to sub-greenschist facies conditions. The meta-mafic rocks comprise actinolite-bearing schists and Na-amphibole-bearing varieties possibly derived from basaltic and gabbroic protoliths. They have a wide range of chemical... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_30096014" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">blueschist to sub-greenschist facies conditions. The meta-mafic rocks comprise actinolite-bearing schists and Na-amphibole-bearing varieties possibly derived from basaltic and gabbroic protoliths. They have a wide range of chemical compositions, displaying N-MORB-, E-MORB-, OIB-BABB-and IAT-type signatures. The Arkot Dağ Mèlange consists of a Late Santonian assemblage of slide-blocks mainly represented by basaltic lithologies showing affinities ranging from N-MORB-and IAT-to BABB-type mag-mas. The geochemical signature of the studied mafic rocks indicates that the tectonic units documented along the two studied transects of the Intra-Pontide Suture Zone have been derived from a supra-subduction zone. This hypothesis corroborates the available data collected from the Aylı Dağ Ophiolite Unit cropping out in the westernmost studied transect. This finding can provide new insights for the reconstruction of the geodynamic history of the Intra-Pon-tide domain.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/30096014" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="07f4845cb586fac51c8a034235547b7d" rel="nofollow" data-download="{"attachment_id":50556041,"asset_id":30096014,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/50556041/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="75904" href="https://metu.academia.edu/MCemalGoncuoglu">M. Cemal Goncuoglu</a><script data-card-contents-for-user="75904" type="text/json">{"id":75904,"first_name":"M. Cemal","last_name":"Goncuoglu","domain_name":"metu","page_name":"MCemalGoncuoglu","display_name":"M. Cemal Goncuoglu","profile_url":"https://metu.academia.edu/MCemalGoncuoglu?f_ri=15989","photo":"https://0.academia-photos.com/75904/20968/19436/s65_m._cemal.goncuoglu.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-30096014">+2</span><div class="hidden js-additional-users-30096014"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://metu.academia.edu/KaanSayit">Kaan Sayit</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://cnr-it.academia.edu/alessandroellero">alessandro ellero</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-30096014'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-30096014').html(); } } new HoverPopover(popoverSettings); 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The meta-mafic rocks comprise actinolite-bearing schists and Na-amphibole-bearing varieties possibly derived from basaltic and gabbroic protoliths. They have a wide range of chemical compositions, displaying N-MORB-, E-MORB-, OIB-BABB-and IAT-type signatures. The Arkot Dağ Mèlange consists of a Late Santonian assemblage of slide-blocks mainly represented by basaltic lithologies showing affinities ranging from N-MORB-and IAT-to BABB-type mag-mas. The geochemical signature of the studied mafic rocks indicates that the tectonic units documented along the two studied transects of the Intra-Pontide Suture Zone have been derived from a supra-subduction zone. This hypothesis corroborates the available data collected from the Aylı Dağ Ophiolite Unit cropping out in the westernmost studied transect. This finding can provide new insights for the reconstruction of the geodynamic history of the Intra-Pon-tide domain.","downloadable_attachments":[{"id":50556041,"asset_id":30096014,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":75904,"first_name":"M. Cemal","last_name":"Goncuoglu","domain_name":"metu","page_name":"MCemalGoncuoglu","display_name":"M. Cemal Goncuoglu","profile_url":"https://metu.academia.edu/MCemalGoncuoglu?f_ri=15989","photo":"https://0.academia-photos.com/75904/20968/19436/s65_m._cemal.goncuoglu.jpg"},{"id":33228092,"first_name":"Kaan","last_name":"Sayit","domain_name":"metu","page_name":"KaanSayit","display_name":"Kaan Sayit","profile_url":"https://metu.academia.edu/KaanSayit?f_ri=15989","photo":"/images/s65_no_pic.png"},{"id":23261104,"first_name":"alessandro","last_name":"ellero","domain_name":"cnr-it","page_name":"alessandroellero","display_name":"alessandro ellero","profile_url":"https://cnr-it.academia.edu/alessandroellero?f_ri=15989","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":10966,"name":"Turkey","url":"https://www.academia.edu/Documents/in/Turkey?f_ri=15989","nofollow":true},{"id":15947,"name":"Geodynamics","url":"https://www.academia.edu/Documents/in/Geodynamics?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":370212,"name":"Pontides","url":"https://www.academia.edu/Documents/in/Pontides?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_8806764" data-work_id="8806764" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/8806764/petrologi_daerah_OKU_selatan">petrologi daerah OKU selatan</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/8806764" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="7c019f77f02b269c08a86955701149b8" rel="nofollow" data-download="{"attachment_id":35153372,"asset_id":8806764,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/35153372/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="17468270" href="https://independent.academia.edu/januardihauw">januardi hauw</a><script data-card-contents-for-user="17468270" type="text/json">{"id":17468270,"first_name":"januardi","last_name":"hauw","domain_name":"independent","page_name":"januardihauw","display_name":"januardi hauw","profile_url":"https://independent.academia.edu/januardihauw?f_ri=15989","photo":"https://0.academia-photos.com/17468270/4856476/5587568/s65_januardi.hauw.jpg_oh_0e8a10a5a6fe15b4addb30b25f5d70e2_oe_54ba6840___gda___1418089174_2951fc31f122bae1f87a67f06ac4671a"}</script></span></span></li><li class="js-paper-rank-work_8806764 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="8806764"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 8806764, container: ".js-paper-rank-work_8806764", }); 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$(".js-view-count[data-work-id=8806764]").text(description); $(".js-view-count-work_8806764").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_8806764").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="8806764"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="2404" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology">Petrology</a>, <script data-card-contents-for-ri="2404" type="text/json">{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="16937" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry">Petrology and Geochemistry</a>, <script data-card-contents-for-ri="16937" type="text/json">{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="255222" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology">Igneous and Metamorphic Petrology</a><script data-card-contents-for-ri="255222" type="text/json">{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=8806764]'), work: {"id":8806764,"title":"petrologi daerah OKU selatan","created_at":"2014-10-15T22:50:53.421-07:00","url":"https://www.academia.edu/8806764/petrologi_daerah_OKU_selatan?f_ri=15989","dom_id":"work_8806764","summary":null,"downloadable_attachments":[{"id":35153372,"asset_id":8806764,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":17468270,"first_name":"januardi","last_name":"hauw","domain_name":"independent","page_name":"januardihauw","display_name":"januardi hauw","profile_url":"https://independent.academia.edu/januardihauw?f_ri=15989","photo":"https://0.academia-photos.com/17468270/4856476/5587568/s65_januardi.hauw.jpg_oh_0e8a10a5a6fe15b4addb30b25f5d70e2_oe_54ba6840___gda___1418089174_2951fc31f122bae1f87a67f06ac4671a"}],"research_interests":[{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989","nofollow":true},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology?f_ri=15989","nofollow":true},{"id":1421355,"name":"Petrologi","url":"https://www.academia.edu/Documents/in/Petrologi?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_27620063" data-work_id="27620063" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/27620063/The_volcanic_plutonic_connection_as_a_stage_for_understanding_crustal_magmatism">The volcanic–plutonic connection as a stage for understanding crustal magmatism</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Earth's magmatism produces both volcanic and plutonic rocks. These two rock types share many similarities, but also display significant differences that have led to a tendency to view (and study) them as separate realms. This review... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_27620063" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Earth's magmatism produces both volcanic and plutonic rocks. These two rock types share many similarities, but also display significant differences that have led to a tendency to view (and study) them as separate realms. This review tries to bridge the gap to provide more incentive to integrate data from all magmatic rocks in a hope to better understand the processes that led to the differentiation of the Earth and generation of a silicic continental crust. We strongly reinforce recent statements made in the literature suggesting that most disparities between volcanic and plutonic rocks can be resolved if volcanic rocks are seen as erupted melt-rich regions (magma "chambers") expelled from crystal-rich (mushy) reservoirs, which later crystallize to form plutons.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/27620063" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="40d82b3735f7ed20c1782289ed676d2a" rel="nofollow" data-download="{"attachment_id":47884988,"asset_id":27620063,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/47884988/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="32322267" href="https://independent.academia.edu/CalvinMiller1">Calvin Miller</a><script data-card-contents-for-user="32322267" type="text/json">{"id":32322267,"first_name":"Calvin","last_name":"Miller","domain_name":"independent","page_name":"CalvinMiller1","display_name":"Calvin Miller","profile_url":"https://independent.academia.edu/CalvinMiller1?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_27620063 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="27620063"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 27620063, container: ".js-paper-rank-work_27620063", }); 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These two rock types share many similarities, but also display significant differences that have led to a tendency to view (and study) them as separate realms. This review tries to bridge the gap to provide more incentive to integrate data from all magmatic rocks in a hope to better understand the processes that led to the differentiation of the Earth and generation of a silicic continental crust. We strongly reinforce recent statements made in the literature suggesting that most disparities between volcanic and plutonic rocks can be resolved if volcanic rocks are seen as erupted melt-rich regions (magma \"chambers\") expelled from crystal-rich (mushy) reservoirs, which later crystallize to form plutons.","downloadable_attachments":[{"id":47884988,"asset_id":27620063,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":32322267,"first_name":"Calvin","last_name":"Miller","domain_name":"independent","page_name":"CalvinMiller1","display_name":"Calvin Miller","profile_url":"https://independent.academia.edu/CalvinMiller1?f_ri=15989","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=15989","nofollow":true},{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":415322,"name":"Magma Chamber","url":"https://www.academia.edu/Documents/in/Magma_Chamber?f_ri=15989"},{"id":421956,"name":"Continental Crust","url":"https://www.academia.edu/Documents/in/Continental_Crust?f_ri=15989"},{"id":688910,"name":"Volcanic Rock","url":"https://www.academia.edu/Documents/in/Volcanic_Rock?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_11310695" data-work_id="11310695" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/11310695/Igneous_petrology">Igneous petrology</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The origin and emplacement of Large Igneous Provinces (LIPs) is a challenging research frontier in earth sciences that has implications for understanding: (a) the dynamics and evolution of the earth's mantle, (b) atmosphere and climatic... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_11310695" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The origin and emplacement of Large Igneous Provinces (LIPs) is a challenging research frontier in earth sciences that has implications for understanding: (a) the dynamics and evolution of the earth's mantle, (b) atmosphere and climatic shifts, (c) redistribution of land and oceans, (d) biosphere involving transfer and migration of flora and fauna and mass extinctions, (e) metallogeny, and (f) source of hydrocarbons. In this review, we appraise contemporary models for the origin of LIPs (plume versus non-plume) to evaluate their strengths and limitations. We also examine vexed issues (e.g. nature and extent of mantle heterogeneity, role of fluids in LIP genesis, relation amongst carbonatites, kimberlites and LIPs, linkage of dyke swarms to LIPs and continental reconstruction and metallogeny) which are not readily explained by any of the models. Pursuable research frontiers in Indian igneous provinces (e.g. identification of new LIPs in the Precambrian, Fe-enrichment, fertility and thermal state of mantle below India, detailed study of lava stratigraphy and palaeomagnetism, assessment of duration of LIP activities, irrespective of compositional variability) are identified for future study. Despite large-scale magma generation, crust-mantle interaction and geodynamic evolution of South Asia through the Phanerozoic, research on modern lines on Indian LIPs is limited. Research on LIPs deserves a major thrust in India for better understanding of the evolution of large magmatic provinces in the Peninsular and Extra-Peninsular regions.