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href="https://nhm.academia.edu/">Natural History Museum, London</a>, <a class="u-tcGrayDarker" href="https://nhm.academia.edu/Departments/Earth_Sciences/Documents">Earth Sciences</a>, <span class="u-tcGrayDarker">Research Leader</span></div></div></div></div><div class="sidebar-cta-container"><button class="ds2-5-button hidden profile-cta-button grow js-profile-follow-button" data-broccoli-component="user-info.follow-button" data-click-track="profile-user-info-follow-button" data-follow-user-fname="Reimar" data-follow-user-id="23017749" data-follow-user-source="profile_button" data-has-google="false"><span class="material-symbols-outlined" style="font-size: 20px" translate="no">add</span>Follow</button><button class="ds2-5-button hidden profile-cta-button grow js-profile-unfollow-button" data-broccoli-component="user-info.unfollow-button" data-click-track="profile-user-info-unfollow-button" data-unfollow-user-id="23017749"><span class="material-symbols-outlined" style="font-size: 20px" translate="no">done</span>Following</button></div></div><div class="user-stats-container"><a><div class="stat-container js-profile-followers"><p class="label">Followers</p><p class="data">115</p></div></a><a><div class="stat-container js-profile-followees" data-broccoli-component="user-info.followees-count" data-click-track="profile-expand-user-info-following"><p class="label">Following</p><p class="data">67</p></div></a><a><div class="stat-container js-profile-coauthors" data-broccoli-component="user-info.coauthors-count" data-click-track="profile-expand-user-info-coauthors"><p class="label">Co-authors</p><p class="data">32</p></div></a><span><div class="stat-container"><p class="label"><span class="js-profile-total-view-text">Public Views</span></p><p class="data"><span class="js-profile-view-count"></span></p></div></span></div><div class="user-bio-container"><div class="profile-bio fake-truncate js-profile-about" style="margin: 0px;"><b>Address: </b>London, United Kingdom<br /><div class="js-profile-less-about u-linkUnstyled u-tcGrayDarker u-textDecorationUnderline u-displayNone">less</div></div></div><div class="ri-section"><div class="ri-section-header"><span>Interests</span></div><div class="ri-tags-container"><a data-click-track="profile-user-info-expand-research-interests" data-has-card-for-ri-list="23017749" href="https://www.academia.edu/Documents/in/Structural_Geology"><div id="js-react-on-rails-context" style="display:none" data-rails-context="{"inMailer":false,"i18nLocale":"en","i18nDefaultLocale":"en","href":"https://nhm.academia.edu/ReimarSeltmann","location":"/ReimarSeltmann","scheme":"https","host":"nhm.academia.edu","port":null,"pathname":"/ReimarSeltmann","search":null,"httpAcceptLanguage":null,"serverSide":false}"></div> <div class="js-react-on-rails-component" style="display:none" data-component-name="Pill" data-props="{"color":"gray","children":["Structural Geology"]}" data-trace="false" 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id="social-redesign-work-container"><div class="upload-header"><h2 class="ds2-5-heading-sans-serif-xs">Uploads</h2></div><div class="nav-container backbone-profile-documents-nav hidden-xs"><ul class="nav-tablist" role="tablist"><li class="nav-chip active" role="presentation"><a data-section-name="" data-toggle="tab" href="#all" role="tab">all</a></li><li class="nav-chip" role="presentation"><a class="js-profile-docs-nav-section u-textTruncate" data-click-track="profile-works-tab" data-section-name="Papers" data-toggle="tab" href="#papers" role="tab" title="Papers"><span>312</span> <span class="ds2-5-body-sm-bold">Papers</span></a></li><li class="nav-chip" role="presentation"><a class="js-profile-docs-nav-section u-textTruncate" data-click-track="profile-works-tab" data-section-name="Conference-Presentations" data-toggle="tab" href="#conferencepresentations" role="tab" title="Conference Presentations"><span>1</span> <span class="ds2-5-body-sm-bold">Conference Presentations</span></a></li></ul></div><div class="divider ds-divider-16" style="margin: 0px;"></div><div class="documents-container backbone-social-profile-documents" style="width: 100%;"><div class="u-taCenter"></div><div class="profile--tab_content_container js-tab-pane tab-pane active" id="all"><div class="profile--tab_heading_container js-section-heading" data-section="Papers" id="Papers"><h3 class="profile--tab_heading_container">Papers by Reimar Seltmann</h3></div><div class="js-work-strip profile--work_container" data-work-id="121086946"><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/121086946/Conference_Reports"><img alt="Research paper thumbnail of Conference Reports" class="work-thumbnail" src="https://attachments.academia-assets.com/116060152/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item 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Die posttektonische nicht-foliierte Granitintrusion mit hohem lntrusionsniveau bei rund 2.000 m stellt einen Apikalbereich (\"Granitrücken\") des \"Mittelerzgebirgischen Teilplutons\" dar, der nach Ergebnissen von Gravimetrie und zahlreichen Explorationsbohrungen weiträumig das Gebiet E'dorf-Annaberg unterlagert. Die mehrphasige Sauberg-Subintrusion besteht aus hochfraktioniertem Alkalifeldspat Protolithionit-Granit mit starker spät-bis postmagmatischer Hochtemperatur Überprägung und charakteristischer F-Metasomatose. Im Endo-Kontaktbereich zu kambrischen Glimmergneisen treten stark wechselkörnige Randpegmatite mit aplitischen Bereichen auf (\"Stockscheider\"), im Exokontakt besteht ein nach dem Gefügebild fliessender Übergang von hydrothermal überprägten, mehrphasigen leukokraten Aplitgängen zu Sn-(W)-mineralisierten Quarzgängen. Schmelzeinschlüsse in Quarzen aus dem Stockscheider und Aplit-/Quarzgängen haben deutlich höhere Äquivalent-Wassergehalte als der experimentellen H 2 O Löslichkeit in einem haplogranitischen Niedrigdruck-System entsprechen und zeigen Solidus-Temperaturen bis \u003c 600°C. Vorläufige E-Mikrosondenanalysen belegen erhöhte Gehalte von F und P im %-Bereich. Die Viskosität der Schmelzen kann auf Werte von bis zu \u003c 1 o 2 Pa•s (bei 800°C) abgeschätzt werden und ist damit um Grössenordnungen niedriger als für normal-granitische Schmelze. Die untersuchten Granitproben haben peralumine Zusammensetzung und gehören zur Ilmenit-Serie (magnetische Suszeptibilitäten =50, 1 x 1 o-3 SI-Einheiten). Es handelt sich durchwegs um hochfraktionierte leukokrate low Ca Granite, wobei die lntrusionssequenz systematische Entwicklungstrends für Ta, Sn, W, F, Cs, U (Anreicherung), sowie Ti, Mg, Ca, Zr, Zr/Hf, }:SEE (Abreicherung) aufweist, und die Aplitgänge den höchsten Fraktionierungsgrad zeigen. Für die hydrothermal am geringsten mobilen Elementpaare lässt sich dabei fraktionierte Kristallisation als dominanter petrogenetischer Prozess definieren, während Streumuster für die meisten Elemente eine Überprägung im spät-oder postmagmatischen Bereich anzeigen. Insbesondere zeigt die ausgeprägte SEE-lnternfraktionierung (Tetraden Effekt) die Überprägung durch eine Komplexbildner-reiche Fluidphase bei hoher Temperatur. Dem hohen Fraktionierungsgrad entspricht auch die chemische Zusammensetzung der Glimmer-Komponente (Protolithionit), mit im Vergleich zur Erzgebirgs Granitsuite extrem niedrigen Ti-und Mg-Gehalten im 1000 bzw. 100 ppm-Bereich. Das Verteilungsmuster von o 18 O-und 6D-Werten von Protolithionit und kogenetischem Quarz macht für den Stockscheider eine primär-magmatische Fluidentwicklung ohne externen Beitrag wahrscheinlich. Die _konsistenten fN d-Werte von Stockscheider-Mineralen mit-17.6 ±0.6 (300 Ma) definieren ein paläoproterozoisches Edukt-Material (To M =","publication_date":{"day":null,"month":null,"year":1995,"errors":{}},"grobid_abstract_attachment_id":116060133},"translated_abstract":null,"internal_url":"https://www.academia.edu/121086944/Der_%C3%9Cbergangsbereich_Pegmatit_Aplit_in_Hydrothermal_Systeme_am_Beispiel_Ehrenfriedersdorf_Erzgebirge","translated_internal_url":"","created_at":"2024-06-16T06:02:23.188-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":116060133,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116060133/thumbnails/1.jpg","file_name":"content.pdf","download_url":"https://www.academia.edu/attachments/116060133/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Der_Ubergangsbereich_Pegmatit_Aplit_in_H.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116060133/content.pdf?1718542943=\u0026response-content-disposition=attachment%3B+filename%3DDer_Ubergangsbereich_Pegmatit_Aplit_in_H.pdf\u0026Expires=1732833586\u0026Signature=QaKm2-UvzmvXonlJoJoEQ4yTD3DWXVzfsuYENo-HlLYWZUvCCbQbyNpcmwJjg~sjcpfn5VPnnnxoSzM8tXIoSuXB4p2YeWZoUkDGtAqJ~TpP9Mbx96yAmyK9yjZ0Vk4FOKUxqDzyJUbK5sScMYZGmHCb1nz~PZRAXGUHnNwdVu~gW9No1SwRrYBEO9~aOtmjARCeKqIb-gqaUpXQmjgIRnoO6gn7pLJtC~6MkFW5Ew-ZgjYKHpCWHaA0BoZRHhRErUpoJiTYP1JwWs6y8LmNUgvnkEZwB~Dq7fK35yt7kDvBrFETDWcIc2M~2cs9e-LdxPXef7WsYVoyREvIbMXLKA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Der_Übergangsbereich_Pegmatit_Aplit_in_Hydrothermal_Systeme_am_Beispiel_Ehrenfriedersdorf_Erzgebirge","translated_slug":"","page_count":114,"language":"de","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[{"id":116060133,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116060133/thumbnails/1.jpg","file_name":"content.pdf","download_url":"https://www.academia.edu/attachments/116060133/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Der_Ubergangsbereich_Pegmatit_Aplit_in_H.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116060133/content.pdf?1718542943=\u0026response-content-disposition=attachment%3B+filename%3DDer_Ubergangsbereich_Pegmatit_Aplit_in_H.pdf\u0026Expires=1732833586\u0026Signature=QaKm2-UvzmvXonlJoJoEQ4yTD3DWXVzfsuYENo-HlLYWZUvCCbQbyNpcmwJjg~sjcpfn5VPnnnxoSzM8tXIoSuXB4p2YeWZoUkDGtAqJ~TpP9Mbx96yAmyK9yjZ0Vk4FOKUxqDzyJUbK5sScMYZGmHCb1nz~PZRAXGUHnNwdVu~gW9No1SwRrYBEO9~aOtmjARCeKqIb-gqaUpXQmjgIRnoO6gn7pLJtC~6MkFW5Ew-ZgjYKHpCWHaA0BoZRHhRErUpoJiTYP1JwWs6y8LmNUgvnkEZwB~Dq7fK35yt7kDvBrFETDWcIc2M~2cs9e-LdxPXef7WsYVoyREvIbMXLKA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"},{"id":116060134,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116060134/thumbnails/1.jpg","file_name":"content.pdf","download_url":"https://www.academia.edu/attachments/116060134/download_file","bulk_download_file_name":"Der_Ubergangsbereich_Pegmatit_Aplit_in_H.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116060134/content.pdf?1718542943=\u0026response-content-disposition=attachment%3B+filename%3DDer_Ubergangsbereich_Pegmatit_Aplit_in_H.pdf\u0026Expires=1732833586\u0026Signature=XvOBaV7L4nDKieLKid78W3ngFS-oPVrYZrNZgv7iUgeQsHqYun22x9IgnDtY2ROg6d5ot5kTzG4dGji6NFOvBYAoHPkT9kn2ygq0ZhscEGtKIoI2LPl-0QgVJ~VCD3srlI7k5yguxWdxar8Zlp5tE1SqIhzSv-nMHWoLFue41z6uhPtuqbM3E~VoNsxn2wBqL7vOmnczu0VvXL39bGE-koVuyjgBpSblFARFyfCe7jfoTfRScJnLA0DaKGgBZymqPVgTu3ugL0Kp94mgKGa4bfh-VTWDgFbP0j-Ub~PGGMZ2-lUHL5I7HdfbzdKhqKnVVPza7dGhaT-ednKKGhwaIw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[{"id":42978798,"url":"https://gfzpublic.gfz-potsdam.de/rest/items/item_229590_3/component/file_5006935/content"}]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="121086942"><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/121086942/Collisional_mafic_magmatism_of_the_fold_thrust_belts_framing_southern_Siberia_Western_Sangilen_southeastern_Tuva_"><img alt="Research paper thumbnail of Collisional mafic magmatism of the fold–thrust belts framing southern Siberia (Western Sangilen, southeastern Tuva)" class="work-thumbnail" src="https://attachments.academia-assets.com/116060150/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/121086942/Collisional_mafic_magmatism_of_the_fold_thrust_belts_framing_southern_Siberia_Western_Sangilen_southeastern_Tuva_">Collisional mafic magmatism of the fold–thrust belts framing southern Siberia (Western Sangilen, southeastern Tuva)</a></div><div class="wp-workCard_item"><span>Russian Geology and Geophysics</span><span>, 2018</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We consider geochemical features of mafic magmatism manifested during the evolution of a 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">We consider geochemical features of mafic magmatism manifested during the evolution of a complex nappe-folded structure in Western Sangilen, resulted from the Cambrian–Ordovician collisional tectogenesis. There are abundant ultramafic–mafic and mafic associations of different types in this region: layered low-Ti low-alkali ultramafic–mafic intrusions, high-Ti medium-alkali gabbroids, gabbro–monzodiorite intrusions, and alkali basalts. Isotope-geochronological data showed that these complexes formed over a wide time interval, from 570 to 440 Ma. At this time, the geodynamic setting in Western Sangilen changed from an island-arc one via a collision one to an intercontinental rift setting. At the early and late stages of the evolution of Western Sangilen, the geochemical features of mafites were typical of their geodynamic settings. The properties of mafites that formed synchronously with the collision are of particular interest. 