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overflow: hidden; text-overflow: ellipsis; -webkit-line-clamp: 3; -webkit-box-orient: vertical; }</style><div class="col-xs-12 clearfix"><div class="u-floatLeft"><h1 class="PageHeader-title u-m0x u-fs30">Metamorphism</h1><div class="u-tcGrayDark">140 Followers</div><div class="u-tcGrayDark u-mt2x">Recent papers in <b>Metamorphism</b></div></div></div></div></div></div><div class="TabbedNavigation"><div class="container"><div class="row"><div class="col-xs-12 clearfix"><ul class="nav u-m0x u-p0x list-inline u-displayFlex"><li class="active"><a href="https://www.academia.edu/Documents/in/Metamorphism">Top Papers</a></li><li><a href="https://www.academia.edu/Documents/in/Metamorphism/MostCited">Most Cited Papers</a></li><li><a href="https://www.academia.edu/Documents/in/Metamorphism/MostDownloaded">Most Downloaded Papers</a></li><li><a href="https://www.academia.edu/Documents/in/Metamorphism/MostRecent">Newest Papers</a></li><li><a class="" href="https://www.academia.edu/People/Metamorphism">People</a></li></ul></div><style type="text/css">ul.nav{flex-direction:row}@media(max-width: 567px){ul.nav{flex-direction:column}.TabbedNavigation li{max-width:100%}.TabbedNavigation li.active{background-color:var(--background-grey, #dddde2)}.TabbedNavigation li.active:before,.TabbedNavigation li.active:after{display:none}}</style></div></div></div><div class="container"><div class="row"><div class="col-xs-12"><div class="u-displayFlex"><div class="u-flexGrow1"><div class="works"><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_41718185" data-work_id="41718185" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/41718185/Remanent_magnetization_mapping_A_tool_for_greenfields_magmatic_Ni_Cu_PGE_exploration_undercover_Part_1">Remanent magnetization mapping: A tool for greenfields magmatic Ni-Cu- PGE exploration undercover: Part 1</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">There are many challenges for greenfields exploration, particularly in vast, sparsely populated, partially covered terrains, e.g., a paucity of prior exploration data, and difficulties in gaining access to land. However, in many cases... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_41718185" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">There are many challenges for greenfields exploration, particularly in vast, sparsely populated, partially covered terrains, e.g., a paucity of prior exploration data, and difficulties in gaining access to land. However, in many cases good aeromagnetic coverage is freely available, and for some styles of mineralization (e.g., magmatic Ni-Cu-PGE), aeromagnetic data alone can provide critical insights into the age, size and depth of multiple targets, across large regions, early in the exploration life cycle. This study investigates whether an understanding of remanent magnetization from three suites of mafic intrusions exposed in the Huckitta area, NT, Australia, can be utilized to provide a first pass exploration tool for exploration under shallow cover to the east. The study demonstrates that although the measured remanent magnetization vectors present were complex in some cases, the majority are sub-parallel (oriented steep down to the south), which implies a common mode of acquisition. It was found that the magnetizations were acquired during the Alice Springs Orogeny (ca 450-300 Ma), with the dominant magnetization occurring at ca 330 Ma. Therefore the magnetizations present do not relate to cooling of the parent magmas, but rather to cooling of lower crustal rocks from temperatures above the Curie point (> 580 °C) during exhumation of the host terrain. Whilst this knowledge does not allow discrimination of the three suites remotely based purely on their remanent magnetization vectors, the recognition of a common magnetization vector present in all mafic rocks does allow us to better map mafic rocks under cover, and better constrain magnetic modelling and exploration targeting, as discussed in the second paper.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/41718185" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="c8873e07585bc65bd9cc768f25a2967a" rel="nofollow" data-download="{"attachment_id":61877891,"asset_id":41718185,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/61877891/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="1395447" href="https://csiro.academia.edu/Jamesaustin">James austin</a><script data-card-contents-for-user="1395447" type="text/json">{"id":1395447,"first_name":"James","last_name":"austin","domain_name":"csiro","page_name":"Jamesaustin","display_name":"James austin","profile_url":"https://csiro.academia.edu/Jamesaustin?f_ri=172299","photo":"https://0.academia-photos.com/1395447/850799/32406503/s65_james.austin.jpg"}</script></span></span></li><li class="js-paper-rank-work_41718185 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="41718185"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 41718185, container: ".js-paper-rank-work_41718185", }); 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$(".js-view-count[data-work-id=41718185]").text(description); $(".js-view-count-work_41718185").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_41718185").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="41718185"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="23434" href="https://www.academia.edu/Documents/in/3D_Modelling_Architecture_">3D Modelling (Architecture)</a>, <script data-card-contents-for-ri="23434" type="text/json">{"id":23434,"name":"3D Modelling (Architecture)","url":"https://www.academia.edu/Documents/in/3D_Modelling_Architecture_?