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/11310695" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="954ead91ed4689852fc523d62597edc0" rel="nofollow" data-download="{"attachment_id":36883409,"asset_id":11310695,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/36883409/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="27349251" href="https://independent.academia.edu/SarajitSensarma">Sarajit Sensarma</a><script data-card-contents-for-user="27349251" type="text/json">{"id":27349251,"first_name":"Sarajit","last_name":"Sensarma","domain_name":"independent","page_name":"SarajitSensarma","display_name":"Sarajit Sensarma","profile_url":"https://independent.academia.edu/SarajitSensarma?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_11310695 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="11310695"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 11310695, container: ".js-paper-rank-work_11310695", }); });</script></li><li class="js-percentile-work_11310695 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 11310695; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_11310695"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_11310695 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="11310695"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 11310695; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=11310695]").text(description); $(".js-view-count-work_11310695").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_11310695").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="11310695"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i></div><span class="InlineList-item-text u-textTruncate u-pl6x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (false) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=11310695]'), work: {"id":11310695,"title":"Igneous petrology","created_at":"2015-03-06T12:16:13.803-08:00","url":"https://www.academia.edu/11310695/Igneous_petrology?f_ri=15989","dom_id":"work_11310695","summary":"The origin and emplacement of Large Igneous Provinces (LIPs) is a challenging research frontier in earth sciences that has implications for understanding: (a) the dynamics and evolution of the earth's mantle, (b) atmosphere and climatic shifts, (c) redistribution of land and oceans, (d) biosphere involving transfer and migration of flora and fauna and mass extinctions, (e) metallogeny, and (f) source of hydrocarbons. In this review, we appraise contemporary models for the origin of LIPs (plume versus non-plume) to evaluate their strengths and limitations. We also examine vexed issues (e.g. nature and extent of mantle heterogeneity, role of fluids in LIP genesis, relation amongst carbonatites, kimberlites and LIPs, linkage of dyke swarms to LIPs and continental reconstruction and metallogeny) which are not readily explained by any of the models. Pursuable research frontiers in Indian igneous provinces (e.g. identification of new LIPs in the Precambrian, Fe-enrichment, fertility and thermal state of mantle below India, detailed study of lava stratigraphy and palaeomagnetism, assessment of duration of LIP activities, irrespective of compositional variability) are identified for future study. Despite large-scale magma generation, crust-mantle interaction and geodynamic evolution of South Asia through the Phanerozoic, research on modern lines on Indian LIPs is limited. Research on LIPs deserves a major thrust in India for better understanding of the evolution of large magmatic provinces in the Peninsular and Extra-Peninsular regions.","downloadable_attachments":[{"id":36883409,"asset_id":11310695,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":27349251,"first_name":"Sarajit","last_name":"Sensarma","domain_name":"independent","page_name":"SarajitSensarma","display_name":"Sarajit Sensarma","profile_url":"https://independent.academia.edu/SarajitSensarma?f_ri=15989","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_32028690 coauthored" data-work_id="32028690" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/32028690/The_Geology_of_the_Tecolotlan_Graben_Jalisco_Mexico">The Geology of the Tecolotlan Graben, Jalisco, Mexico</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Tecolotlan valley is a small graben ~110 km southwest of Guadalajara in the northeastern corner of the Jalisco block of west-central Mexico. The graben trends roughly north-south, is ~10 km wide and 20 km long, with ~500 m of... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_32028690" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Tecolotlan valley is a small graben ~110 km southwest of Guadalajara in the northeastern corner of the Jalisco block of west-central Mexico. The graben trends roughly north-south, is ~10 km wide and 20 km long, with ~500 m of topographic relief. It is bounded to the east by a horst of Cretaceous (Albian/Cenomanian) limestone and to the west by a block of Late Cretaceous volcaniclastic sedimentary rocks, lava fl ows, and ignimbrites (one is 77 Ma). These volcanic rocks have chemical and mineralogical affi nities with continental volcanic arc sequences and record a history of arc volcanism and sedimentation during the Late Cretaceous. The sequence (over 300 m thick) consists of rhyolitic ash-fl ow tuffs and trachytic lava fl ows (lacking pillow structures) interbedded with volcanic debris fl ow deposits, arkosic fl uvial sand-stones, and volcanic conglomerates. This suggests that by the Late Cretaceous the continental arc was emergent, but probably still low-standing as it continued to accumulate sediment after the closure of the Arperos oceanic basin and accretion of the Guerrero arc terrane to Mexico. The Tecolotlan valley contains discontinuously deposited latest Miocene to Recent sediments that are important for their record of extension, magmatism, and diverse vertebrate fauna. Neogene basin fi ll is divided into older, Late Hemphillian age (ca. 5–4.8 Ma) sedimentary rocks (~50–60 m) that are mostly fi ne-grained fl uvial and overbank deposits, and younger, Late Blancan–Recent (younger than ca. 2.7 Ma) sediments (up to 30 m thick) that consist of coarse-grained, high-energy, fl uvial deposits. Intercalated with the basin-fi ll sedimentary rocks are isolated lava fl ows and pyro-clastic-fall beds. It appears that volcanism and extension in the Tecolotlan graben occurred simultaneously with a period of increased volcanic activity along the ESE-WNW–trending Tepic-Zacoalco graben. Although extension and volcanism ceased by</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/32028690" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2f9fce98772ab222fc709e9f071d12dc" rel="nofollow" data-download="{"attachment_id":52292474,"asset_id":32028690,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/52292474/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="1260193" href="https://byu.academia.edu/BartKowallis">Bart Kowallis</a><script data-card-contents-for-user="1260193" type="text/json">{"id":1260193,"first_name":"Bart","last_name":"Kowallis","domain_name":"byu","page_name":"BartKowallis","display_name":"Bart Kowallis","profile_url":"https://byu.academia.edu/BartKowallis?f_ri=15989","photo":"https://0.academia-photos.com/1260193/461177/11953429/s65_bart.kowallis.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-32028690">+2</span><div class="hidden js-additional-users-32028690"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://byu.academia.edu/EricChristiansen">Eric H Christiansen</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://byu.academia.edu/KerynRoss">Keryn Ross</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-32028690'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-32028690').html(); } } new HoverPopover(popoverSettings); })();</script></li><li class="js-paper-rank-work_32028690 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="32028690"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 32028690, container: ".js-paper-rank-work_32028690", }); });</script></li><li class="js-percentile-work_32028690 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 32028690; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_32028690"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_32028690 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="32028690"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 32028690; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=32028690]").text(description); $(".js-view-count-work_32028690").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_32028690").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="32028690"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">8</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="420" rel="nofollow" href="https://www.academia.edu/Documents/in/Sedimentology">Sedimentology</a>, <script data-card-contents-for-ri="420" type="text/json">{"id":420,"name":"Sedimentology","url":"https://www.academia.edu/Documents/in/Sedimentology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1034" rel="nofollow" href="https://www.academia.edu/Documents/in/Stratigraphy">Stratigraphy</a>, <script data-card-contents-for-ri="1034" type="text/json">{"id":1034,"name":"Stratigraphy","url":"https://www.academia.edu/Documents/in/Stratigraphy?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="10769" rel="nofollow" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=32028690]'), work: {"id":32028690,"title":"The Geology of the Tecolotlan Graben, Jalisco, Mexico","created_at":"2017-03-24T11:00:06.707-07:00","url":"https://www.academia.edu/32028690/The_Geology_of_the_Tecolotlan_Graben_Jalisco_Mexico?f_ri=15989","dom_id":"work_32028690","summary":"The Tecolotlan valley is a small graben ~110 km southwest of Guadalajara in the northeastern corner of the Jalisco block of west-central Mexico. The graben trends roughly north-south, is ~10 km wide and 20 km long, with ~500 m of topographic relief. It is bounded to the east by a horst of Cretaceous (Albian/Cenomanian) limestone and to the west by a block of Late Cretaceous volcaniclastic sedimentary rocks, lava fl ows, and ignimbrites (one is 77 Ma). These volcanic rocks have chemical and mineralogical affi nities with continental volcanic arc sequences and record a history of arc volcanism and sedimentation during the Late Cretaceous. The sequence (over 300 m thick) consists of rhyolitic ash-fl ow tuffs and trachytic lava fl ows (lacking pillow structures) interbedded with volcanic debris fl ow deposits, arkosic fl uvial sand-stones, and volcanic conglomerates. This suggests that by the Late Cretaceous the continental arc was emergent, but probably still low-standing as it continued to accumulate sediment after the closure of the Arperos oceanic basin and accretion of the Guerrero arc terrane to Mexico. The Tecolotlan valley contains discontinuously deposited latest Miocene to Recent sediments that are important for their record of extension, magmatism, and diverse vertebrate fauna. Neogene basin fi ll is divided into older, Late Hemphillian age (ca. 5–4.8 Ma) sedimentary rocks (~50–60 m) that are mostly fi ne-grained fl uvial and overbank deposits, and younger, Late Blancan–Recent (younger than ca. 2.7 Ma) sediments (up to 30 m thick) that consist of coarse-grained, high-energy, fl uvial deposits. Intercalated with the basin-fi ll sedimentary rocks are isolated lava fl ows and pyro-clastic-fall beds. It appears that volcanism and extension in the Tecolotlan graben occurred simultaneously with a period of increased volcanic activity along the ESE-WNW–trending Tepic-Zacoalco graben. Although extension and volcanism ceased by","downloadable_attachments":[{"id":52292474,"asset_id":32028690,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":1260193,"first_name":"Bart","last_name":"Kowallis","domain_name":"byu","page_name":"BartKowallis","display_name":"Bart Kowallis","profile_url":"https://byu.academia.edu/BartKowallis?f_ri=15989","photo":"https://0.academia-photos.com/1260193/461177/11953429/s65_bart.kowallis.jpg"},{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H Christiansen","profile_url":"https://byu.academia.edu/EricChristiansen?f_ri=15989","photo":"https://0.academia-photos.com/76756/84665/284057/s65_eric.christiansen.jpg"},{"id":35044206,"first_name":"Keryn","last_name":"Ross","domain_name":"byu","page_name":"KerynRoss","display_name":"Keryn Ross","profile_url":"https://byu.academia.edu/KerynRoss?f_ri=15989","photo":"https://0.academia-photos.com/35044206/10198130/11380930/s65_keryn.ross.jpg"}],"research_interests":[{"id":420,"name":"Sedimentology","url":"https://www.academia.edu/Documents/in/Sedimentology?f_ri=15989","nofollow":true},{"id":1034,"name":"Stratigraphy","url":"https://www.academia.edu/Documents/in/Stratigraphy?f_ri=15989","nofollow":true},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":43881,"name":"Mexico","url":"https://www.academia.edu/Documents/in/Mexico?f_ri=15989"},{"id":63798,"name":"Cretaceous","url":"https://www.academia.edu/Documents/in/Cretaceous?f_ri=15989"},{"id":82227,"name":"Geological mapping","url":"https://www.academia.edu/Documents/in/Geological_mapping?f_ri=15989"},{"id":146480,"name":"Cenozoic","url":"https://www.academia.edu/Documents/in/Cenozoic?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_12187021" data-work_id="12187021" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/12187021/A_review_of_helicopter_borne_electromagnetic_methods_for_groundwater_exploration">A review of helicopter-borne electromagnetic methods for groundwater exploration</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">For about three decades, airborne electromagnetic (AEM) systems have been used for groundwater exploration purposes. Airborne systems are appropriate for large-scale and efficient groundwater surveying. Due to the dependency of the... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_12187021" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">For about three decades, airborne electromagnetic (AEM) systems have been used for groundwater exploration purposes. Airborne systems are appropriate for large-scale and efficient groundwater surveying. Due to the dependency of the electrical conductivity on both the clay content of the host material and the mineralization of the water, electromagnetic systems are suitable for providing information about the aquifer structures and water quality, respectively.