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There are abundant ultramafic–mafic and mafic associations of different types in this region: layered low-Ti low-alkali ultramafic–mafic intrusions, high-Ti medium-alkali gabbroids, gabbro–monzodiorite intrusions, and alkali basalts. Isotope-geochronological data showed that these complexes formed over a wide time interval, from 570 to 440 Ma. At this time, the geodynamic setting in Western Sangilen changed from an island-arc one via a collision one to an intercontinental rift setting. At the early and late stages of the evolution of Western Sangilen, the geochemical features of mafites were typical of their geodynamic settings. The properties of mafites that formed synchronously with the collision are of particular interest. The studies have shown that the chemical composition of ...","publisher":"GeoScienceWorld","publication_date":{"day":null,"month":null,"year":2018,"errors":{}},"publication_name":"Russian Geology and Geophysics"},"translated_abstract":"We consider geochemical features of mafic magmatism manifested during the evolution of a complex nappe-folded structure in Western Sangilen, resulted from the Cambrian–Ordovician collisional tectogenesis. There are abundant ultramafic–mafic and mafic associations of different types in this region: layered low-Ti low-alkali ultramafic–mafic intrusions, high-Ti medium-alkali gabbroids, gabbro–monzodiorite intrusions, and alkali basalts. Isotope-geochronological data showed that these complexes formed over a wide time interval, from 570 to 440 Ma. At this time, the geodynamic setting in Western Sangilen changed from an island-arc one via a collision one to an intercontinental rift setting. 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It com prises a sub-nappe olistostrome in a collisional tec tonic set ting. The olistostrome con tains olistoliths and olistoplaques con tain ing parts of the mid-Pa leo zoic sed i men tary suc ces sions be long ing to the parautochthon and lower nappes of the north ern Bukantau-Kokshaal branch of the South ern Tian Shan nappe belt. The olistostrome ac cu mu lated ahead the ad vanc ing nappes in the foredeep ba sin that was filled with turbidities and de bris-flow de pos its (Tolubai Formathion). The parautochthon was partly dis mem bered into thrust lime stone sheets which dis in te grated and slid into uncon sol i dated sed i ments of the foredeep ba sin, form ing large lime stone olistoliths and olistoplaques. Olistoliths con tain ing shales and bed ded cherts were slid from the lower nappes. Tec tonic brec cias up to melange scale are pres ent in some olistoliths, sug gest ing tec tonic dis in te gra tion within the nappe pile and the sub se quent slid ing of the tectonized blocks into the olistostrome ba sin. Ore-bear ing si lici fied rocks (so-called \"jasperoids\") with an ti mony-mer cury and gold min er al iza tion are lo cated pre dom i nantly along the con tacts of the lime stone olistoliths/olistoplaques with a terrigenous ma trix.","publication_date":{"day":null,"month":null,"year":2012,"errors":{}},"publication_name":"Doklady Earth Sciences","grobid_abstract_attachment_id":116060151},"translated_abstract":null,"internal_url":"https://www.academia.edu/121086940/Structures_of_the_late_palaeozoic_thrust_belt_in_the_Chinese_South_Tian_Shan","translated_internal_url":"","created_at":"2024-06-16T06:02:21.364-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":116060151,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116060151/thumbnails/1.jpg","file_name":"pdf.pdf","download_url":"https://www.academia.edu/attachments/116060151/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Structures_of_the_late_palaeozoic_thrust.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116060151/pdf-libre.pdf?1718549001=\u0026response-content-disposition=attachment%3B+filename%3DStructures_of_the_late_palaeozoic_thrust.pdf\u0026Expires=1732833586\u0026Signature=JmAKgjrrqg6vNsVWifQqmGxby3dqL6o2bLLKi5SQU4ys13WujFVDW5u0H5D2HVuz30nZ7HRe-N6Xcs9zjJuwLjJh9liULAzv48iWc00ZJCTqBX56soOknPjyrA0xOTVbGrPKiYXAsTwORVn8hPUnqPSAICwOXM4swuQ7DtTsGAwXeJtR89cJ3RGdX~OQnIMq4VKrC-H5panO16gu4C3wPwwHeVbLjyi7HU7BOapfIZouGEIeBvkemH~gvyZvB-TeNFHgU8VQS~aZrcnoKoYu0Qd6bpSnFrRq7vt4W9mHoT4ndC9~yWx9RLlAUOHmd6HGLt8R3CLT2XzmQ5ez6isfmw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Structures_of_the_late_palaeozoic_thrust_belt_in_the_Chinese_South_Tian_Shan","translated_slug":"","page_count":17,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[{"id":116060151,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116060151/thumbnails/1.jpg","file_name":"pdf.pdf","download_url":"https://www.academia.edu/attachments/116060151/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Structures_of_the_late_palaeozoic_thrust.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116060151/pdf-libre.pdf?1718549001=\u0026response-content-disposition=attachment%3B+filename%3DStructures_of_the_late_palaeozoic_thrust.pdf\u0026Expires=1732833586\u0026Signature=JmAKgjrrqg6vNsVWifQqmGxby3dqL6o2bLLKi5SQU4ys13WujFVDW5u0H5D2HVuz30nZ7HRe-N6Xcs9zjJuwLjJh9liULAzv48iWc00ZJCTqBX56soOknPjyrA0xOTVbGrPKiYXAsTwORVn8hPUnqPSAICwOXM4swuQ7DtTsGAwXeJtR89cJ3RGdX~OQnIMq4VKrC-H5panO16gu4C3wPwwHeVbLjyi7HU7BOapfIZouGEIeBvkemH~gvyZvB-TeNFHgU8VQS~aZrcnoKoYu0Qd6bpSnFrRq7vt4W9mHoT4ndC9~yWx9RLlAUOHmd6HGLt8R3CLT2XzmQ5ez6isfmw__\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":76748,"name":"Devonian","url":"https://www.academia.edu/Documents/in/Devonian"},{"id":79166,"name":"Ordovician","url":"https://www.academia.edu/Documents/in/Ordovician"},{"id":96185,"name":"Carboniferous","url":"https://www.academia.edu/Documents/in/Carboniferous"},{"id":101506,"name":"Permian","url":"https://www.academia.edu/Documents/in/Permian"},{"id":171492,"name":"Paleozoic","url":"https://www.academia.edu/Documents/in/Paleozoic"},{"id":968099,"name":"Thrust","url":"https://www.academia.edu/Documents/in/Thrust"}],"urls":[{"id":42978796,"url":"http://link.springer.com/content/pdf/10.1134/S1028334X12010060.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="115346706"><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/115346706/Multiple_stages_of_Au_mobilization_in_the_Changshagou_Au_deposit_Eastern_Tianshan_NW_China_insights_from_mineral_chemistry_and_fluid_inclusions"><img alt="Research paper thumbnail of Multiple stages of Au mobilization in the Changshagou Au deposit, Eastern Tianshan, NW China: insights from mineral chemistry and fluid inclusions" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/115346706/Multiple_stages_of_Au_mobilization_in_the_Changshagou_Au_deposit_Eastern_Tianshan_NW_China_insights_from_mineral_chemistry_and_fluid_inclusions">Multiple stages of Au mobilization in the Changshagou Au deposit, Eastern Tianshan, NW China: insights from mineral chemistry and fluid inclusions</a></div><div class="wp-workCard_item"><span>Journal of Asian Earth Sciences</span><span>, Jun 1, 2023</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="115346706"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="115346706"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 115346706; 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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="115346705"><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/115346705/Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting"><img alt="Research paper thumbnail of Late Carboniferous – Early Permian mafic dikes and granitoids in the heart of the Western Tianshan Orogen, NW China: Implications for a tectonic transition from a syn- to post-collisional setting" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/115346705/Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting">Late Carboniferous – Early Permian mafic dikes and granitoids in the heart of the Western Tianshan Orogen, NW China: Implications for a tectonic transition from a syn- to post-collisional setting</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, Nov 1, 2021</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in the Late Carboniferous to Early Permian magmatic rocks of the Awulale Mountains. However, the orogen&#39;s tectono-magmatic evolution remains controversial. In particular, two contrasting genetic models have been proposed, i.e., post-collisional extension vs. mantle plume. Here, we report zircon U-Pb ages, whole-rock geochemical data and Nd-Hf isotopic data from the mafic dikes and granitoids of the western Awulale Mountains. These data better constrain the rock&#39;s petrogenesis and geodynamic processes following the amalgamation of the Tianshan Orogen. In combination with previous data, we have identified two magmatic episodes in the Awulale Mountains. The Late Carboniferous (ca. 319–307 Ma) episode emplaced the mafic gabbro dikes and intermediate-acidic granitoids with I-type and adakitic affinity. The latest Carboniferous-Permian (ca. 302–286 Ma) episode emplaced bimodal intrusions containing mafic diabase dikes, acidic adakite and I- and A-type granites. Mafic dikes and granitoids of both episodes show depleted whole-rock Nd and zircon Hf isotopic compositions (eNd(t): +2.21 ~ +7.54, eHf(t): +6.48 ~ +15.97), indicating a juvenile magmatic source. However, the mafic dikes have variable geochemical features that clearly suggest their derivation from two distinct mantle sources during the two magmatic episodes. The earlier gabbro dikes have lower Th/Yb (0.08–0.12) and Zr/Yb ratios (15.32–25.45) that resemble a normal mid-ocean ridge basalt (N-MORB) from a depleted mantle source. In contrast, the later diabase dikes show enrichment in the light rare earth elements (LREE) with relatively higher Th/Yb (0.22–0.86) and Zr/Yb ratios (38.05–68.97) that are similar to an enriched mid-ocean ridge basalt (E-MORB) mantle source. Also, the Nb/Ta ratios from the earlier adakitic granitoids (21.26–23.28) differ markedly from the later acidic adakites (0.41–19.50), which implies the transition from a thicker to a thinner crust. Integrating our results with the previous geological records, leads us to propose a two-stage tectonic model for the Chinese western Tianshan Orogen&#39;s transition from syn- to post-collision. The Late Carboniferous stage of magmatism was triggered by the break-off of the North Tianshan Oceanic slab as the Yili Block and Junggar Terrane collided. The subsequent latest Carboniferous-Permian stage followed the switch to a post-collisional setting with delamination of the thickened lower crust and the intrusion of voluminous lithospheric mantle-induced bimodal magmatism.