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="32312" href="https://www.academia.edu/Documents/in/Palaeomagnetism">Palaeomagnetism</a>, <script data-card-contents-for-ri="32312" type="text/json">{"id":32312,"name":"Palaeomagnetism","url":"https://www.academia.edu/Documents/in/Palaeomagnetism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a>, <script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="194828" href="https://www.academia.edu/Documents/in/Nickel">Nickel</a><script data-card-contents-for-ri="194828" type="text/json">{"id":194828,"name":"Nickel","url":"https://www.academia.edu/Documents/in/Nickel?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=41718185]'), work: {"id":41718185,"title":"Remanent magnetization mapping: A tool for greenfields magmatic Ni-Cu- PGE exploration undercover: Part 1","created_at":"2020-01-23T20:12:29.776-08:00","url":"https://www.academia.edu/41718185/Remanent_magnetization_mapping_A_tool_for_greenfields_magmatic_Ni_Cu_PGE_exploration_undercover_Part_1?f_ri=172299","dom_id":"work_41718185","summary":"There are many challenges for greenfields exploration, particularly in vast, sparsely populated, partially covered terrains, e.g., a paucity of prior exploration data, and difficulties in gaining access to land. However, in many cases good aeromagnetic coverage is freely available, and for some styles of mineralization (e.g., magmatic Ni-Cu-PGE), aeromagnetic data alone can provide critical insights into the age, size and depth of multiple targets, across large regions, early in the exploration life cycle. This study investigates whether an understanding of remanent magnetization from three suites of mafic intrusions exposed in the Huckitta area, NT, Australia, can be utilized to provide a first pass exploration tool for exploration under shallow cover to the east. The study demonstrates that although the measured remanent magnetization vectors present were complex in some cases, the majority are sub-parallel (oriented steep down to the south), which implies a common mode of acquisition. It was found that the magnetizations were acquired during the Alice Springs Orogeny (ca 450-300 Ma), with the dominant magnetization occurring at ca 330 Ma. Therefore the magnetizations present do not relate to cooling of the parent magmas, but rather to cooling of lower crustal rocks from temperatures above the Curie point (\u003e 580 °C) during exhumation of the host terrain. Whilst this knowledge does not allow discrimination of the three suites remotely based purely on their remanent magnetization vectors, the recognition of a common magnetization vector present in all mafic rocks does allow us to better map mafic rocks under cover, and better constrain magnetic modelling and exploration targeting, as discussed in the second paper.","downloadable_attachments":[{"id":61877891,"asset_id":41718185,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":1395447,"first_name":"James","last_name":"austin","domain_name":"csiro","page_name":"Jamesaustin","display_name":"James austin","profile_url":"https://csiro.academia.edu/Jamesaustin?f_ri=172299","photo":"https://0.academia-photos.com/1395447/850799/32406503/s65_james.austin.jpg"}],"research_interests":[{"id":23434,"name":"3D Modelling (Architecture)","url":"https://www.academia.edu/Documents/in/3D_Modelling_Architecture_?f_ri=172299","nofollow":false},{"id":32312,"name":"Palaeomagnetism","url":"https://www.academia.edu/Documents/in/Palaeomagnetism?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":194828,"name":"Nickel","url":"https://www.academia.edu/Documents/in/Nickel?f_ri=172299","nofollow":false},{"id":1396599,"name":"Ultramafic Rocks","url":"https://www.academia.edu/Documents/in/Ultramafic_Rocks?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_36475842" data-work_id="36475842" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/36475842/Structural_and_metamorphic_evolution_during_tectonic_mixing_is_the_Rocca_Canavese_Thrust_Sheet_Italian_Western_Alps_a_subduction_related_melange">Structural and metamorphic evolution during tectonic mixing: is the Rocca Canavese Thrust Sheet (Italian Western Alps) a subduction-related melange?</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">In the Sesia-Lanzo Zone (SLZ), the subunit Rocca Canavese Thrust Sheet (RCT) is characterised by a mixture of mantle- and crust-derived lithologies and can be a good candidate to be a former subduction-related mélange of the Austroalpine... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_36475842" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">In the Sesia-Lanzo Zone (SLZ), the subunit Rocca Canavese Thrust Sheet (RCT) is characterised by a mixture of mantle- and crust-derived lithologies and can be a good candidate to be a former subduction-related mélange of the Austroalpine domain. The unit consists of metapelites, metagranitoids, metabasics, metagabbro and serpentinised lherzolite lenses from metre to hundred-metre size. According to the literature, PT peak conditions for all lithologies are 0.8-1 GPa at 300-400° C, in lawsonite-blueschist facies conditions recorded during the Alpine subduction. However recent work describes different mineral assemblages for the metamorphic peak, separating rocks with lawsonite from those with jadeite. Therefore, we refined the meso and microstructural analysis of the tectonic slices of RCT and we performed a detailed thermo-barometry of different metamorphic stages in order to quantify Alpine peak conditions and P-T-d-t paths, and to test whether the RCT represents a subduction-related mélange. We focus on metagabbros, Jd-bearing and Lws-bearing glaucophanites since they have the most suitable chemistry allowing to reconstruct the complex evolution of the mixing. Metagabbros and Jd-bearing glaucophanites experienced a D1a metamorphic stage characterised by a pressure of 1.3-1.8 GPa and temperature of 450-550° C, in eclogite facies condition. Lws- bearing glaucophanites experienced a D1b metamorphic stage at a temperature <470° and pressure of ca. 1.2-1.5 GPa, in Lws-blueschist facies condition. The two tectono- metamorphic units (TMUs) were coupled together during the exhumation at D2 stage, under Ep- blueschist facies conditions. Successive evolution occurs at lower pressure, under greenschist facies conditions. D1a peak conditions are compatible with a thermal gradient between a cold and a warm subduction zone while D1b peak is recorded in a thermal gradient compatible with a cold subduction. The coupling between the two TMUs occurred under a cold thermal gradient, suggesting a still active subduction. The different origin and P-T-d-t paths of the blocks, the intense shearing experienced by all lithologies during their coupling and the abundance of serpentinites in the tectonic mixture agree with the interpretation of a subduction-related mélange for RCT, in analogy with other zones of the Alps.