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fake-truncate js-profile-about" style="margin: 0px;">Mike Searle is a structural geologist at the University of Oxford. he works on geological processes including ophiolite formation and obduction, and mountain building processes, particularly in the Himalaya, Karakoram, Tibet, Myanmar, and SE Asia.<br /><div class="js-profile-less-about u-linkUnstyled u-tcGrayDarker u-textDecorationUnderline u-displayNone">less</div></div></div><div class="suggested-academics-container"><div class="suggested-academics--header"><h3 class="ds2-5-heading-sans-serif-xs">Related Authors</h3></div><ul class="suggested-user-card-list" data-nosnippet="true"><div class="suggested-user-card"><div class="suggested-user-card__avatar social-profile-avatar-container"><a data-nosnippet="" href="https://uppsala.academia.edu/HeminKoyi"><img class="profile-avatar u-positionAbsolute" alt="Hemin Koyi related author profile picture" border="0" onerror="if (this.src != '//a.academia-assets.com/images/s200_no_pic.png') 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data-dom-id="Pill-react-component-5ca4efe8-1e8e-4e74-a823-259e420752ce"></div> <div id="Pill-react-component-5ca4efe8-1e8e-4e74-a823-259e420752ce"></div> </a></div></div></div></div><div class="right-panel-container"><div class="user-content-wrapper"><div class="uploads-container" id="social-redesign-work-container"><div class="upload-header"><h2 class="ds2-5-heading-sans-serif-xs">Uploads</h2></div><div class="documents-container backbone-social-profile-documents" style="width: 100%;"><div class="u-taCenter"></div><div class="profile--tab_content_container js-tab-pane tab-pane active" id="all"><div class="profile--tab_heading_container js-section-heading" data-section="Papers" id="Papers"><h3 class="profile--tab_heading_container">Papers by Michael Searle</h3></div><div class="js-work-strip profile--work_container" data-work-id="123800057"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800057/_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting"><img alt="Research paper thumbnail of “Oman Exotics”—Oceanic carbonate build-ups associated with the early stages of continental rifting" class="work-thumbnail" src="https://attachments.academia-assets.com/118148720/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800057/_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting">“Oman Exotics”—Oceanic carbonate build-ups associated with the early stages of continental rifting</a></div><div class="wp-workCard_item"><span>Geology</span><span>, 1982</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The so-called "Oman Exotic" limestones form isolated masses, from boulder size to 1,000 m thick, ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The so-called "Oman Exotic" limestones form isolated masses, from boulder size to 1,000 m thick, of Middle to Upper Permian and Upper Triassic fossiliferous limestones, and crop out within imbricated thrust slices beneath the Semail ophiolite in the Oman Mountains. Permian Exotics are of dominantly reef and forereef facies, whereas Triassic Exotics are more typically of back-reef and lagoonal facies. They are commonly associated with a substrate of alkalic and transitional tholeiitic basalts and are interpreted as a series of reef-associated carbonate buildups deposited in part on oceanic islands or seamounts, close to the site of initial rifting of the Oman continental margin.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="bae680503e97b5c2f9e4c925db9486f7" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148720,"asset_id":123800057,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148720/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800057"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800057"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800057; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800057]").text(description); $(".js-view-count[data-work-id=123800057]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800057; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800057']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "bae680503e97b5c2f9e4c925db9486f7" } } $('.js-work-strip[data-work-id=123800057]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800057,"title":"“Oman Exotics”—Oceanic carbonate build-ups associated with the early stages of continental rifting","translated_title":"","metadata":{"publisher":"Geological Society of America","grobid_abstract":"The so-called \"Oman Exotic\" limestones form isolated masses, from boulder size to 1,000 m thick, of Middle to Upper Permian and Upper Triassic fossiliferous limestones, and crop out within imbricated thrust slices beneath the Semail ophiolite in the Oman Mountains. Permian Exotics are of dominantly reef and forereef facies, whereas Triassic Exotics are more typically of back-reef and lagoonal facies. They are commonly associated with a substrate of alkalic and transitional tholeiitic basalts and are interpreted as a series of reef-associated carbonate buildups deposited in part on oceanic islands or seamounts, close to the site of initial rifting of the Oman continental margin.","publication_date":{"day":null,"month":null,"year":1982,"errors":{}},"publication_name":"Geology","grobid_abstract_attachment_id":118148720},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800057/_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting","translated_internal_url":"","created_at":"2024-09-11T23:37:58.723-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148720,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148720/thumbnails/1.jpg","file_name":"0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is.pdf","download_url":"https://www.academia.edu/attachments/118148720/download_file","bulk_download_file_name":"Oman_Exotics_Oceanic_carbonate_build_up.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148720/0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is-libre.pdf?1726129278=\u0026response-content-disposition=attachment%3B+filename%3DOman_Exotics_Oceanic_carbonate_build_up.pdf\u0026Expires=1742082500\u0026Signature=N-~mFVnrnAFDZLdkFEUKH4ww7NV6elCHmfYW1N~e8Zp8YukCZjnPO8BksHeg~Nxfpymhhe9sytBa1SB2-vRD6ce1OYU6wta8eLJf8mifUjC9JzL0KhOZQbCoQo3zKPMb75iLqOk4LAPGZ6VQ0CRSK7xuGbNRAVr0vc9kYLE3f7-qqcYQrvkiZTrE7q7ThEoHIezduB~xznyvCcZNT-MiiaoqCPEv~4OlEYOxUsZfui47JZCHi2qHupZmbK6RQ1V2X8SmIPi6LclkqC00533x5aQoQFRA63sFDMDoKRJlVTuYYTTx8akZ6e4y1bURKwilBMsdd1GF1Y4xkcxPCFyqZg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting","translated_slug":"","page_count":7,"language":"en","content_type":"Work","summary":"The so-called \"Oman Exotic\" limestones form isolated masses, from boulder size to 1,000 m thick, of Middle to Upper Permian and Upper Triassic fossiliferous limestones, and crop out within imbricated thrust slices beneath the Semail ophiolite in the Oman Mountains. Permian Exotics are of dominantly reef and forereef facies, whereas Triassic Exotics are more typically of back-reef and lagoonal facies. They are commonly associated with a substrate of alkalic and transitional tholeiitic basalts and are interpreted as a series of reef-associated carbonate buildups deposited in part on oceanic islands or seamounts, close to the site of initial rifting of the Oman continental margin.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148720,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148720/thumbnails/1.jpg","file_name":"0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is.pdf","download_url":"https://www.academia.edu/attachments/118148720/download_file","bulk_download_file_name":"Oman_Exotics_Oceanic_carbonate_build_up.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148720/0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is-libre.pdf?1726129278=\u0026response-content-disposition=attachment%3B+filename%3DOman_Exotics_Oceanic_carbonate_build_up.pdf\u0026Expires=1742082500\u0026Signature=N-~mFVnrnAFDZLdkFEUKH4ww7NV6elCHmfYW1N~e8Zp8YukCZjnPO8BksHeg~Nxfpymhhe9sytBa1SB2-vRD6ce1OYU6wta8eLJf8mifUjC9JzL0KhOZQbCoQo3zKPMb75iLqOk4LAPGZ6VQ0CRSK7xuGbNRAVr0vc9kYLE3f7-qqcYQrvkiZTrE7q7ThEoHIezduB~xznyvCcZNT-MiiaoqCPEv~4OlEYOxUsZfui47JZCHi2qHupZmbK6RQ1V2X8SmIPi6LclkqC00533x5aQoQFRA63sFDMDoKRJlVTuYYTTx8akZ6e4y1bURKwilBMsdd1GF1Y4xkcxPCFyqZg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":417,"name":"Paleontology","url":"https://www.academia.edu/Documents/in/Paleontology"},{"id":71553,"name":"Icon","url":"https://www.academia.edu/Documents/in/Icon"},{"id":91258,"name":"Carbonate","url":"https://www.academia.edu/Documents/in/Carbonate"},{"id":151949,"name":"RIFT","url":"https://www.academia.edu/Documents/in/RIFT"},{"id":199319,"name":"Citation","url":"https://www.academia.edu/Documents/in/Citation"},{"id":604905,"name":"Oceanic Islands","url":"https://www.academia.edu/Documents/in/Oceanic_Islands"},{"id":632867,"name":"ICON","url":"https://www.academia.edu/Documents/in/ICON-1"},{"id":1479595,"name":"Continental Margin","url":"https://www.academia.edu/Documents/in/Continental_Margin"}],"urls":[{"id":44622252,"url":"https://doi.org/10.1130/0091-7613(1982)10%3C43:oecbaw%3E2.0.co;2"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800056"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800056/Constraining_the_Timing_of_Prograde_Metamorphism_in_the_Sole_of_the_Semail_Ophiolite_Coupled_Zircon_Tims_U_PB_Dating_and_Trace_Element_Analyses_from_the_Masafi_Sole_Exposure_United_Arab_Emirates_U_A_E_"><img alt="Research paper thumbnail of Constraining the Timing of Prograde Metamorphism in the Sole of the Semail Ophiolite: Coupled Zircon Tims U-PB Dating and Trace Element Analyses from the Masafi Sole Exposure, United Arab Emirates (U.A.E.)" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Constraining the Timing of Prograde Metamorphism in the Sole of the Semail Ophiolite: Coupled Zircon Tims U-PB Dating and Trace Element Analyses from the Masafi Sole Exposure, United Arab Emirates (U.A.E.)</div><div class="wp-workCard_item"><span>GSA Annual Meeting in Phoenix, Arizona, USA - 2019</span><span>, 2019</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800056"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800056"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800056; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800055"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800055/Continentes_en_colisi%C3%B3n_creaci%C3%B3n_de_monta%C3%B1as"><img alt="Research paper thumbnail of Continentes en colisión, creación de montañas" class="work-thumbnail" src="https://attachments.academia-assets.com/118148718/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800055/Continentes_en_colisi%C3%B3n_creaci%C3%B3n_de_monta%C3%B1as">Continentes en colisión, creación de montañas</a></div><div class="wp-workCard_item"><span>Enseñanza de las ciencias de la tierra: Revista de la Asociación Española para la Enseñanza de las Ciencias de la Tierra</span><span>, 2018</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicació...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicación coherente a la formación de las montañas. Para el caso concreto del Himalaya, esta gran cordillera es el fruto de la colisión continental que tuvo lugar hace alrededor de 50 millones de años. La particular disposición de la cadena montañosa, inclinada hacia el norte debido a que la placa india intenta subducir bajo Asia, permite cartografiar estructuras y tomar muestras de su estructura profunda y, por lo tanto, descifrar su origen y evolución a lo largo del tiempo. En concreto, cuatro grandes estructuras (en forma de fallas y cabalgamientos) permiten definir otras tantas unidades estructurales incluidas tanto en la placa litosférica india como en la asiática. Los frecuentes terremotos aportan información acerca de la actividad de estas estructuras. Por otro lado, el acortamiento y engrosamiento cortical provocan el levantamiento de la cordillera, pero el ascenso topográfico incrementa también la intensidad de la erosión, provocando un efecto retroalimentado y el continuo rejuvenecimiento del relieve.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="c21dbe442a5531cfcf3d972995f64a31" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148718,"asset_id":123800055,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148718/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800055"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800055"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800055; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800055]").text(description); $(".js-view-count[data-work-id=123800055]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800055; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800055']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "c21dbe442a5531cfcf3d972995f64a31" } } $('.js-work-strip[data-work-id=123800055]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800055,"title":"Continentes en colisión, creación de montañas","translated_title":"","metadata":{"grobid_abstract":"modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicación coherente a la formación de las montañas. Para el caso concreto del Himalaya, esta gran cordillera es el fruto de la colisión continental que tuvo lugar hace alrededor de 50 millones de años. La particular disposición de la cadena montañosa, inclinada hacia el norte debido a que la placa india intenta subducir bajo Asia, permite cartografiar estructuras y tomar muestras de su estructura profunda y, por lo tanto, descifrar su origen y evolución a lo largo del tiempo. En concreto, cuatro grandes estructuras (en forma de fallas y cabalgamientos) permiten definir otras tantas unidades estructurales incluidas tanto en la placa litosférica india como en la asiática. Los frecuentes terremotos aportan información acerca de la actividad de estas estructuras. Por otro lado, el acortamiento y engrosamiento cortical provocan el levantamiento de la cordillera, pero el ascenso topográfico incrementa también la intensidad de la erosión, provocando un efecto retroalimentado y el continuo rejuvenecimiento del relieve.","publication_date":{"day":null,"month":null,"year":2018,"errors":{}},"publication_name":"Enseñanza de las ciencias de la tierra: Revista de la Asociación Española para la Enseñanza de las Ciencias de la Tierra","grobid_abstract_attachment_id":118148718},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800055/Continentes_en_colisi%C3%B3n_creaci%C3%B3n_de_monta%C3%B1as","translated_internal_url":"","created_at":"2024-09-11T23:37:58.087-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148718,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148718/thumbnails/1.jpg","file_name":"155003812.pdf","download_url":"https://www.academia.edu/attachments/118148718/download_file","bulk_download_file_name":"Continentes_en_colision_creacion_de_mont.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148718/155003812-libre.pdf?1726129240=\u0026response-content-disposition=attachment%3B+filename%3DContinentes_en_colision_creacion_de_mont.pdf\u0026Expires=1742082500\u0026Signature=YDJ6lL4YNa9HRw56UoUrdqei15kFEdvyd3ipoHPJdoaghUZPrK4VwIlQVLh6cYmCj9~~UnzQXWtc4q9uXEtZQQldt1CC0fbksf3CfmF7Wfvg27MZv6mCDuNj9jcBcnHYOkG8LekbrydhDblznke7XX6W0PrhGujdnmaDlwOxb3SEXieNORDvpvHwLjtIgtOUmzcQT9JZPSSGm2Slkhe9~3JRTHf9qaxxeSRx~iJlyVYxKSUT1WbOp3QP0jTd8Cd-9BuO5OZoX8tgh6dDNDKguSd-14B-oi8tm6y-SriBepC2tvtxB0um~c2LYVdCHo194siq3RllYlM116Lk8sQdTQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Continentes_en_colisión_creación_de_montañas","translated_slug":"","page_count":6,"language":"es","content_type":"Work","summary":"modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicación coherente a la formación de las montañas. Para el caso concreto del Himalaya, esta gran cordillera es el fruto de la colisión continental que tuvo lugar hace alrededor de 50 millones de años. La particular disposición de la cadena montañosa, inclinada hacia el norte debido a que la placa india intenta subducir bajo Asia, permite cartografiar estructuras y tomar muestras de su estructura profunda y, por lo tanto, descifrar su origen y evolución a lo largo del tiempo. En concreto, cuatro grandes estructuras (en forma de fallas y cabalgamientos) permiten definir otras tantas unidades estructurales incluidas tanto en la placa litosférica india como en la asiática. Los frecuentes terremotos aportan información acerca de la actividad de estas estructuras. Por otro lado, el acortamiento y engrosamiento cortical provocan el levantamiento de la cordillera, pero el ascenso topográfico incrementa también la intensidad de la erosión, provocando un efecto retroalimentado y el continuo rejuvenecimiento del relieve.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148718,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148718/thumbnails/1.jpg","file_name":"155003812.pdf","download_url":"https://www.academia.edu/attachments/118148718/download_file","bulk_download_file_name":"Continentes_en_colision_creacion_de_mont.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148718/155003812-libre.pdf?1726129240=\u0026response-content-disposition=attachment%3B+filename%3DContinentes_en_colision_creacion_de_mont.pdf\u0026Expires=1742082500\u0026Signature=YDJ6lL4YNa9HRw56UoUrdqei15kFEdvyd3ipoHPJdoaghUZPrK4VwIlQVLh6cYmCj9~~UnzQXWtc4q9uXEtZQQldt1CC0fbksf3CfmF7Wfvg27MZv6mCDuNj9jcBcnHYOkG8LekbrydhDblznke7XX6W0PrhGujdnmaDlwOxb3SEXieNORDvpvHwLjtIgtOUmzcQT9JZPSSGm2Slkhe9~3JRTHf9qaxxeSRx~iJlyVYxKSUT1WbOp3QP0jTd8Cd-9BuO5OZoX8tgh6dDNDKguSd-14B-oi8tm6y-SriBepC2tvtxB0um~c2LYVdCHo194siq3RllYlM116Lk8sQdTQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":951,"name":"Humanities","url":"https://www.academia.edu/Documents/in/Humanities"}],"urls":[{"id":44622250,"url":"https://dialnet.unirioja.es/servlet/articulo?codigo=7103737"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800054"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800054/Melting_Mud_in_the_Mantle_Extreme_Oxygen_Isotope_Signatures_in_Zircon_from_Sub_Moho_Granitoids"><img alt="Research paper thumbnail of Melting Mud in the Mantle: Extreme Oxygen Isotope Signatures in Zircon from Sub-Moho Granitoids" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Melting Mud in the Mantle: Extreme Oxygen Isotope Signatures in Zircon from Sub-Moho Granitoids</div><div class="wp-workCard_item"><span>GSA Annual Meeting in Seattle, Washington, USA - 2017</span><span>, 2017</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800054"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800054"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800054; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800053"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800053/The_metamorphic_sheet_and_underlying_volcanic_rocks_beneath_the_Semail_ophiolite_in_the_northern_Oman_mountains_of_Arabia"><img alt="Research paper thumbnail of The metamorphic sheet and underlying volcanic rocks beneath the Semail ophiolite in the northern Oman mountains of Arabia" class="work-thumbnail" src="https://attachments.academia-assets.com/118148717/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800053/The_metamorphic_sheet_and_underlying_volcanic_rocks_beneath_the_Semail_ophiolite_in_the_northern_Oman_mountains_of_Arabia">The metamorphic sheet and underlying volcanic rocks beneath the Semail ophiolite in the northern Oman mountains of Arabia</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Detailed mapping and structural analysis along the base of the Semail ophiolite thrust sheet in t...