</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="115346705"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="115346705"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 115346705; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=115346705]").text(description); $(".js-view-count[data-work-id=115346705]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 115346705; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='115346705']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 115346705, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=115346705]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":115346705,"title":"Late Carboniferous – Early Permian mafic dikes and granitoids in the heart of the Western Tianshan Orogen, NW China: Implications for a tectonic transition from a syn- to post-collisional setting","translated_title":"","metadata":{"abstract":"Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in the Late Carboniferous to Early Permian magmatic rocks of the Awulale Mountains. However, the orogen\u0026#39;s tectono-magmatic evolution remains controversial. In particular, two contrasting genetic models have been proposed, i.e., post-collisional extension vs. mantle plume. Here, we report zircon U-Pb ages, whole-rock geochemical data and Nd-Hf isotopic data from the mafic dikes and granitoids of the western Awulale Mountains. These data better constrain the rock\u0026#39;s petrogenesis and geodynamic processes following the amalgamation of the Tianshan Orogen. In combination with previous data, we have identified two magmatic episodes in the Awulale Mountains. The Late Carboniferous (ca. 319–307 Ma) episode emplaced the mafic gabbro dikes and intermediate-acidic granitoids with I-type and adakitic affinity. The latest Carboniferous-Permian (ca. 302–286 Ma) episode emplaced bimodal intrusions containing mafic diabase dikes, acidic adakite and I- and A-type granites. Mafic dikes and granitoids of both episodes show depleted whole-rock Nd and zircon Hf isotopic compositions (eNd(t): +2.21 ~ +7.54, eHf(t): +6.48 ~ +15.97), indicating a juvenile magmatic source. However, the mafic dikes have variable geochemical features that clearly suggest their derivation from two distinct mantle sources during the two magmatic episodes. The earlier gabbro dikes have lower Th/Yb (0.08–0.12) and Zr/Yb ratios (15.32–25.45) that resemble a normal mid-ocean ridge basalt (N-MORB) from a depleted mantle source. In contrast, the later diabase dikes show enrichment in the light rare earth elements (LREE) with relatively higher Th/Yb (0.22–0.86) and Zr/Yb ratios (38.05–68.97) that are similar to an enriched mid-ocean ridge basalt (E-MORB) mantle source. Also, the Nb/Ta ratios from the earlier adakitic granitoids (21.26–23.28) differ markedly from the later acidic adakites (0.41–19.50), which implies the transition from a thicker to a thinner crust. Integrating our results with the previous geological records, leads us to propose a two-stage tectonic model for the Chinese western Tianshan Orogen\u0026#39;s transition from syn- to post-collision. The Late Carboniferous stage of magmatism was triggered by the break-off of the North Tianshan Oceanic slab as the Yili Block and Junggar Terrane collided. The subsequent latest Carboniferous-Permian stage followed the switch to a post-collisional setting with delamination of the thickened lower crust and the intrusion of voluminous lithospheric mantle-induced bimodal magmatism.","publisher":"Elsevier BV","publication_date":{"day":1,"month":11,"year":2021,"errors":{}},"publication_name":"Lithos"},"translated_abstract":"Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in the Late Carboniferous to Early Permian magmatic rocks of the Awulale Mountains. However, the orogen\u0026#39;s tectono-magmatic evolution remains controversial. In particular, two contrasting genetic models have been proposed, i.e., post-collisional extension vs. mantle plume. Here, we report zircon U-Pb ages, whole-rock geochemical data and Nd-Hf isotopic data from the mafic dikes and granitoids of the western Awulale Mountains. These data better constrain the rock\u0026#39;s petrogenesis and geodynamic processes following the amalgamation of the Tianshan Orogen. In combination with previous data, we have identified two magmatic episodes in the Awulale Mountains. The Late Carboniferous (ca. 319–307 Ma) episode emplaced the mafic gabbro dikes and intermediate-acidic granitoids with I-type and adakitic affinity. The latest Carboniferous-Permian (ca. 302–286 Ma) episode emplaced bimodal intrusions containing mafic diabase dikes, acidic adakite and I- and A-type granites. Mafic dikes and granitoids of both episodes show depleted whole-rock Nd and zircon Hf isotopic compositions (eNd(t): +2.21 ~ +7.54, eHf(t): +6.48 ~ +15.97), indicating a juvenile magmatic source. However, the mafic dikes have variable geochemical features that clearly suggest their derivation from two distinct mantle sources during the two magmatic episodes. The earlier gabbro dikes have lower Th/Yb (0.08–0.12) and Zr/Yb ratios (15.32–25.45) that resemble a normal mid-ocean ridge basalt (N-MORB) from a depleted mantle source. In contrast, the later diabase dikes show enrichment in the light rare earth elements (LREE) with relatively higher Th/Yb (0.22–0.86) and Zr/Yb ratios (38.05–68.97) that are similar to an enriched mid-ocean ridge basalt (E-MORB) mantle source. Also, the Nb/Ta ratios from the earlier adakitic granitoids (21.26–23.28) differ markedly from the later acidic adakites (0.41–19.50), which implies the transition from a thicker to a thinner crust. Integrating our results with the previous geological records, leads us to propose a two-stage tectonic model for the Chinese western Tianshan Orogen\u0026#39;s transition from syn- to post-collision. The Late Carboniferous stage of magmatism was triggered by the break-off of the North Tianshan Oceanic slab as the Yili Block and Junggar Terrane collided. The subsequent latest Carboniferous-Permian stage followed the switch to a post-collisional setting with delamination of the thickened lower crust and the intrusion of voluminous lithospheric mantle-induced bimodal magmatism.","internal_url":"https://www.academia.edu/115346705/Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting","translated_internal_url":"","created_at":"2024-02-24T04:43:57.527-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":96185,"name":"Carboniferous","url":"https://www.academia.edu/Documents/in/Carboniferous"},{"id":135982,"name":"Rodinia","url":"https://www.academia.edu/Documents/in/Rodinia"},{"id":197587,"name":"Dike","url":"https://www.academia.edu/Documents/in/Dike"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":319882,"name":"Petrogenesis","url":"https://www.academia.edu/Documents/in/Petrogenesis"},{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"}],"urls":[{"id":39753585,"url":"https://doi.org/10.1016/j.lithos.2021.106417"}]}, dispatcherData: dispatcherData }); 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Igneous intrusions in this deposit consist of barren diorite porphyry (U-Pb zircon age of 232.0 ± 2.0 Ma) and ore-bearing quartz diorite and pyroxene diorite (U-Pb zircon ages of 223.3 ± 1.5 and 224.6 ± 2.9 Ma, respectively). Whole-rock major and trace element and accessory mineral (zircon and apatite) composition from these intrusions are studied to examine the different geochemical characteristics of orebearing and barren intrusions. Compared to the barren diorite porphyry, the ore-bearing intrusions have higher Ce 4+ /Ce 3+ ratios of zircon and lower Mn contents of apatite, indicating higher oxidation state. Besides, apatite from the ore-bearing intrusions shows higher Cl contents and lower F/Cl ratios. These characteristics collectively suggest the higher productivity of ore-bearing quartz diorite and pyroxene diorite. When compared with ore-bearing intrusions from global porphyry Cu deposits, those from Cu-Pb-Zn skarn deposits display lower Ce 4+ /Ce 3+ and Eu N /Eu N * ratios of zircon and lower Cl and higher F/Cl ratios of apatite. We conclude that these differences reflect a general geochemical feature, and that zircon and apatite composition is a sensitive tool to infer economic potential of magmas and the resulting mineralization types in intrusion-related exploration targets.","publication_date":{"day":28,"month":12,"year":2017,"errors":{}},"publication_name":"Mineralium Deposita","grobid_abstract_attachment_id":111780766},"translated_abstract":null,"internal_url":"https://www.academia.edu/115346703/Geochemical_contrasts_between_Late_Triassic_ore_bearing_and_barren_intrusions_in_the_Weibao_Cu_Pb_Zn_deposit_East_Kunlun_Mountains_NW_China_constraints_from_accessory_minerals_zircon_and_apatite_","translated_internal_url":"","created_at":"2024-02-24T04:43:56.728-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":111780766,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780766/thumbnails/1.jpg","file_name":"s00126-017-0787-8.pdf","download_url":"https://www.academia.edu/attachments/111780766/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_contrasts_between_Late_Trias.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780766/s00126-017-0787-8-libre.pdf?1708779224=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_contrasts_between_Late_Trias.pdf\u0026Expires=1732833586\u0026Signature=Jvyd-S8kMmjwOyktFGwWZys3vYalC-4~wo5~8qTrJ~FifLufhzyH8bAzVxH9hmj~TERvcvNOh31sqGXleNTV6LKuW9-0IHZOwU~H4F8jLY8IHRXRno6~m0A6MgTyosbnYGyjbanczHyRj7QH5MUTSmjwpdcuUeY5XyUM5M-FA3ug9-P392la3OqogNIqbd0hddNmew7752vfGgvUGeX2JW8gsKJ8tolXQPNYUZIEkJoZemcJaExCaVvVqlFQWbV-BLc8m2Ota4qj4OsnkxYBtmr-Mo9GrqFDR3MyrMrwVt0gE5RPB7zJjV6PbJNWAGhuoC79vn14Usa8fq2o9xWNhg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Geochemical_contrasts_between_Late_Triassic_ore_bearing_and_barren_intrusions_in_the_Weibao_Cu_Pb_Zn_deposit_East_Kunlun_Mountains_NW_China_constraints_from_accessory_minerals_zircon_and_apatite_","translated_slug":"","page_count":16,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[{"id":111780766,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780766/thumbnails/1.jpg","file_name":"s00126-017-0787-8.pdf","download_url":"https://www.academia.edu/attachments/111780766/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_contrasts_between_Late_Trias.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780766/s00126-017-0787-8-libre.pdf?1708779224=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_contrasts_between_Late_Trias.pdf\u0026Expires=1732833586\u0026Signature=Jvyd-S8kMmjwOyktFGwWZys3vYalC-4~wo5~8qTrJ~FifLufhzyH8bAzVxH9hmj~TERvcvNOh31sqGXleNTV6LKuW9-0IHZOwU~H4F8jLY8IHRXRno6~m0A6MgTyosbnYGyjbanczHyRj7QH5MUTSmjwpdcuUeY5XyUM5M-FA3ug9-P392la3OqogNIqbd0hddNmew7752vfGgvUGeX2JW8gsKJ8tolXQPNYUZIEkJoZemcJaExCaVvVqlFQWbV-BLc8m2Ota4qj4OsnkxYBtmr-Mo9GrqFDR3MyrMrwVt0gE5RPB7zJjV6PbJNWAGhuoC79vn14Usa8fq2o9xWNhg__\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":205587,"name":"Apatite","url":"https://www.academia.edu/Documents/in/Apatite"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"}],"urls":[{"id":39753583,"url":"https://doi.org/10.1007/s00126-017-0787-8"}]}, dispatcherData: dispatcherData }); 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The magnitude of the zircon Ce anomaly has been traditionally described by Ce/Ce*, where Ce* is the theoretical Ce value derived from a chondrite-normalized rare earth element (REE) pattern. More recently, the Ce 4+ /Ce 3+ method based on the lattice strain model has been proposed, since the latter method does not need La and Pr contents for zircon, both of which are commonly below the limit of detection and susceptible to contamination from melt/mineral inclusions. In this contribution we show that the Ce 4+ /Ce 3+ method is confronted with some problems in practice and should be further improved. In contrast, by reexamining chondrite-normalized REE patterns of zircon, we find that Ce* can be estimated according to a logarithmic function curve without involvement of La and Pr contents. Application of this new method to zircon data from 11 giant to supergiant porphyry Cu deposits suggests this revised method as a more valid measure in evaluating magmatic oxidation state. The revised Ce/Ce* method is of particular importance for analyses where the provenance of the analyzed zircon is unknown or in question, since the method does not require knowledge of the melt composition.","publication_date":{"day":29,"month":8,"year":2019,"errors":{}},"publication_name":"Mineralogy and Petrology","grobid_abstract_attachment_id":111780764},"translated_abstract":null,"internal_url":"https://www.academia.edu/115346702/Characterization_of_the_zircon_Ce_anomaly_for_estimation_of_oxidation_state_of_magmas_a_revised_Ce_Ce_method","translated_internal_url":"","created_at":"2024-02-24T04:43:56.054-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":111780764,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780764/thumbnails/1.jpg","file_name":"s00710-019-00682-y.pdf","download_url":"https://www.academia.edu/attachments/111780764/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Characterization_of_the_zircon_Ce_anomal.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780764/s00710-019-00682-y-libre.pdf?1708779221=\u0026response-content-disposition=attachment%3B+filename%3DCharacterization_of_the_zircon_Ce_anomal.pdf\u0026Expires=1732833586\u0026Signature=diNdVw6yQ4Q0loS8RZ9Qs3UxAUTLYJ8TQDgF5jBDCzu47N51WK9hWQjCwYX53pYo2p1fY8MpHvM~m-e41T1WDdKOImYZgWK4FkjXsOcB5QTKIFNpNg5Nl1UCqIPyDu8qiITUCAPVAijHF-v2m3W~t5~MAdRezPPz3n7eBu~81TkwFWXjkCtS5DFbqmcz0xpHYtnlKUdiFilo9WYQ--48aHMsI0KcjsQEKFW5HHxpW277eCx25VMhTY3roVBshC0ueFdY8-AJ1G6hYBODSZLSU5z-5k7Ox4B9cPYZSsL2G6CRl9vsbBKBzUnkKlDLy8azSmGJbdXh7VwWuYnlXXxWsQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Characterization_of_the_zircon_Ce_anomaly_for_estimation_of_oxidation_state_of_magmas_a_revised_Ce_Ce_method","translated_slug":"","page_count":9,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[{"id":111780764,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780764/thumbnails/1.jpg","file_name":"s00710-019-00682-y.pdf","download_url":"https://www.academia.edu/attachments/111780764/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Characterization_of_the_zircon_Ce_anomal.