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/36475842" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="96dfcaca22cd213abfe2d08988d1da84" rel="nofollow" data-download="{"attachment_id":56393976,"asset_id":36475842,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/56393976/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="6604514" href="https://unimi.academia.edu/ManuelRoda">Manuel Roda</a><script data-card-contents-for-user="6604514" type="text/json">{"id":6604514,"first_name":"Manuel","last_name":"Roda","domain_name":"unimi","page_name":"ManuelRoda","display_name":"Manuel Roda","profile_url":"https://unimi.academia.edu/ManuelRoda?f_ri=172299","photo":"https://0.academia-photos.com/6604514/2628027/3053139/s65_manuel.roda.jpg"}</script></span></span></li><li class="js-paper-rank-work_36475842 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="36475842"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 36475842, container: ".js-paper-rank-work_36475842", }); 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$(".js-view-count[data-work-id=36475842]").text(description); $(".js-view-count-work_36475842").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_36475842").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="36475842"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">4</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="51914" href="https://www.academia.edu/Documents/in/Alps">Alps</a>, <script data-card-contents-for-ri="51914" type="text/json">{"id":51914,"name":"Alps","url":"https://www.academia.edu/Documents/in/Alps?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a>, <script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="238750" href="https://www.academia.edu/Documents/in/Structural_Geology_and_Tectonics">Structural Geology and Tectonics</a>, <script data-card-contents-for-ri="238750" type="text/json">{"id":238750,"name":"Structural Geology and Tectonics","url":"https://www.academia.edu/Documents/in/Structural_Geology_and_Tectonics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="333831" href="https://www.academia.edu/Documents/in/Subduction_Zones">Subduction Zones</a><script data-card-contents-for-ri="333831" type="text/json">{"id":333831,"name":"Subduction Zones","url":"https://www.academia.edu/Documents/in/Subduction_Zones?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=36475842]'), work: {"id":36475842,"title":"Structural and metamorphic evolution during tectonic mixing: is the Rocca Canavese Thrust Sheet (Italian Western Alps) a subduction-related melange?","created_at":"2018-04-23T03:14:57.502-07:00","url":"https://www.academia.edu/36475842/Structural_and_metamorphic_evolution_during_tectonic_mixing_is_the_Rocca_Canavese_Thrust_Sheet_Italian_Western_Alps_a_subduction_related_melange?f_ri=172299","dom_id":"work_36475842","summary":"In the Sesia-Lanzo Zone (SLZ), the subunit Rocca Canavese Thrust Sheet (RCT) is characterised by a mixture of mantle- and crust-derived lithologies and can be a good candidate to be a former subduction-related mélange of the Austroalpine domain. The unit consists of metapelites, metagranitoids, metabasics, metagabbro and serpentinised lherzolite lenses from metre to hundred-metre size. According to the literature, PT peak conditions for all lithologies are 0.8-1 GPa at 300-400° C, in lawsonite-blueschist facies conditions recorded during the Alpine subduction. However recent work describes different mineral assemblages for the metamorphic peak, separating rocks with lawsonite from those with jadeite. Therefore, we refined the meso and microstructural analysis of the tectonic slices of RCT and we performed a detailed thermo-barometry of different metamorphic stages in order to quantify Alpine peak conditions and P-T-d-t paths, and to test whether the RCT represents a subduction-related mélange. We focus on metagabbros, Jd-bearing and Lws-bearing glaucophanites since they have the most suitable chemistry allowing to reconstruct the complex evolution of the mixing. Metagabbros and Jd-bearing glaucophanites experienced a D1a metamorphic stage characterised by a pressure of 1.3-1.8 GPa and temperature of 450-550° C, in eclogite facies condition. Lws- bearing glaucophanites experienced a D1b metamorphic stage at a temperature \u003c470° and pressure of ca. 1.2-1.5 GPa, in Lws-blueschist facies condition. The two tectono- metamorphic units (TMUs) were coupled together during the exhumation at D2 stage, under Ep- blueschist facies conditions. Successive evolution occurs at lower pressure, under greenschist facies conditions. D1a peak conditions are compatible with a thermal gradient between a cold and a warm subduction zone while D1b peak is recorded in a thermal gradient compatible with a cold subduction. The coupling between the two TMUs occurred under a cold thermal gradient, suggesting a still active subduction. The different origin and P-T-d-t paths of the blocks, the intense shearing experienced by all lithologies during their coupling and the abundance of serpentinites in the tectonic mixture agree with the interpretation of a subduction-related mélange for RCT, in analogy with other zones of the Alps.","downloadable_attachments":[{"id":56393976,"asset_id":36475842,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":6604514,"first_name":"Manuel","last_name":"Roda","domain_name":"unimi","page_name":"ManuelRoda","display_name":"Manuel Roda","profile_url":"https://unimi.academia.edu/ManuelRoda?f_ri=172299","photo":"https://0.academia-photos.com/6604514/2628027/3053139/s65_manuel.roda.jpg"}],"research_interests":[{"id":51914,"name":"Alps","url":"https://www.academia.edu/Documents/in/Alps?