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Detailed mapping and structural analysis along the base of the Semail ophiolite thrust sheet in the northern Oman mountains has revealed a distinct and separate thrust sheet between the underlying marine sediments of the Hawasina Complex, and the overlying 12 km+ thick Semail ophiolite. This thrust sheet is termed the Haybi complex, and consists of sub-ophiolitic metamorphic rocks and serpentinite, alkaline and tholeiitic basalts (the Haybi volcanics), associated with mountain-sized "Exotic" limestones and an Upper Cretaceous sedimentary melange. The rocks of the Haybi complex are bounded by major thrust planes, the Semail thrust above and the Haybi thrust beneath, which truncate all schistosities, fold axes, imbricate thrust and associated features. The Haybi volcanics are mainly Triassic in age and form a substrate to or enclose large, isolated blOCKS of Permian or Triassic "Exotic" limestones, Although they have been considerably disrupted and imbricated during south-westward emplacement, intact sequences show that the lower part is composed mainly of alkaline pyroclastics and lavas, including ankaramites, nephelinites and trachytes, whereas the upper part is predominantly tholeiitic pillow lavas and breccias. Late sills of alkali pyroxenite, wehrlite and kaersutite gabbro intrude the tholeiitic volcanics in a few localities and have been dated as Turonian (Upper Cretaceous). Geochemical studies, particularly of "immobile" elements show that the lower volcanics and the late sills are strongly alkaline with high Ti, p, Zr and Nb contents, low Y /Nb ratios and steep LREE enriched rare earth patterns. They are 1 Professor Ian Gass, my supervisor for obtaining an Open University grant and providing support for three years. 2 Drs. Adrian Lewis, John Smewing, Steve Lippard and John Malpas for providing much help and supervision both in the field and back in England.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e08857625d5dfbe270a94f881b774e58" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148717,"asset_id":123800053,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148717/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800053"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800053"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800053; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800053]").text(description); $(".js-view-count[data-work-id=123800053]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800053; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800053']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "e08857625d5dfbe270a94f881b774e58" } } $('.js-work-strip[data-work-id=123800053]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800053,"title":"The metamorphic sheet and underlying volcanic rocks beneath the Semail ophiolite in the northern Oman mountains of Arabia","translated_title":"","metadata":{"grobid_abstract":"Detailed mapping and structural analysis along the base of the Semail ophiolite thrust sheet in the northern Oman mountains has revealed a distinct and separate thrust sheet between the underlying marine sediments of the Hawasina Complex, and the overlying 12 km+ thick Semail ophiolite. This thrust sheet is termed the Haybi complex, and consists of sub-ophiolitic metamorphic rocks and serpentinite, alkaline and tholeiitic basalts (the Haybi volcanics), associated with mountain-sized \"Exotic\" limestones and an Upper Cretaceous sedimentary melange. The rocks of the Haybi complex are bounded by major thrust planes, the Semail thrust above and the Haybi thrust beneath, which truncate all schistosities, fold axes, imbricate thrust and associated features. The Haybi volcanics are mainly Triassic in age and form a substrate to or enclose large, isolated blOCKS of Permian or Triassic \"Exotic\" limestones, Although they have been considerably disrupted and imbricated during south-westward emplacement, intact sequences show that the lower part is composed mainly of alkaline pyroclastics and lavas, including ankaramites, nephelinites and trachytes, whereas the upper part is predominantly tholeiitic pillow lavas and breccias. Late sills of alkali pyroxenite, wehrlite and kaersutite gabbro intrude the tholeiitic volcanics in a few localities and have been dated as Turonian (Upper Cretaceous). Geochemical studies, particularly of \"immobile\" elements show that the lower volcanics and the late sills are strongly alkaline with high Ti, p, Zr and Nb contents, low Y /Nb ratios and steep LREE enriched rare earth patterns. They are 1 Professor Ian Gass, my supervisor for obtaining an Open University grant and providing support for three years. 2 Drs. Adrian Lewis, John Smewing, Steve Lippard and John Malpas for providing much help and supervision both in the field and back in England.","publication_date":{"day":null,"month":null,"year":1980,"errors":{}},"grobid_abstract_attachment_id":118148717},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800053/The_metamorphic_sheet_and_underlying_volcanic_rocks_beneath_the_Semail_ophiolite_in_the_northern_Oman_mountains_of_Arabia","translated_internal_url":"","created_at":"2024-09-11T23:37:56.570-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148717,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148717/thumbnails/1.jpg","file_name":"354276_2.pdf","download_url":"https://www.academia.edu/attachments/118148717/download_file","bulk_download_file_name":"The_metamorphic_sheet_and_underlying_vol.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148717/354276_2.pdf?1726123138=\u0026response-content-disposition=attachment%3B+filename%3DThe_metamorphic_sheet_and_underlying_vol.pdf\u0026Expires=1742082500\u0026Signature=I49~Z70PXCdN6hna-SlkKgVLaeL9WJK6SkbpNLNBCDNK~GBneQegOCYLBSw1Y2~5hQokRIAAfejpNmbYG6QD2FI7eLkOtS-4bkKgk2zxbbC0l6ETRHevuwYVb9UqEPs-JO0XGsmVpbssW3QuNXcnsyfVwkUXQYvtpmz7qsRS-TPqmZLCHk5AAHpiq8oeGy5Myj88Mayoa7VjwZcewQLYvK1GAYdKM8fouee9EMBSyhMIJFcOw6SpAI2PSkXhQAYiFXaVagR5u97LF3y3i8o89hGlnztlfpf1tAM-sV1Ka0E8f-cqHBz~Aj~n~TknLl~zaoWpz43gyEJ8h~R95etnPA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_metamorphic_sheet_and_underlying_volcanic_rocks_beneath_the_Semail_ophiolite_in_the_northern_Oman_mountains_of_Arabia","translated_slug":"","page_count":393,"language":"en","content_type":"Work","summary":"Detailed mapping and structural analysis along the base of the Semail ophiolite thrust sheet in the northern Oman mountains has revealed a distinct and separate thrust sheet between the underlying marine sediments of the Hawasina Complex, and the overlying 12 km+ thick Semail ophiolite. This thrust sheet is termed the Haybi complex, and consists of sub-ophiolitic metamorphic rocks and serpentinite, alkaline and tholeiitic basalts (the Haybi volcanics), associated with mountain-sized \"Exotic\" limestones and an Upper Cretaceous sedimentary melange. The rocks of the Haybi complex are bounded by major thrust planes, the Semail thrust above and the Haybi thrust beneath, which truncate all schistosities, fold axes, imbricate thrust and associated features. The Haybi volcanics are mainly Triassic in age and form a substrate to or enclose large, isolated blOCKS of Permian or Triassic \"Exotic\" limestones, Although they have been considerably disrupted and imbricated during south-westward emplacement, intact sequences show that the lower part is composed mainly of alkaline pyroclastics and lavas, including ankaramites, nephelinites and trachytes, whereas the upper part is predominantly tholeiitic pillow lavas and breccias. Late sills of alkali pyroxenite, wehrlite and kaersutite gabbro intrude the tholeiitic volcanics in a few localities and have been dated as Turonian (Upper Cretaceous). Geochemical studies, particularly of \"immobile\" elements show that the lower volcanics and the late sills are strongly alkaline with high Ti, p, Zr and Nb contents, low Y /Nb ratios and steep LREE enriched rare earth patterns. They are 1 Professor Ian Gass, my supervisor for obtaining an Open University grant and providing support for three years. 2 Drs. Adrian Lewis, John Smewing, Steve Lippard and John Malpas for providing much help and supervision both in the field and back in England.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148717,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148717/thumbnails/1.jpg","file_name":"354276_2.pdf","download_url":"https://www.academia.edu/attachments/118148717/download_file","bulk_download_file_name":"The_metamorphic_sheet_and_underlying_vol.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148717/354276_2.pdf?1726123138=\u0026response-content-disposition=attachment%3B+filename%3DThe_metamorphic_sheet_and_underlying_vol.pdf\u0026Expires=1742082500\u0026Signature=I49~Z70PXCdN6hna-SlkKgVLaeL9WJK6SkbpNLNBCDNK~GBneQegOCYLBSw1Y2~5hQokRIAAfejpNmbYG6QD2FI7eLkOtS-4bkKgk2zxbbC0l6ETRHevuwYVb9UqEPs-JO0XGsmVpbssW3QuNXcnsyfVwkUXQYvtpmz7qsRS-TPqmZLCHk5AAHpiq8oeGy5Myj88Mayoa7VjwZcewQLYvK1GAYdKM8fouee9EMBSyhMIJFcOw6SpAI2PSkXhQAYiFXaVagR5u97LF3y3i8o89hGlnztlfpf1tAM-sV1Ka0E8f-cqHBz~Aj~n~TknLl~zaoWpz43gyEJ8h~R95etnPA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":330036,"name":"Ophiolite","url":"https://www.academia.edu/Documents/in/Ophiolite"},{"id":688910,"name":"Volcanic Rock","url":"https://www.academia.edu/Documents/in/Volcanic_Rock"}],"urls":[{"id":44622248,"url":"http://oro.open.ac.uk/54606/"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800052"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800052/Comment_on_Interplay_of_deformation_and_magmatism_in_the_Pangong_Transpressional_Zone_Eastern_Ladakh_India_Implications_for_remobilization_of_the_trans_Himalayan_magmatic_arc_and_initiation_of_the_Karakoram_Fault_by_K_Sen_B_K_Mukherjee_and_A_S_Collins_Journal_of_Structural_Geology_62_2_"><img alt="Research paper thumbnail of Comment on “Interplay of deformation and magmatism in the Pangong Transpressional Zone, Eastern Ladakh, India: Implications for remobilization of the trans-Himalayan magmatic arc and initiation of the Karakoram Fault” by K. Sen, B.K. Mukherjee and A.S. Collins, Journal of Structural Geology 62 (2..." class="work-thumbnail" src="https://attachments.academia-assets.com/118148687/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800052/Comment_on_Interplay_of_deformation_and_magmatism_in_the_Pangong_Transpressional_Zone_Eastern_Ladakh_India_Implications_for_remobilization_of_the_trans_Himalayan_magmatic_arc_and_initiation_of_the_Karakoram_Fault_by_K_Sen_B_K_Mukherjee_and_A_S_Collins_Journal_of_Structural_Geology_62_2_">Comment on “Interplay of deformation and magmatism in the Pangong Transpressional Zone, Eastern Ladakh, India: Implications for remobilization of the trans-Himalayan magmatic arc and initiation of the Karakoram Fault” by K. Sen, B.K. Mukherjee and A.S. Collins, Journal of Structural Geology 62 (2...</a></div><div class="wp-workCard_item"><span>Journal of Structural Geology</span><span>, Aug 1, 2014</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d27152e3d94a9da841fdf30089febec8" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148687,"asset_id":123800052,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148687/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800052"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800052"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800052; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800052]").text(description); $(".js-view-count[data-work-id=123800052]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800052; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800052']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d27152e3d94a9da841fdf30089febec8" } } $('.js-work-strip[data-work-id=123800052]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800052,"title":"Comment on “Interplay of deformation and magmatism in the Pangong Transpressional Zone, Eastern Ladakh, India: Implications for remobilization of the trans-Himalayan magmatic arc and initiation of the Karakoram Fault” by K. Sen, B.K. Mukherjee and A.S. Collins, Journal of Structural Geology 62 (2...","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_abstract":"This paper critiques the conclusions drawn by Sen et al. regarding the age and kinematics of the Karakoram Fault Zone (KFZ) and its relationship to the Tangtse-Darbuk leucogranite (TDL). The authors argue that Sen et al.'s interpretations are based on misinterpretations of microstructural evidence and insufficient caution in analyzing anisotropy of magnetic susceptibility (AMS) data. The findings support a model where the KFZ initiated after the TDL cooled, indicating a more recent formation and emphasizing the need for rigorous validation of AMS correlations with deformation fabrics.","publication_date":{"day":1,"month":8,"year":2014,"errors":{}},"publication_name":"Journal of Structural 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Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148687,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148687/thumbnails/1.jpg","file_name":"Wallis_et_al_comment_revision.pdf","download_url":"https://www.academia.edu/attachments/118148687/download_file","bulk_download_file_name":"Comment_on_Interplay_of_deformation_and.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148687/Wallis_et_al_comment_revision-libre.pdf?1726129241=\u0026response-content-disposition=attachment%3B+filename%3DComment_on_Interplay_of_deformation_and.pdf\u0026Expires=1742082500\u0026Signature=KC-mqrJ2pdlkd4yjPBcodsLGNyPOyWnKlf66JpNHjuU99Miw7m5iKNRjtMT1U3QqO897H4pxseVS2VyFUnkjrHm6hxaRNWrblbmywm4xilnm0CSo8AyP3XguZdoPQrQXdmmAXA7EsjNQu81JxP3NiiQ4G5-wU3q~O3XDw~FH280sjxERIp~2zu5errl-i3HgFcRDP2off21P2FFdOZ~UhHFdar5GuwOSboWhpgCIB16JQMTiYEfvAqaP56i5eJFgPtgLxfS6BZKs-Zjpmg~QfZijv-wfsgOl-JeRCZXSDk60etvdl~p0nqX80dNmmnnca42plfT9OvmxghTMkMYEXw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118148686,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148686/thumbnails/1.jpg","file_name":"Wallis_et_al_comment_revision.pdf","download_url":"https://www.academia.edu/attachments/118148686/download_file","bulk_download_file_name":"Comment_on_Interplay_of_deformation_and.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148686/Wallis_et_al_comment_revision-libre.pdf?1726129245=\u0026response-content-disposition=attachment%3B+filename%3DComment_on_Interplay_of_deformation_and.pdf\u0026Expires=1742082500\u0026Signature=OlT6rxuno3nJk3JV3cAB6btK~beibZYIbWqDFjukffNc9p-TkC~DaBa~09nynuvYlkxHC-crAdH1B4ESk8mfyX7~p3kIcaBXS7vfhYXL2Nx3UNTP4EbrQT3TTkJmSQqx6s3q3Je-3uuMpxqJ3phG2ft2168YzDfgp742cTHXYSVxePjr40PV0NmzaKNGIkzupLjo0c5Lv6HdXkbDb7YwT8hxm2g4gstaxLnKj0IuukQx~hoprGZBuFQIYPqW48Y9U430wumddXBKoXFesgTyGMXPLqdxAYr3-wKyHxc9sS9sfnQD89tnyGrv5~ew6ysQqkaPt9RWymbjIW~s-k-Nmg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"}],"urls":[{"id":44622247,"url":"http://eprints.whiterose.ac.uk/80281/1/Wallis_et_al_comment_revision.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800051"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800051/Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow"><img alt="Research paper thumbnail of Constraints on brittle field exhumation of the Everest-Makalu section of the Greater Himalayan Sequence: Implications for models of crustal flow" class="work-thumbnail" src="https://attachments.academia-assets.com/118148711/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800051/Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow">Constraints on brittle field exhumation of the Everest-Makalu section of the Greater Himalayan Sequence: Implications for models of crustal flow</a></div><div class="wp-workCard_item"><span>Tectonics</span><span>, May 26, 2012</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Ba...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Barun, Arun, Dudh Kosi, and Kangshung valleys that drain the Everest and Makalu massifs cover a vertical sample transect of almost 8000 m of the Eastern Nepal Greater Himalayan Sequence (GHS). Apatite FT ages range from 0.9 AE 0.3 Ma to 3.1 AE 0.3 Ma in the GHS with ages increasing systematically with elevation. Apatite FT ages in the Everest Series and summit Ordovician limestones are much older, up to 30.5 AE 5.1 Ma. Zircon FT ages from the GHS range from 3.8 AE 0.4 Ma to 16.3 AE 0.8 Ma. The brittle exhumation rates calculated from these data show the GHS was exhumed, since $9 Ma, at an average rate of 1.0 AE 0.2 mm/a. Pliocene exhumation rates are higher at 1.7 AE 0.3 mm/a. These values are not significantly different from the estimate of ductile exhumation rates of 1.8 mm/a recorded by metamorphic minerals undergoing decompression between 18.7 and 15.6 Ma but are well below the values (up to 10 mm/a) used by thermomechanical models for ductile channel flow in the GHS. If representative of the GHS these models will therefore require further 'tuning'. Higher exhumation rates in the Pliocene have also been observed in other parts of the Himalaya and points to a regional cause, likely increased erosion due to the onset of late Pliocene-Pleistocene glaciation of the high Himalaya.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d583138cc3fcb61187a320524dc062d7" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148711,"asset_id":123800051,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148711/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800051"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800051"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800051; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800051]").text(description); $(".js-view-count[data-work-id=123800051]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800051; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800051']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d583138cc3fcb61187a320524dc062d7" } } $('.js-work-strip[data-work-id=123800051]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800051,"title":"Constraints on brittle field exhumation of the Everest-Makalu section of the Greater Himalayan Sequence: Implications for models of crustal flow","translated_title":"","metadata":{"publisher":"Wiley-Blackwell","grobid_abstract":"New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Barun, Arun, Dudh Kosi, and Kangshung valleys that drain the Everest and Makalu massifs cover a vertical sample transect of almost 8000 m of the Eastern Nepal Greater Himalayan Sequence (GHS). Apatite FT ages range from 0.9 AE 0.3 Ma to 3.1 AE 0.3 Ma in the GHS with ages increasing systematically with elevation. Apatite FT ages in the Everest Series and summit Ordovician limestones are much older, up to 30.5 AE 5.1 Ma. Zircon FT ages from the GHS range from 3.8 AE 0.4 Ma to 16.3 AE 0.8 Ma. The brittle exhumation rates calculated from these data show the GHS was exhumed, since $9 Ma, at an average rate of 1.0 AE 0.2 mm/a. Pliocene exhumation rates are higher at 1.7 AE 0.3 mm/a. These values are not significantly different from the estimate of ductile exhumation rates of 1.8 mm/a recorded by metamorphic minerals undergoing decompression between 18.7 and 15.6 Ma but are well below the values (up to 10 mm/a) used by thermomechanical models for ductile channel flow in the GHS. If representative of the GHS these models will therefore require further 'tuning'. Higher exhumation rates in the Pliocene have also been observed in other parts of the Himalaya and points to a regional cause, likely increased erosion due to the onset of late Pliocene-Pleistocene glaciation of the high Himalaya.","publication_date":{"day":26,"month":5,"year":2012,"errors":{}},"publication_name":"Tectonics","grobid_abstract_attachment_id":118148711},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800051/Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow","translated_internal_url":"","created_at":"2024-09-11T23:37:48.982-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148711,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148711/thumbnails/1.jpg","file_name":"2011tc00306220240912-1-t5ub90.pdf","download_url":"https://www.academia.edu/attachments/118148711/download_file","bulk_download_file_name":"Constraints_on_brittle_field_exhumation.