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780764/s00710-019-00682-y-libre.pdf?1708779221=\u0026response-content-disposition=attachment%3B+filename%3DCharacterization_of_the_zircon_Ce_anomal.pdf\u0026Expires=1732833586\u0026Signature=diNdVw6yQ4Q0loS8RZ9Qs3UxAUTLYJ8TQDgF5jBDCzu47N51WK9hWQjCwYX53pYo2p1fY8MpHvM~m-e41T1WDdKOImYZgWK4FkjXsOcB5QTKIFNpNg5Nl1UCqIPyDu8qiITUCAPVAijHF-v2m3W~t5~MAdRezPPz3n7eBu~81TkwFWXjkCtS5DFbqmcz0xpHYtnlKUdiFilo9WYQ--48aHMsI0KcjsQEKFW5HHxpW277eCx25VMhTY3roVBshC0ueFdY8-AJ1G6hYBODSZLSU5z-5k7Ox4B9cPYZSsL2G6CRl9vsbBKBzUnkKlDLy8azSmGJbdXh7VwWuYnlXXxWsQ__\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":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":517272,"name":"Mineralogy and Petrology","url":"https://www.academia.edu/Documents/in/Mineralogy_and_Petrology"}],"urls":[{"id":39753582,"url":"https://doi.org/10.1007/s00710-019-00682-y"}]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="115346696"><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/115346696/Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China"><img alt="Research paper thumbnail of Unraveling the link between mantle upwelling and formation of Sn-bearing granitic rocks in the world-class Dachang tin district, South China" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/115346696/Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China">Unraveling the link between mantle upwelling and formation of Sn-bearing granitic rocks in the world-class Dachang tin district, South China</a></div><div class="wp-workCard_item"><span>Geological Society of America Bulletin</span><span>, Jun 21, 2021</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing gran...</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">Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing granites worldwide. However, the specific role of mantle in the formation of tin granites and related mineralization remains poorly understood. In the world-class Dachang district, South China, tin mineralization is related to the Longxianggai equigranular/porphyritic biotite granites and tin orebodies are cut by granite porphyry dykes hosting mafic microgranular enclaves (MMEs). A combination of zircon U-Pb dating and Hf-O isotopes, mineral chemistry, and whole-rock elemental and Sr-Nd isotopic compositions—for granitic rocks and MMEs, is employed to constrain the petrogenesis and to unravel the link between tin fertility and mantle upwelling. Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) zircon U-Pb dating indicates that the biotite granites were emplaced at ca. 93 Ma, and the granite porphyry dykes and MMEs were formed at ca. 86 Ma. The biotite granites are silica- and alkali-enriched with A/CNK ratios of 1.04–1.36, and exhibit elevated concentrations of Li, F, P, Rb, Cs, Ta, Sn, W, and U, showing affinities with highly fractionated S-type granites. Whole-rock geochemical and Nd isotopic (εNd(t) = −10.0 to −7.8) data, and in situ zircon Hf-O (εHf(t) = −9.9 to −3.9, δ18O = 6.2–8.9‰) isotopes indicate that the biotite granites were formed by partial melting of metasedimentary rocks at relatively high temperatures (≥782 °C), possibly with minor input of mantle material. Likewise, the post-ore granite porphyry dykes have similar chemical and mineralogical characteristics as fractionated S-type granites. Zircon Hf-O isotopes (εHf(t) = −9.0 to −4.9, δ18O = 6.5–8.2‰) and whole-rock geochemical data suggest they were derived from a similar source as the biotite granites, whereas elevated εNd(t) values of −5.0 to −3.3 for granite porphyry dykes relative to biotite granites reveal an increasing mantle input. Distinct εNd(t) (−0.4 and −0.3) and zircon Hf-O (εHf(t) = 1.5–5.0, δ18O = 6.5–7.2‰) isotopes of the MMEs, suggest that the mafic melt could be sourced from the asthenospheric mantle, contaminated by subcontinental lithospheric mantle/continental crust during magma ascent, and hybridized by felsic melt at emplacement-level. The magmatic sequence in the Dachang district is indicative of an extensional tectonic setting where mantle-derived magmas are predicted to migrate to shallower crustal levels as the crust progressively becomes thinner and hotter. High-temperature partial melting of mature metasedimentary crust triggered by heat input from the upwelled mantle, may contribute to biotite breakdown, which is important for concentrating tin in melts. Fractional crystallization of initially Sn-rich felsic melts under reduced conditions makes further tin enrichment and produces Sn-bearing granites (the Longxianggai pluton). Prolonged mantle upwelling results in distinct magma mixing and the formation of granite porphyry dykes and MMEs. These dykes are highly fractionated with elevated Sn and W contents, which show great potential to form hydrothermal Sn-W mineralization.</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="115346696"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="115346696"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 115346696; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=115346696]").text(description); $(".js-view-count[data-work-id=115346696]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 115346696; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='115346696']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 115346696, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=115346696]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":115346696,"title":"Unraveling the link between mantle upwelling and formation of Sn-bearing granitic rocks in the world-class Dachang tin district, South China","translated_title":"","metadata":{"abstract":"Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing granites worldwide. However, the specific role of mantle in the formation of tin granites and related mineralization remains poorly understood. In the world-class Dachang district, South China, tin mineralization is related to the Longxianggai equigranular/porphyritic biotite granites and tin orebodies are cut by granite porphyry dykes hosting mafic microgranular enclaves (MMEs). A combination of zircon U-Pb dating and Hf-O isotopes, mineral chemistry, and whole-rock elemental and Sr-Nd isotopic compositions—for granitic rocks and MMEs, is employed to constrain the petrogenesis and to unravel the link between tin fertility and mantle upwelling. Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) zircon U-Pb dating indicates that the biotite granites were emplaced at ca. 93 Ma, and the granite porphyry dykes and MMEs were formed at ca. 86 Ma. The biotite granites are silica- and alkali-enriched with A/CNK ratios of 1.04–1.36, and exhibit elevated concentrations of Li, F, P, Rb, Cs, Ta, Sn, W, and U, showing affinities with highly fractionated S-type granites. Whole-rock geochemical and Nd isotopic (εNd(t) = −10.0 to −7.8) data, and in situ zircon Hf-O (εHf(t) = −9.9 to −3.9, δ18O = 6.2–8.9‰) isotopes indicate that the biotite granites were formed by partial melting of metasedimentary rocks at relatively high temperatures (≥782 °C), possibly with minor input of mantle material. Likewise, the post-ore granite porphyry dykes have similar chemical and mineralogical characteristics as fractionated S-type granites. Zircon Hf-O isotopes (εHf(t) = −9.0 to −4.9, δ18O = 6.5–8.2‰) and whole-rock geochemical data suggest they were derived from a similar source as the biotite granites, whereas elevated εNd(t) values of −5.0 to −3.3 for granite porphyry dykes relative to biotite granites reveal an increasing mantle input. Distinct εNd(t) (−0.4 and −0.3) and zircon Hf-O (εHf(t) = 1.5–5.0, δ18O = 6.5–7.2‰) isotopes of the MMEs, suggest that the mafic melt could be sourced from the asthenospheric mantle, contaminated by subcontinental lithospheric mantle/continental crust during magma ascent, and hybridized by felsic melt at emplacement-level. The magmatic sequence in the Dachang district is indicative of an extensional tectonic setting where mantle-derived magmas are predicted to migrate to shallower crustal levels as the crust progressively becomes thinner and hotter. High-temperature partial melting of mature metasedimentary crust triggered by heat input from the upwelled mantle, may contribute to biotite breakdown, which is important for concentrating tin in melts. Fractional crystallization of initially Sn-rich felsic melts under reduced conditions makes further tin enrichment and produces Sn-bearing granites (the Longxianggai pluton). Prolonged mantle upwelling results in distinct magma mixing and the formation of granite porphyry dykes and MMEs. These dykes are highly fractionated with elevated Sn and W contents, which show great potential to form hydrothermal Sn-W mineralization.","publisher":"Geological Society of America","publication_date":{"day":21,"month":6,"year":2021,"errors":{}},"publication_name":"Geological Society of America Bulletin"},"translated_abstract":"Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing granites worldwide. However, the specific role of mantle in the formation of tin granites and related mineralization remains poorly understood. In the world-class Dachang district, South China, tin mineralization is related to the Longxianggai equigranular/porphyritic biotite granites and tin orebodies are cut by granite porphyry dykes hosting mafic microgranular enclaves (MMEs). A combination of zircon U-Pb dating and Hf-O isotopes, mineral chemistry, and whole-rock elemental and Sr-Nd isotopic compositions—for granitic rocks and MMEs, is employed to constrain the petrogenesis and to unravel the link between tin fertility and mantle upwelling. Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) zircon U-Pb dating indicates that the biotite granites were emplaced at ca. 93 Ma, and the granite porphyry dykes and MMEs were formed at ca. 86 Ma. The biotite granites are silica- and alkali-enriched with A/CNK ratios of 1.04–1.36, and exhibit elevated concentrations of Li, F, P, Rb, Cs, Ta, Sn, W, and U, showing affinities with highly fractionated S-type granites. Whole-rock geochemical and Nd isotopic (εNd(t) = −10.0 to −7.8) data, and in situ zircon Hf-O (εHf(t) = −9.9 to −3.9, δ18O = 6.2–8.9‰) isotopes indicate that the biotite granites were formed by partial melting of metasedimentary rocks at relatively high temperatures (≥782 °C), possibly with minor input of mantle material. Likewise, the post-ore granite porphyry dykes have similar chemical and mineralogical characteristics as fractionated S-type granites. Zircon Hf-O isotopes (εHf(t) = −9.0 to −4.9, δ18O = 6.5–8.2‰) and whole-rock geochemical data suggest they were derived from a similar source as the biotite granites, whereas elevated εNd(t) values of −5.0 to −3.3 for granite porphyry dykes relative to biotite granites reveal an increasing mantle input. Distinct εNd(t) (−0.4 and −0.3) and zircon Hf-O (εHf(t) = 1.5–5.0, δ18O = 6.5–7.2‰) isotopes of the MMEs, suggest that the mafic melt could be sourced from the asthenospheric mantle, contaminated by subcontinental lithospheric mantle/continental crust during magma ascent, and hybridized by felsic melt at emplacement-level. The magmatic sequence in the Dachang district is indicative of an extensional tectonic setting where mantle-derived magmas are predicted to migrate to shallower crustal levels as the crust progressively becomes thinner and hotter. High-temperature partial melting of mature metasedimentary crust triggered by heat input from the upwelled mantle, may contribute to biotite breakdown, which is important for concentrating tin in melts. Fractional crystallization of initially Sn-rich felsic melts under reduced conditions makes further tin enrichment and produces Sn-bearing granites (the Longxianggai pluton). Prolonged mantle upwelling results in distinct magma mixing and the formation of granite porphyry dykes and MMEs. These dykes are highly fractionated with elevated Sn and W contents, which show great potential to form hydrothermal Sn-W mineralization.","internal_url":"https://www.academia.edu/115346696/Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China","translated_internal_url":"","created_at":"2024-02-24T04:43:54.400-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":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":456199,"name":"Biotite","url":"https://www.academia.edu/Documents/in/Biotite"}],"urls":[{"id":39753576,"url":"https://doi.org/10.1130/b35492.1"}]}, dispatcherData: dispatcherData }); 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Die posttektonische nicht-foliierte Granitintrusion mit hohem lntrusionsniveau bei rund 2.000 m stellt einen Apikalbereich (\"Granitrücken\") des \"Mittelerzgebirgischen Teilplutons\" dar, der nach Ergebnissen von Gravimetrie und zahlreichen Explorationsbohrungen weiträumig das Gebiet E'dorf-Annaberg unterlagert. Die mehrphasige Sauberg-Subintrusion besteht aus hochfraktioniertem Alkalifeldspat Protolithionit-Granit mit starker spät-bis postmagmatischer Hochtemperatur