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/12187021" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="0810445c69d2c7ebb4a69e6df205dbd7" rel="nofollow" data-download="{"attachment_id":46313143,"asset_id":12187021,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/46313143/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="30630852" href="https://independent.academia.edu/BernhardSiemon">Bernhard Siemon</a><script data-card-contents-for-user="30630852" type="text/json">{"id":30630852,"first_name":"Bernhard","last_name":"Siemon","domain_name":"independent","page_name":"BernhardSiemon","display_name":"Bernhard Siemon","profile_url":"https://independent.academia.edu/BernhardSiemon?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_12187021 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="12187021"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 12187021, container: ".js-paper-rank-work_12187021", }); 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Airborne systems are appropriate for large-scale and efficient groundwater surveying. Due to the dependency of the electrical conductivity on both the clay content of the host material and the mineralization of the water, electromagnetic systems are suitable for providing information about the aquifer structures and water quality, respectively.","downloadable_attachments":[{"id":46313143,"asset_id":12187021,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":30630852,"first_name":"Bernhard","last_name":"Siemon","domain_name":"independent","page_name":"BernhardSiemon","display_name":"Bernhard Siemon","profile_url":"https://independent.academia.edu/BernhardSiemon?f_ri=15989","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":403,"name":"Gemology","url":"https://www.academia.edu/Documents/in/Gemology?f_ri=15989","nofollow":true},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=15989","nofollow":true},{"id":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology?f_ri=15989","nofollow":true},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=15989"},{"id":410,"name":"Glaciology","url":"https://www.academia.edu/Documents/in/Glaciology?f_ri=15989"},{"id":411,"name":"Hydrogeology","url":"https://www.academia.edu/Documents/in/Hydrogeology?f_ri=15989"},{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989"},{"id":417,"name":"Paleontology","url":"https://www.academia.edu/Documents/in/Paleontology?f_ri=15989"},{"id":421,"name":"Soil Science","url":"https://www.academia.edu/Documents/in/Soil_Science?f_ri=15989"},{"id":1034,"name":"Stratigraphy","url":"https://www.academia.edu/Documents/in/Stratigraphy?f_ri=15989"},{"id":2403,"name":"Environmental Geology","url":"https://www.academia.edu/Documents/in/Environmental_Geology?f_ri=15989"},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989"},{"id":2406,"name":"Economic Geology","url":"https://www.academia.edu/Documents/in/Economic_Geology?f_ri=15989"},{"id":3869,"name":"Geobiology","url":"https://www.academia.edu/Documents/in/Geobiology?f_ri=15989"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":20564,"name":"Engineering Geology","url":"https://www.academia.edu/Documents/in/Engineering_Geology?f_ri=15989"},{"id":42192,"name":"Near surface Geophysics","url":"https://www.academia.edu/Documents/in/Near_surface_Geophysics?f_ri=15989"},{"id":64108,"name":"Paleogeography","url":"https://www.academia.edu/Documents/in/Paleogeography?f_ri=15989"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism?f_ri=15989"},{"id":417165,"name":"Volcanism","url":"https://www.academia.edu/Documents/in/Volcanism?f_ri=15989"},{"id":505937,"name":"Regional Geology","url":"https://www.academia.edu/Documents/in/Regional_Geology?f_ri=15989"},{"id":581258,"name":"Hazards","url":"https://www.academia.edu/Documents/in/Hazards?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_19923045" data-work_id="19923045" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/19923045/A_numerical_comparison_of_2D_resistivity_imaging_with_10_electrode_arrays">A numerical comparison of 2D resistivity imaging with 10 electrode arrays</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">This paper compares the resolution and efficiency of 2D resistivity imaging survey with eight electrode arrays by numerical simulations. The arrays analysed include the pole-pole (PP), pole-dipole (PD), pole-bipole (PB), Wenner-α (WN),... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_19923045" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">This paper compares the resolution and efficiency of 2D resistivity imaging survey with eight electrode arrays by numerical simulations. The arrays analysed include the pole-pole (PP), pole-dipole (PD), pole-bipole (PB), Wenner-α (WN), Schlumberger (SC), dipole-dipole (DD), Wenner-β (WB), γ-array (GM), gradient (GD) and midpoint-potential-referred measurements (MPR) arrays. Five synthetic geological models that simulate a buried channel, narrow conductive dyke, narrow resistive dyke, dipping blocks and covered waste ponds were used to examine the surveying efficiency (anomaly effects, signal-noise ratios) and the imaging capabilities of these arrays. Also, the response to variations in data density and noise sensitivities of these electrode configurations were investigated using the robust inversion and smoothness-constrained least-squares ( 2 L -norm) inversion for the five synthetic models. The results show that: (1) GM and WN have less noise contamination than other electrode arrays;</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/19923045" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="94fc84f2c9e9254c8939f61cb7135d21" rel="nofollow" data-download="{"attachment_id":41277414,"asset_id":19923045,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/41277414/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="40776392" href="https://lu.academia.edu/TorleifDahlin">Torleif Dahlin</a><script data-card-contents-for-user="40776392" type="text/json">{"id":40776392,"first_name":"Torleif","last_name":"Dahlin","domain_name":"lu","page_name":"TorleifDahlin","display_name":"Torleif Dahlin","profile_url":"https://lu.academia.edu/TorleifDahlin?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_19923045 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="19923045"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 19923045, container: ".js-paper-rank-work_19923045", }); 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The arrays analysed include the pole-pole (PP), pole-dipole (PD), pole-bipole (PB), Wenner-α (WN), Schlumberger (SC), dipole-dipole (DD), Wenner-β (WB), γ-array (GM), gradient (GD) and midpoint-potential-referred measurements (MPR) arrays. Five synthetic geological models that simulate a buried channel, narrow conductive dyke, narrow resistive dyke, dipping blocks and covered waste ponds were used to examine the surveying efficiency (anomaly effects, signal-noise ratios) and the imaging capabilities of these arrays. Also, the response to variations in data density and noise sensitivities of these electrode configurations were investigated using the robust inversion and smoothness-constrained least-squares ( 2 L -norm) inversion for the five synthetic models. The results show that: (1) GM and WN have less noise contamination than other electrode arrays;","downloadable_attachments":[{"id":41277414,"asset_id":19923045,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":40776392,"first_name":"Torleif","last_name":"Dahlin","domain_name":"lu","page_name":"TorleifDahlin","display_name":"Torleif 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Problem","url":"https://www.academia.edu/Documents/in/Inverse_Problem?f_ri=15989"},{"id":219927,"name":"Efficiency","url":"https://www.academia.edu/Documents/in/Efficiency?f_ri=15989"},{"id":264349,"name":"Dikes","url":"https://www.academia.edu/Documents/in/Dikes?f_ri=15989"},{"id":309086,"name":"High Resolution","url":"https://www.academia.edu/Documents/in/High_Resolution?f_ri=15989"},{"id":417165,"name":"Volcanism","url":"https://www.academia.edu/Documents/in/Volcanism?f_ri=15989"},{"id":505937,"name":"Regional Geology","url":"https://www.academia.edu/Documents/in/Regional_Geology?f_ri=15989"},{"id":537404,"name":"Least Squares","url":"https://www.academia.edu/Documents/in/Least_Squares?f_ri=15989"},{"id":581258,"name":"Hazards","url":"https://www.academia.edu/Documents/in/Hazards?f_ri=15989"},{"id":846015,"name":"Electrodes","url":"https://www.academia.edu/Documents/in/Electrodes?f_ri=15989"},{"id":909150,"name":"Electrode","url":"https://www.academia.edu/Documents/in/Electrode?f_ri=15989"},{"id":991311,"name":"Signal to Noise Ratio","url":"https://www.academia.edu/Documents/in/Signal_to_Noise_Ratio?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_39407266" data-work_id="39407266" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/39407266/THE_NATURE_AND_ORIGIN_OF_PEBBLE_DIKES_AND_ASSOCIATED_ALTERATION_TINTIC_MINING_DISTRICT_AG_PB_ZN_AU_UTAH">THE NATURE AND ORIGIN OF PEBBLE DIKES AND ASSOCIATED ALTERATION: TINTIC MINING DISTRICT (AG-PB-ZN-AU), UTAH</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">In many ore deposits throughout the world, brecciation often accompanies or occurs in association with minerali-zation. Such is the case in the Tintic mining district (Ag-Pb-Zn-Au) of north-central Utah, where unique breccia features... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_39407266" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">In many ore deposits throughout the world, brecciation often accompanies or occurs in association with minerali-zation. Such is the case in the Tintic mining district (Ag-Pb-Zn-Au) of north-central Utah, where unique breccia features called pebble dikes occur alongside significant mineralization. Pebble dikes are tabular bodies of breccia, which consist of angular to rounded clasts of quartzite, shale, carbonate, and minor igneous rock cemented in a fine-grained clastic matrix. All clasts now lie above or adjacent to corresponding source rocks. Dikes are thin, typically less than 0.3 m wide to as much as 1 m, and can exceed 100 m in length. The average of the largest clast size is less than 3 cm but correlates positively with pebble dike width. Contacts are sharp and envelopes of fine breccia surround roughly half of the dikes; parallel sub-vertical fractures are also common. Pebble dikes are mostly hosted in an Eocene rhyolite lava flow, which displays argillic to silicic alteration where in contact with pebble dikes, but the dikes are also hosted in an assortment of deformed Paleozoic sedimentary rocks. The pebble dikes have a strong northeast trend, following a regional fabric of northeast-trending strike-slip and oblique-slip faults. The formation of pebble dikes has been historically attributed to the intrusion of the Silver City stock, the Tintic district's main productive intrusion. However, pebble dikes in the eastern part of the Tintic district are spatially associated with a previously unrecognized andesitic unit, informally named the porphyry of North Lily, which is texturally, mineralogically, and chemically distinct from the Silver City stock, and like pebble dikes, was emplaced in northeast-trending plugs and dikes. In addition to the strong spatial association, there are clasts of the porphyry of North Lily in the pebble dikes, and quartzite clasts like those in the pebble dikes are found as xenoliths in the porphyry of North Lily. Some of the igneous dikes are comingled with the pebble dikes. These similarities and interactions suggest simultaneous formation. Geochemical alteration patterns revealed by isocon analysis show no enrichments in Cu, Pb, or Zn related to the pebble dikes. This is consistent with their formation before major mineralization. Low-grade alteration associated with pebble dikes indicates that they formed at elevated temperatures (100-170°C). Stable isotope (O and H) compositions of rhyolite altered by the pebble dikes show they formed in the presence of heated groundwater, with very low water/rock ratios, and little to no magmatic water association. The overall physical, spatial, and chemical characteristics of pebble dikes of the Tintic mining district suggest that they formed by the mobilization of breccia during the explosive expansion of groundwater that had been heated by the intrusion of the porphyry of North Lily. This escape occurred along pre-existing, northeast-trending faults and fractures and created new fractures with similar orienta-tions. These phreatic explosions released early hydrothermal fluids and enhanced permeability, serving as "ground preparation" by forming pathways for later mineralizing fluids.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/39407266" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="922dcbc1895758b54925833b032d7d4e" rel="nofollow" data-download="{"attachment_id":59552081,"asset_id":39407266,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/59552081/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="76756" href="https://byu.academia.edu/EricChristiansen">Eric H Christiansen</a><script data-card-contents-for-user="76756" type="text/json">{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H Christiansen","profile_url":"https://byu.academia.edu/EricChristiansen?f_ri=15989","photo":"https://0.academia-photos.com/76756/84665/284057/s65_eric.christiansen.jpg"}</script></span></span></li><li class="js-paper-rank-work_39407266 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="39407266"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 39407266, container: ".js-paper-rank-work_39407266", }); 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$(".js-view-count[data-work-id=39407266]").text(description); $(".js-view-count-work_39407266").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_39407266").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="39407266"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">3</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="32424" rel="nofollow" href="https://www.academia.edu/Documents/in/Hydrothermal_systems">Hydrothermal systems</a>, <script data-card-contents-for-ri="32424" type="text/json">{"id":32424,"name":"Hydrothermal systems","url":"https://www.academia.edu/Documents/in/Hydrothermal_systems?