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148711/2011tc00306220240912-1-t5ub90-libre.pdf?1726129241=\u0026response-content-disposition=attachment%3B+filename%3DConstraints_on_brittle_field_exhumation.pdf\u0026Expires=1742082500\u0026Signature=VK9suT4qABral6pO-F1Rz286tOmRHnnWz~fYueF1HD-EaEbuYZudmAHAZBG1ZAFN9HaJmyG1o84im4QF4cZUGAdJcrJTjonmK9LHXqCarn4gSlIkC1R2tOOq0AyEoV9sbsP8mRY3DoPFnM6kAn4IBnXkwXGDXbwS4j65HiHB1-Rei8UljMPB1WYN5eawhJt8Z92sJWFtLqPmzN8pk0AYH3FRxeKJPCegqciIiF6sRd8aHBB~K2AN6EWrTfGtS5tJCPxGF~FDav9IJhySUhzBkfS1furBfnlSfl3Zi4MbaOh9WX2IVc1hzfgr6XqHBN~ax30UN91FzKAN1wKaeWr29Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow","translated_slug":"","page_count":13,"language":"en","content_type":"Work","summary":"New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Barun, Arun, Dudh Kosi, and Kangshung valleys that drain the Everest and Makalu massifs cover a vertical sample transect of almost 8000 m of the Eastern Nepal Greater Himalayan Sequence (GHS). Apatite FT ages range from 0.9 AE 0.3 Ma to 3.1 AE 0.3 Ma in the GHS with ages increasing systematically with elevation. Apatite FT ages in the Everest Series and summit Ordovician limestones are much older, up to 30.5 AE 5.1 Ma. Zircon FT ages from the GHS range from 3.8 AE 0.4 Ma to 16.3 AE 0.8 Ma. The brittle exhumation rates calculated from these data show the GHS was exhumed, since $9 Ma, at an average rate of 1.0 AE 0.2 mm/a. Pliocene exhumation rates are higher at 1.7 AE 0.3 mm/a. These values are not significantly different from the estimate of ductile exhumation rates of 1.8 mm/a recorded by metamorphic minerals undergoing decompression between 18.7 and 15.6 Ma but are well below the values (up to 10 mm/a) used by thermomechanical models for ductile channel flow in the GHS. If representative of the GHS these models will therefore require further 'tuning'. Higher exhumation rates in the Pliocene have also been observed in other parts of the Himalaya and points to a regional cause, likely increased erosion due to the onset of late Pliocene-Pleistocene glaciation of the high Himalaya.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148711,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148711/thumbnails/1.jpg","file_name":"2011tc00306220240912-1-t5ub90.pdf","download_url":"https://www.academia.edu/attachments/118148711/download_file","bulk_download_file_name":"Constraints_on_brittle_field_exhumation.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148711/2011tc00306220240912-1-t5ub90-libre.pdf?1726129241=\u0026response-content-disposition=attachment%3B+filename%3DConstraints_on_brittle_field_exhumation.pdf\u0026Expires=1742082500\u0026Signature=VK9suT4qABral6pO-F1Rz286tOmRHnnWz~fYueF1HD-EaEbuYZudmAHAZBG1ZAFN9HaJmyG1o84im4QF4cZUGAdJcrJTjonmK9LHXqCarn4gSlIkC1R2tOOq0AyEoV9sbsP8mRY3DoPFnM6kAn4IBnXkwXGDXbwS4j65HiHB1-Rei8UljMPB1WYN5eawhJt8Z92sJWFtLqPmzN8pk0AYH3FRxeKJPCegqciIiF6sRd8aHBB~K2AN6EWrTfGtS5tJCPxGF~FDav9IJhySUhzBkfS1furBfnlSfl3Zi4MbaOh9WX2IVc1hzfgr6XqHBN~ax30UN91FzKAN1wKaeWr29Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics"},{"id":13883,"name":"Seismology","url":"https://www.academia.edu/Documents/in/Seismology"},{"id":153407,"name":"Es","url":"https://www.academia.edu/Documents/in/Es"}],"urls":[{"id":44622246,"url":"https://agupubs.onlinelibrary.wiley.com/doi/pdfdirect/10.1029/2011TC003062"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800050"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800050/Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models"><img alt="Research paper thumbnail of Restoration of the Western Himalaya: implications for metamorphic protoliths, thrust and normal faulting, and channel flow models" class="work-thumbnail" src="https://attachments.academia-assets.com/118148684/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800050/Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models">Restoration of the Western Himalaya: implications for metamorphic protoliths, thrust and normal faulting, and channel flow models</a></div><div class="wp-workCard_item"><span>Episodes</span><span>, Dec 1, 2007</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic ro...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic rocks up to kyanite or sillimanite+K-feldspar grade, migmatites, layered stromatic migmatites and leucogranite sheets. These rocks were metamorphosed during the late Eocene to early Miocene, and are bounded below by a large-scale SW-vergent ductile shear zone-thrust fault (Main Central Thrust; MCT), and above by a NE-dipping low-angle normal sense shear zone and fault (Zanskar Shear Zone; ZSZ), part of the South Tibetan Detachment (STD) system. Restoration of the high-grade metamorphic rocks of the GHS reveals that protoliths are Proterozoic shales (Haimanta Group), Cambrian-Ordovician orthogneisses, Permian Panjal volcanics and Palaeozoic-Triassic/ Jurassic sedimentary rocks, lateral equivalent rocks of the adjacent unmetamorphosed Tethyan zone. Structural outliers of low-grade or unmetamorphosed rocks (e.g., Chamba syncline) have been mapped overlying high-grade (usually sillimanite grade) rocks of the GHS. The low-grade klippen are underlain by lowangle north-directed ductile shear zones and normal faults, that are interpreted here as earlier equivalents of the ZSZ. These low-angle normal faults formed during continuous NE-SW compression, crustal thickening and southwestward extrusion of the GHS slab along the footwall. STD normal faults propagated structurally upward (northeast) with time, whereas MCT reverse faults along the base of the GHS propagated structurally downward (southwest) with time. Inverted metamorphic isograds along the base of the slab (MCT zone) can be linked on the map with right way-up isograds along the footwall of the ZSZ normal fault at the top of the slab, demonstrating that the recumbently folded isograd model is a viable geometrical representation of the metamorphic structure of the GHS. Post-metamorphic shearing along the ZSZ and MCT has condensed the isograds by a combination of pure shear and simple shear. These observations support the Channel Flow model of ductile extrusion of a mid-crustal layer of Indian plate rocks during the Miocene, from beneath the passive roof stretching fault of the ZSZ.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="4ce327046c678ee814fb372b52107226" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148684,"asset_id":123800050,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148684/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800050"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800050"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800050; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800050]").text(description); $(".js-view-count[data-work-id=123800050]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800050; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800050']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "4ce327046c678ee814fb372b52107226" } } $('.js-work-strip[data-work-id=123800050]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800050,"title":"Restoration of the Western Himalaya: implications for metamorphic protoliths, thrust and normal faulting, and channel flow models","translated_title":"","metadata":{"publisher":"International Union of Geological Sciences","grobid_abstract":"The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic rocks up to kyanite or sillimanite+K-feldspar grade, migmatites, layered stromatic migmatites and leucogranite sheets. These rocks were metamorphosed during the late Eocene to early Miocene, and are bounded below by a large-scale SW-vergent ductile shear zone-thrust fault (Main Central Thrust; MCT), and above by a NE-dipping low-angle normal sense shear zone and fault (Zanskar Shear Zone; ZSZ), part of the South Tibetan Detachment (STD) system. Restoration of the high-grade metamorphic rocks of the GHS reveals that protoliths are Proterozoic shales (Haimanta Group), Cambrian-Ordovician orthogneisses, Permian Panjal volcanics and Palaeozoic-Triassic/ Jurassic sedimentary rocks, lateral equivalent rocks of the adjacent unmetamorphosed Tethyan zone. Structural outliers of low-grade or unmetamorphosed rocks (e.g., Chamba syncline) have been mapped overlying high-grade (usually sillimanite grade) rocks of the GHS. The low-grade klippen are underlain by lowangle north-directed ductile shear zones and normal faults, that are interpreted here as earlier equivalents of the ZSZ. These low-angle normal faults formed during continuous NE-SW compression, crustal thickening and southwestward extrusion of the GHS slab along the footwall. STD normal faults propagated structurally upward (northeast) with time, whereas MCT reverse faults along the base of the GHS propagated structurally downward (southwest) with time. Inverted metamorphic isograds along the base of the slab (MCT zone) can be linked on the map with right way-up isograds along the footwall of the ZSZ normal fault at the top of the slab, demonstrating that the recumbently folded isograd model is a viable geometrical representation of the metamorphic structure of the GHS. Post-metamorphic shearing along the ZSZ and MCT has condensed the isograds by a combination of pure shear and simple shear. These observations support the Channel Flow model of ductile extrusion of a mid-crustal layer of Indian plate rocks during the Miocene, from beneath the passive roof stretching fault of the ZSZ.","publication_date":{"day":1,"month":12,"year":2007,"errors":{}},"publication_name":"Episodes","grobid_abstract_attachment_id":118148684},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800050/Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models","translated_internal_url":"","created_at":"2024-09-11T23:37:48.320-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148684,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148684/thumbnails/1.jpg","file_name":"download_pdf.pdf","download_url":"https://www.academia.edu/attachments/118148684/download_file","bulk_download_file_name":"Restoration_of_the_Western_Himalaya_impl.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148684/download_pdf-libre.pdf?1726129638=\u0026response-content-disposition=attachment%3B+filename%3DRestoration_of_the_Western_Himalaya_impl.pdf\u0026Expires=1742082500\u0026Signature=dYMzuakB6cL6wawkmg~AnjJf-Q76fVr1bpxjnV9FYI0kxwL~PCmf7yzAIK4g3Te4IcHlzuHS~BSQAMyJ3GsSn75bFxcYX3tLxKWr~ODUSwNW0Lzg~libVS6IjR0WOPNhARE0z4J2JFbjpOiJ3dq6AjnpzeU59u7Hj0fWwM17FJfD0Xf7us1fwzINSdV-OjZ1OCRsl1zjapz7-Rrc2dtBwcLbMht-kUi1kEE2loO7a3cUYHNmEHyUcKZ7p8tmMgN-3ob87U03qkdwi3K2m7Z~6510ZipkE~4Yxz-hzsP3T-p-iewr84W02NvMg~EP7wajXhAkWABfthiP7RRaWxIKwQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models","translated_slug":"","page_count":16,"language":"en","content_type":"Work","summary":"The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic rocks up to kyanite or sillimanite+K-feldspar grade, migmatites, layered stromatic migmatites and leucogranite sheets. These rocks were metamorphosed during the late Eocene to early Miocene, and are bounded below by a large-scale SW-vergent ductile shear zone-thrust fault (Main Central Thrust; MCT), and above by a NE-dipping low-angle normal sense shear zone and fault (Zanskar Shear Zone; ZSZ), part of the South Tibetan Detachment (STD) system. Restoration of the high-grade metamorphic rocks of the GHS reveals that protoliths are Proterozoic shales (Haimanta Group), Cambrian-Ordovician orthogneisses, Permian Panjal volcanics and Palaeozoic-Triassic/ Jurassic sedimentary rocks, lateral equivalent rocks of the adjacent unmetamorphosed Tethyan zone. Structural outliers of low-grade or unmetamorphosed rocks (e.g., Chamba syncline) have been mapped overlying high-grade (usually sillimanite grade) rocks of the GHS. The low-grade klippen are underlain by lowangle north-directed ductile shear zones and normal faults, that are interpreted here as earlier equivalents of the ZSZ. These low-angle normal faults formed during continuous NE-SW compression, crustal thickening and southwestward extrusion of the GHS slab along the footwall. STD normal faults propagated structurally upward (northeast) with time, whereas MCT reverse faults along the base of the GHS propagated structurally downward (southwest) with time. Inverted metamorphic isograds along the base of the slab (MCT zone) can be linked on the map with right way-up isograds along the footwall of the ZSZ normal fault at the top of the slab, demonstrating that the recumbently folded isograd model is a viable geometrical representation of the metamorphic structure of the GHS. Post-metamorphic shearing along the ZSZ and MCT has condensed the isograds by a combination of pure shear and simple shear. These observations support the Channel Flow model of ductile extrusion of a mid-crustal layer of Indian plate rocks during the Miocene, from beneath the passive roof stretching fault of the ZSZ.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148684,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148684/thumbnails/1.jpg","file_name":"download_pdf.pdf","download_url":"https://www.academia.edu/attachments/118148684/download_file","bulk_download_file_name":"Restoration_of_the_Western_Himalaya_impl.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148684/download_pdf-libre.pdf?1726129638=\u0026response-content-disposition=attachment%3B+filename%3DRestoration_of_the_Western_Himalaya_impl.pdf\u0026Expires=1742082500\u0026Signature=dYMzuakB6cL6wawkmg~AnjJf-Q76fVr1bpxjnV9FYI0kxwL~PCmf7yzAIK4g3Te4IcHlzuHS~BSQAMyJ3GsSn75bFxcYX3tLxKWr~ODUSwNW0Lzg~libVS6IjR0WOPNhARE0z4J2JFbjpOiJ3dq6AjnpzeU59u7Hj0fWwM17FJfD0Xf7us1fwzINSdV-OjZ1OCRsl1zjapz7-Rrc2dtBwcLbMht-kUi1kEE2loO7a3cUYHNmEHyUcKZ7p8tmMgN-3ob87U03qkdwi3K2m7Z~6510ZipkE~4Yxz-hzsP3T-p-iewr84W02NvMg~EP7wajXhAkWABfthiP7RRaWxIKwQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":890009,"name":"Normal Fault","url":"https://www.academia.edu/Documents/in/Normal_Fault"},{"id":968099,"name":"Thrust","url":"https://www.academia.edu/Documents/in/Thrust"},{"id":2540869,"name":"Episodes","url":"https://www.academia.edu/Documents/in/Episodes"}],"urls":[{"id":44622245,"url":"http://www.episodes.org/journal/download_pdf.php?doi=10.18814/epiiugs/2007/v30i4/001"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800049"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800049/The_Age_of_the_Potassic_Alkaline_Igneous_Rocks_along_the_Ailao_Shan_Red_River_Shear_Zone_Implications_for_the_Onset_Age_of_Left_Lateral_Shearing_A_Discussion"><img alt="Research paper thumbnail of The Age of the Potassic Alkaline Igneous Rocks along the Ailao Shan–Red River Shear Zone: Implications for the Onset Age of Left‐Lateral Shearing: A Discussion" class="work-thumbnail" src="https://attachments.academia-assets.com/118148683/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800049/The_Age_of_the_Potassic_Alkaline_Igneous_Rocks_along_the_Ailao_Shan_Red_River_Shear_Zone_Implications_for_the_Onset_Age_of_Left_Lateral_Shearing_A_Discussion">The Age of the Potassic Alkaline Igneous Rocks along the Ailao Shan–Red River Shear Zone: Implications for the Onset Age of Left‐Lateral Shearing: A Discussion</a></div><div class="wp-workCard_item"><span>The Journal of Geology</span><span>, Mar 1, 2008</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Liang et al. (2007) reported new U-Pb zircon age data of 12 potassic alkaline intrusions along th...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Liang et al. (2007) reported new U-Pb zircon age data of 12 potassic alkaline intrusions along the Ailao Shan-Red River (ASRR) shear zone and concluded that the ages, ranging from 36.3 to 34.0 Ma, date the initiation of the ASRR left-lateral movement. Although there are numerous articles suggesting this link between alkaline magmatism and strike-slip faulting (e.g.,</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="9fb49d72421201b66f7d430171da0bb5" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148683,"asset_id":123800049,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148683/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800049"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800049"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800049; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800049]").text(description); $(".js-view-count[data-work-id=123800049]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800049; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800049']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "9fb49d72421201b66f7d430171da0bb5" } } $('.js-work-strip[data-work-id=123800049]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800049,"title":"The Age of the Potassic Alkaline Igneous Rocks along the Ailao Shan–Red River Shear Zone: Implications for the Onset Age of Left‐Lateral Shearing: A Discussion","translated_title":"","metadata":{"publisher":"University of Chicago Press","ai_title_tag":"Potassic Alkaline Rocks and ASRR Shearing Age","grobid_abstract":"Liang et al. (2007) reported new U-Pb zircon age data of 12 potassic alkaline intrusions along the Ailao Shan-Red River (ASRR) shear zone and concluded that the ages, ranging from 36.3 to 34.0 Ma, date the initiation of the ASRR left-lateral movement. Although there are numerous articles suggesting this link between alkaline magmatism and strike-slip faulting (e.g.,","publication_date":{"day":1,"month":3,"year":2008,"errors":{}},"publication_name":"The Journal of Geology","grobid_abstract_attachment_id":118148683},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800049/The_Age_of_the_Potassic_Alkaline_Igneous_Rocks_along_the_Ailao_Shan_Red_River_Shear_Zone_Implications_for_the_Onset_Age_of_Left_Lateral_Shearing_A_Discussion","translated_internal_url":"","created_at":"2024-09-11T23:37:47.583-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148683,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148683/thumbnails/1.jpg","file_name":"13.pdf","download_url":"https://www.academia.edu/attachments/118148683/download_file","bulk_download_file_name":"The_Age_of_the_Potassic_Alkaline_Igneous.