Überprägung und charakteristischer F-Metasomatose. Im Endo-Kontaktbereich zu kambrischen Glimmergneisen treten stark wechselkörnige Randpegmatite mit aplitischen Bereichen auf (\"Stockscheider\"), im Exokontakt besteht ein nach dem Gefügebild fliessender Übergang von hydrothermal überprägten, mehrphasigen leukokraten Aplitgängen zu Sn-(W)-mineralisierten Quarzgängen. Schmelzeinschlüsse in Quarzen aus dem Stockscheider und Aplit-/Quarzgängen haben deutlich höhere Äquivalent-Wassergehalte als der experimentellen H 2 O Löslichkeit in einem haplogranitischen Niedrigdruck-System entsprechen und zeigen Solidus-Temperaturen bis \u003c 600°C. Vorläufige E-Mikrosondenanalysen belegen erhöhte Gehalte von F und P im %-Bereich. Die Viskosität der Schmelzen kann auf Werte von bis zu \u003c 1 o 2 Pa•s (bei 800°C) abgeschätzt werden und ist damit um Grössenordnungen niedriger als für normal-granitische Schmelze. Die untersuchten Granitproben haben peralumine Zusammensetzung und gehören zur Ilmenit-Serie (magnetische Suszeptibilitäten =50, 1 x 1 o-3 SI-Einheiten). Es handelt sich durchwegs um hochfraktionierte leukokrate low Ca Granite, wobei die lntrusionssequenz systematische Entwicklungstrends für Ta, Sn, W, F, Cs, U (Anreicherung), sowie Ti, Mg, Ca, Zr, Zr/Hf, }:SEE (Abreicherung) aufweist, und die Aplitgänge den höchsten Fraktionierungsgrad zeigen. Für die hydrothermal am geringsten mobilen Elementpaare lässt sich dabei fraktionierte Kristallisation als dominanter petrogenetischer Prozess definieren, während Streumuster für die meisten Elemente eine Überprägung im spät-oder postmagmatischen Bereich anzeigen. Insbesondere zeigt die ausgeprägte SEE-lnternfraktionierung (Tetraden Effekt) die Überprägung durch eine Komplexbildner-reiche Fluidphase bei hoher Temperatur. Dem hohen Fraktionierungsgrad entspricht auch die chemische Zusammensetzung der Glimmer-Komponente (Protolithionit), mit im Vergleich zur Erzgebirgs Granitsuite extrem niedrigen Ti-und Mg-Gehalten im 1000 bzw. 100 ppm-Bereich. Das Verteilungsmuster von o 18 O-und 6D-Werten von Protolithionit und kogenetischem Quarz macht für den Stockscheider eine primär-magmatische Fluidentwicklung ohne externen Beitrag wahrscheinlich. 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There are abundant ultramafic–mafic and mafic associations of different types in this region: layered low-Ti low-alkali ultramafic–mafic intrusions, high-Ti medium-alkali gabbroids, gabbro–monzodiorite intrusions, and alkali basalts. Isotope-geochronological data showed that these complexes formed over a wide time interval, from 570 to 440 Ma. At this time, the geodynamic setting in Western Sangilen changed from an island-arc one via a collision one to an intercontinental rift setting. At the early and late stages of the evolution of Western Sangilen, the geochemical features of mafites were typical of their geodynamic settings. The properties of mafites that formed synchronously with the collision are of particular interest. 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There are abundant ultramafic–mafic and mafic associations of different types in this region: layered low-Ti low-alkali ultramafic–mafic intrusions, high-Ti medium-alkali gabbroids, gabbro–monzodiorite intrusions, and alkali basalts. Isotope-geochronological data showed that these complexes formed over a wide time interval, from 570 to 440 Ma. At this time, the geodynamic setting in Western Sangilen changed from an island-arc one via a collision one to an intercontinental rift setting. At the early and late stages of the evolution of Western Sangilen, the geochemical features of mafites were typical of their geodynamic settings. The properties of mafites that formed synchronously with the collision are of particular interest. The studies have shown that the chemical composition of ...","publisher":"GeoScienceWorld","publication_date":{"day":null,"month":null,"year":2018,"errors":{}},"publication_name":"Russian Geology and Geophysics"},"translated_abstract":"We consider geochemical features of mafic magmatism manifested during the evolution of a complex nappe-folded structure in Western Sangilen, resulted from the Cambrian–Ordovician collisional tectogenesis. There are abundant ultramafic–mafic and mafic associations of different types in this region: layered low-Ti low-alkali ultramafic–mafic intrusions, high-Ti medium-alkali gabbroids, gabbro–monzodiorite intrusions, and alkali basalts. Isotope-geochronological data showed that these complexes formed over a wide time interval, from 570 to 440 Ma. At this time, the geodynamic setting in Western Sangilen changed from an island-arc one via a collision one to an intercontinental rift setting. At the early and late stages of the evolution of Western Sangilen, the geochemical features of mafites were typical of their geodynamic settings. The properties of mafites that formed synchronously with the collision are of particular interest. 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It com prises a sub-nappe olistostrome in a collisional tec tonic set ting. The olistostrome con tains olistoliths and olistoplaques con tain ing parts of the mid-Pa leo zoic sed i men tary suc ces sions be long ing to the parautochthon and lower nappes of the north ern Bukantau-Kokshaal branch of the South ern Tian Shan nappe belt. The olistostrome ac cu mu lated ahead the ad vanc ing nappes in the foredeep ba sin that was filled with turbidities and de bris-flow de pos its (Tolubai Formathion). The parautochthon was partly dis mem bered into thrust lime stone sheets which dis in te grated and slid into uncon sol i dated sed i ments of the foredeep ba sin, form ing large lime stone olistoliths and olistoplaques. Olistoliths con tain ing shales and bed ded cherts were slid from the lower nappes. Tec tonic brec cias up to melange scale are pres ent in some olistoliths, sug gest ing tec tonic dis in te gra tion within the nappe pile and the sub se quent slid ing of the tectonized blocks into the olistostrome ba sin. Ore-bear ing si lici fied rocks (so-called \"jasperoids\") with an ti mony-mer cury and gold min er al iza tion are lo cated pre dom i nantly along the con tacts of the lime stone olistoliths/olistoplaques with a terrigenous ma trix.","publication_date":{"day":null,"month":null,"year":2012,"errors":{}},"publication_name":"Doklady Earth Sciences","grobid_abstract_attachment_id":116060151},"translated_abstract":null,"internal_url":"https://www.academia.edu/121086940/Structures_of_the_late_palaeozoic_thrust_belt_in_the_Chinese_South_Tian_Shan","translated_internal_url":"","created_at":"2024-06-16T06:02:21.364-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":116060151,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116060151/thumbnails/1.jpg","file_name":"pdf.pdf","download_url":"https://www.academia.edu/attachments/116060151/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Structures_of_the_late_palaeozoic_thrust.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116060151/pdf-libre.pdf?1718549001=\u0026response-content-disposition=attachment%3B+filename%3DStructures_of_the_late_palaeozoic_thrust.pdf\u0026Expires=1732833586\u0026Signature=JmAKgjrrqg6vNsVWifQqmGxby3dqL6o2bLLKi5SQU4ys13WujFVDW5u0H5D2HVuz30nZ7HRe-N6Xcs9zjJuwLjJh9liULAzv48iWc00ZJCTqBX56soOknPjyrA0xOTVbGrPKiYXAsTwORVn8hPUnqPSAICwOXM4swuQ7DtTsGAwXeJtR89cJ3RGdX~OQnIMq4VKrC-H5panO16gu4C3wPwwHeVbLjyi7HU7BOapfIZouGEIeBvkemH~gvyZvB-TeNFHgU8VQS~aZrcnoKoYu0Qd6bpSnFrRq7vt4W9mHoT4ndC9~yWx9RLlAUOHmd6HGLt8R3CLT2XzmQ5ez6isfmw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Structures_of_the_late_palaeozoic_thrust_belt_in_the_Chinese_South_Tian_Shan","translated_slug":"","page_count":17,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[{"id":116060151,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/116060151/thumbnails/1.jpg","file_name":"pdf.pdf","download_url":"https://www.academia.edu/attachments/116060151/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Structures_of_the_late_palaeozoic_thrust.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/116060151/pdf-libre.pdf?1718549001=\u0026response-content-disposition=attachment%3B+filename%3DStructures_of_the_late_palaeozoic_thrust.pdf\u0026Expires=1732833586\u0026Signature=JmAKgjrrqg6vNsVWifQqmGxby3dqL6o2bLLKi5SQU4ys13WujFVDW5u0H5D2HVuz30nZ7HRe-N6Xcs9zjJuwLjJh9liULAzv48iWc00ZJCTqBX56soOknPjyrA0xOTVbGrPKiYXAsTwORVn8hPUnqPSAICwOXM4swuQ7DtTsGAwXeJtR89cJ3RGdX~OQnIMq4VKrC-H5panO16gu4C3wPwwHeVbLjyi7HU7BOapfIZouGEIeBvkemH~gvyZvB-TeNFHgU8VQS~aZrcnoKoYu0Qd6bpSnFrRq7vt4W9mHoT4ndC9~yWx9RLlAUOHmd6HGLt8R3CLT2XzmQ5ez6isfmw__\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":76748,"name":"Devonian","url":"https://www.academia.edu/Documents/in/Devonian"},{"id":79166,"name":"Ordovician","url":"https://www.academia.edu/Documents/in/Ordovician"},{"id":96185,"name":"Carboniferous","url":"https://www.academia.edu/Documents/in/Carboniferous"},{"id":101506,"name":"Permian","url":"https://www.academia.edu/Documents/in/Permian"},{"id":171492,"name":"Paleozoic","url":"https://www.academia.edu/Documents/in/Paleozoic"},{"id":968099,"name":"Thrust","url":"https://www.academia.edu/Documents/in/Thrust"}],"urls":[{"id":42978796,"url":"http://link.springer.com/content/pdf/10.1134/S1028334X12010060.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="115346706"><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/115346706/Multiple_stages_of_Au_mobilization_in_the_Changshagou_Au_deposit_Eastern_Tianshan_NW_China_insights_from_mineral_chemistry_and_fluid_inclusions"><img alt="Research paper thumbnail of Multiple stages of Au mobilization in the Changshagou Au deposit, Eastern Tianshan, NW China: insights from mineral chemistry and fluid inclusions" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/115346706/Multiple_stages_of_Au_mobilization_in_the_Changshagou_Au_deposit_Eastern_Tianshan_NW_China_insights_from_mineral_chemistry_and_fluid_inclusions">Multiple stages of Au mobilization in the Changshagou Au deposit, Eastern Tianshan, NW China: insights from mineral chemistry and fluid inclusions</a></div><div class="wp-workCard_item"><span>Journal of Asian Earth Sciences</span><span>, Jun 1, 2023</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="115346706"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="115346706"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 115346706; 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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="115346705"><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/115346705/Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting"><img alt="Research paper thumbnail of Late Carboniferous – Early Permian mafic dikes and granitoids in the heart of the Western Tianshan Orogen, NW China: Implications for a tectonic transition from a syn- to post-collisional setting" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/115346705/Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting">Late Carboniferous – Early Permian mafic dikes and granitoids in the heart of the Western Tianshan Orogen, NW China: Implications for a tectonic transition from a syn- to post-collisional setting</a></div><div class="wp-workCard_item"><span>Lithos</span><span>, Nov 1, 2021</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in the Late Carboniferous to Early Permian magmatic rocks of the Awulale Mountains. However, the orogen&#39;s tectono-magmatic evolution remains controversial. In particular, two contrasting genetic models have been proposed, i.e., post-collisional extension vs. mantle plume. Here, we report zircon U-Pb ages, whole-rock geochemical data and Nd-Hf isotopic data from the mafic dikes and granitoids of the western Awulale Mountains. These data better constrain the rock&#39;s petrogenesis and geodynamic processes following the amalgamation of the Tianshan Orogen. In combination with previous data, we have identified two magmatic episodes in the Awulale Mountains. The Late Carboniferous (ca. 319–307 Ma) episode emplaced the mafic gabbro dikes and intermediate-acidic granitoids with I-type and adakitic affinity. The latest Carboniferous-Permian (ca. 302–286 Ma) episode emplaced bimodal intrusions containing mafic diabase dikes, acidic adakite and I- and A-type granites. Mafic dikes and granitoids of both episodes show depleted whole-rock Nd and zircon Hf isotopic compositions (eNd(t): +2.21 ~ +7.54, eHf(t): +6.48 ~ +15.97), indicating a juvenile magmatic source. However, the mafic dikes have variable geochemical features that clearly suggest their derivation from two distinct mantle sources during the two magmatic episodes. The earlier gabbro dikes have lower Th/Yb (0.08–0.12) and Zr/Yb ratios (15.32–25.45) that resemble a normal mid-ocean ridge basalt (N-MORB) from a depleted mantle source. In contrast, the later diabase dikes show enrichment in the light rare earth elements (LREE) with relatively higher Th/Yb (0.22–0.86) and Zr/Yb ratios (38.05–68.97) that are similar to an enriched mid-ocean ridge basalt (E-MORB) mantle source. Also, the Nb/Ta ratios from the earlier adakitic granitoids (21.26–23.28) differ markedly from the later acidic adakites (0.41–19.50), which implies the transition from a thicker to a thinner crust. Integrating our results with the previous geological records, leads us to propose a two-stage tectonic model for the Chinese western Tianshan Orogen&#39;s transition from syn- to post-collision. The Late Carboniferous stage of magmatism was triggered by the break-off of the North Tianshan Oceanic slab as the Yili Block and Junggar Terrane collided. The subsequent latest Carboniferous-Permian stage followed the switch to a post-collisional setting with delamination of the thickened lower crust and the intrusion of voluminous lithospheric mantle-induced bimodal magmatism.