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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 Haibo Zou</h3></div><div class="js-work-strip profile--work_container" data-work-id="79193468"><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/79193468/Uranium_series_Disequilibrium_Modeling"><img alt="Research paper thumbnail of Uranium-series Disequilibrium Modeling" 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">Uranium-series Disequilibrium Modeling</div><div class="wp-workCard_item"><span>Quantitative Geochemistry</span><span>, 2007</span></div><div 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-79193466-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193465"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/79193465/Inverse_Geochemical_Modeling"><img alt="Research paper thumbnail of Inverse Geochemical Modeling" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Inverse Geochemical Modeling</div><div class="wp-workCard_item"><span>Quantitative Geochemistry</span><span>, 2007</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193465"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193465"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193465; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193465]").text(description); $(".js-view-count[data-work-id=79193465]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x 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dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=79193465]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193465,"title":"Inverse Geochemical Modeling","translated_title":"","metadata":{"publisher":"PUBLISHED BY IMPERIAL COLLEGE PRESS AND DISTRIBUTED BY WORLD SCIENTIFIC PUBLISHING CO.","publication_date":{"day":null,"month":null,"year":2007,"errors":{}},"publication_name":"Quantitative 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true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-79193465-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193464"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/79193464/U_Series_Ages_of_Young_Tengchong_Volcanoes_Southeast_Tibetan_Plateau"><img alt="Research paper thumbnail of U-Series Ages of Young Tengchong Volcanoes, Southeast Tibetan Plateau" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">U-Series Ages of Young Tengchong Volcanoes, Southeast Tibetan Plateau</div><div class="wp-workCard_item"><span>Goldschmidt Abstracts</span><span>, 2020</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193464"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193464"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193464; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193464]").text(description); $(".js-view-count[data-work-id=79193464]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193464; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193464']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ 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Abstracts"},"translated_abstract":null,"internal_url":"https://www.academia.edu/79193464/U_Series_Ages_of_Young_Tengchong_Volcanoes_Southeast_Tibetan_Plateau","translated_internal_url":"","created_at":"2022-05-15T22:31:50.982-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":89685072,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"U_Series_Ages_of_Young_Tengchong_Volcanoes_Southeast_Tibetan_Plateau","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":null,"impression_tracking_id":null,"owner":{"id":89685072,"first_name":"Haibo","middle_initials":null,"last_name":"Zou","page_name":"HaiboZou","domain_name":"auburn","created_at":"2018-08-29T11:15:27.832-07:00","display_name":"Haibo Zou","url":"https://auburn.academia.edu/HaiboZou"},"attachments":[],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-79193464-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193463"><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/79193463/U_series_ages_of_young_volcanoes_from_the_Southeastern_Tibetan_Plateau_Holocene_eruptions_and_magma_evolution_timescales"><img alt="Research paper thumbnail of U-series ages of young volcanoes from the Southeastern Tibetan Plateau: Holocene eruptions and magma evolution timescales" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">U-series ages of young volcanoes from the Southeastern Tibetan Plateau: Holocene eruptions and magma evolution timescales</div><div class="wp-workCard_item"><span>Lithos</span><span>, 2020</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic e...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193463"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193463"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193463; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193463]").text(description); $(".js-view-count[data-work-id=79193463]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193463; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193463']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=79193463]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193463,"title":"U-series ages of young volcanoes from the Southeastern Tibetan Plateau: Holocene eruptions and magma evolution timescales","translated_title":"","metadata":{"abstract":"Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.","publisher":"Elsevier BV","publication_date":{"day":null,"month":null,"year":2020,"errors":{}},"publication_name":"Lithos"},"translated_abstract":"Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.","internal_url":"https://www.academia.edu/79193463/U_series_ages_of_young_volcanoes_from_the_Southeastern_Tibetan_Plateau_Holocene_eruptions_and_magma_evolution_timescales","translated_internal_url":"","created_at":"2022-05-15T22:31:50.770-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":89685072,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"U_series_ages_of_young_volcanoes_from_the_Southeastern_Tibetan_Plateau_Holocene_eruptions_and_magma_evolution_timescales","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.","impression_tracking_id":null,"owner":{"id":89685072,"first_name":"Haibo","middle_initials":null,"last_name":"Zou","page_name":"HaiboZou","domain_name":"auburn","created_at":"2018-08-29T11:15:27.832-07:00","display_name":"Haibo Zou","url":"https://auburn.academia.edu/HaiboZou"},"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"}],"urls":[{"id":20488061,"url":"https://api.elsevier.com/content/article/PII:S0024493720302802?httpAccept=text/xml"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-79193463-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193462"><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/79193462/Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities"><img alt="Research paper thumbnail of Two episodes of volcanism in the Wudalianchi volcanic belt, NE China: Evidence for tectonic controls on volcanic activities" class="work-thumbnail" src="https://attachments.academia-assets.com/85991617/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/79193462/Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities">Two episodes of volcanism in the Wudalianchi volcanic belt, NE China: Evidence for tectonic controls on volcanic activities</a></div><div class="wp-workCard_item"><span>Journal of Volcanology and Geothermal Research</span><span>, 2014</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volca...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volcanoes in Menlu River area, Keluo, Wudalianchi and Erkeshan. K-Ar radiometric dating suggests two episodes of volcanism in the WVB. Specifically, the Pliocene to early Pleistocene volcanism is distributed only in the northern part of WVB, whereas middle Pleistocene to Holocene volcanism occurred over the entire WVB. Geomorphological analyses further delineate four northeast-striking linear alignments of cones in the Wudalianchi and Keluo volcanic fields, probably related to magma feeding fractures with en echelon arrangement. No age progression is observed along these alignments. We propose that a NNW-trending rift may have controlled the eruption from Pliocene to early Pleistocene and a dextral transpression stress field may have influenced the volcanism from middle Pleistocene to Holocene. We suggest that the Pliocene and early Pleistocene volcanism is associated with far effect of the India-Eurasia collision, while the middle Pleistocene to Holocene volcanism in WVB may have resulted from interaction between the India-Eurasia collision and the subduction of the Pacific plate.