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148683/13-libre.pdf?1726129240=\u0026response-content-disposition=attachment%3B+filename%3DThe_Age_of_the_Potassic_Alkaline_Igneous.pdf\u0026Expires=1742082500\u0026Signature=fu4q8kg4NQq2r5VuF6zYf-ZZz1-nzyRZXmdpZXNx7Kr9OgR-cD1zAa-Kop~o5~i1GoTY1i82~3phWZH1HtC375xQiz~YVNU9ehwFZNGgNPugMoXVuDPgfuw2TiULJNVzwio5hym6EgZQhNMGpRSYDEx9z2BO3N57jEJvATA-zYltzN7JT2ziCozqxO57JLVxYfY-YRneQHDm2kuGwR-JQIReLHRygOblcUgbJsKfXDxZpc4K6XkKnYOZp1gzeotNKrvMyPbn6O1-WKed49kUUthA35Aqoa9KeALc5yzScVcZ5CGmqbAfZRxIDx1vFulivxw7KW3FKFAnm76IEJBTGQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_Age_of_the_Potassic_Alkaline_Igneous_Rocks_along_the_Ailao_Shan_Red_River_Shear_Zone_Implications_for_the_Onset_Age_of_Left_Lateral_Shearing_A_Discussion","translated_slug":"","page_count":4,"language":"en","content_type":"Work","summary":"Liang et al. (2007) reported new U-Pb zircon age data of 12 potassic alkaline intrusions along the Ailao Shan-Red River (ASRR) shear zone and concluded that the ages, ranging from 36.3 to 34.0 Ma, date the initiation of the ASRR left-lateral movement. Although there are numerous articles suggesting this link between alkaline magmatism and strike-slip faulting (e.g.,","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148683,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148683/thumbnails/1.jpg","file_name":"13.pdf","download_url":"https://www.academia.edu/attachments/118148683/download_file","bulk_download_file_name":"The_Age_of_the_Potassic_Alkaline_Igneous.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148683/13-libre.pdf?1726129240=\u0026response-content-disposition=attachment%3B+filename%3DThe_Age_of_the_Potassic_Alkaline_Igneous.pdf\u0026Expires=1742082500\u0026Signature=fu4q8kg4NQq2r5VuF6zYf-ZZz1-nzyRZXmdpZXNx7Kr9OgR-cD1zAa-Kop~o5~i1GoTY1i82~3phWZH1HtC375xQiz~YVNU9ehwFZNGgNPugMoXVuDPgfuw2TiULJNVzwio5hym6EgZQhNMGpRSYDEx9z2BO3N57jEJvATA-zYltzN7JT2ziCozqxO57JLVxYfY-YRneQHDm2kuGwR-JQIReLHRygOblcUgbJsKfXDxZpc4K6XkKnYOZp1gzeotNKrvMyPbn6O1-WKed49kUUthA35Aqoa9KeALc5yzScVcZ5CGmqbAfZRxIDx1vFulivxw7KW3FKFAnm76IEJBTGQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":161176,"name":"The","url":"https://www.academia.edu/Documents/in/The"},{"id":284025,"name":"Shear Zone","url":"https://www.academia.edu/Documents/in/Shear_Zone"},{"id":304909,"name":"THE GEOLOGY","url":"https://www.academia.edu/Documents/in/THE_GEOLOGY"}],"urls":[{"id":44622244,"url":"http://ntur.lib.ntu.edu.tw/bitstream/246246/172593/1/13.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800040"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800040/U_Pb_zircon_age_of_the_Andaman_ophiolite_implications_for_the_beginning_of_subduction_beneath_the_Andaman_Sumatra_arc"><img alt="Research paper thumbnail of U–Pb zircon age of the Andaman ophiolite: implications for the beginning of subduction beneath the Andaman–Sumatra arc" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">U–Pb zircon age of the Andaman ophiolite: implications for the beginning of subduction beneath the Andaman–Sumatra arc</div><div class="wp-workCard_item"><span>Journal of the Geological Society</span><span>, Oct 19, 2010</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">... 2003, 2006), and the eruption of these lavas is associated with the accretion of the complex ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... 2003, 2006), and the eruption of these lavas is associated with the accretion of the complex at the Oman palaeo ... Journal of Volcanology and Geothermal Research, 149, 177212.[CrossRef][ Web of Science][GeoRef]. ... 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Structural evolution of the High Himalayan Gneiss sequence, Langtang Valley, Nepal STEVEN...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Page 1. Structural evolution of the High Himalayan Gneiss sequence, Langtang Valley, Nepal STEVEN M. REDDY 1&amp;amp;#x27;3, MICHAEL P. SEARLE 2 &amp;amp;amp; JOHN A. 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SR Noble Natural Environment Research Council Isotope Geosciences ...","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":1590367,"name":"Monazite","url":"https://www.academia.edu/Documents/in/Monazite"},{"id":1648287,"name":"Leucogranite","url":"https://www.academia.edu/Documents/in/Leucogranite"}],"urls":[{"id":44622236,"url":"https://doi.org/10.1130/0091-7613(1995)023%3C1135:aocmal%3E2.3.co;2"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800034"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800034/Contemporaneous_crust_derived_I_and_S_type_granite_magmatism_and_normal_faulting_on_Tinos_Delos_and_Naxos_Greece_Constraints_on_Aegean_orogenic_collapse"><img alt="Research paper thumbnail of Contemporaneous crust-derived I- and S-type granite magmatism and normal faulting on Tinos, Delos, and Naxos, Greece: Constraints on Aegean orogenic collapse" class="work-thumbnail" src="https://attachments.academia-assets.com/118148679/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800034/Contemporaneous_crust_derived_I_and_S_type_granite_magmatism_and_normal_faulting_on_Tinos_Delos_and_Naxos_Greece_Constraints_on_Aegean_orogenic_collapse">Contemporaneous crust-derived I- and S-type granite magmatism and normal faulting on Tinos, Delos, and Naxos, Greece: Constraints on Aegean orogenic collapse</a></div><div class="wp-workCard_item"><span>Geological Society of America Bulletin</span><span>, Feb 16, 2023</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Geochemical Sample Preparation and Methods All samples were thoroughly washed and cleaned then cr...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Geochemical Sample Preparation and Methods All samples were thoroughly washed and cleaned then crushed into a < 80-micron powder using a Jaw crusher, followed by running through a Tema Mill using an agate crucible to avoid contamination by tungsten carbide. The crucible was thoroughly cleaned and run through separately with in house sand and the resultant powder was then passed through an 80-micron sieve. Some of the resultant powders were then sent off to the Franklin and Marshall College, Pennsylvania, USA, for X-ray fluorescence by Dr Stanley Mertzman. The remaining powder was weighed and prepared for ICP-MS in house at the Department of Earth Sciences, University of Oxford. Full descriptions for each method are outlined below. X-Ray Fluorescence XRF was carried out by weighing 0.4000 ± 0.0001 grams of crushed rock powder and mixing with lithium tetraborate (3.6000 ± 0.0002 grams). The subsequent solution was then placed in a platinum crucible and heated with a meeker burner until molten. The molten material was transferred to a platinum casting dish and quenched. This procedure produced a glass disk that is used for XRF analysis of SiO 2, Al2O3, CaO, K2O, P2O5, TiO2, total iron reported as Fe2O3T, MnO, Na2O and MgO. Trace element analysis was achieved by weighing 7.0000 ± 0.0004 grams of whole rock powder and adding 1.4000±0.0002 of high purity copolywax powder. This was mixed for 10 minutes, and the powder was pressed into a briquette. Data are reported as parts per million (ppm) for Rb,</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="18f813b05e5b0750113a7b219591f419" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148679,"asset_id":123800034,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148679/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800034"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800034"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800034; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800034]").text(description); $(".js-view-count[data-work-id=123800034]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800034; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800034']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "18f813b05e5b0750113a7b219591f419" } } $('.js-work-strip[data-work-id=123800034]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800034,"title":"Contemporaneous crust-derived I- and S-type granite magmatism and normal faulting on Tinos, Delos, and Naxos, Greece: Constraints on Aegean orogenic collapse","translated_title":"","metadata":{"publisher":"Geological Society of America","grobid_abstract":"Geochemical Sample Preparation and Methods All samples were thoroughly washed and cleaned then crushed into a \u003c 80-micron powder using a Jaw crusher, followed by running through a Tema Mill using an agate crucible to avoid contamination by tungsten carbide. 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Trace element analysis was achieved by weighing 7.0000 ± 0.0004 grams of whole rock powder and adding 1.4000±0.0002 of high purity copolywax powder. This was mixed for 10 minutes, and the powder was pressed into a briquette. 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The crucible was thoroughly cleaned and run through separately with in house sand and the resultant powder was then passed through an 80-micron sieve. Some of the resultant powders were then sent off to the Franklin and Marshall College, Pennsylvania, USA, for X-ray fluorescence by Dr Stanley Mertzman. The remaining powder was weighed and prepared for ICP-MS in house at the Department of Earth Sciences, University of Oxford. Full descriptions for each method are outlined below. X-Ray Fluorescence XRF was carried out by weighing 0.4000 ± 0.0001 grams of crushed rock powder and mixing with lithium tetraborate (3.6000 ± 0.0002 grams). The subsequent solution was then placed in a platinum crucible and heated with a meeker burner until molten. The molten material was transferred to a platinum casting dish and quenched. This procedure produced a glass disk that is used for XRF analysis of SiO 2, Al2O3, CaO, K2O, P2O5, TiO2, total iron reported as Fe2O3T, MnO, Na2O and MgO. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800033"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800033/Tectonic_significance_of_24_Ma_crustal_melting_in_the_eastern_Hindu_Kush_Pakistan"><img alt="Research paper thumbnail of Tectonic significance of 24 Ma crustal melting in the eastern Hindu Kush, Pakistan" class="work-thumbnail" src="https://attachments.academia-assets.com/118148709/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800033/Tectonic_significance_of_24_Ma_crustal_melting_in_the_eastern_Hindu_Kush_Pakistan">Tectonic significance of 24 Ma crustal melting in the eastern Hindu Kush, Pakistan</a></div><div class="wp-workCard_item"><span>Geology</span><span>, Oct 1, 1998</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="c5867d6339a24f8e4b23d1faeee61f73" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148709,"asset_id":123800033,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148709/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800033"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800033"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800033; 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New geological mapping and U-Pb geochronology reveal the existence of the Gharam Chasma pluton, with implications for the thermal history and metamorphic events along the southern margin of the Asian plate. 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The leucogranite comprises the assemblage: K-feldspar + quartz + plagioclase + tourmaline + ...","internal_url":"https://www.academia.edu/123800029/Field_relations_petrogenesis_and_emplacement_of_the_Bhagirathi_leucogranite_Garhwal_Himalaya","translated_internal_url":"","created_at":"2024-09-11T23:37:34.467-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Field_relations_petrogenesis_and_emplacement_of_the_Bhagirathi_leucogranite_Garhwal_Himalaya","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Abstract: The Bhagirathi leucogranite forms a series of low-angle en echelon, lensoidal intrusions at the top of the High Himalayan slab in the central Himalaya of Garhwal, northern India. The leucogranite comprises the assemblage: K-feldspar + quartz + plagioclase + tourmaline + ...","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":319882,"name":"Petrogenesis","url":"https://www.academia.edu/Documents/in/Petrogenesis"},{"id":926279,"name":"GEological Society of London","url":"https://www.academia.edu/Documents/in/GEological_Society_of_London"},{"id":1648287,"name":"Leucogranite","url":"https://www.academia.edu/Documents/in/Leucogranite"}],"urls":[{"id":44622231,"url":"https://doi.org/10.1144/gsl.sp.1993.074.01.29"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800028"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800028/The_Timing_of_Metamorphism_Magmatism_and_Cooling_in_the_Zanskar_Garhwal_and_Nepal_Himalaya"><img alt="Research paper thumbnail of The Timing of Metamorphism, Magmatism, and Cooling in the Zanskar, Garhwal, and Nepal Himalaya" class="work-thumbnail" src="https://attachments.academia-assets.com/118148708/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800028/The_Timing_of_Metamorphism_Magmatism_and_Cooling_in_the_Zanskar_Garhwal_and_Nepal_Himalaya">The Timing of Metamorphism, Magmatism, and Cooling in the Zanskar, Garhwal, and Nepal Himalaya</a></div><div class="wp-workCard_item"><span>Journal of Nepal Geological Society</span><span>, Dec 1, 1995</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="bd8b2534aa91b4cbaacd84af2a23316c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148708,"asset_id":123800028,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148708/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800028"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800028"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800028; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800027"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800027/Spatial_and_Temporal_Distributions_of_Deformation_in_Strike_Slip_Faults_The_Karakoram_Fault_in_the_India_Asia_Collision_Zone"><img alt="Research paper thumbnail of Spatial and Temporal Distributions of Deformation in Strike-Slip Faults: The Karakoram Fault in the India-Asia Collision Zone" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Spatial and Temporal Distributions of Deformation in Strike-Slip Faults: The Karakoram Fault in the India-Asia Collision Zone</div><div class="wp-workCard_item"><span>Elsevier eBooks</span><span>, 2019</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract Assessments of spatial and temporal distributions of deformation within fault zones, inc...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract Assessments of spatial and temporal distributions of deformation within fault zones, including their ductile shear zones, are critical for characterizing wider deformation of the lithosphere and associated seismic hazard. However, deformation within fault zones, often quantified as slip rate or strain rate, is potentially heterogeneous in any of the three spatial dimensions (i.e., along strike, across strike, and with depth) and in time. The complex distributions of deformation that result present a challenge for assessments of the present and past behavior of individual faults and for establishing models of the roles of faults in deforming regions. In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. The KFZ offers a potential analog for other major strike-slip faults for which portions of this record (in space and/or time) may not be accessible.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800027"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800027"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800027; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800027]").text(description); $(".js-view-count[data-work-id=123800027]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800027; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800027']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=123800027]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800027,"title":"Spatial and Temporal Distributions of Deformation in Strike-Slip Faults: The Karakoram Fault in the India-Asia Collision Zone","translated_title":"","metadata":{"abstract":"Abstract Assessments of spatial and temporal distributions of deformation within fault zones, including their ductile shear zones, are critical for characterizing wider deformation of the lithosphere and associated seismic hazard. However, deformation within fault zones, often quantified as slip rate or strain rate, is potentially heterogeneous in any of the three spatial dimensions (i.e., along strike, across strike, and with depth) and in time. The complex distributions of deformation that result present a challenge for assessments of the present and past behavior of individual faults and for establishing models of the roles of faults in deforming regions. In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. The KFZ offers a potential analog for other major strike-slip faults for which portions of this record (in space and/or time) may not be accessible.","publisher":"Elsevier BV","publication_date":{"day":null,"month":null,"year":2019,"errors":{}},"publication_name":"Elsevier eBooks"},"translated_abstract":"Abstract Assessments of spatial and temporal distributions of deformation within fault zones, including their ductile shear zones, are critical for characterizing wider deformation of the lithosphere and associated seismic hazard. However, deformation within fault zones, often quantified as slip rate or strain rate, is potentially heterogeneous in any of the three spatial dimensions (i.e., along strike, across strike, and with depth) and in time. The complex distributions of deformation that result present a challenge for assessments of the present and past behavior of individual faults and for establishing models of the roles of faults in deforming regions. In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. The KFZ offers a potential analog for other major strike-slip faults for which portions of this record (in space and/or time) may not be accessible.","internal_url":"https://www.academia.edu/123800027/Spatial_and_Temporal_Distributions_of_Deformation_in_Strike_Slip_Faults_The_Karakoram_Fault_in_the_India_Asia_Collision_Zone","translated_internal_url":"","created_at":"2024-09-11T23:37:32.976-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Spatial_and_Temporal_Distributions_of_Deformation_in_Strike_Slip_Faults_The_Karakoram_Fault_in_the_India_Asia_Collision_Zone","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Abstract Assessments of spatial and temporal distributions of deformation within fault zones, including their ductile shear zones, are critical for characterizing wider deformation of the lithosphere and associated seismic hazard. However, deformation within fault zones, often quantified as slip rate or strain rate, is potentially heterogeneous in any of the three spatial dimensions (i.e., along strike, across strike, and with depth) and in time. The complex distributions of deformation that result present a challenge for assessments of the present and past behavior of individual faults and for establishing models of the roles of faults in deforming regions. In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. The KFZ offers a potential analog for other major strike-slip faults for which portions of this record (in space and/or time) may not be accessible.