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":238750,"name":"Structural Geology and Tectonics","url":"https://www.academia.edu/Documents/in/Structural_Geology_and_Tectonics?f_ri=172299","nofollow":false},{"id":333831,"name":"Subduction Zones","url":"https://www.academia.edu/Documents/in/Subduction_Zones?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_39750130" data-work_id="39750130" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/39750130/Petrology_and_40_Ar_39_Ar_dating_of_paragneisses_from_the_Devrekani_Massif_Central_Pontides_Northern_Turkey_Implications_for_the_Jurassic_high_T_metamorphism_in_an_extensional_tectonic_environment">Petrology and 40 Ar-39 Ar dating of paragneisses from the Devrekani Massif (Central Pontides, Northern Turkey): Implications for the Jurassic high-T metamorphism in an extensional tectonic environment</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Devrekani Massif in the northern part of the Central Pontides (Northern Turkey) provides important clues to the regional tectonics and geodynamic processes associated with Jurassic high grade metamorphic conditions. This study reports... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_39750130" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Devrekani Massif in the northern part of the Central Pontides (Northern Turkey) provides important clues to the regional tectonics and geodynamic processes associated with Jurassic high grade metamorphic conditions. This study reports new paragenetic assemblages, mineral compositions, whole-rock geochemistry and 40 Ar-39 Ar geochronological data from the paragneisses in the massif, and, discusses the P-T conditions and geodynamic implications of the Jurassic metamorphism during continental extension in the Central Pontides. Upper am-phibolite to lower granulite facies paragneisses form one of the main lithological units in the massif. Within these, there are five different mineral parageneses with diagnostic mineral assemblages of: quartz, K-feldspar (An 0-1 Ab 4-26 Or 73-96), plagioclase (An 18-35), biotite [X Phl : 0.28-0.57; Mg/(Mg + Fe 2+): 0.33-0.61], sillimanite, cordierite [Mg/(Mg + Fe 2+): 0.48-0.71] and garnet (Alm 43-80 Grs 0-18 Prp 5-23 And 0-4 Sps 10-33) with minor hercy-nite. Based on Na-in-Crd thermometry and GASP barometry results, the peak metamorphic conditions are 775 ± 25 °C and 6 ± 1 kbar in the massif. The field relations, petrography and bulk chemical data suggest that the paragneisses, derived from shale-wackestone and pelitic sedimentary protoliths, are typical rock lithologies of an active continental margin. They display enrichments in LILE over HFSE, coupled with negative Nb and Ti anomalies, which are geochemical signatures of subduction-related sources. It is likely that the peak meta-morphism took place during the Middle-Upper Jurassic period (ca. 174-156 Ma), suggesting that the meta-morphic rocks cooled to 300-350 °C at ca. 156 Ma. The mineral assemblages reveal that the prograde history passed from sillimanite zone conditions up to the cordierite-garnet-K-feldspar zone. The petrological and geo-chronological data indicate that the protoliths are related to multiple sources such as volcano-sedimentary successions. We conclude that the Devrekani Massif represents the products of pre-Jurassic sedimentation, and Permo-Carboniferous continental arc magmatism, overprinted by Jurassic metamorphism.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/39750130" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="f1822fdae3b79b55fe4d21e62f1dfd88" rel="nofollow" data-download="{"attachment_id":59930562,"asset_id":39750130,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/59930562/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="3727428" href="https://gumushane.academia.edu/MehmetAliG%C3%BCcer">Mehmet Ali Gücer</a><script data-card-contents-for-user="3727428" type="text/json">{"id":3727428,"first_name":"Mehmet Ali","last_name":"Gücer","domain_name":"gumushane","page_name":"MehmetAliGücer","display_name":"Mehmet Ali Gücer","profile_url":"https://gumushane.academia.edu/MehmetAliG%C3%BCcer?f_ri=172299","photo":"https://0.academia-photos.com/3727428/1336180/146910014/s65_mehmet_ali.g_cer.jpg"}</script></span></span></li><li class="js-paper-rank-work_39750130 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="39750130"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 39750130, container: ".js-paper-rank-work_39750130", }); 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$(".js-view-count[data-work-id=39750130]").text(description); $(".js-view-count-work_39750130").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_39750130").