</span></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-79193462-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-79193462-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037619/figure-1-distribution-of-cenozoic-volcanic-rocks-in-ne-asia"><img alt="Fig. 1. Distribution of Cenozoic volcanic rocks in NE Asia. Modified from Ren et al., 2002. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_001.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037633/figure-2-distribution-of-volcanic-rocks-in-wvb-erkeshan"><img alt="Fig. 2. Distribution of volcanic rocks in WVB 1 — Erkeshan volcanic field, 2 — Wudalianchi volcanic field, 3 — Keluo volcanic field, 4 — Menlu river volcanic field, a — Nenjiang fault, b — Nemuoer fault, c — Sunwu fault. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_002.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037640/figure-3-geological-map-of-the-wudalianchi-volcanic-field"><img alt="Fig. 3. Geological map of the Wudalianchi volcanic field. Most of the volcanic products formed since the middle Pleistocene, except for Laoshantou. Two Holocene volcanoes, Laoheisha and Huoshaoshan, are in the middle of the field. Three cone alignment lines are sub-parallel to each other. Whole-rock K-Ar dating has been undertaken to constrain the timing of volcanism in the WVB. Eight samples are selected according to their geographical location, freshness and content of phenocryst. The K-Ar dating experiments were performed in the Geochronology Laboratory of the Institute of Geology, China Earthquake Administra- tion. Rock samples were crushed and sorted to grains size between 0.4 We collected samples in the study areas during three field seasons, and selected the samples to cover a wide range in ages and locations. All the samples in WVB are collected from fresh lava flows. These samples are porphyritic, with a phenocryst content of less than 5%. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_003.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037653/figure-4-geology-map-of-keluo-volcanic-field-the-pliocene"><img alt="Fig. 4. Geology map of Keluo volcanic field. The Pliocene and early Pleistocene volcanoes are in the periphery of the field. However, volcanoes formed in the middle of the field since th middle Pleistocene. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_004.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037668/figure-5-comparison-of-volcanoes-formed-in-two-episode"><img alt="Fig. 5. A comparison of volcanoes formed in two episode volcanism. A — Heishan volcano in Keluo field, B — section in Heishan volcano, C — Dayishan in Keluo field, D — section of Dayishan cone. Heishan shows a gentle slope and large volume and it is made up of lava. In contrast, Dayishan volcano has a volcanic cone, featuring a relatively steep slope and small volume, and it is made up of lapilli. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_005.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037684/figure-6-volcanic-height-vs-volcanic-base-diameter-volcanoes"><img alt="Fig. 6. Volcanic height vs. volcanic base diameter. Volcanoes in two episodes show an ap- parent difference in geomorphology features. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_006.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037699/figure-7-ig-vent-centers-of-cone-and-regression-lines-the"><img alt="‘ig. 7. Vent centers of cone and regression lines. The vent center points of WVB trends NNW, but the four alignment lines of the vent center points in Wudalianchi and Keluo tren NE-NE. The breaching of cone rim is one of the most common morphological features of basaltic volcanoes. The breaching azimuths in cones are commonly affected by the strike and dip of fractures feeding magma Previous study by satellite imaging of the Wudalianchi field indicat- ed that regional faults or lineaments trending display three directions (NE, NW, and EW) and the volcanoes are located at the intersections of these three lineament groups (Feng and Whitford-Stark, 1986). " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_007.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037713/figure-8-frequency-of-azimuths-in-cone-breaching-cones-of"><img alt="Fig. 8. Frequency of azimuths in cone breaching. Cones of Wudalianchi and Keluo show preferred breaching azimuths of NE and NNW striking In this paper, however, significant differences between the two episodes of volcanism are identified. The first episode of volcanism is characterized by effusive eruption and generated large shield-like volcanoes composed of lava flows. In comparison, the second episode of volcanism is characterized by Strombolian eruption and produced cinder cones, with NE-striking fracture system co-existing with NNW- striking volcanic belt. According to the simultaneous changes of volcanic episodes and tectonic reorganization, we propose a new model for the origin of the WVB that emphasizes the tectonic control on volcanism (Fig. 9). During Pliocene and early Pleistocene, a NNW rift was formed in northern Songliao Basin, resulting in NNW-striking dispersed distribution of lava flows in the WVB. Since the middle Pleistocene, a NNW-trending dextral transpression stress regime (parallel to T;) controlled the volca- nism, resulting in en echelon arrangement of NNE-trending fractures " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_008.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037726/figure-9-model-for-tectonic-control-on-volcanism-in-wvb-two"><img alt="Fig. 9. Model for tectonic control on volcanism in WVB. Two episodes of volcanism are consistent with two different tectonic settings, Welfare Research Institute of Geology China Earthquake Administration (Grant No. IGCEA1102), National Natural Science Foundation of China (NSFC Grant No. 41172305, 41072250), and the China Scholarship Council. We thank two anonymous reviewers and journal editor Lionel Wilson for their constructive reviews that have significantly improved the quality of this paper. (parallel too1) in the deep lithosphere. These fractures reach deep lithosphere, triggering decompression melting of mantle source rocks. The magmas ascend through these fractures, forming NE-oriented volcanic alignments. It is noteworthy that similar two-episode age distribution also occurs in Nuomin River volcanic field and Halaha-Chaoer River field in the NE China, and even in the Datong volcanic field in the North China Craton (Xu et al., 2005; Fan et al., 2011, 2012; Zhao et al., 2013, 2014). Moreover, rapid deformation and uplift of the NE Tibetan Plateau oc- curred since the middle Pleistocene (Liu et al., 2010). All these simulta- neous changes at ~1 Ma may imply the tectonic reorganization in the late stage of Early Pleistocene occurred not only in the WVB, but also likely in other volcanic fields in eastern China and even in Tibet. The cause for the tectonic reorganization is still unclear. However, since the India-Eurasian collision and the Pacific subduction have dominated the Cenozoic tectonic evolution of China (Tapponnier et al., 1986; Ye et al., 1987; Flower et al., 1998), the changes of convergence rates of India-Eurasia and Pacific-Eurasia may lead to the changes of stress fields (Ren et al., 2002). Assuming the changes of convergence rates control the tectonic reorganization, in our new model, the first episode volca- nism occurred during the period when the South-north extrusion and East-west extension (India-Eurasia collision) may have the dominant influence on NE China. Since the middle Pleistocene, the second episode volcanism in WVB and the East-west compression and dextral strike- slip form under the dominant influence from the Pacific-Eurasia sub- duction. During the second episode, the India-Eurasia collision may give way to the Pacific-Eurasia subduction as the dominant tectonic control in NE China. This transformation may take place in the early Pleistocene time. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_009.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037745/table-1-parameters-used-in-calculation-yr-ne-yr-np-yr-atom"><img alt="Parameters used in calculation:\ = 5.543 x 107! yr, Ne = 0.581 x 107!° yr~!, Np, = 4.962 x 107 1° yr", 4° K/K = 1.167 x 10~4 (atom ratio). The data marked by asterisks a from Liu et al. (2001). K-Ar isotopic dates of volcanic rocks in the Wudalianchi volcanic belt. Table 1 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_001.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037760/table-2-means-data-is-not-available-for-cones-or-were"><img alt="n.a. Means data is not available for cones or were destroyed by mining. Main characteristics of volcanoes formed in the first episode of volcanism. Table 2 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_002.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037776/table-3-main-characteristics-of-four-alignments-of-vent"><img alt="Main characteristics of four alignments of vent centers and cones in the second episode of volcanism. n.a. Means data is not available for cones or were destroyed by mining. Wco = the base diameter of cone; Hco = the height of cone; Wcr = the crater diameter. Table 3 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_003.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037792/table-4-parameters-of-volcanic-cones-in-the-wudalianchi"><img alt="Parameters of volcanic cones in the Wudalianchi volcanic belt. Table 4 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_004.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037806/table-5-two-episodes-of-volcanism-in-the-wudalianchi"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_005.jpg" width="114" height="68" /></a></figure></div><div class="next-slide-container js-next-button-container"><button aria-label="Next" class="carousel-navigation-button js-profile-work-79193462-figures-next"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_forward_ios</span></button></div></div></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="7adacd069a26e3922e54691a59d1ba53" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":85991617,"asset_id":79193462,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/85991617/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193462"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193462"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193462; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193462]").text(description); $(".js-view-count[data-work-id=79193462]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193462; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193462']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "7adacd069a26e3922e54691a59d1ba53" } } $('.js-work-strip[data-work-id=79193462]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193462,"title":"Two episodes of volcanism in the Wudalianchi volcanic belt, NE China: Evidence for tectonic controls on volcanic activities","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_title_tag":"Tectonic Controls on Wudalianchi Volcanism","grobid_abstract":"The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volcanoes in Menlu River area, Keluo, Wudalianchi and Erkeshan. K-Ar radiometric dating suggests two episodes of volcanism in the WVB. Specifically, the Pliocene to early Pleistocene volcanism is distributed only in the northern part of WVB, whereas middle Pleistocene to Holocene volcanism occurred over the entire WVB. Geomorphological analyses further delineate four northeast-striking linear alignments of cones in the Wudalianchi and Keluo volcanic fields, probably related to magma feeding fractures with en echelon arrangement. No age progression is observed along these alignments. We propose that a NNW-trending rift may have controlled the eruption from Pliocene to early Pleistocene and a dextral transpression stress field may have influenced the volcanism from middle Pleistocene to Holocene. We suggest that the Pliocene and early Pleistocene volcanism is associated with far effect of the India-Eurasia collision, while the middle Pleistocene to Holocene volcanism in WVB may have resulted from interaction between the India-Eurasia collision and the subduction of the Pacific plate.","publication_date":{"day":null,"month":null,"year":2014,"errors":{}},"publication_name":"Journal of Volcanology and Geothermal Research","grobid_abstract_attachment_id":85991617},"translated_abstract":null,"internal_url":"https://www.academia.edu/79193462/Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities","translated_internal_url":"","created_at":"2022-05-15T22:31:50.619-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":89685072,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":85991617,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/85991617/thumbnails/1.jpg","file_name":"5oeoPO6oahQ9.pdf","download_url":"https://www.academia.edu/attachments/85991617/download_file","bulk_download_file_name":"Two_episodes_of_volcanism_in_the_Wudalia.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/85991617/5oeoPO6oahQ9-libre.pdf?1652680119=\u0026response-content-disposition=attachment%3B+filename%3DTwo_episodes_of_volcanism_in_the_Wudalia.pdf\u0026Expires=1744340798\u0026Signature=GyiLePXHFmSQovzH270oQ7Q3DwWmfLsElgikNfLq~GvYw2vS0Fi14bBj4yRkpsltZ9XIbNN-i7qvF035QxTiVbBtUAHiwE-CgfUiQ7KmovDEajh0QpIyZEq8~ZjfWBxUMBCFpbrY7aiu9LvsoaC8-F2EAq1Feuvu1MRgVahA-SMTOJfStBfp3aoeKJcpU7yUyfMg0MzQXlBZ29MH26bslfM0ceHq2I1bH4868CUUMXNfR53ma-cSWr5zsTYUSxxIELP8LBuGbtuA1HCccDMQA9fIT4KUh2f~jS-Y9-faCrZB7UGkPKe8Wo6KDIhMTAMj52dlr5Rej5vWOX8mN~vHJg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities","translated_slug":"","page_count":11,"language":"en","content_type":"Work","summary":"The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volcanoes in Menlu River area, Keluo, Wudalianchi and Erkeshan. K-Ar radiometric dating suggests two episodes of volcanism in the WVB. Specifically, the Pliocene to early Pleistocene volcanism is distributed only in the northern part of WVB, whereas middle Pleistocene to Holocene volcanism occurred over the entire WVB. Geomorphological analyses further delineate four northeast-striking linear alignments of cones in the Wudalianchi and Keluo volcanic fields, probably related to magma feeding fractures with en echelon arrangement. No age progression is observed along these alignments. We propose that a NNW-trending rift may have controlled the eruption from Pliocene to early Pleistocene and a dextral transpression stress field may have influenced the volcanism from middle Pleistocene to Holocene. We suggest that the Pliocene and early Pleistocene volcanism is associated with far effect of the India-Eurasia collision, while the middle Pleistocene to Holocene volcanism in WVB may have resulted from interaction between the India-Eurasia collision and the subduction of the Pacific plate.","impression_tracking_id":null,"owner":{"id":89685072,"first_name":"Haibo","middle_initials":null,"last_name":"Zou","page_name":"HaiboZou","domain_name":"auburn","created_at":"2018-08-29T11:15:27.832-07:00","display_name":"Haibo Zou","url":"https://auburn.academia.edu/HaiboZou"},"attachments":[{"id":85991617,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/85991617/thumbnails/1.jpg","file_name":"5oeoPO6oahQ9.pdf","download_url":"https://www.academia.edu/attachments/85991617/download_file","bulk_download_file_name":"Two_episodes_of_volcanism_in_the_Wudalia.