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":3157,"name":"Seismic Hazard","url":"https://www.academia.edu/Documents/in/Seismic_Hazard"},{"id":13883,"name":"Seismology","url":"https://www.academia.edu/Documents/in/Seismology"},{"id":284025,"name":"Shear Zone","url":"https://www.academia.edu/Documents/in/Shear_Zone"},{"id":897823,"name":"Elsevier","url":"https://www.academia.edu/Documents/in/Elsevier"},{"id":1208243,"name":"Strike Slip Tectonics","url":"https://www.academia.edu/Documents/in/Strike_Slip_Tectonics"}],"urls":[{"id":44622229,"url":"https://doi.org/10.1016/b978-0-12-812064-4.00011-6"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800026"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800026/Age_and_petrogenesis_of_the_Lundy_granite_Paleocene_intraplate_peraluminous_magmatism_in_the_Bristol_Channel_UK"><img alt="Research paper thumbnail of Age and petrogenesis of the Lundy granite: Paleocene intraplate peraluminous magmatism in the Bristol Channel, UK" class="work-thumbnail" src="https://attachments.academia-assets.com/118148676/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800026/Age_and_petrogenesis_of_the_Lundy_granite_Paleocene_intraplate_peraluminous_magmatism_in_the_Bristol_Channel_UK">Age and petrogenesis of the Lundy granite: Paleocene intraplate peraluminous magmatism in the Bristol Channel, UK</a></div><div class="wp-workCard_item"><span>Journal of the Geological Society</span><span>, Oct 2, 2017</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Lundy granite forms part of the Lundy Igneous Complex which is the southernmost substantive e...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Lundy granite forms part of the Lundy Igneous Complex which is the southernmost substantive expression of the British Cenozoic Igneous Province (BCIP). Its Qz+Pl+Kfs+Bt±Grt±Tpz 16 mineralogy and peraluminous character contrast with other BCIP granites farther north but are similar to the granites of the adjacent Early Permian Cornubian Batholith. We present the results of mapping, petrographical and mineral chemical analysis, and the first U-Pb zircon ages for the granite (59.8 ± 19 0.4-58.4 ± 0.4 Ma) and crosscutting basic dykes (57.2 ± 0.5 Ma) which confirm a Palaeocene age 20 for magmatism. Zircon inheritance is limited but two cores imply the presence of Lower Palaeozoic igneous rocks in the unexposed basement of SW England. The anomalous southerly location of the Lundy Igneous Complex is a consequence of mantle melting arising from the superposition of localised lithospheric extension, related to intraplate strike-slip tectonics, with the distal ancestral Icelandic plume. Granite generation primarily reflects crustal partial melting during the emplacement of mantle-derived melts. The change in geochemical character between the Lundy granite (peraluminous) and other BCIP granites (metaluminous / subalkaline) indicates a fundamental crustal source control between contrasting peri-Gondwanan and Laurentian basement provinces.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d76a0a3921c06e9b5f2edb06a89fc643" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148676,"asset_id":123800026,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148676/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800026"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800026"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800026; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800026]").text(description); $(".js-view-count[data-work-id=123800026]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800026; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800026']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d76a0a3921c06e9b5f2edb06a89fc643" } } $('.js-work-strip[data-work-id=123800026]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800026,"title":"Age and petrogenesis of the Lundy granite: Paleocene intraplate peraluminous magmatism in the Bristol Channel, UK","translated_title":"","metadata":{"publisher":"Geological Society of London","grobid_abstract":"The Lundy granite forms part of the Lundy Igneous Complex which is the southernmost substantive expression of the British Cenozoic Igneous Province (BCIP). Its Qz+Pl+Kfs+Bt±Grt±Tpz 16 mineralogy and peraluminous character contrast with other BCIP granites farther north but are similar to the granites of the adjacent Early Permian Cornubian Batholith. We present the results of mapping, petrographical and mineral chemical analysis, and the first U-Pb zircon ages for the granite (59.8 ± 19 0.4-58.4 ± 0.4 Ma) and crosscutting basic dykes (57.2 ± 0.5 Ma) which confirm a Palaeocene age 20 for magmatism. Zircon inheritance is limited but two cores imply the presence of Lower Palaeozoic igneous rocks in the unexposed basement of SW England. The anomalous southerly location of the Lundy Igneous Complex is a consequence of mantle melting arising from the superposition of localised lithospheric extension, related to intraplate strike-slip tectonics, with the distal ancestral Icelandic plume. Granite generation primarily reflects crustal partial melting during the emplacement of mantle-derived melts. 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The change in geochemical character between the Lundy granite (peraluminous) and other BCIP granites (metaluminous / subalkaline) indicates a fundamental crustal source control between contrasting peri-Gondwanan and Laurentian basement provinces.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148676,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148676/thumbnails/1.jpg","file_name":"Charles_20et_20al_20JGSL_20Lundy.pdf","download_url":"https://www.academia.edu/attachments/118148676/download_file","bulk_download_file_name":"Age_and_petrogenesis_of_the_Lundy_granit.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148676/Charles_20et_20al_20JGSL_20Lundy-libre.pdf?1726129281=\u0026response-content-disposition=attachment%3B+filename%3DAge_and_petrogenesis_of_the_Lundy_granit.pdf\u0026Expires=1742323207\u0026Signature=Dee1m~XME-P60sIrUNmr4Wt1dNYq-u-Qgy6H7ojz-In3-sZg-pUW2JerFK1zyuCAKoC1AZ61~wI48-ZY~ACw~4El4JKXzeWrE6h~qWB-Jp2v1MAOFO3XS24m27I82zdVbRgMvM4I0twVXeTvp4AlSysPSUIEgB4fvMlMP0ywn~nlPCd60GsCLm8t6vfazrBBVVAKIlCdE-35klqeVQS6TBPJHlCwWbMu3oIrzf9TYkT5CSehM3re2vRD0DhNzUk5IdiwpDu0If~PBcFb60c9zeaFfydiIkkOIJoKgVUNF48HFkgOouOoVymd7UPL2dvmu6s~nm5O~ukgN50tB1J5-A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":118148675,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148675/thumbnails/1.jpg","file_name":"Charles_20et_20al_20JGSL_20Lundy.pdf","download_url":"https://www.academia.edu/attachments/118148675/download_file","bulk_download_file_name":"Age_and_petrogenesis_of_the_Lundy_granit.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148675/Charles_20et_20al_20JGSL_20Lundy-libre.pdf?1726129299=\u0026response-content-disposition=attachment%3B+filename%3DAge_and_petrogenesis_of_the_Lundy_granit.pdf\u0026Expires=1742323207\u0026Signature=gMOC1f5lM6rLTLk0kGB0WyhLAB8N2dVWYlYgjH~Xhoozs1E9YYeG~OfsHA5s57j26joFO2SuUfzga53bnDcBN9jVX2e4Kt49h4f1qZW0qrrXNCGXdYvgRBYhXpkOkfb6jR591svCnq0rrUU7xVFz-DTofRwJ45ZmY227NqopsdZC0vCK4lz7v7x4eabKbG0OgR3NpzlHb9Takiva98TtQMnTFXw~XNWIVcciI~92lxbQsGAjCD4-OdYaNHd7WXr2DRJEEmkZ5694bAaDyk-KzkRK09JUdOkG1L1kUyyohh5LEPAtZoTZmephJ3HKbw37A4bWKz5dMneB1aaCneUF3A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"},{"id":319882,"name":"Petrogenesis","url":"https://www.academia.edu/Documents/in/Petrogenesis"}],"urls":[{"id":44622228,"url":"https://ore.exeter.ac.uk/repository/bitstream/10871/29676/1/Charles%20et%20al%20(JGSL)%20Lundy.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="3376027" id="papers"><div class="js-work-strip profile--work_container" data-work-id="123800057"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800057/_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting"><img alt="Research paper thumbnail of “Oman Exotics”—Oceanic carbonate build-ups associated with the early stages of continental rifting" class="work-thumbnail" src="https://attachments.academia-assets.com/118148720/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800057/_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting">“Oman Exotics”—Oceanic carbonate build-ups associated with the early stages of continental rifting</a></div><div class="wp-workCard_item"><span>Geology</span><span>, 1982</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The so-called "Oman Exotic" limestones form isolated masses, from boulder size to 1,000 m thick, ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The so-called "Oman Exotic" limestones form isolated masses, from boulder size to 1,000 m thick, of Middle to Upper Permian and Upper Triassic fossiliferous limestones, and crop out within imbricated thrust slices beneath the Semail ophiolite in the Oman Mountains. Permian Exotics are of dominantly reef and forereef facies, whereas Triassic Exotics are more typically of back-reef and lagoonal facies. They are commonly associated with a substrate of alkalic and transitional tholeiitic basalts and are interpreted as a series of reef-associated carbonate buildups deposited in part on oceanic islands or seamounts, close to the site of initial rifting of the Oman continental margin.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="bae680503e97b5c2f9e4c925db9486f7" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148720,"asset_id":123800057,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148720/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800057"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800057"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800057; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800057]").text(description); $(".js-view-count[data-work-id=123800057]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800057; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800057']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "bae680503e97b5c2f9e4c925db9486f7" } } $('.js-work-strip[data-work-id=123800057]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800057,"title":"“Oman Exotics”—Oceanic carbonate build-ups associated with the early stages of continental rifting","translated_title":"","metadata":{"publisher":"Geological Society of America","grobid_abstract":"The so-called \"Oman Exotic\" limestones form isolated masses, from boulder size to 1,000 m thick, of Middle to Upper Permian and Upper Triassic fossiliferous limestones, and crop out within imbricated thrust slices beneath the Semail ophiolite in the Oman Mountains. Permian Exotics are of dominantly reef and forereef facies, whereas Triassic Exotics are more typically of back-reef and lagoonal facies. They are commonly associated with a substrate of alkalic and transitional tholeiitic basalts and are interpreted as a series of reef-associated carbonate buildups deposited in part on oceanic islands or seamounts, close to the site of initial rifting of the Oman continental margin.","publication_date":{"day":null,"month":null,"year":1982,"errors":{}},"publication_name":"Geology","grobid_abstract_attachment_id":118148720},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800057/_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting","translated_internal_url":"","created_at":"2024-09-11T23:37:58.723-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148720,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148720/thumbnails/1.jpg","file_name":"0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is.pdf","download_url":"https://www.academia.edu/attachments/118148720/download_file","bulk_download_file_name":"Oman_Exotics_Oceanic_carbonate_build_up.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148720/0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is-libre.pdf?1726129278=\u0026response-content-disposition=attachment%3B+filename%3DOman_Exotics_Oceanic_carbonate_build_up.pdf\u0026Expires=1742082500\u0026Signature=N-~mFVnrnAFDZLdkFEUKH4ww7NV6elCHmfYW1N~e8Zp8YukCZjnPO8BksHeg~Nxfpymhhe9sytBa1SB2-vRD6ce1OYU6wta8eLJf8mifUjC9JzL0KhOZQbCoQo3zKPMb75iLqOk4LAPGZ6VQ0CRSK7xuGbNRAVr0vc9kYLE3f7-qqcYQrvkiZTrE7q7ThEoHIezduB~xznyvCcZNT-MiiaoqCPEv~4OlEYOxUsZfui47JZCHi2qHupZmbK6RQ1V2X8SmIPi6LclkqC00533x5aQoQFRA63sFDMDoKRJlVTuYYTTx8akZ6e4y1bURKwilBMsdd1GF1Y4xkcxPCFyqZg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"_Oman_Exotics_Oceanic_carbonate_build_ups_associated_with_the_early_stages_of_continental_rifting","translated_slug":"","page_count":7,"language":"en","content_type":"Work","summary":"The so-called \"Oman Exotic\" limestones form isolated masses, from boulder size to 1,000 m thick, of Middle to Upper Permian and Upper Triassic fossiliferous limestones, and crop out within imbricated thrust slices beneath the Semail ophiolite in the Oman Mountains. Permian Exotics are of dominantly reef and forereef facies, whereas Triassic Exotics are more typically of back-reef and lagoonal facies. They are commonly associated with a substrate of alkalic and transitional tholeiitic basalts and are interpreted as a series of reef-associated carbonate buildups deposited in part on oceanic islands or seamounts, close to the site of initial rifting of the Oman continental margin.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148720,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148720/thumbnails/1.jpg","file_name":"0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is.pdf","download_url":"https://www.academia.edu/attachments/118148720/download_file","bulk_download_file_name":"Oman_Exotics_Oceanic_carbonate_build_up.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148720/0091-761328198229103C433AOECBAW3E2.0.CO3B220240912-1-u2w8is-libre.pdf?1726129278=\u0026response-content-disposition=attachment%3B+filename%3DOman_Exotics_Oceanic_carbonate_build_up.pdf\u0026Expires=1742082500\u0026Signature=N-~mFVnrnAFDZLdkFEUKH4ww7NV6elCHmfYW1N~e8Zp8YukCZjnPO8BksHeg~Nxfpymhhe9sytBa1SB2-vRD6ce1OYU6wta8eLJf8mifUjC9JzL0KhOZQbCoQo3zKPMb75iLqOk4LAPGZ6VQ0CRSK7xuGbNRAVr0vc9kYLE3f7-qqcYQrvkiZTrE7q7ThEoHIezduB~xznyvCcZNT-MiiaoqCPEv~4OlEYOxUsZfui47JZCHi2qHupZmbK6RQ1V2X8SmIPi6LclkqC00533x5aQoQFRA63sFDMDoKRJlVTuYYTTx8akZ6e4y1bURKwilBMsdd1GF1Y4xkcxPCFyqZg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":417,"name":"Paleontology","url":"https://www.academia.edu/Documents/in/Paleontology"},{"id":71553,"name":"Icon","url":"https://www.academia.edu/Documents/in/Icon"},{"id":91258,"name":"Carbonate","url":"https://www.academia.edu/Documents/in/Carbonate"},{"id":151949,"name":"RIFT","url":"https://www.academia.edu/Documents/in/RIFT"},{"id":199319,"name":"Citation","url":"https://www.academia.edu/Documents/in/Citation"},{"id":604905,"name":"Oceanic Islands","url":"https://www.academia.edu/Documents/in/Oceanic_Islands"},{"id":632867,"name":"ICON","url":"https://www.academia.edu/Documents/in/ICON-1"},{"id":1479595,"name":"Continental Margin","url":"https://www.academia.edu/Documents/in/Continental_Margin"}],"urls":[{"id":44622252,"url":"https://doi.org/10.1130/0091-7613(1982)10%3C43:oecbaw%3E2.0.co;2"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800056"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800056/Constraining_the_Timing_of_Prograde_Metamorphism_in_the_Sole_of_the_Semail_Ophiolite_Coupled_Zircon_Tims_U_PB_Dating_and_Trace_Element_Analyses_from_the_Masafi_Sole_Exposure_United_Arab_Emirates_U_A_E_"><img alt="Research paper thumbnail of Constraining the Timing of Prograde Metamorphism in the Sole of the Semail Ophiolite: Coupled Zircon Tims U-PB Dating and Trace Element Analyses from the Masafi Sole Exposure, United Arab Emirates (U.A.E.)" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Constraining the Timing of Prograde Metamorphism in the Sole of the Semail Ophiolite: Coupled Zircon Tims U-PB Dating and Trace Element Analyses from the Masafi Sole Exposure, United Arab Emirates (U.A.E.)</div><div class="wp-workCard_item"><span>GSA Annual Meeting in Phoenix, Arizona, USA - 2019</span><span>, 2019</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800056"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800056"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800056; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800055"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800055/Continentes_en_colisi%C3%B3n_creaci%C3%B3n_de_monta%C3%B1as"><img alt="Research paper thumbnail of Continentes en colisión, creación de montañas" class="work-thumbnail" src="https://attachments.academia-assets.com/118148718/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800055/Continentes_en_colisi%C3%B3n_creaci%C3%B3n_de_monta%C3%B1as">Continentes en colisión, creación de montañas</a></div><div class="wp-workCard_item"><span>Enseñanza de las ciencias de la tierra: Revista de la Asociación Española para la Enseñanza de las Ciencias de la Tierra</span><span>, 2018</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicació...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicación coherente a la formación de las montañas. Para el caso concreto del Himalaya, esta gran cordillera es el fruto de la colisión continental que tuvo lugar hace alrededor de 50 millones de años. La particular disposición de la cadena montañosa, inclinada hacia el norte debido a que la placa india intenta subducir bajo Asia, permite cartografiar estructuras y tomar muestras de su estructura profunda y, por lo tanto, descifrar su origen y evolución a lo largo del tiempo. En concreto, cuatro grandes estructuras (en forma de fallas y cabalgamientos) permiten definir otras tantas unidades estructurales incluidas tanto en la placa litosférica india como en la asiática. Los frecuentes terremotos aportan información acerca de la actividad de estas estructuras. Por otro lado, el acortamiento y engrosamiento cortical provocan el levantamiento de la cordillera, pero el ascenso topográfico incrementa también la intensidad de la erosión, provocando un efecto retroalimentado y el continuo rejuvenecimiento del relieve.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="c21dbe442a5531cfcf3d972995f64a31" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148718,"asset_id":123800055,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148718/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800055"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800055"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800055; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800055]").text(description); $(".js-view-count[data-work-id=123800055]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800055; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800055']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "c21dbe442a5531cfcf3d972995f64a31" } } $('.js-work-strip[data-work-id=123800055]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800055,"title":"Continentes en colisión, creación de montañas","translated_title":"","metadata":{"grobid_abstract":"modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicación coherente a la formación de las montañas. Para el caso concreto del Himalaya, esta gran cordillera es el fruto de la colisión continental que tuvo lugar hace alrededor de 50 millones de años. La particular disposición de la cadena montañosa, inclinada hacia el norte debido a que la placa india intenta subducir bajo Asia, permite cartografiar estructuras y tomar muestras de su estructura profunda y, por lo tanto, descifrar su origen y evolución a lo largo del tiempo. En concreto, cuatro grandes estructuras (en forma de fallas y cabalgamientos) permiten definir otras tantas unidades estructurales incluidas tanto en la placa litosférica india como en la asiática. Los frecuentes terremotos aportan información acerca de la actividad de estas estructuras. Por otro lado, el acortamiento y engrosamiento cortical provocan el levantamiento de la cordillera, pero el ascenso topográfico incrementa también la intensidad de la erosión, provocando un efecto retroalimentado y el continuo rejuvenecimiento del relieve.","publication_date":{"day":null,"month":null,"year":2018,"errors":{}},"publication_name":"Enseñanza de las ciencias de la tierra: Revista de la Asociación Española para la Enseñanza de las Ciencias de la Tierra","grobid_abstract_attachment_id":118148718},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800055/Continentes_en_colisi%C3%B3n_creaci%C3%B3n_de_monta%C3%B1as","translated_internal_url":"","created_at":"2024-09-11T23:37:58.087-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148718,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148718/thumbnails/1.jpg","file_name":"155003812.pdf","download_url":"https://www.academia.edu/attachments/118148718/download_file","bulk_download_file_name":"Continentes_en_colision_creacion_de_mont.