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="39750130"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">3</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="2635" href="https://www.academia.edu/Documents/in/Metamorphic_Petrology">Metamorphic Petrology</a>, <script data-card-contents-for-ri="2635" type="text/json">{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=39750130]'), work: {"id":39750130,"title":"Petrology and 40 Ar-39 Ar dating of paragneisses from the Devrekani Massif (Central Pontides, Northern Turkey): Implications for the Jurassic high-T metamorphism in an extensional tectonic environment","created_at":"2019-07-04T08:19:11.563-07:00","url":"https://www.academia.edu/39750130/Petrology_and_40_Ar_39_Ar_dating_of_paragneisses_from_the_Devrekani_Massif_Central_Pontides_Northern_Turkey_Implications_for_the_Jurassic_high_T_metamorphism_in_an_extensional_tectonic_environment?f_ri=172299","dom_id":"work_39750130","summary":"The Devrekani Massif in the northern part of the Central Pontides (Northern Turkey) provides important clues to the regional tectonics and geodynamic processes associated with Jurassic high grade metamorphic conditions. This study reports new paragenetic assemblages, mineral compositions, whole-rock geochemistry and 40 Ar-39 Ar geochronological data from the paragneisses in the massif, and, discusses the P-T conditions and geodynamic implications of the Jurassic metamorphism during continental extension in the Central Pontides. Upper am-phibolite to lower granulite facies paragneisses form one of the main lithological units in the massif. Within these, there are five different mineral parageneses with diagnostic mineral assemblages of: quartz, K-feldspar (An 0-1 Ab 4-26 Or 73-96), plagioclase (An 18-35), biotite [X Phl : 0.28-0.57; Mg/(Mg + Fe 2+): 0.33-0.61], sillimanite, cordierite [Mg/(Mg + Fe 2+): 0.48-0.71] and garnet (Alm 43-80 Grs 0-18 Prp 5-23 And 0-4 Sps 10-33) with minor hercy-nite. Based on Na-in-Crd thermometry and GASP barometry results, the peak metamorphic conditions are 775 ± 25 °C and 6 ± 1 kbar in the massif. The field relations, petrography and bulk chemical data suggest that the paragneisses, derived from shale-wackestone and pelitic sedimentary protoliths, are typical rock lithologies of an active continental margin. They display enrichments in LILE over HFSE, coupled with negative Nb and Ti anomalies, which are geochemical signatures of subduction-related sources. It is likely that the peak meta-morphism took place during the Middle-Upper Jurassic period (ca. 174-156 Ma), suggesting that the meta-morphic rocks cooled to 300-350 °C at ca. 156 Ma. The mineral assemblages reveal that the prograde history passed from sillimanite zone conditions up to the cordierite-garnet-K-feldspar zone. The petrological and geo-chronological data indicate that the protoliths are related to multiple sources such as volcano-sedimentary successions. We conclude that the Devrekani Massif represents the products of pre-Jurassic sedimentation, and Permo-Carboniferous continental arc magmatism, overprinted by Jurassic metamorphism.","downloadable_attachments":[{"id":59930562,"asset_id":39750130,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":3727428,"first_name":"Mehmet Ali","last_name":"Gücer","domain_name":"gumushane","page_name":"MehmetAliGücer","display_name":"Mehmet Ali Gücer","profile_url":"https://gumushane.academia.edu/MehmetAliG%C3%BCcer?f_ri=172299","photo":"https://0.academia-photos.com/3727428/1336180/146910014/s65_mehmet_ali.g_cer.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_31697731" data-work_id="31697731" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/31697731/Manganocummingtonite_from_the_Mesoproterozoic_Sausar_Fold_Belt_Central_India">Manganocummingtonite from the Mesoproterozoic, Sausar Fold Belt, Central India</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Manganocummingtonite occurs with spessartine, quartz and pyrolusite in the Chikmara area, Sausar fold belt, central India. Its composition is [Ca 0.3–0.35 (Mg 3.3–3.5 Mn 1.6–1.8 Fe 2+ 1.4–1.5)(Si 7.931-7.997 Al iv 0.003-0.069)O 22 (OH... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_31697731" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Manganocummingtonite occurs with spessartine, quartz and pyrolusite in the Chikmara area, Sausar fold belt, central India. Its composition is [Ca 0.3–0.35 (Mg 3.3–3.5 Mn 1.6–1.8 Fe 2+ 1.4–1.5)(Si 7.931-7.997 Al iv 0.003-0.069)O 22 (OH 1.5-2.0 F 0.0-0.5)] being fairly rich in Ca, which is indicative of metamorphic temperature in the amphibolite facies. The garnet contains 77.5% spessartine, 13% almandine and minor andradite, grossular and pyrope components. Unusually, there is no carbonate, pyroxene, pyroxmangite, rhodonite, magnetite or hematite. The available Al in the rock stabilized garnet and this mineral incorporated minor Fe 3+ present in the rock as andradite component. The manganocummingtonite–garnet pairs developed at ~600°C during amphibolite facies metamorphism in low X CO 2 system, stabilized with X Mn/(Mn+Fe 2+ +Mg) = 0.25 to 0.28 in the amphibole and 0.85 in the garnet and formed under unusually low fO 2 conditions for the Sausar region, near channelized fluids which deposited quartz may have controlled the fO 2 .</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/31697731" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="d35368132826eccaf24f42d756b544cc" rel="nofollow" data-download="{"attachment_id":52014086,"asset_id":31697731,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/52014086/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="60674932" href="https://independent.academia.edu/DillipRanjanKanungo">Dillip Ranjan Kanungo</a><script data-card-contents-for-user="60674932" type="text/json">{"id":60674932,"first_name":"Dillip Ranjan","last_name":"Kanungo","domain_name":"independent","page_name":"DillipRanjanKanungo","display_name":"Dillip Ranjan Kanungo","profile_url":"https://independent.academia.edu/DillipRanjanKanungo?f_ri=172299","photo":"https://0.academia-photos.com/60674932/27090305/25509003/s65_dillip_ranjan.kanungo.jpg"}</script></span></span></li><li class="js-paper-rank-work_31697731 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="31697731"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 31697731, container: ".js-paper-rank-work_31697731", }); 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$(".js-view-count[data-work-id=31697731]").text(description); $(".js-view-count-work_31697731").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_31697731").