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="46378" rel="nofollow" href="https://www.academia.edu/Documents/in/Ore_Geology">Ore Geology</a><script data-card-contents-for-ri="46378" type="text/json">{"id":46378,"name":"Ore Geology","url":"https://www.academia.edu/Documents/in/Ore_Geology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=39407266]'), work: {"id":39407266,"title":"THE NATURE AND ORIGIN OF PEBBLE DIKES AND ASSOCIATED ALTERATION: TINTIC MINING DISTRICT (AG-PB-ZN-AU), UTAH","created_at":"2019-06-06T10:11:29.206-07:00","url":"https://www.academia.edu/39407266/THE_NATURE_AND_ORIGIN_OF_PEBBLE_DIKES_AND_ASSOCIATED_ALTERATION_TINTIC_MINING_DISTRICT_AG_PB_ZN_AU_UTAH?f_ri=15989","dom_id":"work_39407266","summary":"In many ore deposits throughout the world, brecciation often accompanies or occurs in association with minerali-zation. Such is the case in the Tintic mining district (Ag-Pb-Zn-Au) of north-central Utah, where unique breccia features called pebble dikes occur alongside significant mineralization. Pebble dikes are tabular bodies of breccia, which consist of angular to rounded clasts of quartzite, shale, carbonate, and minor igneous rock cemented in a fine-grained clastic matrix. All clasts now lie above or adjacent to corresponding source rocks. Dikes are thin, typically less than 0.3 m wide to as much as 1 m, and can exceed 100 m in length. The average of the largest clast size is less than 3 cm but correlates positively with pebble dike width. Contacts are sharp and envelopes of fine breccia surround roughly half of the dikes; parallel sub-vertical fractures are also common. Pebble dikes are mostly hosted in an Eocene rhyolite lava flow, which displays argillic to silicic alteration where in contact with pebble dikes, but the dikes are also hosted in an assortment of deformed Paleozoic sedimentary rocks. The pebble dikes have a strong northeast trend, following a regional fabric of northeast-trending strike-slip and oblique-slip faults. The formation of pebble dikes has been historically attributed to the intrusion of the Silver City stock, the Tintic district's main productive intrusion. However, pebble dikes in the eastern part of the Tintic district are spatially associated with a previously unrecognized andesitic unit, informally named the porphyry of North Lily, which is texturally, mineralogically, and chemically distinct from the Silver City stock, and like pebble dikes, was emplaced in northeast-trending plugs and dikes. In addition to the strong spatial association, there are clasts of the porphyry of North Lily in the pebble dikes, and quartzite clasts like those in the pebble dikes are found as xenoliths in the porphyry of North Lily. Some of the igneous dikes are comingled with the pebble dikes. These similarities and interactions suggest simultaneous formation. Geochemical alteration patterns revealed by isocon analysis show no enrichments in Cu, Pb, or Zn related to the pebble dikes. This is consistent with their formation before major mineralization. Low-grade alteration associated with pebble dikes indicates that they formed at elevated temperatures (100-170°C). Stable isotope (O and H) compositions of rhyolite altered by the pebble dikes show they formed in the presence of heated groundwater, with very low water/rock ratios, and little to no magmatic water association. The overall physical, spatial, and chemical characteristics of pebble dikes of the Tintic mining district suggest that they formed by the mobilization of breccia during the explosive expansion of groundwater that had been heated by the intrusion of the porphyry of North Lily. This escape occurred along pre-existing, northeast-trending faults and fractures and created new fractures with similar orienta-tions. These phreatic explosions released early hydrothermal fluids and enhanced permeability, serving as \"ground preparation\" by forming pathways for later mineralizing fluids.","downloadable_attachments":[{"id":59552081,"asset_id":39407266,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H Christiansen","profile_url":"https://byu.academia.edu/EricChristiansen?f_ri=15989","photo":"https://0.academia-photos.com/76756/84665/284057/s65_eric.christiansen.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":32424,"name":"Hydrothermal systems","url":"https://www.academia.edu/Documents/in/Hydrothermal_systems?f_ri=15989","nofollow":true},{"id":46378,"name":"Ore Geology","url":"https://www.academia.edu/Documents/in/Ore_Geology?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_11106677 coauthored" data-work_id="11106677" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/11106677/First_report_on_Mesozoic_eclogite_facies_metamorphism_preceding_Barrovian_overprint_from_the_western_Rhodope_Chalkidiki_northern_Greece_">First-report on Mesozoic eclogite-facies metamorphism preceding Barrovian overprint from the western Rhodope (Chalkidiki, northern Greece)</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Chalkidiki block in Northern Greece represents the southwesternmost piece of the ultrahigh-pressure Rhodope and has played an important role in the evolution of the North Aegean. The eastern part of the Chalkidiki block is a basement... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_11106677" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Chalkidiki block in Northern Greece represents the southwesternmost piece of the ultrahigh-pressure Rhodope<br />and has played an important role in the evolution of the North Aegean. The eastern part of the Chalkidiki block is<br />a basement complex (Vertiskos Unit) that is made largely of Palaeozoic granitoids and clastic sediments that<br />metamorphosed during the Mesozoic. This basement is traditionally considered as part of the Rhodopean<br />hanging-wall, an assignment mainly supported by the absence of high-pressure mineral indicators and the<br />presence of a regional medium-pressure/medium-temperature amphibolite-facies Barrovian metamorphic<br />imprint. Toward the west, the basement is juxtaposed with meta-sedimentary (Circum-Rhodope belt) and arc<br />units (Chortiatis Magmatic Suite) that carry evidence of a Mesozoic high-pressure/low-temperature event. In<br />this study, garnet–staurolite-mica schists from the eastern part of the basement were examined by means of<br />micro-textures, mineral chemistry and isochemical phase-diagram sections in the system NCKFMASHMn(Ti)<br />[Na2O–CaO–K2O–FeO–MgO–Al2O3–SiO2–H2O–MnO–(TiO2)]. The schists represent former Mesozoic sedimentary<br />sequences deposited on the Palaeozoic basement. We document the presence of a relict eclogite-facies<br />mineral assemblage (garnet + chloritoid + phengite + rutile) in an amphibolite-facies matrix composed of<br />garnet + staurolite + phengite ± kyanite. Model results suggest the existence of a high-pressure/<br />medium-temperature metamorphic event (1.9 GPa/520 °C) that preceded regional re-equilibration at<br />medium-pressure/medium-temperature conditions (1.2 GPa/620 °C). Clearly, the eastern part of the Chalkidiki<br />block (basement complex) retains memory of an as yet unidentified Mesozoic eclogitic metamorphic event<br />that was largely erased by the later Barrovian overprint. In light of our findings, the basement complex of the<br />Chalkidiki block shares a common tectono-metamorphic evolution with both the high-pressure units to<br />the west, and the high-grade Rhodopean gneisses further to the northeast. Our results are consequential for<br />the geodynamic reconstruction of the Rhodope since they require participation of the Chalkidiki block to the<br />well-established Mesozoic subduction system.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/11106677" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="48c54bc462b1218d0d92a2c9d2eb4a0c" rel="nofollow" data-download="{"attachment_id":36779895,"asset_id":11106677,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/36779895/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="32756580" href="https://univ-rennes1.academia.edu/JeanPierreBrun">Jean-Pierre Brun</a><script data-card-contents-for-user="32756580" type="text/json">{"id":32756580,"first_name":"Jean-Pierre","last_name":"Brun","domain_name":"univ-rennes1","page_name":"JeanPierreBrun","display_name":"Jean-Pierre Brun","profile_url":"https://univ-rennes1.academia.edu/JeanPierreBrun?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-11106677">+2</span><div class="hidden js-additional-users-11106677"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://uoa.academia.edu/DimitriosKostopoulos">Dimitrios Kostopoulos</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://univ-rennes1.academia.edu/KonstantinosKydonakis">Konstantinos Kydonakis</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-11106677'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-11106677').html(); 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container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_11106677 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="11106677"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 11106677; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=11106677]").text(description); $(".js-view-count-work_11106677").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_11106677").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="11106677"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">15</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="414" rel="nofollow" href="https://www.academia.edu/Documents/in/Mineralogy">Mineralogy</a>, <script data-card-contents-for-ri="414" type="text/json">{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1419" rel="nofollow" href="https://www.academia.edu/Documents/in/Structural_Geology">Structural Geology</a>, <script data-card-contents-for-ri="1419" type="text/json">{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="2404" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrology">Petrology</a><script data-card-contents-for-ri="2404" type="text/json">{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=11106677]'), work: {"id":11106677,"title":"First-report on Mesozoic eclogite-facies metamorphism preceding Barrovian overprint from the western Rhodope (Chalkidiki, northern Greece)","created_at":"2015-02-26T03:08:36.805-08:00","url":"https://www.academia.edu/11106677/First_report_on_Mesozoic_eclogite_facies_metamorphism_preceding_Barrovian_overprint_from_the_western_Rhodope_Chalkidiki_northern_Greece_?f_ri=15989","dom_id":"work_11106677","summary":"The Chalkidiki block in Northern Greece represents the southwesternmost piece of the ultrahigh-pressure Rhodope\nand has played an important role in the evolution of the North Aegean. The eastern part of the Chalkidiki block is\na basement complex (Vertiskos Unit) that is made largely of Palaeozoic granitoids and clastic sediments that\nmetamorphosed during the Mesozoic. This basement is traditionally considered as part of the Rhodopean\nhanging-wall, an assignment mainly supported by the absence of high-pressure mineral indicators and the\npresence of a regional medium-pressure/medium-temperature amphibolite-facies Barrovian metamorphic\nimprint. Toward the west, the basement is juxtaposed with meta-sedimentary (Circum-Rhodope belt) and arc\nunits (Chortiatis Magmatic Suite) that carry evidence of a Mesozoic high-pressure/low-temperature event. In\nthis study, garnet–staurolite-mica schists from the eastern part of the basement were examined by means of\nmicro-textures, mineral chemistry and isochemical phase-diagram sections in the system NCKFMASHMn(Ti)\n[Na2O–CaO–K2O–FeO–MgO–Al2O3–SiO2–H2O–MnO–(TiO2)]. The schists represent former Mesozoic sedimentary\nsequences deposited on the Palaeozoic basement. We document the presence of a relict eclogite-facies\nmineral assemblage (garnet + chloritoid + phengite + rutile) in an amphibolite-facies matrix composed of\ngarnet + staurolite + phengite ± kyanite. Model results suggest the existence of a high-pressure/\nmedium-temperature metamorphic event (1.9 GPa/520 °C) that preceded regional re-equilibration at\nmedium-pressure/medium-temperature conditions (1.2 GPa/620 °C). Clearly, the eastern part of the Chalkidiki\nblock (basement complex) retains memory of an as yet unidentified Mesozoic eclogitic metamorphic event\nthat was largely erased by the later Barrovian overprint. In light of our findings, the basement complex of the\nChalkidiki block shares a common tectono-metamorphic evolution with both the high-pressure units to\nthe west, and the high-grade Rhodopean gneisses further to the northeast. Our results are consequential for\nthe geodynamic reconstruction of the Rhodope since they require participation of the Chalkidiki block to the\nwell-established Mesozoic subduction system.","downloadable_attachments":[{"id":36779895,"asset_id":11106677,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":32756580,"first_name":"Jean-Pierre","last_name":"Brun","domain_name":"univ-rennes1","page_name":"JeanPierreBrun","display_name":"Jean-Pierre Brun","profile_url":"https://univ-rennes1.academia.edu/JeanPierreBrun?f_ri=15989","photo":"/images/s65_no_pic.png"},{"id":77293,"first_name":"Dimitrios","last_name":"Kostopoulos","domain_name":"uoa","page_name":"DimitriosKostopoulos","display_name":"Dimitrios Kostopoulos","profile_url":"https://uoa.academia.edu/DimitriosKostopoulos?f_ri=15989","photo":"https://0.academia-photos.com/77293/21425/19557489/s65_dimitrios.kostopoulos.png"},{"id":956971,"first_name":"Konstantinos","last_name":"Kydonakis","domain_name":"univ-rennes1","page_name":"KonstantinosKydonakis","display_name":"Konstantinos Kydonakis","profile_url":"https://univ-rennes1.academia.edu/KonstantinosKydonakis?f_ri=15989","photo":"https://0.academia-photos.com/956971/420782/518286/s65_konstantinos.kydonakis.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=15989","nofollow":true},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989","nofollow":true},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=15989","nofollow":true},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=15989"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989"},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":16073,"name":"Continental Subduction","url":"https://www.academia.edu/Documents/in/Continental_Subduction?f_ri=15989"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=15989"},{"id":17285,"name":"Field Geology","url":"https://www.academia.edu/Documents/in/Field_Geology?f_ri=15989"},{"id":44748,"name":"Subduction Zone Processes","url":"https://www.academia.edu/Documents/in/Subduction_Zone_Processes?f_ri=15989"},{"id":94128,"name":"Subduction Zone Metamorphism","url":"https://www.academia.edu/Documents/in/Subduction_Zone_Metamorphism?f_ri=15989"},{"id":122773,"name":"Subduction","url":"https://www.academia.edu/Documents/in/Subduction?f_ri=15989"},{"id":315416,"name":"Subduction tectonics","url":"https://www.academia.edu/Documents/in/Subduction_tectonics?f_ri=15989"},{"id":333831,"name":"Subduction Zones","url":"https://www.academia.edu/Documents/in/Subduction_Zones?