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148718/155003812-libre.pdf?1726129240=\u0026response-content-disposition=attachment%3B+filename%3DContinentes_en_colision_creacion_de_mont.pdf\u0026Expires=1742082500\u0026Signature=YDJ6lL4YNa9HRw56UoUrdqei15kFEdvyd3ipoHPJdoaghUZPrK4VwIlQVLh6cYmCj9~~UnzQXWtc4q9uXEtZQQldt1CC0fbksf3CfmF7Wfvg27MZv6mCDuNj9jcBcnHYOkG8LekbrydhDblznke7XX6W0PrhGujdnmaDlwOxb3SEXieNORDvpvHwLjtIgtOUmzcQT9JZPSSGm2Slkhe9~3JRTHf9qaxxeSRx~iJlyVYxKSUT1WbOp3QP0jTd8Cd-9BuO5OZoX8tgh6dDNDKguSd-14B-oi8tm6y-SriBepC2tvtxB0um~c2LYVdCHo194siq3RllYlM116Lk8sQdTQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Continentes_en_colisión_creación_de_montañas","translated_slug":"","page_count":6,"language":"es","content_type":"Work","summary":"modelizaciones numéricas y otro tipo de investigaciones, la geología actual ofrece una explicación coherente a la formación de las montañas. Para el caso concreto del Himalaya, esta gran cordillera es el fruto de la colisión continental que tuvo lugar hace alrededor de 50 millones de años. La particular disposición de la cadena montañosa, inclinada hacia el norte debido a que la placa india intenta subducir bajo Asia, permite cartografiar estructuras y tomar muestras de su estructura profunda y, por lo tanto, descifrar su origen y evolución a lo largo del tiempo. En concreto, cuatro grandes estructuras (en forma de fallas y cabalgamientos) permiten definir otras tantas unidades estructurales incluidas tanto en la placa litosférica india como en la asiática. Los frecuentes terremotos aportan información acerca de la actividad de estas estructuras. Por otro lado, el acortamiento y engrosamiento cortical provocan el levantamiento de la cordillera, pero el ascenso topográfico incrementa también la intensidad de la erosión, provocando un efecto retroalimentado y el continuo rejuvenecimiento del relieve.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148718,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148718/thumbnails/1.jpg","file_name":"155003812.pdf","download_url":"https://www.academia.edu/attachments/118148718/download_file","bulk_download_file_name":"Continentes_en_colision_creacion_de_mont.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148718/155003812-libre.pdf?1726129240=\u0026response-content-disposition=attachment%3B+filename%3DContinentes_en_colision_creacion_de_mont.pdf\u0026Expires=1742082500\u0026Signature=YDJ6lL4YNa9HRw56UoUrdqei15kFEdvyd3ipoHPJdoaghUZPrK4VwIlQVLh6cYmCj9~~UnzQXWtc4q9uXEtZQQldt1CC0fbksf3CfmF7Wfvg27MZv6mCDuNj9jcBcnHYOkG8LekbrydhDblznke7XX6W0PrhGujdnmaDlwOxb3SEXieNORDvpvHwLjtIgtOUmzcQT9JZPSSGm2Slkhe9~3JRTHf9qaxxeSRx~iJlyVYxKSUT1WbOp3QP0jTd8Cd-9BuO5OZoX8tgh6dDNDKguSd-14B-oi8tm6y-SriBepC2tvtxB0um~c2LYVdCHo194siq3RllYlM116Lk8sQdTQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":951,"name":"Humanities","url":"https://www.academia.edu/Documents/in/Humanities"}],"urls":[{"id":44622250,"url":"https://dialnet.unirioja.es/servlet/articulo?codigo=7103737"}]}, dispatcherData: dispatcherData }); 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This thrust sheet is termed the Haybi complex, and consists of sub-ophiolitic metamorphic rocks and serpentinite, alkaline and tholeiitic basalts (the Haybi volcanics), associated with mountain-sized "Exotic" limestones and an Upper Cretaceous sedimentary melange. The rocks of the Haybi complex are bounded by major thrust planes, the Semail thrust above and the Haybi thrust beneath, which truncate all schistosities, fold axes, imbricate thrust and associated features. The Haybi volcanics are mainly Triassic in age and form a substrate to or enclose large, isolated blOCKS of Permian or Triassic "Exotic" limestones, Although they have been considerably disrupted and imbricated during south-westward emplacement, intact sequences show that the lower part is composed mainly of alkaline pyroclastics and lavas, including ankaramites, nephelinites and trachytes, whereas the upper part is predominantly tholeiitic pillow lavas and breccias. Late sills of alkali pyroxenite, wehrlite and kaersutite gabbro intrude the tholeiitic volcanics in a few localities and have been dated as Turonian (Upper Cretaceous). Geochemical studies, particularly of "immobile" elements show that the lower volcanics and the late sills are strongly alkaline with high Ti, p, Zr and Nb contents, low Y /Nb ratios and steep LREE enriched rare earth patterns. They are 1 Professor Ian Gass, my supervisor for obtaining an Open University grant and providing support for three years. 2 Drs. 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Adrian Lewis, John Smewing, Steve Lippard and John Malpas for providing much help and supervision both in the field and back in England.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148717,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148717/thumbnails/1.jpg","file_name":"354276_2.pdf","download_url":"https://www.academia.edu/attachments/118148717/download_file","bulk_download_file_name":"The_metamorphic_sheet_and_underlying_vol.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148717/354276_2.pdf?1726123138=\u0026response-content-disposition=attachment%3B+filename%3DThe_metamorphic_sheet_and_underlying_vol.pdf\u0026Expires=1742082500\u0026Signature=I49~Z70PXCdN6hna-SlkKgVLaeL9WJK6SkbpNLNBCDNK~GBneQegOCYLBSw1Y2~5hQokRIAAfejpNmbYG6QD2FI7eLkOtS-4bkKgk2zxbbC0l6ETRHevuwYVb9UqEPs-JO0XGsmVpbssW3QuNXcnsyfVwkUXQYvtpmz7qsRS-TPqmZLCHk5AAHpiq8oeGy5Myj88Mayoa7VjwZcewQLYvK1GAYdKM8fouee9EMBSyhMIJFcOw6SpAI2PSkXhQAYiFXaVagR5u97LF3y3i8o89hGlnztlfpf1tAM-sV1Ka0E8f-cqHBz~Aj~n~TknLl~zaoWpz43gyEJ8h~R95etnPA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":330036,"name":"Ophiolite","url":"https://www.academia.edu/Documents/in/Ophiolite"},{"id":688910,"name":"Volcanic Rock","url":"https://www.academia.edu/Documents/in/Volcanic_Rock"}],"urls":[{"id":44622248,"url":"http://oro.open.ac.uk/54606/"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800052"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800052/Comment_on_Interplay_of_deformation_and_magmatism_in_the_Pangong_Transpressional_Zone_Eastern_Ladakh_India_Implications_for_remobilization_of_the_trans_Himalayan_magmatic_arc_and_initiation_of_the_Karakoram_Fault_by_K_Sen_B_K_Mukherjee_and_A_S_Collins_Journal_of_Structural_Geology_62_2_"><img alt="Research paper thumbnail of Comment on “Interplay of deformation and magmatism in the Pangong Transpressional Zone, Eastern Ladakh, India: Implications for remobilization of the trans-Himalayan magmatic arc and initiation of the Karakoram Fault” by K. Sen, B.K. Mukherjee and A.S. Collins, Journal of Structural Geology 62 (2..." class="work-thumbnail" src="https://attachments.academia-assets.com/118148687/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800052/Comment_on_Interplay_of_deformation_and_magmatism_in_the_Pangong_Transpressional_Zone_Eastern_Ladakh_India_Implications_for_remobilization_of_the_trans_Himalayan_magmatic_arc_and_initiation_of_the_Karakoram_Fault_by_K_Sen_B_K_Mukherjee_and_A_S_Collins_Journal_of_Structural_Geology_62_2_">Comment on “Interplay of deformation and magmatism in the Pangong Transpressional Zone, Eastern Ladakh, India: Implications for remobilization of the trans-Himalayan magmatic arc and initiation of the Karakoram Fault” by K. Sen, B.K. Mukherjee and A.S. Collins, Journal of Structural Geology 62 (2...</a></div><div class="wp-workCard_item"><span>Journal of Structural Geology</span><span>, Aug 1, 2014</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d27152e3d94a9da841fdf30089febec8" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148687,"asset_id":123800052,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148687/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800052"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800052"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800052; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800052]").text(description); $(".js-view-count[data-work-id=123800052]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800052; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800052']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d27152e3d94a9da841fdf30089febec8" } } $('.js-work-strip[data-work-id=123800052]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800052,"title":"Comment on “Interplay of deformation and magmatism in the Pangong Transpressional Zone, Eastern Ladakh, India: Implications for remobilization of the trans-Himalayan magmatic arc and initiation of the Karakoram Fault” by K. Sen, B.K. Mukherjee and A.S. Collins, Journal of Structural Geology 62 (2...","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_abstract":"This paper critiques the conclusions drawn by Sen et al. regarding the age and kinematics of the Karakoram Fault Zone (KFZ) and its relationship to the Tangtse-Darbuk leucogranite (TDL). The authors argue that Sen et al.'s interpretations are based on misinterpretations of microstructural evidence and insufficient caution in analyzing anisotropy of magnetic susceptibility (AMS) data. The findings support a model where the KFZ initiated after the TDL cooled, indicating a more recent formation and emphasizing the need for rigorous validation of AMS correlations with deformation fabrics.","publication_date":{"day":1,"month":8,"year":2014,"errors":{}},"publication_name":"Journal of Structural 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Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology"},{"id":191873,"name":"Magmatism","url":"https://www.academia.edu/Documents/in/Magmatism"}],"urls":[{"id":44622247,"url":"http://eprints.whiterose.ac.uk/80281/1/Wallis_et_al_comment_revision.pdf"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800051"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800051/Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow"><img alt="Research paper thumbnail of Constraints on brittle field exhumation of the Everest-Makalu section of the Greater Himalayan Sequence: Implications for models of crustal flow" class="work-thumbnail" src="https://attachments.academia-assets.com/118148711/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800051/Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow">Constraints on brittle field exhumation of the Everest-Makalu section of the Greater Himalayan Sequence: Implications for models of crustal flow</a></div><div class="wp-workCard_item"><span>Tectonics</span><span>, May 26, 2012</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Ba...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Barun, Arun, Dudh Kosi, and Kangshung valleys that drain the Everest and Makalu massifs cover a vertical sample transect of almost 8000 m of the Eastern Nepal Greater Himalayan Sequence (GHS). Apatite FT ages range from 0.9 AE 0.3 Ma to 3.1 AE 0.3 Ma in the GHS with ages increasing systematically with elevation. Apatite FT ages in the Everest Series and summit Ordovician limestones are much older, up to 30.5 AE 5.1 Ma. Zircon FT ages from the GHS range from 3.8 AE 0.4 Ma to 16.3 AE 0.8 Ma. The brittle exhumation rates calculated from these data show the GHS was exhumed, since $9 Ma, at an average rate of 1.0 AE 0.2 mm/a. Pliocene exhumation rates are higher at 1.7 AE 0.3 mm/a. These values are not significantly different from the estimate of ductile exhumation rates of 1.8 mm/a recorded by metamorphic minerals undergoing decompression between 18.7 and 15.6 Ma but are well below the values (up to 10 mm/a) used by thermomechanical models for ductile channel flow in the GHS. If representative of the GHS these models will therefore require further 'tuning'. Higher exhumation rates in the Pliocene have also been observed in other parts of the Himalaya and points to a regional cause, likely increased erosion due to the onset of late Pliocene-Pleistocene glaciation of the high Himalaya.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d583138cc3fcb61187a320524dc062d7" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148711,"asset_id":123800051,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148711/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800051"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800051"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800051; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800051]").text(description); $(".js-view-count[data-work-id=123800051]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800051; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800051']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d583138cc3fcb61187a320524dc062d7" } } $('.js-work-strip[data-work-id=123800051]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800051,"title":"Constraints on brittle field exhumation of the Everest-Makalu section of the Greater Himalayan Sequence: Implications for models of crustal flow","translated_title":"","metadata":{"publisher":"Wiley-Blackwell","grobid_abstract":"New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Barun, Arun, Dudh Kosi, and Kangshung valleys that drain the Everest and Makalu massifs cover a vertical sample transect of almost 8000 m of the Eastern Nepal Greater Himalayan Sequence (GHS). Apatite FT ages range from 0.9 AE 0.3 Ma to 3.1 AE 0.3 Ma in the GHS with ages increasing systematically with elevation. Apatite FT ages in the Everest Series and summit Ordovician limestones are much older, up to 30.5 AE 5.1 Ma. Zircon FT ages from the GHS range from 3.8 AE 0.4 Ma to 16.3 AE 0.8 Ma. The brittle exhumation rates calculated from these data show the GHS was exhumed, since $9 Ma, at an average rate of 1.0 AE 0.2 mm/a. Pliocene exhumation rates are higher at 1.7 AE 0.3 mm/a. These values are not significantly different from the estimate of ductile exhumation rates of 1.8 mm/a recorded by metamorphic minerals undergoing decompression between 18.7 and 15.6 Ma but are well below the values (up to 10 mm/a) used by thermomechanical models for ductile channel flow in the GHS. If representative of the GHS these models will therefore require further 'tuning'. Higher exhumation rates in the Pliocene have also been observed in other parts of the Himalaya and points to a regional cause, likely increased erosion due to the onset of late Pliocene-Pleistocene glaciation of the high Himalaya.","publication_date":{"day":26,"month":5,"year":2012,"errors":{}},"publication_name":"Tectonics","grobid_abstract_attachment_id":118148711},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800051/Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow","translated_internal_url":"","created_at":"2024-09-11T23:37:48.982-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148711,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148711/thumbnails/1.jpg","file_name":"2011tc00306220240912-1-t5ub90.pdf","download_url":"https://www.academia.edu/attachments/118148711/download_file","bulk_download_file_name":"Constraints_on_brittle_field_exhumation.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148711/2011tc00306220240912-1-t5ub90-libre.pdf?1726129241=\u0026response-content-disposition=attachment%3B+filename%3DConstraints_on_brittle_field_exhumation.pdf\u0026Expires=1742082500\u0026Signature=VK9suT4qABral6pO-F1Rz286tOmRHnnWz~fYueF1HD-EaEbuYZudmAHAZBG1ZAFN9HaJmyG1o84im4QF4cZUGAdJcrJTjonmK9LHXqCarn4gSlIkC1R2tOOq0AyEoV9sbsP8mRY3DoPFnM6kAn4IBnXkwXGDXbwS4j65HiHB1-Rei8UljMPB1WYN5eawhJt8Z92sJWFtLqPmzN8pk0AYH3FRxeKJPCegqciIiF6sRd8aHBB~K2AN6EWrTfGtS5tJCPxGF~FDav9IJhySUhzBkfS1furBfnlSfl3Zi4MbaOh9WX2IVc1hzfgr6XqHBN~ax30UN91FzKAN1wKaeWr29Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Constraints_on_brittle_field_exhumation_of_the_Everest_Makalu_section_of_the_Greater_Himalayan_Sequence_Implications_for_models_of_crustal_flow","translated_slug":"","page_count":13,"language":"en","content_type":"Work","summary":"New apatite and zircon fission track (FT) data from the summit slopes of Everest and along the Barun, Arun, Dudh Kosi, and Kangshung valleys that drain the Everest and Makalu massifs cover a vertical sample transect of almost 8000 m of the Eastern Nepal Greater Himalayan Sequence (GHS). Apatite FT ages range from 0.9 AE 0.3 Ma to 3.1 AE 0.3 Ma in the GHS with ages increasing systematically with elevation. Apatite FT ages in the Everest Series and summit Ordovician limestones are much older, up to 30.5 AE 5.1 Ma. Zircon FT ages from the GHS range from 3.8 AE 0.4 Ma to 16.3 AE 0.8 Ma. The brittle exhumation rates calculated from these data show the GHS was exhumed, since $9 Ma, at an average rate of 1.0 AE 0.2 mm/a. Pliocene exhumation rates are higher at 1.7 AE 0.3 mm/a. These values are not significantly different from the estimate of ductile exhumation rates of 1.8 mm/a recorded by metamorphic minerals undergoing decompression between 18.7 and 15.6 Ma but are well below the values (up to 10 mm/a) used by thermomechanical models for ductile channel flow in the GHS. If representative of the GHS these models will therefore require further 'tuning'. Higher exhumation rates in the Pliocene have also been observed in other parts of the Himalaya and points to a regional cause, likely increased erosion due to the onset of late Pliocene-Pleistocene glaciation of the high Himalaya.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148711,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148711/thumbnails/1.jpg","file_name":"2011tc00306220240912-1-t5ub90.pdf","download_url":"https://www.academia.edu/attachments/118148711/download_file","bulk_download_file_name":"Constraints_on_brittle_field_exhumation.