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="31697731"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">7</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="406" href="https://www.academia.edu/Documents/in/Geology">Geology</a>, <script data-card-contents-for-ri="406" type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="414" href="https://www.academia.edu/Documents/in/Mineralogy">Mineralogy</a>, <script data-card-contents-for-ri="414" type="text/json">{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="16023" href="https://www.academia.edu/Documents/in/Mineral_Chemistry">Mineral Chemistry</a>, <script data-card-contents-for-ri="16023" type="text/json">{"id":16023,"name":"Mineral Chemistry","url":"https://www.academia.edu/Documents/in/Mineral_Chemistry?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="16937" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry">Petrology and Geochemistry</a><script data-card-contents-for-ri="16937" type="text/json">{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=31697731]'), work: {"id":31697731,"title":"Manganocummingtonite from the Mesoproterozoic, Sausar Fold Belt, Central India","created_at":"2017-03-03T10:30:51.747-08:00","url":"https://www.academia.edu/31697731/Manganocummingtonite_from_the_Mesoproterozoic_Sausar_Fold_Belt_Central_India?f_ri=172299","dom_id":"work_31697731","summary":"Manganocummingtonite occurs with spessartine, quartz and pyrolusite in the Chikmara area, Sausar fold belt, central India. Its composition is [Ca 0.3–0.35 (Mg 3.3–3.5 Mn 1.6–1.8 Fe 2+ 1.4–1.5)(Si 7.931-7.997 Al iv 0.003-0.069)O 22 (OH 1.5-2.0 F 0.0-0.5)] being fairly rich in Ca, which is indicative of metamorphic temperature in the amphibolite facies. The garnet contains 77.5% spessartine, 13% almandine and minor andradite, grossular and pyrope components. Unusually, there is no carbonate, pyroxene, pyroxmangite, rhodonite, magnetite or hematite. The available Al in the rock stabilized garnet and this mineral incorporated minor Fe 3+ present in the rock as andradite component. The manganocummingtonite–garnet pairs developed at ~600°C during amphibolite facies metamorphism in low X CO 2 system, stabilized with X Mn/(Mn+Fe 2+ +Mg) = 0.25 to 0.28 in the amphibole and 0.85 in the garnet and formed under unusually low fO 2 conditions for the Sausar region, near channelized fluids which deposited quartz may have controlled the fO 2 .","downloadable_attachments":[{"id":52014086,"asset_id":31697731,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":60674932,"first_name":"Dillip Ranjan","last_name":"Kanungo","domain_name":"independent","page_name":"DillipRanjanKanungo","display_name":"Dillip Ranjan Kanungo","profile_url":"https://independent.academia.edu/DillipRanjanKanungo?f_ri=172299","photo":"https://0.academia-photos.com/60674932/27090305/25509003/s65_dillip_ranjan.kanungo.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=172299","nofollow":false},{"id":16023,"name":"Mineral Chemistry","url":"https://www.academia.edu/Documents/in/Mineral_Chemistry?f_ri=172299","nofollow":false},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299","nofollow":false},{"id":121772,"name":"EPMA","url":"https://www.academia.edu/Documents/in/EPMA?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":2440113,"name":"Manganese Ores","url":"https://www.academia.edu/Documents/in/Manganese_Ores?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_7479565 coauthored" data-work_id="7479565" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/7479565/Minerales_del_grupo_del_espinelo_en_metaperidotitas_de_la_faja_del_R%C3%ADo_de_Las_Tunas_Cordillera_Frontal_de_Mendoza_su_relaci%C3%B3n_con_el_metamorfismo_regional">Minerales del grupo del espinelo en metaperidotitas de la faja del Río de Las Tunas, Cordillera Frontal de Mendoza: su relación con el metamorfismo regional</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a 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u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Производство технического кремния на заводе ТОО «Tau-Ken Temir» (ТКТ) в г. Караганде (Казахстан) осуществляется путем карботермического восстановления кремния из квар-ца в дуговых руднотермических печах открытого типа пол-ной мощностью... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_38762207" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Производство технического кремния на заводе ТОО «Tau-Ken Temir» (ТКТ) в г. Караганде (Казахстан) осуществляется путем карботермического восстановления кремния из квар-ца в дуговых руднотермических печах открытого типа пол-ной мощностью 30МВА с последующим рафинированием расплава кислородом воздуха в ковшах. Кремний произво-дят в соответствии с требованиями стандарта организации, по технологическому регламенту предприятия [1]. Химиче-ский состав кремния должен соответствовать установлен-ным требованиям стандарта по содержанию кремния бо-лее 99,7% и примесей Fe, Al, Ca, Ti, P. Технический кремний применяется для производства кремнийсодержащих спла-вов, кремнийорганической продукции, полупроводниково-го кремния, также для других специальных целей. Целью работы является изучение закономерности распре-деления оксидов элементов примесей в углях месторожде-ния Шубарколь как одного из влияющих факторов, опреде-ляющих использование углей при электротермическом по-лучении технического кремния. Ключевые слова: технический кремний, кремнийсодер-жащие сплавы, углесодержащий восстановитель, элек-трическое сопротивление, зольность, мацеральный со-став, свиты, горизонты, малые элементы, возраст, ме-таморфизм, кокс.