</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="115346705"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="115346705"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 115346705; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=115346705]").text(description); $(".js-view-count[data-work-id=115346705]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 115346705; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='115346705']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 115346705, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=115346705]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":115346705,"title":"Late Carboniferous – Early Permian mafic dikes and granitoids in the heart of the Western Tianshan Orogen, NW China: Implications for a tectonic transition from a syn- to post-collisional setting","translated_title":"","metadata":{"abstract":"Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in the Late Carboniferous to Early Permian magmatic rocks of the Awulale Mountains. However, the orogen\u0026#39;s tectono-magmatic evolution remains controversial. In particular, two contrasting genetic models have been proposed, i.e., post-collisional extension vs. mantle plume. Here, we report zircon U-Pb ages, whole-rock geochemical data and Nd-Hf isotopic data from the mafic dikes and granitoids of the western Awulale Mountains. These data better constrain the rock\u0026#39;s petrogenesis and geodynamic processes following the amalgamation of the Tianshan Orogen. In combination with previous data, we have identified two magmatic episodes in the Awulale Mountains. The Late Carboniferous (ca. 319–307 Ma) episode emplaced the mafic gabbro dikes and intermediate-acidic granitoids with I-type and adakitic affinity. The latest Carboniferous-Permian (ca. 302–286 Ma) episode emplaced bimodal intrusions containing mafic diabase dikes, acidic adakite and I- and A-type granites. Mafic dikes and granitoids of both episodes show depleted whole-rock Nd and zircon Hf isotopic compositions (eNd(t): +2.21 ~ +7.54, eHf(t): +6.48 ~ +15.97), indicating a juvenile magmatic source. However, the mafic dikes have variable geochemical features that clearly suggest their derivation from two distinct mantle sources during the two magmatic episodes. The earlier gabbro dikes have lower Th/Yb (0.08–0.12) and Zr/Yb ratios (15.32–25.45) that resemble a normal mid-ocean ridge basalt (N-MORB) from a depleted mantle source. In contrast, the later diabase dikes show enrichment in the light rare earth elements (LREE) with relatively higher Th/Yb (0.22–0.86) and Zr/Yb ratios (38.05–68.97) that are similar to an enriched mid-ocean ridge basalt (E-MORB) mantle source. Also, the Nb/Ta ratios from the earlier adakitic granitoids (21.26–23.28) differ markedly from the later acidic adakites (0.41–19.50), which implies the transition from a thicker to a thinner crust. Integrating our results with the previous geological records, leads us to propose a two-stage tectonic model for the Chinese western Tianshan Orogen\u0026#39;s transition from syn- to post-collision. The Late Carboniferous stage of magmatism was triggered by the break-off of the North Tianshan Oceanic slab as the Yili Block and Junggar Terrane collided. The subsequent latest Carboniferous-Permian stage followed the switch to a post-collisional setting with delamination of the thickened lower crust and the intrusion of voluminous lithospheric mantle-induced bimodal magmatism.","publisher":"Elsevier BV","publication_date":{"day":1,"month":11,"year":2021,"errors":{}},"publication_name":"Lithos"},"translated_abstract":"Abstract Syn- to post-collisional magmatism in the Chinese western Tianshan Orogen is recorded in the Late Carboniferous to Early Permian magmatic rocks of the Awulale Mountains. However, the orogen\u0026#39;s tectono-magmatic evolution remains controversial. In particular, two contrasting genetic models have been proposed, i.e., post-collisional extension vs. mantle plume. Here, we report zircon U-Pb ages, whole-rock geochemical data and Nd-Hf isotopic data from the mafic dikes and granitoids of the western Awulale Mountains. These data better constrain the rock\u0026#39;s petrogenesis and geodynamic processes following the amalgamation of the Tianshan Orogen. In combination with previous data, we have identified two magmatic episodes in the Awulale Mountains. The Late Carboniferous (ca. 319–307 Ma) episode emplaced the mafic gabbro dikes and intermediate-acidic granitoids with I-type and adakitic affinity. The latest Carboniferous-Permian (ca. 302–286 Ma) episode emplaced bimodal intrusions containing mafic diabase dikes, acidic adakite and I- and A-type granites. Mafic dikes and granitoids of both episodes show depleted whole-rock Nd and zircon Hf isotopic compositions (eNd(t): +2.21 ~ +7.54, eHf(t): +6.48 ~ +15.97), indicating a juvenile magmatic source. However, the mafic dikes have variable geochemical features that clearly suggest their derivation from two distinct mantle sources during the two magmatic episodes. The earlier gabbro dikes have lower Th/Yb (0.08–0.12) and Zr/Yb ratios (15.32–25.45) that resemble a normal mid-ocean ridge basalt (N-MORB) from a depleted mantle source. In contrast, the later diabase dikes show enrichment in the light rare earth elements (LREE) with relatively higher Th/Yb (0.22–0.86) and Zr/Yb ratios (38.05–68.97) that are similar to an enriched mid-ocean ridge basalt (E-MORB) mantle source. Also, the Nb/Ta ratios from the earlier adakitic granitoids (21.26–23.28) differ markedly from the later acidic adakites (0.41–19.50), which implies the transition from a thicker to a thinner crust. Integrating our results with the previous geological records, leads us to propose a two-stage tectonic model for the Chinese western Tianshan Orogen\u0026#39;s transition from syn- to post-collision. The Late Carboniferous stage of magmatism was triggered by the break-off of the North Tianshan Oceanic slab as the Yili Block and Junggar Terrane collided. The subsequent latest Carboniferous-Permian stage followed the switch to a post-collisional setting with delamination of the thickened lower crust and the intrusion of voluminous lithospheric mantle-induced bimodal magmatism.","internal_url":"https://www.academia.edu/115346705/Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting","translated_internal_url":"","created_at":"2024-02-24T04:43:57.527-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Late_Carboniferous_Early_Permian_mafic_dikes_and_granitoids_in_the_heart_of_the_Western_Tianshan_Orogen_NW_China_Implications_for_a_tectonic_transition_from_a_syn_to_post_collisional_setting","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":96185,"name":"Carboniferous","url":"https://www.academia.edu/Documents/in/Carboniferous"},{"id":135982,"name":"Rodinia","url":"https://www.academia.edu/Documents/in/Rodinia"},{"id":197587,"name":"Dike","url":"https://www.academia.edu/Documents/in/Dike"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":319882,"name":"Petrogenesis","url":"https://www.academia.edu/Documents/in/Petrogenesis"},{"id":587615,"name":"Mantle plume","url":"https://www.academia.edu/Documents/in/Mantle_plume"}],"urls":[{"id":39753585,"url":"https://doi.org/10.1016/j.lithos.2021.106417"}]}, dispatcherData: dispatcherData }); 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Igneous intrusions in this deposit consist of barren diorite porphyry (U-Pb zircon age of 232.0 ± 2.0 Ma) and ore-bearing quartz diorite and pyroxene diorite (U-Pb zircon ages of 223.3 ± 1.5 and 224.6 ± 2.9 Ma, respectively). Whole-rock major and trace element and accessory mineral (zircon and apatite) composition from these intrusions are studied to examine the different geochemical characteristics of orebearing and barren intrusions. Compared to the barren diorite porphyry, the ore-bearing intrusions have higher Ce 4+ /Ce 3+ ratios of zircon and lower Mn contents of apatite, indicating higher oxidation state. Besides, apatite from the ore-bearing intrusions shows higher Cl contents and lower F/Cl ratios. These characteristics collectively suggest the higher productivity of ore-bearing quartz diorite and pyroxene diorite. When compared with ore-bearing intrusions from global porphyry Cu deposits, those from Cu-Pb-Zn skarn deposits display lower Ce 4+ /Ce 3+ and Eu N /Eu N * ratios of zircon and lower Cl and higher F/Cl ratios of apatite. We conclude that these differences reflect a general geochemical feature, and that zircon and apatite composition is a sensitive tool to infer economic potential of magmas and the resulting mineralization types in intrusion-related exploration targets.","publication_date":{"day":28,"month":12,"year":2017,"errors":{}},"publication_name":"Mineralium Deposita","grobid_abstract_attachment_id":111780766},"translated_abstract":null,"internal_url":"https://www.academia.edu/115346703/Geochemical_contrasts_between_Late_Triassic_ore_bearing_and_barren_intrusions_in_the_Weibao_Cu_Pb_Zn_deposit_East_Kunlun_Mountains_NW_China_constraints_from_accessory_minerals_zircon_and_apatite_","translated_internal_url":"","created_at":"2024-02-24T04:43:56.728-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":111780766,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780766/thumbnails/1.jpg","file_name":"s00126-017-0787-8.pdf","download_url":"https://www.academia.edu/attachments/111780766/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_contrasts_between_Late_Trias.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780766/s00126-017-0787-8-libre.pdf?1708779224=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_contrasts_between_Late_Trias.pdf\u0026Expires=1732833586\u0026Signature=Jvyd-S8kMmjwOyktFGwWZys3vYalC-4~wo5~8qTrJ~FifLufhzyH8bAzVxH9hmj~TERvcvNOh31sqGXleNTV6LKuW9-0IHZOwU~H4F8jLY8IHRXRno6~m0A6MgTyosbnYGyjbanczHyRj7QH5MUTSmjwpdcuUeY5XyUM5M-FA3ug9-P392la3OqogNIqbd0hddNmew7752vfGgvUGeX2JW8gsKJ8tolXQPNYUZIEkJoZemcJaExCaVvVqlFQWbV-BLc8m2Ota4qj4OsnkxYBtmr-Mo9GrqFDR3MyrMrwVt0gE5RPB7zJjV6PbJNWAGhuoC79vn14Usa8fq2o9xWNhg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Geochemical_contrasts_between_Late_Triassic_ore_bearing_and_barren_intrusions_in_the_Weibao_Cu_Pb_Zn_deposit_East_Kunlun_Mountains_NW_China_constraints_from_accessory_minerals_zircon_and_apatite_","translated_slug":"","page_count":16,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[{"id":111780766,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780766/thumbnails/1.jpg","file_name":"s00126-017-0787-8.pdf","download_url":"https://www.academia.edu/attachments/111780766/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Geochemical_contrasts_between_Late_Trias.