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148711/2011tc00306220240912-1-t5ub90-libre.pdf?1726129241=\u0026response-content-disposition=attachment%3B+filename%3DConstraints_on_brittle_field_exhumation.pdf\u0026Expires=1742082500\u0026Signature=VK9suT4qABral6pO-F1Rz286tOmRHnnWz~fYueF1HD-EaEbuYZudmAHAZBG1ZAFN9HaJmyG1o84im4QF4cZUGAdJcrJTjonmK9LHXqCarn4gSlIkC1R2tOOq0AyEoV9sbsP8mRY3DoPFnM6kAn4IBnXkwXGDXbwS4j65HiHB1-Rei8UljMPB1WYN5eawhJt8Z92sJWFtLqPmzN8pk0AYH3FRxeKJPCegqciIiF6sRd8aHBB~K2AN6EWrTfGtS5tJCPxGF~FDav9IJhySUhzBkfS1furBfnlSfl3Zi4MbaOh9WX2IVc1hzfgr6XqHBN~ax30UN91FzKAN1wKaeWr29Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics"},{"id":13883,"name":"Seismology","url":"https://www.academia.edu/Documents/in/Seismology"},{"id":153407,"name":"Es","url":"https://www.academia.edu/Documents/in/Es"}],"urls":[{"id":44622246,"url":"https://agupubs.onlinelibrary.wiley.com/doi/pdfdirect/10.1029/2011TC003062"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800050"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800050/Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models"><img alt="Research paper thumbnail of Restoration of the Western Himalaya: implications for metamorphic protoliths, thrust and normal faulting, and channel flow models" class="work-thumbnail" src="https://attachments.academia-assets.com/118148684/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800050/Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models">Restoration of the Western Himalaya: implications for metamorphic protoliths, thrust and normal faulting, and channel flow models</a></div><div class="wp-workCard_item"><span>Episodes</span><span>, Dec 1, 2007</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic ro...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic rocks up to kyanite or sillimanite+K-feldspar grade, migmatites, layered stromatic migmatites and leucogranite sheets. These rocks were metamorphosed during the late Eocene to early Miocene, and are bounded below by a large-scale SW-vergent ductile shear zone-thrust fault (Main Central Thrust; MCT), and above by a NE-dipping low-angle normal sense shear zone and fault (Zanskar Shear Zone; ZSZ), part of the South Tibetan Detachment (STD) system. Restoration of the high-grade metamorphic rocks of the GHS reveals that protoliths are Proterozoic shales (Haimanta Group), Cambrian-Ordovician orthogneisses, Permian Panjal volcanics and Palaeozoic-Triassic/ Jurassic sedimentary rocks, lateral equivalent rocks of the adjacent unmetamorphosed Tethyan zone. Structural outliers of low-grade or unmetamorphosed rocks (e.g., Chamba syncline) have been mapped overlying high-grade (usually sillimanite grade) rocks of the GHS. The low-grade klippen are underlain by lowangle north-directed ductile shear zones and normal faults, that are interpreted here as earlier equivalents of the ZSZ. These low-angle normal faults formed during continuous NE-SW compression, crustal thickening and southwestward extrusion of the GHS slab along the footwall. STD normal faults propagated structurally upward (northeast) with time, whereas MCT reverse faults along the base of the GHS propagated structurally downward (southwest) with time. Inverted metamorphic isograds along the base of the slab (MCT zone) can be linked on the map with right way-up isograds along the footwall of the ZSZ normal fault at the top of the slab, demonstrating that the recumbently folded isograd model is a viable geometrical representation of the metamorphic structure of the GHS. Post-metamorphic shearing along the ZSZ and MCT has condensed the isograds by a combination of pure shear and simple shear. These observations support the Channel Flow model of ductile extrusion of a mid-crustal layer of Indian plate rocks during the Miocene, from beneath the passive roof stretching fault of the ZSZ.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="4ce327046c678ee814fb372b52107226" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148684,"asset_id":123800050,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148684/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800050"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800050"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800050; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800050]").text(description); $(".js-view-count[data-work-id=123800050]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800050; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800050']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "4ce327046c678ee814fb372b52107226" } } $('.js-work-strip[data-work-id=123800050]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800050,"title":"Restoration of the Western Himalaya: implications for metamorphic protoliths, thrust and normal faulting, and channel flow models","translated_title":"","metadata":{"publisher":"International Union of Geological Sciences","grobid_abstract":"The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic rocks up to kyanite or sillimanite+K-feldspar grade, migmatites, layered stromatic migmatites and leucogranite sheets. These rocks were metamorphosed during the late Eocene to early Miocene, and are bounded below by a large-scale SW-vergent ductile shear zone-thrust fault (Main Central Thrust; MCT), and above by a NE-dipping low-angle normal sense shear zone and fault (Zanskar Shear Zone; ZSZ), part of the South Tibetan Detachment (STD) system. Restoration of the high-grade metamorphic rocks of the GHS reveals that protoliths are Proterozoic shales (Haimanta Group), Cambrian-Ordovician orthogneisses, Permian Panjal volcanics and Palaeozoic-Triassic/ Jurassic sedimentary rocks, lateral equivalent rocks of the adjacent unmetamorphosed Tethyan zone. Structural outliers of low-grade or unmetamorphosed rocks (e.g., Chamba syncline) have been mapped overlying high-grade (usually sillimanite grade) rocks of the GHS. The low-grade klippen are underlain by lowangle north-directed ductile shear zones and normal faults, that are interpreted here as earlier equivalents of the ZSZ. These low-angle normal faults formed during continuous NE-SW compression, crustal thickening and southwestward extrusion of the GHS slab along the footwall. STD normal faults propagated structurally upward (northeast) with time, whereas MCT reverse faults along the base of the GHS propagated structurally downward (southwest) with time. Inverted metamorphic isograds along the base of the slab (MCT zone) can be linked on the map with right way-up isograds along the footwall of the ZSZ normal fault at the top of the slab, demonstrating that the recumbently folded isograd model is a viable geometrical representation of the metamorphic structure of the GHS. Post-metamorphic shearing along the ZSZ and MCT has condensed the isograds by a combination of pure shear and simple shear. These observations support the Channel Flow model of ductile extrusion of a mid-crustal layer of Indian plate rocks during the Miocene, from beneath the passive roof stretching fault of the ZSZ.","publication_date":{"day":1,"month":12,"year":2007,"errors":{}},"publication_name":"Episodes","grobid_abstract_attachment_id":118148684},"translated_abstract":null,"internal_url":"https://www.academia.edu/123800050/Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models","translated_internal_url":"","created_at":"2024-09-11T23:37:48.320-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":118148684,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148684/thumbnails/1.jpg","file_name":"download_pdf.pdf","download_url":"https://www.academia.edu/attachments/118148684/download_file","bulk_download_file_name":"Restoration_of_the_Western_Himalaya_impl.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148684/download_pdf-libre.pdf?1726129638=\u0026response-content-disposition=attachment%3B+filename%3DRestoration_of_the_Western_Himalaya_impl.pdf\u0026Expires=1742082500\u0026Signature=dYMzuakB6cL6wawkmg~AnjJf-Q76fVr1bpxjnV9FYI0kxwL~PCmf7yzAIK4g3Te4IcHlzuHS~BSQAMyJ3GsSn75bFxcYX3tLxKWr~ODUSwNW0Lzg~libVS6IjR0WOPNhARE0z4J2JFbjpOiJ3dq6AjnpzeU59u7Hj0fWwM17FJfD0Xf7us1fwzINSdV-OjZ1OCRsl1zjapz7-Rrc2dtBwcLbMht-kUi1kEE2loO7a3cUYHNmEHyUcKZ7p8tmMgN-3ob87U03qkdwi3K2m7Z~6510ZipkE~4Yxz-hzsP3T-p-iewr84W02NvMg~EP7wajXhAkWABfthiP7RRaWxIKwQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Restoration_of_the_Western_Himalaya_implications_for_metamorphic_protoliths_thrust_and_normal_faulting_and_channel_flow_models","translated_slug":"","page_count":16,"language":"en","content_type":"Work","summary":"The Greater Himalayan Sequence (GHS) is composed of a sequence of Barrovian facies metamorphic rocks up to kyanite or sillimanite+K-feldspar grade, migmatites, layered stromatic migmatites and leucogranite sheets. These rocks were metamorphosed during the late Eocene to early Miocene, and are bounded below by a large-scale SW-vergent ductile shear zone-thrust fault (Main Central Thrust; MCT), and above by a NE-dipping low-angle normal sense shear zone and fault (Zanskar Shear Zone; ZSZ), part of the South Tibetan Detachment (STD) system. Restoration of the high-grade metamorphic rocks of the GHS reveals that protoliths are Proterozoic shales (Haimanta Group), Cambrian-Ordovician orthogneisses, Permian Panjal volcanics and Palaeozoic-Triassic/ Jurassic sedimentary rocks, lateral equivalent rocks of the adjacent unmetamorphosed Tethyan zone. Structural outliers of low-grade or unmetamorphosed rocks (e.g., Chamba syncline) have been mapped overlying high-grade (usually sillimanite grade) rocks of the GHS. The low-grade klippen are underlain by lowangle north-directed ductile shear zones and normal faults, that are interpreted here as earlier equivalents of the ZSZ. These low-angle normal faults formed during continuous NE-SW compression, crustal thickening and southwestward extrusion of the GHS slab along the footwall. STD normal faults propagated structurally upward (northeast) with time, whereas MCT reverse faults along the base of the GHS propagated structurally downward (southwest) with time. Inverted metamorphic isograds along the base of the slab (MCT zone) can be linked on the map with right way-up isograds along the footwall of the ZSZ normal fault at the top of the slab, demonstrating that the recumbently folded isograd model is a viable geometrical representation of the metamorphic structure of the GHS. Post-metamorphic shearing along the ZSZ and MCT has condensed the isograds by a combination of pure shear and simple shear. These observations support the Channel Flow model of ductile extrusion of a mid-crustal layer of Indian plate rocks during the Miocene, from beneath the passive roof stretching fault of the ZSZ.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[{"id":118148684,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/118148684/thumbnails/1.jpg","file_name":"download_pdf.pdf","download_url":"https://www.academia.edu/attachments/118148684/download_file","bulk_download_file_name":"Restoration_of_the_Western_Himalaya_impl.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/118148684/download_pdf-libre.pdf?1726129638=\u0026response-content-disposition=attachment%3B+filename%3DRestoration_of_the_Western_Himalaya_impl.pdf\u0026Expires=1742082500\u0026Signature=dYMzuakB6cL6wawkmg~AnjJf-Q76fVr1bpxjnV9FYI0kxwL~PCmf7yzAIK4g3Te4IcHlzuHS~BSQAMyJ3GsSn75bFxcYX3tLxKWr~ODUSwNW0Lzg~libVS6IjR0WOPNhARE0z4J2JFbjpOiJ3dq6AjnpzeU59u7Hj0fWwM17FJfD0Xf7us1fwzINSdV-OjZ1OCRsl1zjapz7-Rrc2dtBwcLbMht-kUi1kEE2loO7a3cUYHNmEHyUcKZ7p8tmMgN-3ob87U03qkdwi3K2m7Z~6510ZipkE~4Yxz-hzsP3T-p-iewr84W02NvMg~EP7wajXhAkWABfthiP7RRaWxIKwQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":890009,"name":"Normal Fault","url":"https://www.academia.edu/Documents/in/Normal_Fault"},{"id":968099,"name":"Thrust","url":"https://www.academia.edu/Documents/in/Thrust"},{"id":2540869,"name":"Episodes","url":"https://www.academia.edu/Documents/in/Episodes"}],"urls":[{"id":44622245,"url":"http://www.episodes.org/journal/download_pdf.php?doi=10.18814/epiiugs/2007/v30i4/001"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800049"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800049/The_Age_of_the_Potassic_Alkaline_Igneous_Rocks_along_the_Ailao_Shan_Red_River_Shear_Zone_Implications_for_the_Onset_Age_of_Left_Lateral_Shearing_A_Discussion"><img alt="Research paper thumbnail of The Age of the Potassic Alkaline Igneous Rocks along the Ailao Shan–Red River Shear Zone: Implications for the Onset Age of Left‐Lateral Shearing: A Discussion" class="work-thumbnail" src="https://attachments.academia-assets.com/118148683/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800049/The_Age_of_the_Potassic_Alkaline_Igneous_Rocks_along_the_Ailao_Shan_Red_River_Shear_Zone_Implications_for_the_Onset_Age_of_Left_Lateral_Shearing_A_Discussion">The Age of the Potassic Alkaline Igneous Rocks along the Ailao Shan–Red River Shear Zone: Implications for the Onset Age of Left‐Lateral Shearing: A Discussion</a></div><div class="wp-workCard_item"><span>The Journal of Geology</span><span>, Mar 1, 2008</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Liang et al. (2007) reported new U-Pb zircon age data of 12 potassic alkaline intrusions along th...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Liang et al. (2007) reported new U-Pb zircon age data of 12 potassic alkaline intrusions along the Ailao Shan-Red River (ASRR) shear zone and concluded that the ages, ranging from 36.3 to 34.0 Ma, date the initiation of the ASRR left-lateral movement. 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Journal of Volcanology and Geothermal Research, 149, 177212.[CrossRef][ Web of Science][GeoRef]. ... 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Structural evolution of the High Himalayan Gneiss sequence, Langtang Valley, Nepal STEVEN...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Page 1. Structural evolution of the High Himalayan Gneiss sequence, Langtang Valley, Nepal STEVEN M. REDDY 1&amp;amp;#x27;3, MICHAEL P. SEARLE 2 &amp;amp;amp; JOHN A. MASSEY 1 1 Department of Earth Sciences, The Open University, Milton ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800036"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800036"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800036; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800036]").text(description); $(".js-view-count[data-work-id=123800036]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800036; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800036']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=123800036]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800036,"title":"Structural evolution of the High Himalayan Gneiss sequence, Langtang Valley, Nepal","translated_title":"","metadata":{"abstract":"Page 1. 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SR Noble Natural Environment Research Council Isotope Geosciences ...","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":1590367,"name":"Monazite","url":"https://www.academia.edu/Documents/in/Monazite"},{"id":1648287,"name":"Leucogranite","url":"https://www.academia.edu/Documents/in/Leucogranite"}],"urls":[{"id":44622236,"url":"https://doi.org/10.1130/0091-7613(1995)023%3C1135:aocmal%3E2.3.co;2"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800034"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800034/Contemporaneous_crust_derived_I_and_S_type_granite_magmatism_and_normal_faulting_on_Tinos_Delos_and_Naxos_Greece_Constraints_on_Aegean_orogenic_collapse"><img alt="Research paper thumbnail of Contemporaneous crust-derived I- and S-type granite magmatism and normal faulting on Tinos, Delos, and Naxos, Greece: Constraints on Aegean orogenic collapse" class="work-thumbnail" src="https://attachments.academia-assets.com/118148679/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800034/Contemporaneous_crust_derived_I_and_S_type_granite_magmatism_and_normal_faulting_on_Tinos_Delos_and_Naxos_Greece_Constraints_on_Aegean_orogenic_collapse">Contemporaneous crust-derived I- and S-type granite magmatism and normal faulting on Tinos, Delos, and Naxos, Greece: Constraints on Aegean orogenic collapse</a></div><div class="wp-workCard_item"><span>Geological Society of America Bulletin</span><span>, Feb 16, 2023</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Geochemical Sample Preparation and Methods All samples were thoroughly washed and cleaned then cr...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Geochemical Sample Preparation and Methods All samples were thoroughly washed and cleaned then crushed into a < 80-micron powder using a Jaw crusher, followed by running through a Tema Mill using an agate crucible to avoid contamination by tungsten carbide. The crucible was thoroughly cleaned and run through separately with in house sand and the resultant powder was then passed through an 80-micron sieve. Some of the resultant powders were then sent off to the Franklin and Marshall College, Pennsylvania, USA, for X-ray fluorescence by Dr Stanley Mertzman. The remaining powder was weighed and prepared for ICP-MS in house at the Department of Earth Sciences, University of Oxford. Full descriptions for each method are outlined below. X-Ray Fluorescence XRF was carried out by weighing 0.4000 ± 0.0001 grams of crushed rock powder and mixing with lithium tetraborate (3.6000 ± 0.0002 grams). The subsequent solution was then placed in a platinum crucible and heated with a meeker burner until molten. The molten material was transferred to a platinum casting dish and quenched. This procedure produced a glass disk that is used for XRF analysis of SiO 2, Al2O3, CaO, K2O, P2O5, TiO2, total iron reported as Fe2O3T, MnO, Na2O and MgO. Trace element analysis was achieved by weighing 7.0000 ± 0.0004 grams of whole rock powder and adding 1.4000±0.0002 of high purity copolywax powder. This was mixed for 10 minutes, and the powder was pressed into a briquette. Data are reported as parts per million (ppm) for Rb,</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="18f813b05e5b0750113a7b219591f419" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148679,"asset_id":123800034,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148679/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800034"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800034"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800034; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800034]").text(description); $(".js-view-count[data-work-id=123800034]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800034; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800034']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "18f813b05e5b0750113a7b219591f419" } } $('.js-work-strip[data-work-id=123800034]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800034,"title":"Contemporaneous crust-derived I- and S-type granite magmatism and normal faulting on Tinos, Delos, and Naxos, Greece: Constraints on Aegean orogenic collapse","translated_title":"","metadata":{"publisher":"Geological Society of America","grobid_abstract":"Geochemical Sample Preparation and Methods All samples were thoroughly washed and cleaned then crushed into a \u003c 80-micron powder using a Jaw crusher, followed by running through a Tema Mill using an agate crucible to avoid contamination by tungsten carbide. 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The crucible was thoroughly cleaned and run through separately with in house sand and the resultant powder was then passed through an 80-micron sieve. Some of the resultant powders were then sent off to the Franklin and Marshall College, Pennsylvania, USA, for X-ray fluorescence by Dr Stanley Mertzman. The remaining powder was weighed and prepared for ICP-MS in house at the Department of Earth Sciences, University of Oxford. Full descriptions for each method are outlined below. X-Ray Fluorescence XRF was carried out by weighing 0.4000 ± 0.0001 grams of crushed rock powder and mixing with lithium tetraborate (3.6000 ± 0.0002 grams). The subsequent solution was then placed in a platinum crucible and heated with a meeker burner until molten. The molten material was transferred to a platinum casting dish and quenched. This procedure produced a glass disk that is used for XRF analysis of SiO 2, Al2O3, CaO, K2O, P2O5, TiO2, total iron reported as Fe2O3T, MnO, Na2O and MgO. Trace element analysis was achieved by weighing 7.0000 ± 0.0004 grams of whole rock powder and adding 1.4000±0.0002 of high purity copolywax powder. This was mixed for 10 minutes, and the powder was pressed into a briquette. 