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/38762207" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2f559146e8cdcfeef767c13f13920167" rel="nofollow" data-download="{"attachment_id":58850769,"asset_id":38762207,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/58850769/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="69083756" href="https://kstu-kz.academia.edu/AliyaMaussymbayeva">Aliya Maussymbayeva</a><script data-card-contents-for-user="69083756" type="text/json">{"id":69083756,"first_name":"Aliya","last_name":"Maussymbayeva","domain_name":"kstu-kz","page_name":"AliyaMaussymbayeva","display_name":"Aliya Maussymbayeva","profile_url":"https://kstu-kz.academia.edu/AliyaMaussymbayeva?f_ri=172299","photo":"https://0.academia-photos.com/69083756/17925304/24103007/s65_aliya.maussymbayeva.jpg"}</script></span></span></li><li class="js-paper-rank-work_38762207 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="38762207"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 38762207, container: ".js-paper-rank-work_38762207", }); 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Караганде (Казахстан) осуществляется путем карботермического восстановления кремния из квар-ца в дуговых руднотермических печах открытого типа пол-ной мощностью 30МВА с последующим рафинированием расплава кислородом воздуха в ковшах. Кремний произво-дят в соответствии с требованиями стандарта организации, по технологическому регламенту предприятия [1]. Химиче-ский состав кремния должен соответствовать установлен-ным требованиям стандарта по содержанию кремния бо-лее 99,7% и примесей Fe, Al, Ca, Ti, P. Технический кремний применяется для производства кремнийсодержащих спла-вов, кремнийорганической продукции, полупроводниково-го кремния, также для других специальных целей. Целью работы является изучение закономерности распре-деления оксидов элементов примесей в углях месторожде-ния Шубарколь как одного из влияющих факторов, опреде-ляющих использование углей при электротермическом по-лучении технического кремния. Ключевые слова: технический кремний, кремнийсодер-жащие сплавы, углесодержащий восстановитель, элек-трическое сопротивление, зольность, мацеральный со-став, свиты, горизонты, малые элементы, возраст, ме-таморфизм, кокс.","downloadable_attachments":[{"id":58850769,"asset_id":38762207,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":69083756,"first_name":"Aliya","last_name":"Maussymbayeva","domain_name":"kstu-kz","page_name":"AliyaMaussymbayeva","display_name":"Aliya Maussymbayeva","profile_url":"https://kstu-kz.academia.edu/AliyaMaussymbayeva?f_ri=172299","photo":"https://0.academia-photos.com/69083756/17925304/24103007/s65_aliya.maussymbayeva.jpg"}],"research_interests":[{"id":58,"name":"Metallurgical 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href="https://www.academia.edu/31600202/Hypersaline_fluids_generated_by_high_grade_metamorphism_of_evaporites_fluid_inclusion_study_of_uranium_occurrences_in_the_Western_Zambian_Copperbelt_Online_Supplementary_Material">Hypersaline fluids generated by high-grade metamorphism of evaporites: fluid inclusion study of uranium occurrences in the Western Zambian Copperbelt - Online Supplementary Material</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/31600202" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="a196110dae03b147a8de111fe46c429c" rel="nofollow" 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type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="2406" href="https://www.academia.edu/Documents/in/Economic_Geology">Economic Geology</a>, <script data-card-contents-for-ri="2406" type="text/json">{"id":2406,"name":"Economic Geology","url":"https://www.academia.edu/Documents/in/Economic_Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="82911" href="https://www.academia.edu/Documents/in/fluid_Inclusions">fluid Inclusions</a><script data-card-contents-for-ri="82911" type="text/json">{"id":82911,"name":"fluid Inclusions","url":"https://www.academia.edu/Documents/in/fluid_Inclusions?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=31600202]'), work: {"id":31600202,"title":"Hypersaline fluids generated by high-grade metamorphism of evaporites: fluid inclusion study of uranium occurrences in the Western Zambian Copperbelt - Online Supplementary Material","created_at":"2017-02-25T02:35:26.669-08:00","url":"https://www.academia.edu/31600202/Hypersaline_fluids_generated_by_high_grade_metamorphism_of_evaporites_fluid_inclusion_study_of_uranium_occurrences_in_the_Western_Zambian_Copperbelt_Online_Supplementary_Material?f_ri=172299","dom_id":"work_31600202","summary":null,"downloadable_attachments":[{"id":51930044,"asset_id":31600202,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":2909958,"first_name":"Olivier","last_name":"Vanderhaeghe","domain_name":"univ-tlse3","page_name":"OlivierVanderhaeghe","display_name":"Olivier Vanderhaeghe","profile_url":"https://univ-tlse3.academia.edu/OlivierVanderhaeghe?f_ri=172299","photo":"https://0.academia-photos.com/2909958/956006/1198185/s65_olivier.vanderhaeghe.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":2406,"name":"Economic Geology","url":"https://www.academia.edu/Documents/in/Economic_Geology?f_ri=172299","nofollow":false},{"id":82911,"name":"fluid Inclusions","url":"https://www.academia.edu/Documents/in/fluid_Inclusions?f_ri=172299","nofollow":false},{"id":83556,"name":"Evaporites","url":"https://www.academia.edu/Documents/in/Evaporites?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":644878,"name":"Copperbelt","url":"https://www.academia.edu/Documents/in/Copperbelt?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_14048307" data-work_id="14048307" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/14048307/Metamorfismo_de_Presiones_medias_en_el_Macizo_de_Santander_Garc%C3%ADa_et_al_2005">Metamorfismo de Presiones medias en el Macizo de Santander, García et al, 2005</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/14048307" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="d828f863bf34d5050525722e388a081d" rel="nofollow" data-download="{"attachment_id":38189418,"asset_id":14048307,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/38189418/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i 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$(".js-view-count-work_14048307").