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/85991617/5oeoPO6oahQ9-libre.pdf?1652680119=\u0026response-content-disposition=attachment%3B+filename%3DTwo_episodes_of_volcanism_in_the_Wudalia.pdf\u0026Expires=1744340798\u0026Signature=GyiLePXHFmSQovzH270oQ7Q3DwWmfLsElgikNfLq~GvYw2vS0Fi14bBj4yRkpsltZ9XIbNN-i7qvF035QxTiVbBtUAHiwE-CgfUiQ7KmovDEajh0QpIyZEq8~ZjfWBxUMBCFpbrY7aiu9LvsoaC8-F2EAq1Feuvu1MRgVahA-SMTOJfStBfp3aoeKJcpU7yUyfMg0MzQXlBZ29MH26bslfM0ceHq2I1bH4868CUUMXNfR53ma-cSWr5zsTYUSxxIELP8LBuGbtuA1HCccDMQA9fIT4KUh2f~jS-Y9-faCrZB7UGkPKe8Wo6KDIhMTAMj52dlr5Rej5vWOX8mN~vHJg__\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":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":14228,"name":"Geochronology","url":"https://www.academia.edu/Documents/in/Geochronology"}],"urls":[{"id":20488060,"url":"http://api.elsevier.com/content/article/PII:S037702731400256X?httpAccept=text/xml"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (true) { Aedu.setUpFigureCarousel('profile-work-79193462-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193461"><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/79193461/Neoproterozoic_sedimentary_basin_evolution_in_southwestern_Tarim_NW_China_New_evidence_from_field_observations_detrital_zircon_U_Pb_ages_and_Hf_isotope_compositions"><img alt="Research paper thumbnail of Neoproterozoic sedimentary basin evolution in southwestern Tarim, NW China: New evidence from field observations, detrital zircon U–Pb ages and Hf isotope compositions" class="work-thumbnail" src="https://attachments.academia-assets.com/85991616/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/79193461/Neoproterozoic_sedimentary_basin_evolution_in_southwestern_Tarim_NW_China_New_evidence_from_field_observations_detrital_zircon_U_Pb_ages_and_Hf_isotope_compositions">Neoproterozoic sedimentary basin evolution in southwestern Tarim, NW China: New evidence from field observations, detrital zircon U–Pb ages and Hf isotope compositions</a></div><div class="wp-workCard_item"><span>Precambrian Research</span><span>, 2016</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Sedimentary basin evolution is intimately related to tectonic background and thus can serve as on...</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">Sedimentary basin evolution is intimately related to tectonic background and thus can serve as one of the most important indicators in deciphering the regional tectonic evolution process. Neoproterozoic volcanic-sedimentary sequences are well preserved along the southwestern margin of the Tarim Block in NW China and</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="cad59cc27392a0f8d4ae847d98e6852c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":85991616,"asset_id":79193461,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/85991616/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193461"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193461"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193461; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193461]").text(description); $(".js-view-count[data-work-id=79193461]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193461; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193461']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "cad59cc27392a0f8d4ae847d98e6852c" } } $('.js-work-strip[data-work-id=79193461]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193461,"title":"Neoproterozoic sedimentary basin evolution in southwestern Tarim, NW China: New evidence from field observations, detrital zircon U–Pb ages and Hf isotope compositions","translated_title":"","metadata":{"publisher":"Elsevier BV","grobid_abstract":"Sedimentary basin evolution is intimately related to tectonic background and thus can serve as one of the most important indicators in deciphering the regional tectonic evolution process. 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The spinels of the ultramafic rocks have very high Cr' [lo0 x Cr/(Cr + Al) = 0.851, and the gabbros contain abundant calcic plagioclases, Fe-Ti oxides and amphiboles, are are rich in TiOz, total iron, and light rare earth elements. It is probable that the mafic-ultramafic rocks are originally formed at a local extensional environment on the continental side of the subduction zone and eventually thrust in the compressional environment onto the Jurassic volcanic rocks or metamorphic rocks in the Yenshan (upper Triassic-upper Cretaceous) orogen. It is likely that the Yenshan subduction zone exists along the East Taiwan longitudinal valley rather than the ChangleNanao fracture zone. The pre-Cenozoic tectonic evolution of the eastern Fujian coastal area and Taiwan is also discussed.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="ed6870a1964db35a28b87cfa55d10209" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":85991619,"asset_id":79193460,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/85991619/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193460"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193460"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193460; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193460]").text(description); $(".js-view-count[data-work-id=79193460]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193460; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193460']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "ed6870a1964db35a28b87cfa55d10209" } } $('.js-work-strip[data-work-id=79193460]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193460,"title":"A mafic-ultramafic rock belt in the Fujian coastal area, southeastern China: a geochemical study","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_title_tag":"Mafic-Ultramafic Rocks in Fujian, China","grobid_abstract":"Geological and geochemical evidence supports the non-ophiolitic origin of the mafic-ultramafic rocks exclusively exposed along the Changle-Nanao fracture zone in the Fujian coastal area, southeastern China. The spinels of the ultramafic rocks have very high Cr' [lo0 x Cr/(Cr + Al) = 0.851, and the gabbros contain abundant calcic plagioclases, Fe-Ti oxides and amphiboles, are are rich in TiOz, total iron, and light rare earth elements. It is probable that the mafic-ultramafic rocks are originally formed at a local extensional environment on the continental side of the subduction zone and eventually thrust in the compressional environment onto the Jurassic volcanic rocks or metamorphic rocks in the Yenshan (upper Triassic-upper Cretaceous) orogen. It is likely that the Yenshan subduction zone exists along the East Taiwan longitudinal valley rather than the ChangleNanao fracture zone. The pre-Cenozoic tectonic evolution of the eastern Fujian coastal area and Taiwan is also discussed.","publication_date":{"day":null,"month":null,"year":1995,"errors":{}},"publication_name":"Journal of Southeast Asian Earth Sciences","grobid_abstract_attachment_id":85991619},"translated_abstract":null,"internal_url":"https://www.academia.edu/79193460/A_mafic_ultramafic_rock_belt_in_the_Fujian_coastal_area_southeastern_China_a_geochemical_study","translated_internal_url":"","created_at":"2022-05-15T22:31:50.380-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":89685072,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":85991619,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/85991619/thumbnails/1.jpg","file_name":"0743-9547_2895_2900014-320220516-1-p87l2d.pdf","download_url":"https://www.academia.edu/attachments/85991619/download_file","bulk_download_file_name":"A_mafic_ultramafic_rock_belt_in_the_Fuji.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/85991619/0743-9547_2895_2900014-320220516-1-p87l2d-libre.pdf?1652680126=\u0026response-content-disposition=attachment%3B+filename%3DA_mafic_ultramafic_rock_belt_in_the_Fuji.pdf\u0026Expires=1744340798\u0026Signature=Vq0NhP67IK7Fr4FcW6UU9GoRQ9DGLEPyg0InDjQr7Loi4HQQsJEZqj0r-IyjtdieM-2TERNtiqZINMxDZLcERt8106kGdBLtT~kXev~e2xqnmR8-XqCb6hj7Yvpo4k6t2TozZFH0pv-ysLesejNQ8svXi7Vl1pt2V05sC2xMUQEJzbwaP4HnVsiIN63PzpTwRhtNZ0jCCBQbXx~7O1RkvwrNFk9-m-C6Lhk9yaF4id~QvbHp08~1nBPPo1TLZRokYI4KACjbexJHgvW21kn31V9dcMuugNp2jlWY5Djnm2tJJOzFmncDiLFeODFXfuGRC01cJX8nGXdCFra3sK9D1Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"A_mafic_ultramafic_rock_belt_in_the_Fujian_coastal_area_southeastern_China_a_geochemical_study","translated_slug":"","page_count":7,"language":"en","content_type":"Work","summary":"Geological and geochemical evidence supports the non-ophiolitic origin of the mafic-ultramafic rocks exclusively exposed along the Changle-Nanao fracture zone in the Fujian coastal area, southeastern China. 