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New geological mapping and U-Pb geochronology reveal the existence of the Gharam Chasma pluton, with implications for the thermal history and metamorphic events along the southern margin of the Asian plate. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800030"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800030/Structure_of_the_Jebel_Sumeini_Jebel_Ghawil_area_Northern_Oman"><img alt="Research paper thumbnail of Structure of the Jebel Sumeini-Jebel Ghawil area, Northern Oman" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Structure of the Jebel Sumeini-Jebel Ghawil area, Northern Oman</div><div class="wp-workCard_item"><span>Geological Society, London, Special Publications</span><span>, 1990</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">... 3) has a total thickness of about 2500 m and is divided into two for-mations, namely the Perm...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">... 3) has a total thickness of about 2500 m and is divided into two for-mations, namely the Permian to Triassic Maqam Formation, subdivided into Members A to F, and the Jurassic to Cretaceous Mayhah For-mation, subdivided into Members A to D (Glennie et al. ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800030"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800030"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800030; 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dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=123800030]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800030,"title":"Structure of the Jebel Sumeini-Jebel Ghawil area, Northern Oman","translated_title":"","metadata":{"abstract":"... 3) has a total thickness of about 2500 m and is divided into two for-mations, namely the Permian to Triassic Maqam Formation, subdivided into Members A to F, and the Jurassic to Cretaceous Mayhah For-mation, subdivided into Members A to D (Glennie et al. ...","publisher":"Geological Society of London","publication_date":{"day":null,"month":null,"year":1990,"errors":{}},"publication_name":"Geological Society, London, Special Publications"},"translated_abstract":"... 3) has a total thickness of about 2500 m and is divided into two for-mations, namely the Permian to Triassic Maqam Formation, subdivided into Members A to F, and the Jurassic to Cretaceous Mayhah For-mation, subdivided into Members A to D (Glennie et al. ...","internal_url":"https://www.academia.edu/123800030/Structure_of_the_Jebel_Sumeini_Jebel_Ghawil_area_Northern_Oman","translated_internal_url":"","created_at":"2024-09-11T23:37:35.080-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Structure_of_the_Jebel_Sumeini_Jebel_Ghawil_area_Northern_Oman","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"... 3) has a total thickness of about 2500 m and is divided into two for-mations, namely the Permian to Triassic Maqam Formation, subdivided into Members A to F, and the Jurassic to Cretaceous Mayhah For-mation, subdivided into Members A to D (Glennie et al. ...","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[],"research_interests":[{"id":261,"name":"Geography","url":"https://www.academia.edu/Documents/in/Geography"},{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"}],"urls":[{"id":44622232,"url":"https://doi.org/10.1144/gsl.sp.1992.049.01.22"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800029"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800029/Field_relations_petrogenesis_and_emplacement_of_the_Bhagirathi_leucogranite_Garhwal_Himalaya"><img alt="Research paper thumbnail of Field relations, petrogenesis and emplacement of the Bhagirathi leucogranite, Garhwal Himalaya" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Field relations, petrogenesis and emplacement of the Bhagirathi leucogranite, Garhwal Himalaya</div><div class="wp-workCard_item"><span>Geological Society, London, Special Publications</span><span>, 1993</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract: The Bhagirathi leucogranite forms a series of low-angle en echelon, lensoidal intrusion...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract: The Bhagirathi leucogranite forms a series of low-angle en echelon, lensoidal intrusions at the top of the High Himalayan slab in the central Himalaya of Garhwal, northern India. The leucogranite comprises the assemblage: K-feldspar + quartz + plagioclase + tourmaline + ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800029"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800029"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800029; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800029]").text(description); $(".js-view-count[data-work-id=123800029]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800029; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800029']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=123800029]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800029,"title":"Field relations, petrogenesis and emplacement of the Bhagirathi leucogranite, Garhwal Himalaya","translated_title":"","metadata":{"abstract":"Abstract: The Bhagirathi leucogranite forms a series of low-angle en echelon, lensoidal intrusions at the top of the High Himalayan slab in the central Himalaya of Garhwal, northern India. The leucogranite comprises the assemblage: K-feldspar + quartz + plagioclase + tourmaline + ...","publisher":"Geological Society of London","publication_date":{"day":null,"month":null,"year":1993,"errors":{}},"publication_name":"Geological Society, London, Special Publications"},"translated_abstract":"Abstract: The Bhagirathi leucogranite forms a series of low-angle en echelon, lensoidal intrusions at the top of the High Himalayan slab in the central Himalaya of Garhwal, northern India. The leucogranite comprises the assemblage: K-feldspar + quartz + plagioclase + tourmaline + ...","internal_url":"https://www.academia.edu/123800029/Field_relations_petrogenesis_and_emplacement_of_the_Bhagirathi_leucogranite_Garhwal_Himalaya","translated_internal_url":"","created_at":"2024-09-11T23:37:34.467-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Field_relations_petrogenesis_and_emplacement_of_the_Bhagirathi_leucogranite_Garhwal_Himalaya","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Abstract: The Bhagirathi leucogranite forms a series of low-angle en echelon, lensoidal intrusions at the top of the High Himalayan slab in the central Himalaya of Garhwal, northern India. The leucogranite comprises the assemblage: K-feldspar + quartz + plagioclase + tourmaline + ...","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":319882,"name":"Petrogenesis","url":"https://www.academia.edu/Documents/in/Petrogenesis"},{"id":926279,"name":"GEological Society of London","url":"https://www.academia.edu/Documents/in/GEological_Society_of_London"},{"id":1648287,"name":"Leucogranite","url":"https://www.academia.edu/Documents/in/Leucogranite"}],"urls":[{"id":44622231,"url":"https://doi.org/10.1144/gsl.sp.1993.074.01.29"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800028"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800028/The_Timing_of_Metamorphism_Magmatism_and_Cooling_in_the_Zanskar_Garhwal_and_Nepal_Himalaya"><img alt="Research paper thumbnail of The Timing of Metamorphism, Magmatism, and Cooling in the Zanskar, Garhwal, and Nepal Himalaya" class="work-thumbnail" src="https://attachments.academia-assets.com/118148708/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800028/The_Timing_of_Metamorphism_Magmatism_and_Cooling_in_the_Zanskar_Garhwal_and_Nepal_Himalaya">The Timing of Metamorphism, Magmatism, and Cooling in the Zanskar, Garhwal, and Nepal Himalaya</a></div><div class="wp-workCard_item"><span>Journal of Nepal Geological Society</span><span>, Dec 1, 1995</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="bd8b2534aa91b4cbaacd84af2a23316c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148708,"asset_id":123800028,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148708/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800028"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800028"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800028; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800028]").text(description); $(".js-view-count[data-work-id=123800028]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800028; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800028']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800027"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123800027/Spatial_and_Temporal_Distributions_of_Deformation_in_Strike_Slip_Faults_The_Karakoram_Fault_in_the_India_Asia_Collision_Zone"><img alt="Research paper thumbnail of Spatial and Temporal Distributions of Deformation in Strike-Slip Faults: The Karakoram Fault in the India-Asia Collision Zone" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Spatial and Temporal Distributions of Deformation in Strike-Slip Faults: The Karakoram Fault in the India-Asia Collision Zone</div><div class="wp-workCard_item"><span>Elsevier eBooks</span><span>, 2019</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract Assessments of spatial and temporal distributions of deformation within fault zones, inc...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract Assessments of spatial and temporal distributions of deformation within fault zones, including their ductile shear zones, are critical for characterizing wider deformation of the lithosphere and associated seismic hazard. However, deformation within fault zones, often quantified as slip rate or strain rate, is potentially heterogeneous in any of the three spatial dimensions (i.e., along strike, across strike, and with depth) and in time. The complex distributions of deformation that result present a challenge for assessments of the present and past behavior of individual faults and for establishing models of the roles of faults in deforming regions. In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. The KFZ offers a potential analog for other major strike-slip faults for which portions of this record (in space and/or time) may not be accessible.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800027"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800027"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800027; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800027]").text(description); $(".js-view-count[data-work-id=123800027]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800027; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800027']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=123800027]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800027,"title":"Spatial and Temporal Distributions of Deformation in Strike-Slip Faults: The Karakoram Fault in the India-Asia Collision Zone","translated_title":"","metadata":{"abstract":"Abstract Assessments of spatial and temporal distributions of deformation within fault zones, including their ductile shear zones, are critical for characterizing wider deformation of the lithosphere and associated seismic hazard. However, deformation within fault zones, often quantified as slip rate or strain rate, is potentially heterogeneous in any of the three spatial dimensions (i.e., along strike, across strike, and with depth) and in time. The complex distributions of deformation that result present a challenge for assessments of the present and past behavior of individual faults and for establishing models of the roles of faults in deforming regions. In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. 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In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. The KFZ offers a potential analog for other major strike-slip faults for which portions of this record (in space and/or time) may not be accessible.","internal_url":"https://www.academia.edu/123800027/Spatial_and_Temporal_Distributions_of_Deformation_in_Strike_Slip_Faults_The_Karakoram_Fault_in_the_India_Asia_Collision_Zone","translated_internal_url":"","created_at":"2024-09-11T23:37:32.976-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33871120,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Spatial_and_Temporal_Distributions_of_Deformation_in_Strike_Slip_Faults_The_Karakoram_Fault_in_the_India_Asia_Collision_Zone","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Abstract Assessments of spatial and temporal distributions of deformation within fault zones, including their ductile shear zones, are critical for characterizing wider deformation of the lithosphere and associated seismic hazard. However, deformation within fault zones, often quantified as slip rate or strain rate, is potentially heterogeneous in any of the three spatial dimensions (i.e., along strike, across strike, and with depth) and in time. The complex distributions of deformation that result present a challenge for assessments of the present and past behavior of individual faults and for establishing models of the roles of faults in deforming regions. In this review, we present a case study of the strike-slip Karakoram fault zone (KFZ) in the India-Asia collision zone to summarize evidence for the spatial and temporal distributions of deformation within the fault zone and highlight the challenges that heterogeneous deformation presents for constructing models of fault behavior at the present day and during the history of a deforming region. The KFZ provides an ideal case study because its fault rocks are exhumed and well exposed, and due to its key location within the collision zone. Geological, geomorphological, and geodetic observations constrain the behavior of the fault during the Neogene, Quaternary, and present day. Since initiating at ~ 15 Ma, the KFZ has accumulated strike-slip offsets that vary along its length from ~ 52 to ~ 150 km. Offset Quaternary landforms indicate spatial (along and across strike) and temporal heterogeneities in slip rate of several mm yr− 1. The upper-crustal portion of the fault generates large earthquakes with recurrence intervals of at least several hundred years, whereas deformation in the mid-crust is aseismic, ductile, and more broadly distributed. The KFZ offers a potential analog for other major strike-slip faults for which portions of this record (in space and/or time) may not be accessible.","owner":{"id":33871120,"first_name":"Michael","middle_initials":null,"last_name":"Searle","page_name":"MichaelSearle","domain_name":"oxford","created_at":"2015-08-12T23:13:19.721-07:00","display_name":"Michael Searle","url":"https://oxford.academia.edu/MichaelSearle"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":3157,"name":"Seismic Hazard","url":"https://www.academia.edu/Documents/in/Seismic_Hazard"},{"id":13883,"name":"Seismology","url":"https://www.academia.edu/Documents/in/Seismology"},{"id":284025,"name":"Shear Zone","url":"https://www.academia.edu/Documents/in/Shear_Zone"},{"id":897823,"name":"Elsevier","url":"https://www.academia.edu/Documents/in/Elsevier"},{"id":1208243,"name":"Strike Slip Tectonics","url":"https://www.academia.edu/Documents/in/Strike_Slip_Tectonics"}],"urls":[{"id":44622229,"url":"https://doi.org/10.1016/b978-0-12-812064-4.00011-6"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="123800026"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123800026/Age_and_petrogenesis_of_the_Lundy_granite_Paleocene_intraplate_peraluminous_magmatism_in_the_Bristol_Channel_UK"><img alt="Research paper thumbnail of Age and petrogenesis of the Lundy granite: Paleocene intraplate peraluminous magmatism in the Bristol Channel, UK" class="work-thumbnail" src="https://attachments.academia-assets.com/118148676/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123800026/Age_and_petrogenesis_of_the_Lundy_granite_Paleocene_intraplate_peraluminous_magmatism_in_the_Bristol_Channel_UK">Age and petrogenesis of the Lundy granite: Paleocene intraplate peraluminous magmatism in the Bristol Channel, UK</a></div><div class="wp-workCard_item"><span>Journal of the Geological Society</span><span>, Oct 2, 2017</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Lundy granite forms part of the Lundy Igneous Complex which is the southernmost substantive e...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Lundy granite forms part of the Lundy Igneous Complex which is the southernmost substantive expression of the British Cenozoic Igneous Province (BCIP). Its Qz+Pl+Kfs+Bt±Grt±Tpz 16 mineralogy and peraluminous character contrast with other BCIP granites farther north but are similar to the granites of the adjacent Early Permian Cornubian Batholith. We present the results of mapping, petrographical and mineral chemical analysis, and the first U-Pb zircon ages for the granite (59.8 ± 19 0.4-58.4 ± 0.4 Ma) and crosscutting basic dykes (57.2 ± 0.5 Ma) which confirm a Palaeocene age 20 for magmatism. Zircon inheritance is limited but two cores imply the presence of Lower Palaeozoic igneous rocks in the unexposed basement of SW England. The anomalous southerly location of the Lundy Igneous Complex is a consequence of mantle melting arising from the superposition of localised lithospheric extension, related to intraplate strike-slip tectonics, with the distal ancestral Icelandic plume. Granite generation primarily reflects crustal partial melting during the emplacement of mantle-derived melts. The change in geochemical character between the Lundy granite (peraluminous) and other BCIP granites (metaluminous / subalkaline) indicates a fundamental crustal source control between contrasting peri-Gondwanan and Laurentian basement provinces.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d76a0a3921c06e9b5f2edb06a89fc643" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":118148676,"asset_id":123800026,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/118148676/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123800026"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="123800026"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 123800026; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=123800026]").text(description); $(".js-view-count[data-work-id=123800026]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 123800026; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='123800026']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d76a0a3921c06e9b5f2edb06a89fc643" } } $('.js-work-strip[data-work-id=123800026]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":123800026,"title":"Age and petrogenesis of the Lundy granite: Paleocene intraplate peraluminous magmatism in the Bristol Channel, UK","translated_title":"","metadata":{"publisher":"Geological Society of London","grobid_abstract":"The Lundy granite forms part of the Lundy Igneous Complex which is the southernmost substantive expression of the British Cenozoic Igneous Province (BCIP). 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