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780766/s00126-017-0787-8-libre.pdf?1708779224=\u0026response-content-disposition=attachment%3B+filename%3DGeochemical_contrasts_between_Late_Trias.pdf\u0026Expires=1732833586\u0026Signature=Jvyd-S8kMmjwOyktFGwWZys3vYalC-4~wo5~8qTrJ~FifLufhzyH8bAzVxH9hmj~TERvcvNOh31sqGXleNTV6LKuW9-0IHZOwU~H4F8jLY8IHRXRno6~m0A6MgTyosbnYGyjbanczHyRj7QH5MUTSmjwpdcuUeY5XyUM5M-FA3ug9-P392la3OqogNIqbd0hddNmew7752vfGgvUGeX2JW8gsKJ8tolXQPNYUZIEkJoZemcJaExCaVvVqlFQWbV-BLc8m2Ota4qj4OsnkxYBtmr-Mo9GrqFDR3MyrMrwVt0gE5RPB7zJjV6PbJNWAGhuoC79vn14Usa8fq2o9xWNhg__\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":205587,"name":"Apatite","url":"https://www.academia.edu/Documents/in/Apatite"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"}],"urls":[{"id":39753583,"url":"https://doi.org/10.1007/s00126-017-0787-8"}]}, dispatcherData: dispatcherData }); 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The magnitude of the zircon Ce anomaly has been traditionally described by Ce/Ce*, where Ce* is the theoretical Ce value derived from a chondrite-normalized rare earth element (REE) pattern. More recently, the Ce 4+ /Ce 3+ method based on the lattice strain model has been proposed, since the latter method does not need La and Pr contents for zircon, both of which are commonly below the limit of detection and susceptible to contamination from melt/mineral inclusions. In this contribution we show that the Ce 4+ /Ce 3+ method is confronted with some problems in practice and should be further improved. In contrast, by reexamining chondrite-normalized REE patterns of zircon, we find that Ce* can be estimated according to a logarithmic function curve without involvement of La and Pr contents. Application of this new method to zircon data from 11 giant to supergiant porphyry Cu deposits suggests this revised method as a more valid measure in evaluating magmatic oxidation state. The revised Ce/Ce* method is of particular importance for analyses where the provenance of the analyzed zircon is unknown or in question, since the method does not require knowledge of the melt composition.","publication_date":{"day":29,"month":8,"year":2019,"errors":{}},"publication_name":"Mineralogy and Petrology","grobid_abstract_attachment_id":111780764},"translated_abstract":null,"internal_url":"https://www.academia.edu/115346702/Characterization_of_the_zircon_Ce_anomaly_for_estimation_of_oxidation_state_of_magmas_a_revised_Ce_Ce_method","translated_internal_url":"","created_at":"2024-02-24T04:43:56.054-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":111780764,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780764/thumbnails/1.jpg","file_name":"s00710-019-00682-y.pdf","download_url":"https://www.academia.edu/attachments/111780764/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Characterization_of_the_zircon_Ce_anomal.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780764/s00710-019-00682-y-libre.pdf?1708779221=\u0026response-content-disposition=attachment%3B+filename%3DCharacterization_of_the_zircon_Ce_anomal.pdf\u0026Expires=1732833586\u0026Signature=diNdVw6yQ4Q0loS8RZ9Qs3UxAUTLYJ8TQDgF5jBDCzu47N51WK9hWQjCwYX53pYo2p1fY8MpHvM~m-e41T1WDdKOImYZgWK4FkjXsOcB5QTKIFNpNg5Nl1UCqIPyDu8qiITUCAPVAijHF-v2m3W~t5~MAdRezPPz3n7eBu~81TkwFWXjkCtS5DFbqmcz0xpHYtnlKUdiFilo9WYQ--48aHMsI0KcjsQEKFW5HHxpW277eCx25VMhTY3roVBshC0ueFdY8-AJ1G6hYBODSZLSU5z-5k7Ox4B9cPYZSsL2G6CRl9vsbBKBzUnkKlDLy8azSmGJbdXh7VwWuYnlXXxWsQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Characterization_of_the_zircon_Ce_anomaly_for_estimation_of_oxidation_state_of_magmas_a_revised_Ce_Ce_method","translated_slug":"","page_count":9,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[{"id":111780764,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/111780764/thumbnails/1.jpg","file_name":"s00710-019-00682-y.pdf","download_url":"https://www.academia.edu/attachments/111780764/download_file?st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&st=MTczMjgyOTk4Niw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Characterization_of_the_zircon_Ce_anomal.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/111780764/s00710-019-00682-y-libre.pdf?1708779221=\u0026response-content-disposition=attachment%3B+filename%3DCharacterization_of_the_zircon_Ce_anomal.pdf\u0026Expires=1732833586\u0026Signature=diNdVw6yQ4Q0loS8RZ9Qs3UxAUTLYJ8TQDgF5jBDCzu47N51WK9hWQjCwYX53pYo2p1fY8MpHvM~m-e41T1WDdKOImYZgWK4FkjXsOcB5QTKIFNpNg5Nl1UCqIPyDu8qiITUCAPVAijHF-v2m3W~t5~MAdRezPPz3n7eBu~81TkwFWXjkCtS5DFbqmcz0xpHYtnlKUdiFilo9WYQ--48aHMsI0KcjsQEKFW5HHxpW277eCx25VMhTY3roVBshC0ueFdY8-AJ1G6hYBODSZLSU5z-5k7Ox4B9cPYZSsL2G6CRl9vsbBKBzUnkKlDLy8azSmGJbdXh7VwWuYnlXXxWsQ__\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":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"},{"id":517272,"name":"Mineralogy and Petrology","url":"https://www.academia.edu/Documents/in/Mineralogy_and_Petrology"}],"urls":[{"id":39753582,"url":"https://doi.org/10.1007/s00710-019-00682-y"}]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="115346696"><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/115346696/Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China"><img alt="Research paper thumbnail of Unraveling the link between mantle upwelling and formation of Sn-bearing granitic rocks in the world-class Dachang tin district, South China" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/115346696/Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China">Unraveling the link between mantle upwelling and formation of Sn-bearing granitic rocks in the world-class Dachang tin district, South China</a></div><div class="wp-workCard_item"><span>Geological Society of America Bulletin</span><span>, Jun 21, 2021</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing gran...</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">Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing granites worldwide. However, the specific role of mantle in the formation of tin granites and related mineralization remains poorly understood. In the world-class Dachang district, South China, tin mineralization is related to the Longxianggai equigranular/porphyritic biotite granites and tin orebodies are cut by granite porphyry dykes hosting mafic microgranular enclaves (MMEs). A combination of zircon U-Pb dating and Hf-O isotopes, mineral chemistry, and whole-rock elemental and Sr-Nd isotopic compositions—for granitic rocks and MMEs, is employed to constrain the petrogenesis and to unravel the link between tin fertility and mantle upwelling. Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) zircon U-Pb dating indicates that the biotite granites were emplaced at ca. 93 Ma, and the granite porphyry dykes and MMEs were formed at ca. 86 Ma. The biotite granites are silica- and alkali-enriched with A/CNK ratios of 1.04–1.36, and exhibit elevated concentrations of Li, F, P, Rb, Cs, Ta, Sn, W, and U, showing affinities with highly fractionated S-type granites. Whole-rock geochemical and Nd isotopic (εNd(t) = −10.0 to −7.8) data, and in situ zircon Hf-O (εHf(t) = −9.9 to −3.9, δ18O = 6.2–8.9‰) isotopes indicate that the biotite granites were formed by partial melting of metasedimentary rocks at relatively high temperatures (≥782 °C), possibly with minor input of mantle material. Likewise, the post-ore granite porphyry dykes have similar chemical and mineralogical characteristics as fractionated S-type granites. Zircon Hf-O isotopes (εHf(t) = −9.0 to −4.9, δ18O = 6.5–8.2‰) and whole-rock geochemical data suggest they were derived from a similar source as the biotite granites, whereas elevated εNd(t) values of −5.0 to −3.3 for granite porphyry dykes relative to biotite granites reveal an increasing mantle input. Distinct εNd(t) (−0.4 and −0.3) and zircon Hf-O (εHf(t) = 1.5–5.0, δ18O = 6.5–7.2‰) isotopes of the MMEs, suggest that the mafic melt could be sourced from the asthenospheric mantle, contaminated by subcontinental lithospheric mantle/continental crust during magma ascent, and hybridized by felsic melt at emplacement-level. The magmatic sequence in the Dachang district is indicative of an extensional tectonic setting where mantle-derived magmas are predicted to migrate to shallower crustal levels as the crust progressively becomes thinner and hotter. High-temperature partial melting of mature metasedimentary crust triggered by heat input from the upwelled mantle, may contribute to biotite breakdown, which is important for concentrating tin in melts. Fractional crystallization of initially Sn-rich felsic melts under reduced conditions makes further tin enrichment and produces Sn-bearing granites (the Longxianggai pluton). Prolonged mantle upwelling results in distinct magma mixing and the formation of granite porphyry dykes and MMEs. These dykes are highly fractionated with elevated Sn and W contents, which show great potential to form hydrothermal Sn-W mineralization.</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="115346696"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="115346696"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 115346696; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=115346696]").text(description); $(".js-view-count[data-work-id=115346696]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 115346696; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='115346696']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 115346696, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=115346696]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":115346696,"title":"Unraveling the link between mantle upwelling and formation of Sn-bearing granitic rocks in the world-class Dachang tin district, South China","translated_title":"","metadata":{"abstract":"Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing granites worldwide. However, the specific role of mantle in the formation of tin granites and related mineralization remains poorly understood. In the world-class Dachang district, South China, tin mineralization is related to the Longxianggai equigranular/porphyritic biotite granites and tin orebodies are cut by granite porphyry dykes hosting mafic microgranular enclaves (MMEs). A combination of zircon U-Pb dating and Hf-O isotopes, mineral chemistry, and whole-rock elemental and Sr-Nd isotopic compositions—for granitic rocks and MMEs, is employed to constrain the petrogenesis and to unravel the link between tin fertility and mantle upwelling. Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) zircon U-Pb dating indicates that the biotite granites were emplaced at ca. 93 Ma, and the granite porphyry dykes and MMEs were formed at ca. 86 Ma. The biotite granites are silica- and alkali-enriched with A/CNK ratios of 1.04–1.36, and exhibit elevated concentrations of Li, F, P, Rb, Cs, Ta, Sn, W, and U, showing affinities with highly fractionated S-type granites. Whole-rock geochemical and Nd isotopic (εNd(t) = −10.0 to −7.8) data, and in situ zircon Hf-O (εHf(t) = −9.9 to −3.9, δ18O = 6.2–8.9‰) isotopes indicate that the biotite granites were formed by partial melting of metasedimentary rocks at relatively high temperatures (≥782 °C), possibly with minor input of mantle material. Likewise, the post-ore granite porphyry dykes have similar chemical and mineralogical characteristics as fractionated S-type granites. Zircon Hf-O isotopes (εHf(t) = −9.0 to −4.9, δ18O = 6.5–8.2‰) and whole-rock geochemical data suggest they were derived from a similar source as the biotite granites, whereas elevated εNd(t) values of −5.0 to −3.3 for granite porphyry dykes relative to biotite granites reveal an increasing mantle input. Distinct εNd(t) (−0.4 and −0.3) and zircon Hf-O (εHf(t) = 1.5–5.0, δ18O = 6.5–7.2‰) isotopes of the MMEs, suggest that the mafic melt could be sourced from the asthenospheric mantle, contaminated by subcontinental lithospheric mantle/continental crust during magma ascent, and hybridized by felsic melt at emplacement-level. The magmatic sequence in the Dachang district is indicative of an extensional tectonic setting where mantle-derived magmas are predicted to migrate to shallower crustal levels as the crust progressively becomes thinner and hotter. High-temperature partial melting of mature metasedimentary crust triggered by heat input from the upwelled mantle, may contribute to biotite breakdown, which is important for concentrating tin in melts. Fractional crystallization of initially Sn-rich felsic melts under reduced conditions makes further tin enrichment and produces Sn-bearing granites (the Longxianggai pluton). Prolonged mantle upwelling results in distinct magma mixing and the formation of granite porphyry dykes and MMEs. These dykes are highly fractionated with elevated Sn and W contents, which show great potential to form hydrothermal Sn-W mineralization.","publisher":"Geological Society of America","publication_date":{"day":21,"month":6,"year":2021,"errors":{}},"publication_name":"Geological Society of America Bulletin"},"translated_abstract":"Increasing evidence shows that the mantle contributes (directly or indirectly) to Sn-bearing granites worldwide. However, the specific role of mantle in the formation of tin granites and related mineralization remains poorly understood. In the world-class Dachang district, South China, tin mineralization is related to the Longxianggai equigranular/porphyritic biotite granites and tin orebodies are cut by granite porphyry dykes hosting mafic microgranular enclaves (MMEs). A combination of zircon U-Pb dating and Hf-O isotopes, mineral chemistry, and whole-rock elemental and Sr-Nd isotopic compositions—for granitic rocks and MMEs, is employed to constrain the petrogenesis and to unravel the link between tin fertility and mantle upwelling. Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) zircon U-Pb dating indicates that the biotite granites were emplaced at ca. 93 Ma, and the granite porphyry dykes and MMEs were formed at ca. 86 Ma. The biotite granites are silica- and alkali-enriched with A/CNK ratios of 1.04–1.36, and exhibit elevated concentrations of Li, F, P, Rb, Cs, Ta, Sn, W, and U, showing affinities with highly fractionated S-type granites. Whole-rock geochemical and Nd isotopic (εNd(t) = −10.0 to −7.8) data, and in situ zircon Hf-O (εHf(t) = −9.9 to −3.9, δ18O = 6.2–8.9‰) isotopes indicate that the biotite granites were formed by partial melting of metasedimentary rocks at relatively high temperatures (≥782 °C), possibly with minor input of mantle material. Likewise, the post-ore granite porphyry dykes have similar chemical and mineralogical characteristics as fractionated S-type granites. Zircon Hf-O isotopes (εHf(t) = −9.0 to −4.9, δ18O = 6.5–8.2‰) and whole-rock geochemical data suggest they were derived from a similar source as the biotite granites, whereas elevated εNd(t) values of −5.0 to −3.3 for granite porphyry dykes relative to biotite granites reveal an increasing mantle input. Distinct εNd(t) (−0.4 and −0.3) and zircon Hf-O (εHf(t) = 1.5–5.0, δ18O = 6.5–7.2‰) isotopes of the MMEs, suggest that the mafic melt could be sourced from the asthenospheric mantle, contaminated by subcontinental lithospheric mantle/continental crust during magma ascent, and hybridized by felsic melt at emplacement-level. The magmatic sequence in the Dachang district is indicative of an extensional tectonic setting where mantle-derived magmas are predicted to migrate to shallower crustal levels as the crust progressively becomes thinner and hotter. High-temperature partial melting of mature metasedimentary crust triggered by heat input from the upwelled mantle, may contribute to biotite breakdown, which is important for concentrating tin in melts. Fractional crystallization of initially Sn-rich felsic melts under reduced conditions makes further tin enrichment and produces Sn-bearing granites (the Longxianggai pluton). Prolonged mantle upwelling results in distinct magma mixing and the formation of granite porphyry dykes and MMEs. These dykes are highly fractionated with elevated Sn and W contents, which show great potential to form hydrothermal Sn-W mineralization.","internal_url":"https://www.academia.edu/115346696/Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China","translated_internal_url":"","created_at":"2024-02-24T04:43:54.400-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":23017749,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Unraveling_the_link_between_mantle_upwelling_and_formation_of_Sn_bearing_granitic_rocks_in_the_world_class_Dachang_tin_district_South_China","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":23017749,"first_name":"Reimar","middle_initials":null,"last_name":"Seltmann","page_name":"ReimarSeltmann","domain_name":"nhm","created_at":"2014-12-06T07:11:25.986-08:00","display_name":"Reimar Seltmann","url":"https://nhm.academia.edu/ReimarSeltmann"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":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":456199,"name":"Biotite","url":"https://www.academia.edu/Documents/in/Biotite"}],"urls":[{"id":39753576,"url":"https://doi.org/10.1130/b35492.1"}]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="7589891" id="conferencepresentations"><div class="js-work-strip profile--work_container" data-work-id="34908423"><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/34908423/Sn_mineralization_in_W_skarns_from_Douro_Scheelite_Belt_the_example_of_Tabua%C3%A7o_Portugal_"><img alt="Research paper thumbnail of Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/34908423/Sn_mineralization_in_W_skarns_from_Douro_Scheelite_Belt_the_example_of_Tabua%C3%A7o_Portugal_">Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://uec.academia.edu/VioletaRamos">Violeta Ramos</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://nhm.academia.edu/ReimarSeltmann">Reimar Seltmann</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">In this contribution, we present the mineralogy and geochemistry of Tabuaço skarn deposit, one of...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">In this contribution, we present the mineralogy and geochemistry of Tabuaço skarn deposit, one of the most important tungsten deposits of the “Douro Scheelite Belt”, Portugal. Tabuaço is a W-(Sn) proximal skarn deposit located at the contact between “Bateiras Formation” from the Schist Greywacke Complex and Tabuaço Granite. The Tabuaço deposit has scheelite as the primary target mineral. However, minor Sn minerals also occur. Three types of skarn are distinguished: M-type, the richest in W (>10000 ppm; scheelite average 1.7 vol%); F-type, the richest in Sn (7770 ppm; malayaite and malayaite-titanite average 0.68 vol%, cassiterite 0.37 vol% and stokesite); and L-type, the poorest in scheelite (130 – 7710 W ppm; Sn < 1840 ppm). This study confirms that despite the occurrence of cassiterite other Sn-bearing minerals, such as malayaite, malayaite-titanite and stokesite, also occur. The whole rock geochemistry demonstrates that enriched Sn and F are a typical characteristic of the W (Sn) skarn of Tabuaço. Tungsten is more abundant in skarns richer in F due to the presence of scheelite ± fluorite. These W (Sn) skarns can be also distinguished by their rare earth elements (REE). The higher values of REE are registered in L-type skarn lithologies, which include barren skarns, suggesting that the hydrothermal metasomatism contemporaneous with the W mineralization stage results in a decrease of REE up to 36.40 ppm, a value found in M-type skarns.</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="34908423"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="34908423"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 34908423; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=34908423]").text(description); $(".js-view-count[data-work-id=34908423]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 34908423; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='34908423']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 34908423, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=34908423]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":34908423,"title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)","translated_title":"","metadata":{"abstract":"In this contribution, we present the mineralogy and geochemistry of Tabuaço skarn deposit, one of the most important tungsten deposits of the “Douro Scheelite Belt”, Portugal. Tabuaço is a W-(Sn) proximal skarn deposit located at the contact between “Bateiras Formation” from the Schist Greywacke Complex and Tabuaço Granite. The Tabuaço deposit has scheelite as the primary target mineral. However, minor Sn minerals also occur. Three types of skarn are distinguished: M-type, the richest in W (\u003e10000 ppm; scheelite average 1.7 vol%); F-type, the richest in Sn (7770 ppm; malayaite and malayaite-titanite average 0.68 vol%, cassiterite 0.37 vol% and stokesite); and L-type, the poorest in scheelite (130 – 7710 W ppm; Sn \u003c 1840 ppm). This study confirms that despite the occurrence of cassiterite other Sn-bearing minerals, such as malayaite, malayaite-titanite and stokesite, also occur. The whole rock geochemistry demonstrates that enriched Sn and F are a typical characteristic of the W (Sn) skarn of Tabuaço. Tungsten is more abundant in skarns richer in F due to the presence of scheelite ± fluorite. These W (Sn) skarns can be also distinguished by their rare earth elements (REE). The higher values of REE are registered in L-type skarn lithologies, which include barren skarns, suggesting that the hydrothermal metasomatism contemporaneous with the W mineralization stage results in a decrease of REE up to 36.40 ppm, a value found in M-type skarns.\n\n"},"translated_abstract":"In this contribution, we present the mineralogy and geochemistry of Tabuaço skarn deposit, one of the most important tungsten deposits of the “Douro Scheelite Belt”, Portugal. Tabuaço is a W-(Sn) proximal skarn deposit located at the contact between “Bateiras Formation” from the Schist Greywacke Complex and Tabuaço Granite. The Tabuaço deposit has scheelite as the primary target mineral. However, minor Sn minerals also occur. Three types of skarn are distinguished: M-type, the richest in W (\u003e10000 ppm; scheelite average 1.7 vol%); F-type, the richest in Sn (7770 ppm; malayaite and malayaite-titanite average 0.68 vol%, cassiterite 0.37 vol% and stokesite); and L-type, the poorest in scheelite (130 – 7710 W ppm; Sn \u003c 1840 ppm). This study confirms that despite the occurrence of cassiterite other Sn-bearing minerals, such as malayaite, malayaite-titanite and stokesite, also occur. The whole rock geochemistry demonstrates that enriched Sn and F are a typical characteristic of the W (Sn) skarn of Tabuaço. Tungsten is more abundant in skarns richer in F due to the presence of scheelite ± fluorite. These W (Sn) skarns can be also distinguished by their rare earth elements (REE). The higher values of REE are registered in L-type skarn lithologies, which include barren skarns, suggesting that the hydrothermal metasomatism contemporaneous with the W mineralization stage results in a decrease of REE up to 36.40 ppm, a value found in M-type skarns.\n\n","internal_url":"https://www.academia.edu/34908423/Sn_mineralization_in_W_skarns_from_Douro_Scheelite_Belt_the_example_of_Tabua%C3%A7o_Portugal_","translated_internal_url":"","created_at":"2017-10-20T08:38:19.095-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":37776732,"coauthors_can_edit":true,"document_type":"conference_presentation","co_author_tags":[{"id":30504688,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":23019597,"co_author_invite_id":null,"email":"a***g@gmail.com","display_order":0,"name":"Alexandra Guedes","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504689,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":14401557,"co_author_invite_id":null,"email":"f***c@hotmail.com","display_order":4194304,"name":"Fernando Noronha","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504690,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":25222272,"co_author_invite_id":null,"email":"a***l@hotmail.com","display_order":6291456,"name":"Alla Dolgopolova","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504691,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":23017749,"co_author_invite_id":null,"email":"c***s@nhm.ac.uk","affiliation":"Natural History Museum, London","display_order":7340032,"name":"Reimar Seltmann","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504692,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":1699307,"co_author_invite_id":null,"email":"R***g@nhm.ac.uk","affiliation":"Natural History Museum, London","display_order":7864320,"name":"Robin N Armstrong","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504693,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":54038756,"co_author_invite_id":null,"email":"c***7@hotmail.com","display_order":8126464,"name":"Chris Stanley","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504694,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":12183202,"co_author_invite_id":null,"email":"b***s@avantihs.com","display_order":8257536,"name":"Beth Simons","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504695,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":47151184,"co_author_invite_id":null,"email":"j***a@km.dk","display_order":8323072,"name":"Jens Andersen","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"},{"id":30504696,"work_id":34908423,"tagging_user_id":37776732,"tagged_user_id":39739482,"co_author_invite_id":null,"email":"g***n@exeter.ac.uk","display_order":8355840,"name":"Gavyn Rollinson","title":"Sn mineralization in W skarns from “Douro Scheelite Belt”: the example of Tabuaço (Portugal)"}],"downloadable_attachments":[],"slug":"Sn_mineralization_in_W_skarns_from_Douro_Scheelite_Belt_the_example_of_Tabuaço_Portugal_","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":37776732,"first_name":"Violeta","middle_initials":"","last_name":"Ramos","page_name":"VioletaRamos","domain_name":"uec","created_at":"2015-11-06T07:14:23.550-08:00","display_name":"Violeta Ramos","url":"https://uec.academia.edu/VioletaRamos"},"attachments":[],"research_interests":[{"id":215014,"name":"Skarn","url":"https://www.academia.edu/Documents/in/Skarn"},{"id":500007,"name":"Tungsten","url":"https://www.academia.edu/Documents/in/Tungsten"}],"urls":[]}, dispatcherData: dispatcherData }); 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