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The origin of columnar jointing had been explained by the traditional hypothesis of cooling-contraction for a long time. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-79193464-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193463"><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/79193463/U_series_ages_of_young_volcanoes_from_the_Southeastern_Tibetan_Plateau_Holocene_eruptions_and_magma_evolution_timescales"><img alt="Research paper thumbnail of U-series ages of young volcanoes from the Southeastern Tibetan Plateau: Holocene eruptions and magma evolution timescales" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">U-series ages of young volcanoes from the Southeastern Tibetan Plateau: Holocene eruptions and magma evolution timescales</div><div class="wp-workCard_item"><span>Lithos</span><span>, 2020</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic e...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193463"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193463"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193463; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193463]").text(description); $(".js-view-count[data-work-id=79193463]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193463; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193463']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=79193463]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193463,"title":"U-series ages of young volcanoes from the Southeastern Tibetan Plateau: Holocene eruptions and magma evolution timescales","translated_title":"","metadata":{"abstract":"Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.","publisher":"Elsevier BV","publication_date":{"day":null,"month":null,"year":2020,"errors":{}},"publication_name":"Lithos"},"translated_abstract":"Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.","internal_url":"https://www.academia.edu/79193463/U_series_ages_of_young_volcanoes_from_the_Southeastern_Tibetan_Plateau_Holocene_eruptions_and_magma_evolution_timescales","translated_internal_url":"","created_at":"2022-05-15T22:31:50.770-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":89685072,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"U_series_ages_of_young_volcanoes_from_the_Southeastern_Tibetan_Plateau_Holocene_eruptions_and_magma_evolution_timescales","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Abstract The Tengchong volcanic field in southwestern China represents rare Quaternary volcanic eruptions and associated active geothermal activities on the southeastern margin of the Tibetan plateau. The reported eruption ages for the 3 youngest Tengchong volcanoes (Heikongshan, Dayingshan, Maanshan) are highly variable (3.0–482 ka) because of the challenge to accurately and precisely date young volcanic rocks by radiometric methods. Here we use high-resolution 238U-230Th-226Ra disequilibria to constrain the eruption ages and magma evolution timescales. All 3 young volcanoes exhibit whole-rock (226Ra/230Th) disequilibrium ranging from 1.27 to 1.71, indicating eruption ages of 230Th ages of zircons from Heikongshan, Dayingshan, and Maanshan. Zircon age populations are 54.6 ± 13 ka and 94.9 ± 4.1 ka for Heikongshan, 59.6 ± 5.8 and 90.1 ± 8.4 for Dayingshan, and 53.8 ± 8.7 ka and 76.5 ± 11 ka for Maanshan. Magma residence times for all 3 volcanoes are ~50 kyr for a shallow stage and 85 kyr for a deep stage in a two-stage magma chamber system below Tengchong. The similar zircon age distributions for the 3 volcanoes from Tengchong indicate simultaneous magmatism at 90 ka and 55 ka and imply interconnected nature of these volcanoes.","impression_tracking_id":null,"owner":{"id":89685072,"first_name":"Haibo","middle_initials":null,"last_name":"Zou","page_name":"HaiboZou","domain_name":"auburn","created_at":"2018-08-29T11:15:27.832-07:00","display_name":"Haibo Zou","url":"https://auburn.academia.edu/HaiboZou"},"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"}],"urls":[{"id":20488061,"url":"https://api.elsevier.com/content/article/PII:S0024493720302802?httpAccept=text/xml"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-79193463-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193462"><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/79193462/Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities"><img alt="Research paper thumbnail of Two episodes of volcanism in the Wudalianchi volcanic belt, NE China: Evidence for tectonic controls on volcanic activities" class="work-thumbnail" src="https://attachments.academia-assets.com/85991617/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/79193462/Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities">Two episodes of volcanism in the Wudalianchi volcanic belt, NE China: Evidence for tectonic controls on volcanic activities</a></div><div class="wp-workCard_item"><span>Journal of Volcanology and Geothermal Research</span><span>, 2014</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volca...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volcanoes in Menlu River area, Keluo, Wudalianchi and Erkeshan. K-Ar radiometric dating suggests two episodes of volcanism in the WVB. Specifically, the Pliocene to early Pleistocene volcanism is distributed only in the northern part of WVB, whereas middle Pleistocene to Holocene volcanism occurred over the entire WVB. Geomorphological analyses further delineate four northeast-striking linear alignments of cones in the Wudalianchi and Keluo volcanic fields, probably related to magma feeding fractures with en echelon arrangement. No age progression is observed along these alignments. We propose that a NNW-trending rift may have controlled the eruption from Pliocene to early Pleistocene and a dextral transpression stress field may have influenced the volcanism from middle Pleistocene to Holocene. We suggest that the Pliocene and early Pleistocene volcanism is associated with far effect of the India-Eurasia collision, while the middle Pleistocene to Holocene volcanism in WVB may have resulted from interaction between the India-Eurasia collision and the subduction of the Pacific plate.</span></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-79193462-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-79193462-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037619/figure-1-distribution-of-cenozoic-volcanic-rocks-in-ne-asia"><img alt="Fig. 1. Distribution of Cenozoic volcanic rocks in NE Asia. Modified from Ren et al., 2002. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_001.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037633/figure-2-distribution-of-volcanic-rocks-in-wvb-erkeshan"><img alt="Fig. 2. Distribution of volcanic rocks in WVB 1 — Erkeshan volcanic field, 2 — Wudalianchi volcanic field, 3 — Keluo volcanic field, 4 — Menlu river volcanic field, a — Nenjiang fault, b — Nemuoer fault, c — Sunwu fault. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_002.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037640/figure-3-geological-map-of-the-wudalianchi-volcanic-field"><img alt="Fig. 3. Geological map of the Wudalianchi volcanic field. Most of the volcanic products formed since the middle Pleistocene, except for Laoshantou. Two Holocene volcanoes, Laoheisha and Huoshaoshan, are in the middle of the field. Three cone alignment lines are sub-parallel to each other. Whole-rock K-Ar dating has been undertaken to constrain the timing of volcanism in the WVB. Eight samples are selected according to their geographical location, freshness and content of phenocryst. The K-Ar dating experiments were performed in the Geochronology Laboratory of the Institute of Geology, China Earthquake Administra- tion. Rock samples were crushed and sorted to grains size between 0.4 We collected samples in the study areas during three field seasons, and selected the samples to cover a wide range in ages and locations. All the samples in WVB are collected from fresh lava flows. These samples are porphyritic, with a phenocryst content of less than 5%. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_003.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037653/figure-4-geology-map-of-keluo-volcanic-field-the-pliocene"><img alt="Fig. 4. Geology map of Keluo volcanic field. The Pliocene and early Pleistocene volcanoes are in the periphery of the field. However, volcanoes formed in the middle of the field since th middle Pleistocene. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_004.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037668/figure-5-comparison-of-volcanoes-formed-in-two-episode"><img alt="Fig. 5. A comparison of volcanoes formed in two episode volcanism. A — Heishan volcano in Keluo field, B — section in Heishan volcano, C — Dayishan in Keluo field, D — section of Dayishan cone. Heishan shows a gentle slope and large volume and it is made up of lava. In contrast, Dayishan volcano has a volcanic cone, featuring a relatively steep slope and small volume, and it is made up of lapilli. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_005.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037684/figure-6-volcanic-height-vs-volcanic-base-diameter-volcanoes"><img alt="Fig. 6. Volcanic height vs. volcanic base diameter. Volcanoes in two episodes show an ap- parent difference in geomorphology features. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_006.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037699/figure-7-ig-vent-centers-of-cone-and-regression-lines-the"><img alt="‘ig. 7. Vent centers of cone and regression lines. The vent center points of WVB trends NNW, but the four alignment lines of the vent center points in Wudalianchi and Keluo tren NE-NE. The breaching of cone rim is one of the most common morphological features of basaltic volcanoes. The breaching azimuths in cones are commonly affected by the strike and dip of fractures feeding magma Previous study by satellite imaging of the Wudalianchi field indicat- ed that regional faults or lineaments trending display three directions (NE, NW, and EW) and the volcanoes are located at the intersections of these three lineament groups (Feng and Whitford-Stark, 1986). " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_007.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037713/figure-8-frequency-of-azimuths-in-cone-breaching-cones-of"><img alt="Fig. 8. Frequency of azimuths in cone breaching. Cones of Wudalianchi and Keluo show preferred breaching azimuths of NE and NNW striking In this paper, however, significant differences between the two episodes of volcanism are identified. The first episode of volcanism is characterized by effusive eruption and generated large shield-like volcanoes composed of lava flows. In comparison, the second episode of volcanism is characterized by Strombolian eruption and produced cinder cones, with NE-striking fracture system co-existing with NNW- striking volcanic belt. According to the simultaneous changes of volcanic episodes and tectonic reorganization, we propose a new model for the origin of the WVB that emphasizes the tectonic control on volcanism (Fig. 9). During Pliocene and early Pleistocene, a NNW rift was formed in northern Songliao Basin, resulting in NNW-striking dispersed distribution of lava flows in the WVB. Since the middle Pleistocene, a NNW-trending dextral transpression stress regime (parallel to T;) controlled the volca- nism, resulting in en echelon arrangement of NNE-trending fractures " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_008.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037726/figure-9-model-for-tectonic-control-on-volcanism-in-wvb-two"><img alt="Fig. 9. Model for tectonic control on volcanism in WVB. Two episodes of volcanism are consistent with two different tectonic settings, Welfare Research Institute of Geology China Earthquake Administration (Grant No. IGCEA1102), National Natural Science Foundation of China (NSFC Grant No. 41172305, 41072250), and the China Scholarship Council. We thank two anonymous reviewers and journal editor Lionel Wilson for their constructive reviews that have significantly improved the quality of this paper. (parallel too1) in the deep lithosphere. These fractures reach deep lithosphere, triggering decompression melting of mantle source rocks. The magmas ascend through these fractures, forming NE-oriented volcanic alignments. It is noteworthy that similar two-episode age distribution also occurs in Nuomin River volcanic field and Halaha-Chaoer River field in the NE China, and even in the Datong volcanic field in the North China Craton (Xu et al., 2005; Fan et al., 2011, 2012; Zhao et al., 2013, 2014). Moreover, rapid deformation and uplift of the NE Tibetan Plateau oc- curred since the middle Pleistocene (Liu et al., 2010). All these simulta- neous changes at ~1 Ma may imply the tectonic reorganization in the late stage of Early Pleistocene occurred not only in the WVB, but also likely in other volcanic fields in eastern China and even in Tibet. The cause for the tectonic reorganization is still unclear. However, since the India-Eurasian collision and the Pacific subduction have dominated the Cenozoic tectonic evolution of China (Tapponnier et al., 1986; Ye et al., 1987; Flower et al., 1998), the changes of convergence rates of India-Eurasia and Pacific-Eurasia may lead to the changes of stress fields (Ren et al., 2002). Assuming the changes of convergence rates control the tectonic reorganization, in our new model, the first episode volca- nism occurred during the period when the South-north extrusion and East-west extension (India-Eurasia collision) may have the dominant influence on NE China. Since the middle Pleistocene, the second episode volcanism in WVB and the East-west compression and dextral strike- slip form under the dominant influence from the Pacific-Eurasia sub- duction. During the second episode, the India-Eurasia collision may give way to the Pacific-Eurasia subduction as the dominant tectonic control in NE China. This transformation may take place in the early Pleistocene time. " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/figure_009.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037745/table-1-parameters-used-in-calculation-yr-ne-yr-np-yr-atom"><img alt="Parameters used in calculation:\ = 5.543 x 107! yr, Ne = 0.581 x 107!° yr~!, Np, = 4.962 x 107 1° yr", 4° K/K = 1.167 x 10~4 (atom ratio). The data marked by asterisks a from Liu et al. (2001). K-Ar isotopic dates of volcanic rocks in the Wudalianchi volcanic belt. Table 1 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_001.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037760/table-2-means-data-is-not-available-for-cones-or-were"><img alt="n.a. Means data is not available for cones or were destroyed by mining. Main characteristics of volcanoes formed in the first episode of volcanism. Table 2 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_002.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037776/table-3-main-characteristics-of-four-alignments-of-vent"><img alt="Main characteristics of four alignments of vent centers and cones in the second episode of volcanism. n.a. Means data is not available for cones or were destroyed by mining. Wco = the base diameter of cone; Hco = the height of cone; Wcr = the crater diameter. Table 3 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_003.