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_1232264" data-work_id="1232264" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/1232264/The_formation_and_fate_of_large_oceanic_igneous_provinces">The formation and fate of large oceanic igneous provinces</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Large igneous provinces are conspicuous features of late Phanerozoic geology, and include continental flood basalts, rifted continental margin volcanic sequences and oceanic plateaus. The latter are formed in an environment which... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_1232264" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Large igneous provinces are conspicuous features of late Phanerozoic geology, and include continental flood basalts, rifted continental margin volcanic sequences and oceanic plateaus. The latter are formed in an environment which typically recycles back into the mantle on a time scale of < 200 m.y., but because comparisons have recently been made between oceanic plateaus and Precambrian greenstone belt sequences, new questions arise about their formation, their fate and their preservation. Here we review some critical aspects of three oceanic plateaus, Ontong Java, Kerguelen and the Caribbean/Colombian obducted plateau, and comment on their make-up and the factors governing their preservation, with particular relevance to ancient terranes.Many large igneous provinces can be linked to mantle plumes. Where plumes ascend beneath spreading ridges, their energy is transformed into a large melt volume, producing over-thickened plateau crust. Where the spreading rate is low in relation to magma supply, the plateau may become subaerial (e.g. Iceland), but with fast spreading the plateau remains submarine. Thicker lithosphere may result in plume incubation before magma extrusion, and there are many intermediate situations where plumes could readily break through thin lithosphere (oceanic or continental). Because magma supply exceeds extension rate, plateaus may be characterised by thick sequences of flows and sills rather than the sheeted dykes typical of Phanerozoic ophiolites. Precambrian greenstones could represent imbricated oceanic plateaus, or plumes penetrating thin continental lithosphere.The initial high temperature and the buoyant nature of the depleted refractory keel of plateaus contributes to their preservation relative to normal oceanic crust. When they collide with active margins they choke the subduction zone, causing subduction “flip” or “backstep” and the development of extensive calc-alkaline arc volcanism on top of the plateau sequences. However, after ⪢ 100 m.y. they are potentially negatively buoyant, so if fluids become available to promote transformation of the deeper zones to eclogite, they may be able to spontaneously subduct.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/1232264" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="b8b37fba736d1a15f95940155deb7174" rel="nofollow" data-download="{"attachment_id":18990508,"asset_id":1232264,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/18990508/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="1278771" href="https://cardiff.academia.edu/AndrewKerr">Andrew Kerr</a><script data-card-contents-for-user="1278771" type="text/json">{"id":1278771,"first_name":"Andrew","last_name":"Kerr","domain_name":"cardiff","page_name":"AndrewKerr","display_name":"Andrew Kerr","profile_url":"https://cardiff.academia.edu/AndrewKerr?f_ri=15989","photo":"https://0.academia-photos.com/1278771/469059/590910/s65_andrew.kerr.jpg"}</script></span></span></li><li class="js-paper-rank-work_1232264 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="1232264"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 1232264, container: ".js-paper-rank-work_1232264", }); });</script></li><li class="js-percentile-work_1232264 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 1232264; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_1232264"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_1232264 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="1232264"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 1232264; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=1232264]").text(description); $(".js-view-count-work_1232264").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_1232264").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="1232264"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">3</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="45278" rel="nofollow" href="https://www.academia.edu/Documents/in/Large_Igneous_Provinces">Large Igneous Provinces</a>, <script data-card-contents-for-ri="45278" type="text/json">{"id":45278,"name":"Large Igneous Provinces","url":"https://www.academia.edu/Documents/in/Large_Igneous_Provinces?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="294416" rel="nofollow" href="https://www.academia.edu/Documents/in/Mechanism_of_Obduction">Mechanism of Obduction</a><script data-card-contents-for-ri="294416" type="text/json">{"id":294416,"name":"Mechanism of Obduction","url":"https://www.academia.edu/Documents/in/Mechanism_of_Obduction?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=1232264]'), work: {"id":1232264,"title":"The formation and fate of large oceanic igneous provinces","created_at":"2012-06-17T21:34:56.820-07:00","url":"https://www.academia.edu/1232264/The_formation_and_fate_of_large_oceanic_igneous_provinces?f_ri=15989","dom_id":"work_1232264","summary":"Large igneous provinces are conspicuous features of late Phanerozoic geology, and include continental flood basalts, rifted continental margin volcanic sequences and oceanic plateaus. The latter are formed in an environment which typically recycles back into the mantle on a time scale of \u003c 200 m.y., but because comparisons have recently been made between oceanic plateaus and Precambrian greenstone belt sequences, new questions arise about their formation, their fate and their preservation. Here we review some critical aspects of three oceanic plateaus, Ontong Java, Kerguelen and the Caribbean/Colombian obducted plateau, and comment on their make-up and the factors governing their preservation, with particular relevance to ancient terranes.Many large igneous provinces can be linked to mantle plumes. Where plumes ascend beneath spreading ridges, their energy is transformed into a large melt volume, producing over-thickened plateau crust. Where the spreading rate is low in relation to magma supply, the plateau may become subaerial (e.g. Iceland), but with fast spreading the plateau remains submarine. Thicker lithosphere may result in plume incubation before magma extrusion, and there are many intermediate situations where plumes could readily break through thin lithosphere (oceanic or continental). Because magma supply exceeds extension rate, plateaus may be characterised by thick sequences of flows and sills rather than the sheeted dykes typical of Phanerozoic ophiolites. Precambrian greenstones could represent imbricated oceanic plateaus, or plumes penetrating thin continental lithosphere.The initial high temperature and the buoyant nature of the depleted refractory keel of plateaus contributes to their preservation relative to normal oceanic crust. When they collide with active margins they choke the subduction zone, causing subduction “flip” or “backstep” and the development of extensive calc-alkaline arc volcanism on top of the plateau sequences. However, after ⪢ 100 m.y. they are potentially negatively buoyant, so if fluids become available to promote transformation of the deeper zones to eclogite, they may be able to spontaneously subduct.","downloadable_attachments":[{"id":18990508,"asset_id":1232264,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":1278771,"first_name":"Andrew","last_name":"Kerr","domain_name":"cardiff","page_name":"AndrewKerr","display_name":"Andrew Kerr","profile_url":"https://cardiff.academia.edu/AndrewKerr?f_ri=15989","photo":"https://0.academia-photos.com/1278771/469059/590910/s65_andrew.kerr.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":45278,"name":"Large Igneous Provinces","url":"https://www.academia.edu/Documents/in/Large_Igneous_Provinces?f_ri=15989","nofollow":true},{"id":294416,"name":"Mechanism of Obduction","url":"https://www.academia.edu/Documents/in/Mechanism_of_Obduction?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_362218" data-work_id="362218" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/362218/Trends_in_rhyolite_geochemistry_mineralogy_and_magma_storage_during_the_last_50_kyr_at_Okataina_and_Taupo_volcanic_centres_Taupo_Volcanic_Zone_New_Zealand"> Trends in rhyolite geochemistry, mineralogy, and magma storage during the last 50 kyr at Okataina and Taupo volcanic centres, Taupo Volcanic Zone, New Zealand</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div 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class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="276352" href="https://oxford.academia.edu/VictoriaSmith">Victoria Smith</a><script data-card-contents-for-user="276352" type="text/json">{"id":276352,"first_name":"Victoria","last_name":"Smith","domain_name":"oxford","page_name":"VictoriaSmith","display_name":"Victoria Smith","profile_url":"https://oxford.academia.edu/VictoriaSmith?f_ri=15989","photo":"https://0.academia-photos.com/276352/57054/1063748/s65_victoria.smith.jpg"}</script></span></span></li><li class="js-paper-rank-work_362218 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="362218"><i class="u-m1x fa fa-bar-chart"></i><strong 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href="https://www.academia.edu/14185384/Monogenetic_volcanic_fields_Origin_sedimentary_record_and_relationship_with_polygenetic_volcanism">Monogenetic volcanic fields: Origin, sedimentary record, and relationship with polygenetic volcanism</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/14185384" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="ab67c6de2d904a8f54109ba2678bd610" rel="nofollow" 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}); });</script></span><script>$(function() { $(".js-view-count-work_14185384").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="14185384"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">4</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="420" rel="nofollow" href="https://www.academia.edu/Documents/in/Sedimentology">Sedimentology</a>, <script data-card-contents-for-ri="420" type="text/json">{"id":420,"name":"Sedimentology","url":"https://www.academia.edu/Documents/in/Sedimentology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1370" rel="nofollow" href="https://www.academia.edu/Documents/in/Volcanology">Volcanology</a>, <script data-card-contents-for-ri="1370" type="text/json">{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=14185384]'), work: {"id":14185384,"title":"Monogenetic volcanic fields: Origin, sedimentary record, and relationship with polygenetic volcanism","created_at":"2015-07-19T03:19:24.755-07:00","url":"https://www.academia.edu/14185384/Monogenetic_volcanic_fields_Origin_sedimentary_record_and_relationship_with_polygenetic_volcanism?f_ri=15989","dom_id":"work_14185384","summary":null,"downloadable_attachments":[{"id":44525513,"asset_id":14185384,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":33170306,"first_name":"Karoly","last_name":"Nemeth","domain_name":"massey","page_name":"KarolyNemeth","display_name":"Karoly 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u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/27597286/Pengertian_Batuan_Beku">Pengertian Batuan Beku</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest">Berisikan tentang pengertian  batuan beku , petrogenesa atau asal usul  batuan beku , dan klasifikasi  batuan beku</div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/27597286" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="0a5cd9157fafafee29d15229b11a3064" rel="nofollow" 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}); });</script></span><script>$(function() { $(".js-view-count-work_27597286").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="27597286"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">3</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1411207" rel="nofollow" href="https://www.academia.edu/Documents/in/Batuan_Beku">Batuan Beku</a>, <script data-card-contents-for-ri="1411207" type="text/json">{"id":1411207,"name":"Batuan Beku","url":"https://www.academia.edu/Documents/in/Batuan_Beku?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1421355" rel="nofollow" href="https://www.academia.edu/Documents/in/Petrologi">Petrologi</a><script data-card-contents-for-ri="1421355" type="text/json">{"id":1421355,"name":"Petrologi","url":"https://www.academia.edu/Documents/in/Petrologi?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=27597286]'), work: {"id":27597286,"title":"Pengertian Batuan Beku","created_at":"2016-08-07T06:15:30.047-07:00","url":"https://www.academia.edu/27597286/Pengertian_Batuan_Beku?f_ri=15989","dom_id":"work_27597286","summary":"Berisikan tentang pengertian batuan beku , petrogenesa atau asal usul batuan beku , dan klasifikasi batuan beku","downloadable_attachments":[{"id":47859553,"asset_id":27597286,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":16313645,"first_name":"As","last_name":"Sunnah","domain_name":"independent","page_name":"AryoMaulana","display_name":"As Sunnah","profile_url":"https://independent.academia.edu/AryoMaulana?f_ri=15989","photo":"https://0.academia-photos.com/16313645/4426738/14834014/s65_aryo.maulana.jpg"}],"research_interests":[{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":1411207,"name":"Batuan Beku","url":"https://www.academia.edu/Documents/in/Batuan_Beku?f_ri=15989","nofollow":true},{"id":1421355,"name":"Petrologi","url":"https://www.academia.edu/Documents/in/Petrologi?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_11934228" data-work_id="11934228" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/11934228/Fatima_suture_A_new_amalgamation_zone_in_the_western_Arabian_Shield_Saudi_Arabia">Fatima suture: A new amalgamation zone in the western Arabian Shield, Saudi Arabia</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">We describe a new amalgamation zone between Jiddah and Asir juvenile arc terranes in the western Arabian Shield. Ophiolitic rocks in this zone were deformed by a NE-SW oriented belt of opposite-verging... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_11934228" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">We  describe  a  new  amalgamation  zone  between  Jiddah  and  Asir  juvenile  arc  terranes  in  the  western  Arabian  Shield.  Ophiolitic  rocks  in  this  zone  were  deformed  by  a  NE-SW  oriented  belt  of  opposite-verging<br />overturned  folds  and  thrust  faults,  whereas  two  granitic  complexes  intruded  mainly  through  its  axial<br />uplift.  Chemical  characteristics  of  these  rocks  indicate  that  they  formed  in  an  arc  suprasubduction  zone<br />setting.  The  amalgamation  between  Jiddah  and  Asir  terranes  is  explained  mainly  in  terms  of  two  events<br />followed  by  two  more  events  related  to  convergence  between  eastern  and  western  Arabian  superterranes.<br />NW-SE  shortenings  and  dextral  transpression  of  the  first  three  events  induced  more  structural  elements<br />and  tectonic  fabrics  than  those  developed  during  the  youngest  shortening  event.  Tectonic  fabrics  differentiate  between  the  stress  orientations  during  the  oldest  deformation  events.  Variations  in  attitudes  and<br />shear  senses  throughout  these  structural  and  tectonic  elements  support  strain  partitioning.  Deformation  related  to  assembly  of  the  Jiddah  and  Asir  terranes  started  during  ophiolite  emplacement  at  812  Ma<br />and  ended  before  the  deposition  of  the  post-amalgamation  Fatima  basin.  A  northwestward  shortening<br />inverted  this  basin  and  developed  NW-verging  thrust  faults  and  folds.  Tectonic  evolution  of  Fatima  suture<br />zone  is  correlated  with  the  major  tectonic  settings  of  the  Arabian  Shield.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/11934228" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="dea6db5e8dcf087b553c5b448d692f63" rel="nofollow" data-download="{"attachment_id":37298130,"asset_id":11934228,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/37298130/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="3777116" href="https://kau.academia.edu/AhmedHassan">Ahmed Hassan</a><script data-card-contents-for-user="3777116" type="text/json">{"id":3777116,"first_name":"Ahmed","last_name":"Hassan","domain_name":"kau","page_name":"AhmedHassan","display_name":"Ahmed Hassan","profile_url":"https://kau.academia.edu/AhmedHassan?f_ri=15989","photo":"https://0.academia-photos.com/3777116/1368630/1687583/s65_ahmed.hassan.jpg"}</script></span></span></li><li class="js-paper-rank-work_11934228 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="11934228"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 11934228, container: ".js-paper-rank-work_11934228", }); });</script></li><li class="js-percentile-work_11934228 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 11934228; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_11934228"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_11934228 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="11934228"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 11934228; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=11934228]").text(description); $(".js-view-count-work_11934228").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_11934228").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="11934228"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">2</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="1419" rel="nofollow" href="https://www.academia.edu/Documents/in/Structural_Geology">Structural Geology</a>, <script data-card-contents-for-ri="1419" type="text/json">{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a><script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=11934228]'), work: {"id":11934228,"title":"Fatima suture: A new amalgamation zone in the western Arabian Shield, Saudi Arabia","created_at":"2015-04-13T21:20:43.245-07:00","url":"https://www.academia.edu/11934228/Fatima_suture_A_new_amalgamation_zone_in_the_western_Arabian_Shield_Saudi_Arabia?f_ri=15989","dom_id":"work_11934228","summary":"We describe a new amalgamation zone between Jiddah and Asir juvenile arc terranes in the western Arabian Shield. Ophiolitic rocks in this zone were deformed by a NE-SW oriented belt of opposite-verging\noverturned folds and thrust faults, whereas two granitic complexes intruded mainly through its axial\nuplift. Chemical characteristics of these rocks indicate that they formed in an arc suprasubduction zone\nsetting. The amalgamation between Jiddah and Asir terranes is explained mainly in terms of two events\nfollowed by two more events related to convergence between eastern and western Arabian superterranes.\nNW-SE shortenings and dextral transpression of the first three events induced more structural elements\nand tectonic fabrics than those developed during the youngest shortening event. Tectonic fabrics differentiate between the stress orientations during the oldest deformation events. Variations in attitudes and\nshear senses throughout these structural and tectonic elements support strain partitioning. Deformation related to assembly of the Jiddah and Asir terranes started during ophiolite emplacement at 812 Ma\nand ended before the deposition of the post-amalgamation Fatima basin. A northwestward shortening\ninverted this basin and developed NW-verging thrust faults and folds. Tectonic evolution of Fatima suture\nzone is correlated with the major tectonic settings of the Arabian Shield.","downloadable_attachments":[{"id":37298130,"asset_id":11934228,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":3777116,"first_name":"Ahmed","last_name":"Hassan","domain_name":"kau","page_name":"AhmedHassan","display_name":"Ahmed Hassan","profile_url":"https://kau.academia.edu/AhmedHassan?f_ri=15989","photo":"https://0.academia-photos.com/3777116/1368630/1687583/s65_ahmed.hassan.jpg"}],"research_interests":[{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_36216566" data-work_id="36216566" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/36216566/Extensive_young_silicic_volcanism_produces_large_deep_submarine_lava_flows_in_the_NE_Lau_Basin">Extensive young silicic volcanism produces large deep submarine lava flows in the NE Lau Basin</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">New field observations reveal that extensive (up to ~ 402 km 2) aphyric, glassy dacite lavas were erupted at multiple sites in the recent past in the NE Lau basin, located about 200 km southwest of Samoa. This discovery of volumetrically... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_36216566" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">New field observations reveal that extensive (up to ~ 402 km 2) aphyric, glassy dacite lavas were erupted at multiple sites in the recent past in the NE Lau basin, located about 200 km southwest of Samoa. This discovery of volumetrically significant and widespread submarine dacite lava flows extends the domain for siliceous effusive volcanism into the deep seafloor. Although several lava flow fields were discovered on the flank of a large silicic seamount, Niuatahi, two of the largest lava fields and several smaller ones (Bnorthern lava flow fields^) were found well north of the seamount. The most distal portion of the northernmost of these fields is 60 km north of the center of Niuatahi caldera. We estimate that lava flow lengths from probable eruptive vents to the distal ends of flows range from a few km to more than 10 km. Camera tows on the shallower, near-vent areas show complex lava morphology that includes anastomosing tube-like pillow flows and ropey surfaces, endogenous domes and/or ridges, some with Bcrease-like^ extrusion ridges, and inflated lobes with extrusion structures. A 2 × 1.5 km, 30-m deep depression could be an eruption center for one of the lava flow fields. The Lau lava flow fields appear to have erupted at presumptive high effusion rates and possibly reduced viscosity induced by presumptive high magmatic water content and/or a high eruption temperature, consistent with both erupted composition (~ 66% SiO 2) and glassy low crystallinity groundmass textures. The large areal extent (236 km 2) and relatively small range of compositional variation (σ = 0.60 for wt% Si0 2 %) within the northern lava flow fields imply the existence of large, eruptible batches of differentiated melt in the upper mantle or lower crust of the NE Lau basin. At this site, the volcanism could be controlled by deep crustal fractures caused by the long-term extension in this rear-arc region. Submarine dacite flows exhibiting similar morphology have been described in ancient sequences from the Archaean through the Miocene and in small batches on present-day seafloor spreading centers. This study shows that extensive siliceous lavas can erupt on the modern seafloor under the right conditions.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/36216566" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2ee1da2999759448452ec22969c286df" rel="nofollow" data-download="{"attachment_id":56119419,"asset_id":36216566,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/56119419/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="32620320" href="https://uri.academia.edu/KennaRubin">Kenna H Rubin</a><script data-card-contents-for-user="32620320" type="text/json">{"id":32620320,"first_name":"Kenna","last_name":"Rubin","domain_name":"uri","page_name":"KennaRubin","display_name":"Kenna H Rubin","profile_url":"https://uri.academia.edu/KennaRubin?f_ri=15989","photo":"https://0.academia-photos.com/32620320/19331405/167187107/s65_kenna.rubin.jpg"}</script></span></span></li><li class="js-paper-rank-work_36216566 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="36216566"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 36216566, container: ".js-paper-rank-work_36216566", }); });</script></li><li class="js-percentile-work_36216566 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 36216566; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_36216566"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_36216566 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="36216566"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 36216566; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=36216566]").text(description); $(".js-view-count-work_36216566").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_36216566").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="36216566"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">7</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" rel="nofollow" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="408" rel="nofollow" href="https://www.academia.edu/Documents/in/Geomorphology">Geomorphology</a>, <script data-card-contents-for-ri="408" type="text/json">{"id":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="1370" rel="nofollow" href="https://www.academia.edu/Documents/in/Volcanology">Volcanology</a>, <script data-card-contents-for-ri="1370" type="text/json">{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="10769" rel="nofollow" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a><script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=36216566]'), work: {"id":36216566,"title":"Extensive young silicic volcanism produces large deep submarine lava flows in the NE Lau Basin","created_at":"2018-03-21T02:31:53.059-07:00","url":"https://www.academia.edu/36216566/Extensive_young_silicic_volcanism_produces_large_deep_submarine_lava_flows_in_the_NE_Lau_Basin?f_ri=15989","dom_id":"work_36216566","summary":"New field observations reveal that extensive (up to ~ 402 km 2) aphyric, glassy dacite lavas were erupted at multiple sites in the recent past in the NE Lau basin, located about 200 km southwest of Samoa. This discovery of volumetrically significant and widespread submarine dacite lava flows extends the domain for siliceous effusive volcanism into the deep seafloor. Although several lava flow fields were discovered on the flank of a large silicic seamount, Niuatahi, two of the largest lava fields and several smaller ones (Bnorthern lava flow fields^) were found well north of the seamount. The most distal portion of the northernmost of these fields is 60 km north of the center of Niuatahi caldera. We estimate that lava flow lengths from probable eruptive vents to the distal ends of flows range from a few km to more than 10 km. Camera tows on the shallower, near-vent areas show complex lava morphology that includes anastomosing tube-like pillow flows and ropey surfaces, endogenous domes and/or ridges, some with Bcrease-like^ extrusion ridges, and inflated lobes with extrusion structures. A 2 × 1.5 km, 30-m deep depression could be an eruption center for one of the lava flow fields. The Lau lava flow fields appear to have erupted at presumptive high effusion rates and possibly reduced viscosity induced by presumptive high magmatic water content and/or a high eruption temperature, consistent with both erupted composition (~ 66% SiO 2) and glassy low crystallinity groundmass textures. The large areal extent (236 km 2) and relatively small range of compositional variation (σ = 0.60 for wt% Si0 2 %) within the northern lava flow fields imply the existence of large, eruptible batches of differentiated melt in the upper mantle or lower crust of the NE Lau basin. At this site, the volcanism could be controlled by deep crustal fractures caused by the long-term extension in this rear-arc region. Submarine dacite flows exhibiting similar morphology have been described in ancient sequences from the Archaean through the Miocene and in small batches on present-day seafloor spreading centers. This study shows that extensive siliceous lavas can erupt on the modern seafloor under the right conditions.","downloadable_attachments":[{"id":56119419,"asset_id":36216566,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":32620320,"first_name":"Kenna","last_name":"Rubin","domain_name":"uri","page_name":"KennaRubin","display_name":"Kenna H Rubin","profile_url":"https://uri.academia.edu/KennaRubin?f_ri=15989","photo":"https://0.academia-photos.com/32620320/19331405/167187107/s65_kenna.rubin.