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037792/table-4-parameters-of-volcanic-cones-in-the-wudalianchi"><img alt="Parameters of volcanic cones in the Wudalianchi volcanic belt. Table 4 " class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_004.jpg" width="114" height="68" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/52037806/table-5-two-episodes-of-volcanism-in-the-wudalianchi"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/85991617/table_005.jpg" width="114" height="68" /></a></figure></div><div class="next-slide-container js-next-button-container"><button aria-label="Next" class="carousel-navigation-button js-profile-work-79193462-figures-next"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_forward_ios</span></button></div></div></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="7adacd069a26e3922e54691a59d1ba53" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":85991617,"asset_id":79193462,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/85991617/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193462"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193462"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193462; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193462]").text(description); $(".js-view-count[data-work-id=79193462]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193462; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193462']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "7adacd069a26e3922e54691a59d1ba53" } } $('.js-work-strip[data-work-id=79193462]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193462,"title":"Two episodes of volcanism in the Wudalianchi volcanic belt, NE China: Evidence for tectonic controls on volcanic activities","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_title_tag":"Tectonic Controls on Wudalianchi Volcanism","grobid_abstract":"The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volcanoes in Menlu River area, Keluo, Wudalianchi and Erkeshan. K-Ar radiometric dating suggests two episodes of volcanism in the WVB. Specifically, the Pliocene to early Pleistocene volcanism is distributed only in the northern part of WVB, whereas middle Pleistocene to Holocene volcanism occurred over the entire WVB. Geomorphological analyses further delineate four northeast-striking linear alignments of cones in the Wudalianchi and Keluo volcanic fields, probably related to magma feeding fractures with en echelon arrangement. No age progression is observed along these alignments. We propose that a NNW-trending rift may have controlled the eruption from Pliocene to early Pleistocene and a dextral transpression stress field may have influenced the volcanism from middle Pleistocene to Holocene. We suggest that the Pliocene and early Pleistocene volcanism is associated with far effect of the India-Eurasia collision, while the middle Pleistocene to Holocene volcanism in WVB may have resulted from interaction between the India-Eurasia collision and the subduction of the Pacific plate.","publication_date":{"day":null,"month":null,"year":2014,"errors":{}},"publication_name":"Journal of Volcanology and Geothermal Research","grobid_abstract_attachment_id":85991617},"translated_abstract":null,"internal_url":"https://www.academia.edu/79193462/Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities","translated_internal_url":"","created_at":"2022-05-15T22:31:50.619-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":89685072,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":85991617,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/85991617/thumbnails/1.jpg","file_name":"5oeoPO6oahQ9.pdf","download_url":"https://www.academia.edu/attachments/85991617/download_file","bulk_download_file_name":"Two_episodes_of_volcanism_in_the_Wudalia.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/85991617/5oeoPO6oahQ9-libre.pdf?1652680119=\u0026response-content-disposition=attachment%3B+filename%3DTwo_episodes_of_volcanism_in_the_Wudalia.pdf\u0026Expires=1744340798\u0026Signature=GyiLePXHFmSQovzH270oQ7Q3DwWmfLsElgikNfLq~GvYw2vS0Fi14bBj4yRkpsltZ9XIbNN-i7qvF035QxTiVbBtUAHiwE-CgfUiQ7KmovDEajh0QpIyZEq8~ZjfWBxUMBCFpbrY7aiu9LvsoaC8-F2EAq1Feuvu1MRgVahA-SMTOJfStBfp3aoeKJcpU7yUyfMg0MzQXlBZ29MH26bslfM0ceHq2I1bH4868CUUMXNfR53ma-cSWr5zsTYUSxxIELP8LBuGbtuA1HCccDMQA9fIT4KUh2f~jS-Y9-faCrZB7UGkPKe8Wo6KDIhMTAMj52dlr5Rej5vWOX8mN~vHJg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Two_episodes_of_volcanism_in_the_Wudalianchi_volcanic_belt_NE_China_Evidence_for_tectonic_controls_on_volcanic_activities","translated_slug":"","page_count":11,"language":"en","content_type":"Work","summary":"The NNW striking Wudalianchi Cenozoic volcanic belt (WVB) in NE China is mainly composed of volcanoes in Menlu River area, Keluo, Wudalianchi and Erkeshan. K-Ar radiometric dating suggests two episodes of volcanism in the WVB. Specifically, the Pliocene to early Pleistocene volcanism is distributed only in the northern part of WVB, whereas middle Pleistocene to Holocene volcanism occurred over the entire WVB. Geomorphological analyses further delineate four northeast-striking linear alignments of cones in the Wudalianchi and Keluo volcanic fields, probably related to magma feeding fractures with en echelon arrangement. No age progression is observed along these alignments. We propose that a NNW-trending rift may have controlled the eruption from Pliocene to early Pleistocene and a dextral transpression stress field may have influenced the volcanism from middle Pleistocene to Holocene. We suggest that the Pliocene and early Pleistocene volcanism is associated with far effect of the India-Eurasia collision, while the middle Pleistocene to Holocene volcanism in WVB may have resulted from interaction between the India-Eurasia collision and the subduction of the Pacific plate.","impression_tracking_id":null,"owner":{"id":89685072,"first_name":"Haibo","middle_initials":null,"last_name":"Zou","page_name":"HaiboZou","domain_name":"auburn","created_at":"2018-08-29T11:15:27.832-07:00","display_name":"Haibo Zou","url":"https://auburn.academia.edu/HaiboZou"},"attachments":[{"id":85991617,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/85991617/thumbnails/1.jpg","file_name":"5oeoPO6oahQ9.pdf","download_url":"https://www.academia.edu/attachments/85991617/download_file","bulk_download_file_name":"Two_episodes_of_volcanism_in_the_Wudalia.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/85991617/5oeoPO6oahQ9-libre.pdf?1652680119=\u0026response-content-disposition=attachment%3B+filename%3DTwo_episodes_of_volcanism_in_the_Wudalia.pdf\u0026Expires=1744340798\u0026Signature=GyiLePXHFmSQovzH270oQ7Q3DwWmfLsElgikNfLq~GvYw2vS0Fi14bBj4yRkpsltZ9XIbNN-i7qvF035QxTiVbBtUAHiwE-CgfUiQ7KmovDEajh0QpIyZEq8~ZjfWBxUMBCFpbrY7aiu9LvsoaC8-F2EAq1Feuvu1MRgVahA-SMTOJfStBfp3aoeKJcpU7yUyfMg0MzQXlBZ29MH26bslfM0ceHq2I1bH4868CUUMXNfR53ma-cSWr5zsTYUSxxIELP8LBuGbtuA1HCccDMQA9fIT4KUh2f~jS-Y9-faCrZB7UGkPKe8Wo6KDIhMTAMj52dlr5Rej5vWOX8mN~vHJg__\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":408,"name":"Geomorphology","url":"https://www.academia.edu/Documents/in/Geomorphology"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":14228,"name":"Geochronology","url":"https://www.academia.edu/Documents/in/Geochronology"}],"urls":[{"id":20488060,"url":"http://api.elsevier.com/content/article/PII:S037702731400256X?httpAccept=text/xml"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (true) { Aedu.setUpFigureCarousel('profile-work-79193462-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193461"><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/79193461/Neoproterozoic_sedimentary_basin_evolution_in_southwestern_Tarim_NW_China_New_evidence_from_field_observations_detrital_zircon_U_Pb_ages_and_Hf_isotope_compositions"><img alt="Research paper thumbnail of Neoproterozoic sedimentary basin evolution in southwestern Tarim, NW China: New evidence from field observations, detrital zircon U–Pb ages and Hf isotope compositions" class="work-thumbnail" src="https://attachments.academia-assets.com/85991616/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/79193461/Neoproterozoic_sedimentary_basin_evolution_in_southwestern_Tarim_NW_China_New_evidence_from_field_observations_detrital_zircon_U_Pb_ages_and_Hf_isotope_compositions">Neoproterozoic sedimentary basin evolution in southwestern Tarim, NW China: New evidence from field observations, detrital zircon U–Pb ages and Hf isotope compositions</a></div><div class="wp-workCard_item"><span>Precambrian Research</span><span>, 2016</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Sedimentary basin evolution is intimately related to tectonic background and thus can serve as on...</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">Sedimentary basin evolution is intimately related to tectonic background and thus can serve as one of the most important indicators in deciphering the regional tectonic evolution process. Neoproterozoic volcanic-sedimentary sequences are well preserved along the southwestern margin of the Tarim Block in NW China and</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="cad59cc27392a0f8d4ae847d98e6852c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":85991616,"asset_id":79193461,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/85991616/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193461"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193461"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193461; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193461]").text(description); $(".js-view-count[data-work-id=79193461]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193461; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193461']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "cad59cc27392a0f8d4ae847d98e6852c" } } $('.js-work-strip[data-work-id=79193461]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193461,"title":"Neoproterozoic sedimentary basin evolution in southwestern Tarim, NW China: New evidence from field observations, detrital zircon U–Pb ages and Hf isotope compositions","translated_title":"","metadata":{"publisher":"Elsevier BV","grobid_abstract":"Sedimentary basin evolution is intimately related to tectonic background and thus can serve as one of the most important indicators in deciphering the regional tectonic evolution process. 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Neoproterozoic volcanic-sedimentary sequences are well preserved along the southwestern margin of the Tarim Block in NW China and","impression_tracking_id":null,"owner":{"id":89685072,"first_name":"Haibo","middle_initials":null,"last_name":"Zou","page_name":"HaiboZou","domain_name":"auburn","created_at":"2018-08-29T11:15:27.832-07:00","display_name":"Haibo Zou","url":"https://auburn.academia.edu/HaiboZou"},"attachments":[{"id":85991616,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/85991616/thumbnails/1.jpg","file_name":"S0301926816300948.pdf","download_url":"https://www.academia.edu/attachments/85991616/download_file","bulk_download_file_name":"Neoproterozoic_sedimentary_basin_evoluti.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/85991616/S0301926816300948-libre.pdf?1652680179=\u0026response-content-disposition=attachment%3B+filename%3DNeoproterozoic_sedimentary_basin_evoluti.pdf\u0026Expires=1744340798\u0026Signature=Q92KRrhthsiqDNiBtbYxDgYmtZU7hkdIabC-XzW21S~6kX65yedWbY~Gwaqw48KBBRdTAibg~Xw36GWe3gtHdNdZK6-3mI3SSDxT7uHnyGJAZonl4EDaxwpCBbq2gmkFxE4bundRZtGdpoMlmVpx2onE~G0iOdxYoXHK6NinNsnRVAVESkM5MuKro4-guahEQKcuXPvbUPSI1m2zKxsnmD44ghPnXFjlYS96w6w~bk~Kxpuwh6EuUYHQ9i0gaq~m2HS80l74pK67urSFkikRsl7DcqAEr14Uf26O235OuKtBE4SbEG8E~tkYZsros1LBHenNp2mHZSTBjqmCYtc-Gg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":78114,"name":"Precambrian","url":"https://www.academia.edu/Documents/in/Precambrian"},{"id":206457,"name":"Zircon","url":"https://www.academia.edu/Documents/in/Zircon"}],"urls":[{"id":20488059,"url":"http://api.elsevier.com/content/article/PII:S0301926816300948?httpAccept=text/xml"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-79193461-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="79193460"><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/79193460/A_mafic_ultramafic_rock_belt_in_the_Fujian_coastal_area_southeastern_China_a_geochemical_study"><img alt="Research paper thumbnail of A mafic-ultramafic rock belt in the Fujian coastal area, southeastern China: a geochemical study" class="work-thumbnail" src="https://attachments.academia-assets.com/85991619/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/79193460/A_mafic_ultramafic_rock_belt_in_the_Fujian_coastal_area_southeastern_China_a_geochemical_study">A mafic-ultramafic rock belt in the Fujian coastal area, southeastern China: a geochemical study</a></div><div class="wp-workCard_item"><span>Journal of Southeast Asian Earth Sciences</span><span>, 1995</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Geological and geochemical evidence supports the non-ophiolitic origin of the mafic-ultramafic ro...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Geological and geochemical evidence supports the non-ophiolitic origin of the mafic-ultramafic rocks exclusively exposed along the Changle-Nanao fracture zone in the Fujian coastal area, southeastern China. The spinels of the ultramafic rocks have very high Cr' [lo0 x Cr/(Cr + Al) = 0.851, and the gabbros contain abundant calcic plagioclases, Fe-Ti oxides and amphiboles, are are rich in TiOz, total iron, and light rare earth elements. It is probable that the mafic-ultramafic rocks are originally formed at a local extensional environment on the continental side of the subduction zone and eventually thrust in the compressional environment onto the Jurassic volcanic rocks or metamorphic rocks in the Yenshan (upper Triassic-upper Cretaceous) orogen. It is likely that the Yenshan subduction zone exists along the East Taiwan longitudinal valley rather than the ChangleNanao fracture zone. The pre-Cenozoic tectonic evolution of the eastern Fujian coastal area and Taiwan is also discussed.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="ed6870a1964db35a28b87cfa55d10209" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":85991619,"asset_id":79193460,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/85991619/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="79193460"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="79193460"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 79193460; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=79193460]").text(description); $(".js-view-count[data-work-id=79193460]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 79193460; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='79193460']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "ed6870a1964db35a28b87cfa55d10209" } } $('.js-work-strip[data-work-id=79193460]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":79193460,"title":"A mafic-ultramafic rock belt in the Fujian coastal area, southeastern China: a geochemical study","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_title_tag":"Mafic-Ultramafic Rocks in Fujian, China","grobid_abstract":"Geological and geochemical evidence supports the non-ophiolitic origin of the mafic-ultramafic rocks exclusively exposed along the Changle-Nanao fracture zone in the Fujian coastal area, southeastern China. The spinels of the ultramafic rocks have very high Cr' [lo0 x Cr/(Cr + Al) = 0.851, and the gabbros contain abundant calcic plagioclases, Fe-Ti oxides and amphiboles, are are rich in TiOz, total iron, and light rare earth elements. It is probable that the mafic-ultramafic rocks are originally formed at a local extensional environment on the continental side of the subduction zone and eventually thrust in the compressional environment onto the Jurassic volcanic rocks or metamorphic rocks in the Yenshan (upper Triassic-upper Cretaceous) orogen. It is likely that the Yenshan subduction zone exists along the East Taiwan longitudinal valley rather than the ChangleNanao fracture zone. 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The origin of columnar jointing had been explained by the traditional hypothesis of cooling-contraction for a long time. 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