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=15989","nofollow":true},{"id":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology?f_ri=15989","nofollow":true},{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989"},{"id":16441,"name":"Marine Science","url":"https://www.academia.edu/Documents/in/Marine_Science?f_ri=15989"},{"id":74033,"name":"Mapping","url":"https://www.academia.edu/Documents/in/Mapping?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_23152101" data-work_id="23152101" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/23152101/Tectonic_evolution_of_the_Lachlan_Orogen_southeast_Australia_historical_review_data_synthesis_and_modern_perspectives">Tectonic evolution of the Lachlan Orogen, southeast Australia: historical review, data synthesis and modern perspectives</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Lachlan Orogen, like many other orogenic belts, has undergone paradigm shifts from geosynclinal to plate-tectonic theory of evolution over the past 40 years. Initial plate-tectonic interpretations were based on lithologic associations... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_23152101" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Lachlan Orogen, like many other orogenic belts, has undergone paradigm shifts from geosynclinal to plate-tectonic theory of evolution over the past 40 years. Initial plate-tectonic interpretations were based on lithologic associations and recognition of key plate-tectonic elements such as andesites and palaeo-subduction complexes. Understanding and knowledge of modern plate settings led to the application of actualistic models and the development of palaeogeographical reconstructions, commonly using a non-palinspastic base. Igneous petrology and geochemistry led to characterisation of granite types into 'I' and 'S', the delineation of granite basement terranes, and to nonmobilistic tectonic scenarios involving plumes as a heat source to drive crustal melting and lithospheric deformation. More recently, measurements of isotopic tracers (Nd, Sr, Pb) and U-Pb SHRIMP age determinations on inherited zircons from granitoids and detrital zircons from sedimentary successions led to the development of multiple component mixing models to explain granite geochemistry. These have focused tectonic arguments for magma genesis again more on plate interactions. The recognition of fault zones in the turbidites, their polydeformed character and their thin-skinned nature, as well as belts of distinct tectonic vergence has led to a major reassessment of tectonic development. Other geochemical studies on Cambrian metavolcanic belts showed that the basement was partly backarc basin-and forearc basin-type oceanic crust. The application of 40 Ar-39 Ar geochronology and thermochronology on slates, schist and granitoids has better constrained the timing of deformation and plutonism, and illite crystallinity and b o mica spacing studies on slates have better defined the background metamorphic conditions in the low-grade parts. The Lachlan deformation pattern involves three thrust systems that constitute the western Lachlan Orogen, central Lachlan Orogen and eastern Lachlan Orogen. The faults in the western Lachlan Orogen show a generalised east-younging (450-395 Ma), which probably relates to imbrication and rock uplift of the sediment wedge, because detailed analyses show that the décollement system is as old in the east as it is in the west. Overall, deformation in the eastern Lachlan Orogen is younger (400-380 Ma), apart from the Narooma Accretionary Complex ( ca 445 Ma). Preservation of extensional basins and evidence for basin inversion are largely restricted to the central and eastern parts of the Lachlan Orogen. The presence of dismembered ophiolite slivers along some major fault zones, as well as the recognition of relict blueschist metamorphism and serpentinite-matrix mélanges requires an oceanic setting involving oceanic underthrusting (subduction) for the western Lachlan Orogen and central Lachlan Orogen for parts of their history. Inhibited by deep weathering and a general lack of exposure, the recent application of geophysical techniques including gravity, aeromagnetic imaging and deep crustal seismic reflection profiling has led to greater recognition of structural elements through the subcrop, a better delineation of their lateral continuity, and a better understanding of the crustal-scale architecture of the orogen. The Lachlan Orogen clearly represents a class of orogen, distinct from the Alps, Canadian Rockies and Appalachians, and is an excellent example of a Palaeozoic accretionary orogen.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/23152101" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="f146ded62ec578dbe6f7b26f75d994cc" rel="nofollow" data-download="{"attachment_id":43638251,"asset_id":23152101,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/43638251/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="44930134" href="https://independent.academia.edu/DavidGray54">David Gray</a><script data-card-contents-for-user="44930134" type="text/json">{"id":44930134,"first_name":"David","last_name":"Gray","domain_name":"independent","page_name":"DavidGray54","display_name":"David Gray","profile_url":"https://independent.academia.edu/DavidGray54?f_ri=15989","photo":"https://0.academia-photos.com/44930134/14335980/20333296/s65_david.gray.jpg"}</script></span></span></li><li class="js-paper-rank-work_23152101 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="23152101"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 23152101, container: ".js-paper-rank-work_23152101", }); 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$(".js-view-count[data-work-id=23152101]").text(description); $(".js-view-count-work_23152101").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_23152101").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="23152101"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">10</a>  </div><span class="InlineList-item-text u-textTruncate u-pl10x"><a class="InlineList-item-text" data-has-card-for-ri="400" rel="nofollow" href="https://www.academia.edu/Documents/in/Earth_Sciences">Earth Sciences</a>, <script data-card-contents-for-ri="400" type="text/json">{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="44747" rel="nofollow" href="https://www.academia.edu/Documents/in/Plate_Tectonics">Plate Tectonics</a>, <script data-card-contents-for-ri="44747" type="text/json">{"id":44747,"name":"Plate Tectonics","url":"https://www.academia.edu/Documents/in/Plate_Tectonics?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="58054" rel="nofollow" href="https://www.academia.edu/Documents/in/Environmental_Sciences">Environmental Sciences</a><script data-card-contents-for-ri="58054" type="text/json">{"id":58054,"name":"Environmental Sciences","url":"https://www.academia.edu/Documents/in/Environmental_Sciences?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=23152101]'), work: {"id":23152101,"title":"Tectonic evolution of the Lachlan Orogen, southeast Australia: historical review, data synthesis and modern perspectives","created_at":"2016-03-11T14:03:41.862-08:00","url":"https://www.academia.edu/23152101/Tectonic_evolution_of_the_Lachlan_Orogen_southeast_Australia_historical_review_data_synthesis_and_modern_perspectives?f_ri=15989","dom_id":"work_23152101","summary":"The Lachlan Orogen, like many other orogenic belts, has undergone paradigm shifts from geosynclinal to plate-tectonic theory of evolution over the past 40 years. Initial plate-tectonic interpretations were based on lithologic associations and recognition of key plate-tectonic elements such as andesites and palaeo-subduction complexes. Understanding and knowledge of modern plate settings led to the application of actualistic models and the development of palaeogeographical reconstructions, commonly using a non-palinspastic base. Igneous petrology and geochemistry led to characterisation of granite types into 'I' and 'S', the delineation of granite basement terranes, and to nonmobilistic tectonic scenarios involving plumes as a heat source to drive crustal melting and lithospheric deformation. More recently, measurements of isotopic tracers (Nd, Sr, Pb) and U-Pb SHRIMP age determinations on inherited zircons from granitoids and detrital zircons from sedimentary successions led to the development of multiple component mixing models to explain granite geochemistry. These have focused tectonic arguments for magma genesis again more on plate interactions. The recognition of fault zones in the turbidites, their polydeformed character and their thin-skinned nature, as well as belts of distinct tectonic vergence has led to a major reassessment of tectonic development. Other geochemical studies on Cambrian metavolcanic belts showed that the basement was partly backarc basin-and forearc basin-type oceanic crust. The application of 40 Ar-39 Ar geochronology and thermochronology on slates, schist and granitoids has better constrained the timing of deformation and plutonism, and illite crystallinity and b o mica spacing studies on slates have better defined the background metamorphic conditions in the low-grade parts. The Lachlan deformation pattern involves three thrust systems that constitute the western Lachlan Orogen, central Lachlan Orogen and eastern Lachlan Orogen. The faults in the western Lachlan Orogen show a generalised east-younging (450-395 Ma), which probably relates to imbrication and rock uplift of the sediment wedge, because detailed analyses show that the décollement system is as old in the east as it is in the west. Overall, deformation in the eastern Lachlan Orogen is younger (400-380 Ma), apart from the Narooma Accretionary Complex ( ca 445 Ma). Preservation of extensional basins and evidence for basin inversion are largely restricted to the central and eastern parts of the Lachlan Orogen. The presence of dismembered ophiolite slivers along some major fault zones, as well as the recognition of relict blueschist metamorphism and serpentinite-matrix mélanges requires an oceanic setting involving oceanic underthrusting (subduction) for the western Lachlan Orogen and central Lachlan Orogen for parts of their history. Inhibited by deep weathering and a general lack of exposure, the recent application of geophysical techniques including gravity, aeromagnetic imaging and deep crustal seismic reflection profiling has led to greater recognition of structural elements through the subcrop, a better delineation of their lateral continuity, and a better understanding of the crustal-scale architecture of the orogen. The Lachlan Orogen clearly represents a class of orogen, distinct from the Alps, Canadian Rockies and Appalachians, and is an excellent example of a Palaeozoic accretionary orogen.","downloadable_attachments":[{"id":43638251,"asset_id":23152101,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":44930134,"first_name":"David","last_name":"Gray","domain_name":"independent","page_name":"DavidGray54","display_name":"David Gray","profile_url":"https://independent.academia.edu/DavidGray54?f_ri=15989","photo":"https://0.academia-photos.com/44930134/14335980/20333296/s65_david.gray.jpg"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":44747,"name":"Plate Tectonics","url":"https://www.academia.edu/Documents/in/Plate_Tectonics?f_ri=15989","nofollow":true},{"id":58054,"name":"Environmental Sciences","url":"https://www.academia.edu/Documents/in/Environmental_Sciences?f_ri=15989","nofollow":true},{"id":104901,"name":"Age Determination","url":"https://www.academia.edu/Documents/in/Age_Determination?f_ri=15989"},{"id":104996,"name":"Paradigm Shift","url":"https://www.academia.edu/Documents/in/Paradigm_Shift?f_ri=15989"},{"id":118582,"name":"Physical sciences","url":"https://www.academia.edu/Documents/in/Physical_sciences?f_ri=15989"},{"id":702522,"name":"Tethys Oceanic Crust","url":"https://www.academia.edu/Documents/in/Tethys_Oceanic_Crust?f_ri=15989"},{"id":716370,"name":"Seismic reflection","url":"https://www.academia.edu/Documents/in/Seismic_reflection?f_ri=15989"},{"id":814934,"name":"Plate tectonic","url":"https://www.academia.edu/Documents/in/Plate_tectonic?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_887428" data-work_id="887428" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/887428/The_Great_Basin_Altiplano_during_the_middle_Cenozoic_ignimbrite_flareup_Insights_from_volcanic_rocks">The Great Basin Altiplano during the middle Cenozoic ignimbrite flareup: Insights from volcanic rocks</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Uncertainty surrounds the fate of the orogenic plateau in what is now the Great Basin in western Utah and Nevada, which resulted from the Mesozoic and earliest Cenozoic contractile deformations and crustal thickening. Although there is... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_887428" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Uncertainty surrounds the fate of the orogenic plateau in what is now the Great Basin in western Utah and Nevada, which resulted from the Mesozoic and earliest Cenozoic contractile deformations and crustal thickening. Although there is some consensus regarding the gravitational collapse of the plateau by extensional faulting and consequent crustal thinning, whether or not the plateau existed during the middle Cenozoic Great Basin ignimbrite flareup – one of the grandest expressions of continental volcanism in the geologic record – had remained in doubt. We use compositions of contemporaneous calc-alkaline lava flows as well as configurations of the ignimbrite sheets to show that the Great Basin area during the middle Cenozoic was a relatively smooth plateau underlain by unusually thick crust. We compare analyses of 376 intermediate-composition lava flows in the Great Basin that were extruded at 42–17 Ma with compositions of >6000 analyses of the late Cenozoic lava flows in continental volcanic arcs that correlate roughly with known crustal thickness. This comparison indicates that the middle Cenozoic Great Basin crust was much thicker than the present ca. 30 km thickness, likely as much as 60–70 km. If isostatic equilibrium prevailed, this unusually thick continental crust must have supported high topography. This high terrain in SE Nevada and SW Utah was progressively smoothed as successive ignimbrite outflow sheets were emplaced over areas currently as much as tens of thousands of square kilometres to aggregate thicknesses of as much as hundreds of metres. The generally small between-site variations in the palaeomagnetic directions of individual sheets lend further support for a relatively smooth landscape over which the sheets were draped. We conclude that during the middle Cenozoic, especially towards the close of the ignimbrite flareup, this Great Basin area was a relatively flat plateau, and because it was also high in elevation, we refer to it as an Altiplano. It was not unlike the present-day Altiplano-Puna in the tectonically similar central Andes, where an ignimbrite flareup comparable to that in the Great Basin occurred at ca. 9–3 Ma. Outflow ignimbrite sheets that were deposited from 35 to 23 Ma on the progressively smoothed Altiplano in south-eastern Nevada were derived from source calderas to the west. Of the 12 major sheets from seven sources, nine are distributed unevenly east of their sources while the remaining three sheets are spread about as far east as west of their sources. This eccentricity of sources near the western margin of 75% of the sheets indicates the existence of a NS-trending topographic barrier in central Nevada that restricted westward dispersal of ash flows. In a symmetric manner, eastward dispersal of ash flows from sources farther west seemed to have been impeded by this same topographic barrier. The westward dispersal was controlled in part by westward-draining stream valleys incised in the sloping flank of the Great Basin Altiplano in western Nevada and adjacent California; at least one of these ash flows travelled as far west as the western foothills of the Sierra Nevada. The nature and origin of the implied topographic barrier are uncertain. It is possible that heavy orographic precipitation on the western slope of the Altiplano and consequent focused denudation and isostatic uplift created a NS-trending topographic high at the crest of the western slope and facing the smoothed Altiplano to the east. The barrier also lies near and essentially parallel to the buried western edge of the Precambrian basement and to a zone of thermal-diapiric domes that were spawned in thickened crust as the basement edge was overrun by late Palaeozoic–Mesozoic thrust sheets.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/887428" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="595fb7da6fead7183f74ecbe1b6bbf18" rel="nofollow" data-download="{"attachment_id":5361602,"asset_id":887428,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/5361602/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="76756" href="https://byu.academia.edu/EricChristiansen">Eric H Christiansen</a><script data-card-contents-for-user="76756" type="text/json">{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H Christiansen","profile_url":"https://byu.academia.edu/EricChristiansen?f_ri=15989","photo":"https://0.academia-photos.com/76756/84665/284057/s65_eric.christiansen.jpg"}</script></span></span></li><li class="js-paper-rank-work_887428 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="887428"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 887428, container: ".js-paper-rank-work_887428", }); 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$(".js-view-count[data-work-id=887428]").text(description); $(".js-view-count-work_887428").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_887428").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="887428"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="1370" rel="nofollow" href="https://www.academia.edu/Documents/in/Volcanology">Volcanology</a>, <script data-card-contents-for-ri="1370" type="text/json">{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="10769" rel="nofollow" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="15989" rel="nofollow" href="https://www.academia.edu/Documents/in/Igneous_petrology">Igneous petrology</a>, <script data-card-contents-for-ri="15989" type="text/json">{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true}</script><a class="InlineList-item-text" data-has-card-for-ri="275969" rel="nofollow" href="https://www.academia.edu/Documents/in/Ignimbrite">Ignimbrite</a><script data-card-contents-for-ri="275969" type="text/json">{"id":275969,"name":"Ignimbrite","url":"https://www.academia.edu/Documents/in/Ignimbrite?f_ri=15989","nofollow":true}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=887428]'), work: {"id":887428,"title":"The Great Basin Altiplano during the middle Cenozoic ignimbrite flareup: Insights from volcanic rocks","created_at":"2011-09-05T01:56:39.751-07:00","url":"https://www.academia.edu/887428/The_Great_Basin_Altiplano_during_the_middle_Cenozoic_ignimbrite_flareup_Insights_from_volcanic_rocks?f_ri=15989","dom_id":"work_887428","summary":"Uncertainty surrounds the fate of the orogenic plateau in what is now the Great Basin in western Utah and Nevada, which resulted from the Mesozoic and earliest Cenozoic contractile deformations and crustal thickening. Although there is some consensus regarding the gravitational collapse of the plateau by extensional faulting and consequent crustal thinning, whether or not the plateau existed during the middle Cenozoic Great Basin ignimbrite flareup – one of the grandest expressions of continental volcanism in the geologic record – had remained in doubt. We use compositions of contemporaneous calc-alkaline lava flows as well as configurations of the ignimbrite sheets to show that the Great Basin area during the middle Cenozoic was a relatively smooth plateau underlain by unusually thick crust. We compare analyses of 376 intermediate-composition lava flows in the Great Basin that were extruded at 42–17 Ma with compositions of \u003e6000 analyses of the late Cenozoic lava flows in continental volcanic arcs that correlate roughly with known crustal thickness. This comparison indicates that the middle Cenozoic Great Basin crust was much thicker than the present ca. 30 km thickness, likely as much as 60–70 km. If isostatic equilibrium prevailed, this unusually thick continental crust must have supported high topography. This high terrain in SE Nevada and SW Utah was progressively smoothed as successive ignimbrite outflow sheets were emplaced over areas currently as much as tens of thousands of square kilometres to aggregate thicknesses of as much as hundreds of metres. The generally small between-site variations in the palaeomagnetic directions of individual sheets lend further support for a relatively smooth landscape over which the sheets were draped. We conclude that during the middle Cenozoic, especially towards the close of the ignimbrite flareup, this Great Basin area was a relatively flat plateau, and because it was also high in elevation, we refer to it as an Altiplano. It was not unlike the present-day Altiplano-Puna in the tectonically similar central Andes, where an ignimbrite flareup comparable to that in the Great Basin occurred at ca. 9–3 Ma. Outflow ignimbrite sheets that were deposited from 35 to 23 Ma on the progressively smoothed Altiplano in south-eastern Nevada were derived from source calderas to the west. Of the 12 major sheets from seven sources, nine are distributed unevenly east of their sources while the remaining three sheets are spread about as far east as west of their sources. This eccentricity of sources near the western margin of 75% of the sheets indicates the existence of a NS-trending topographic barrier in central Nevada that restricted westward dispersal of ash flows. In a symmetric manner, eastward dispersal of ash flows from sources farther west seemed to have been impeded by this same topographic barrier. The westward dispersal was controlled in part by westward-draining stream valleys incised in the sloping flank of the Great Basin Altiplano in western Nevada and adjacent California; at least one of these ash flows travelled as far west as the western foothills of the Sierra Nevada. The nature and origin of the implied topographic barrier are uncertain. It is possible that heavy orographic precipitation on the western slope of the Altiplano and consequent focused denudation and isostatic uplift created a NS-trending topographic high at the crest of the western slope and facing the smoothed Altiplano to the east. The barrier also lies near and essentially parallel to the buried western edge of the Precambrian basement and to a zone of thermal-diapiric domes that were spawned in thickened crust as the basement edge was overrun by late Palaeozoic–Mesozoic thrust sheets.","downloadable_attachments":[{"id":5361602,"asset_id":887428,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H Christiansen","profile_url":"https://byu.academia.edu/EricChristiansen?f_ri=15989","photo":"https://0.academia-photos.com/76756/84665/284057/s65_eric.christiansen.jpg"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology?f_ri=15989","nofollow":true},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=15989","nofollow":true},{"id":15989,"name":"Igneous petrology","url":"https://www.academia.edu/Documents/in/Igneous_petrology?f_ri=15989","nofollow":true},{"id":275969,"name":"Ignimbrite","url":"https://www.academia.edu/Documents/in/Ignimbrite?f_ri=15989","nofollow":true},{"id":551042,"name":"Basin and Range","url":"https://www.academia.edu/Documents/in/Basin_and_Range?f_ri=15989"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_887397 coauthored" data-work_id="887397" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/887397/Contrasting_origins_of_Cenozoic_silicic_volcanic_rocks_from_the_western_Cordillera_of_the_United_States">Contrasting origins of Cenozoic silicic volcanic rocks from the western Cordillera of the United States</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Two fundamentally different types of silicic volcanic rocks formed during the Cenozoic of the western Cordillera of the United States. Large volumes of dacite and rhyolite, mostly ignimbrites, erupted in the Oligocene in what is now the... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_887397" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Two fundamentally different types of silicic volcanic rocks formed during the Cenozoic of the western Cordillera of the United States. Large volumes of dacite and rhyolite, mostly ignimbrites, erupted in the Oligocene in what is now the Great Basin and contrast with rhyolites erupted along the Snake River Plain during the Late Cenozoic. The Great Basin dacites and rhyolites are generally calc-alkaline, magnesian, oxidized, wet, cool (<850°C), Sr-and Al-rich, and Fe-poor. These silicic rocks are interpreted to have been derived from mafic parent magmas generated by dehydration of oceanic lithosphere and melting in the mantle wedge above a subduction zone. Plagioclase fractionation was minimized by the high water fugacity and oxide precipitation was enhanced by high oxygen fugacity. This resulted in the formation of Si-, Al-, and Sr-rich differentiates with low Fe/Mg ratios, relatively low temperatures, and declining densities. Magma mixing, large proportions of crustal assimilation, and polybaric crystal fractionation were all important processes in generating this Oligocene suite.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/887397" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="41a806f0704505a82988d69f82346741" rel="nofollow" data-download="{"attachment_id":5361537,"asset_id":887397,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/5361537/download_file?st=MTczOTgyNjA5Miw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="4176033" href="https://idahostate.academia.edu/MikeMcCurry">Mike McCurry</a><script data-card-contents-for-user="4176033" type="text/json">{"id":4176033,"first_name":"Mike","last_name":"McCurry","domain_name":"idahostate","page_name":"MikeMcCurry","display_name":"Mike McCurry","profile_url":"https://idahostate.academia.edu/MikeMcCurry?f_ri=15989","photo":"/images/s65_no_pic.png"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-887397">+1</span><div class="hidden js-additional-users-887397"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://byu.academia.edu/EricChristiansen">Eric H Christiansen</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-887397'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-887397').html(); 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Large volumes of dacite and rhyolite, mostly ignimbrites, erupted in the Oligocene in what is now the Great Basin and contrast with rhyolites erupted along the Snake River Plain during the Late Cenozoic. The Great Basin dacites and rhyolites are generally calc-alkaline, magnesian, oxidized, wet, cool (\u003c850°C), Sr-and Al-rich, and Fe-poor. These silicic rocks are interpreted to have been derived from mafic parent magmas generated by dehydration of oceanic lithosphere and melting in the mantle wedge above a subduction zone. Plagioclase fractionation was minimized by the high water fugacity and oxide precipitation was enhanced by high oxygen fugacity. This resulted in the formation of Si-, Al-, and Sr-rich differentiates with low Fe/Mg ratios, relatively low temperatures, and declining densities. Magma mixing, large proportions of crustal assimilation, and polybaric crystal fractionation were all important processes in generating this Oligocene suite.","downloadable_attachments":[{"id":5361537,"asset_id":887397,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":4176033,"first_name":"Mike","last_name":"McCurry","domain_name":"idahostate","page_name":"MikeMcCurry","display_name":"Mike McCurry","profile_url":"https://idahostate.academia.edu/MikeMcCurry?f_ri=15989","photo":"/images/s65_no_pic.png"},{"id":76756,"first_name":"Eric","last_name":"Christiansen","domain_name":"byu","page_name":"EricChristiansen","display_name":"Eric H 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