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="14048307"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">3</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="10769" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="171868" href="https://www.academia.edu/Documents/in/COLLISION">COLLISION</a>, <script data-card-contents-for-ri="171868" 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2005","created_at":"2015-07-14T12:51:55.151-07:00","url":"https://www.academia.edu/14048307/Metamorfismo_de_Presiones_medias_en_el_Macizo_de_Santander_Garc%C3%ADa_et_al_2005?f_ri=172299","dom_id":"work_14048307","summary":null,"downloadable_attachments":[{"id":38189418,"asset_id":14048307,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":33068749,"first_name":"Andres","last_name":"Tarazona","domain_name":"independent","page_name":"TarazonaAndres","display_name":"Andres Tarazona","profile_url":"https://independent.academia.edu/TarazonaAndres?f_ri=172299","photo":"https://0.academia-photos.com/33068749/9818344/10941051/s65_andres.tarazona.jpg_oh_be086adba1c383f0c900cc9fdbda748a_oe_565a23f7___gda___1444765792_57dea79dfaaa7236f4e3aba63fb1236f"}],"research_interests":[{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":171868,"name":"COLLISION","url":"https://www.academia.edu/Documents/in/COLLISION?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_74483174" data-work_id="74483174" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/74483174/Metamorphism_of_the_Dizi_Series_Rocks_the_Greater_Caucasus_Petrography_Mineralogy_and_Evolution_of_Metamorphic_Assemblages">Metamorphism of the Dizi Series Rocks (the Greater Caucasus): Petrography, Mineralogy and Evolution of Metamorphic Assemblages</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Dizi Series is exposed within the Southern Slope zone of the Greater Caucasus, in the core of the Svaneti anticlinorium. It is mainly composed of terrigenous, volcanogenic and carbonate rocks faunistically dated from the Devonian to... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_74483174" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Dizi Series is exposed within the Southern Slope zone of the Greater Caucasus, in the core of the Svaneti anticlinorium. It is mainly composed of terrigenous, volcanogenic and carbonate rocks faunistically dated from the Devonian to the Triassic inclusive. Regional and contact metamorphism of the Dizi Series rocks was studied. It is stated that the degree of regional metamorphism corresponds to the chlorite-sericite subfacies of the greenschist facies, occurring at a temperature of 300–350°C and a pressure of 1.5–2.3 kbar. As a result of the action of the Middle Jurassic intrusive rock bodies, the regionally metamorphosed rocks of the Dizi Series underwent contact metamorphism. Three zones of contact metamorphism were distinguished corresponding to albite-epidote-hornfels, andalusite-biotite-muscovite-chlorite-hornfels and andalusite-biotite-muscovite-hornfels subfacies. Contact metamorphism took place at a significantly higher temperature and lower pressure than the preceding regional metamorphism. The maximum temperature of the contact metamorphism reached ≈ 570°С, while pressure varied within the range of ≈ 0.3–0.8 kbar. The evolution of rock associations of regional and contact metamorphism of the Dizi Series was studied. The fields of facies and subfacies of regional and contact metamorphism are shown in the Ps-T diagram. Three age populations of zircons were identified using U-Pb LA-ICP-MS dating of the diorite-porphyrite intrusion in the Dizi Series: Zrn1 (ca. 2200 Ma) and Zrn2 (458 ± 29 Ma) that were captured by the diorite-porphyrite magma from the ancient magmatic and metamorphic rocks of the crystalline basement, and Zrn3 (166.5 ± 4.6 Ma) that corresponds to the age of diorite-porphyrite crystallization.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/74483174" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="349d3fe3d757431dfd46d0cf2e8f3ebd" rel="nofollow" data-download="{"attachment_id":82620269,"asset_id":74483174,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/82620269/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="218666021" href="https://independent.academia.edu/JavakhishviliI">Irakli Javakhishvili</a><script data-card-contents-for-user="218666021" type="text/json">{"id":218666021,"first_name":"Irakli","last_name":"Javakhishvili","domain_name":"independent","page_name":"JavakhishviliI","display_name":"Irakli Javakhishvili","profile_url":"https://independent.academia.edu/JavakhishviliI?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_74483174 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="74483174"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 74483174, container: ".js-paper-rank-work_74483174", }); 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$(".js-view-count[data-work-id=74483174]").text(description); $(".js-view-count-work_74483174").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_74483174").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="74483174"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">4</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="94129" href="https://www.academia.edu/Documents/in/High-Temperature_Metamorphism">High-Temperature Metamorphism</a>, <script data-card-contents-for-ri="94129" type="text/json">{"id":94129,"name":"High-Temperature Metamorphism","url":"https://www.academia.edu/Documents/in/High-Temperature_Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a>, <script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="669455" href="https://www.academia.edu/Documents/in/Low-grade_metamorphism">Low-grade metamorphism</a>, <script data-card-contents-for-ri="669455" type="text/json">{"id":669455,"name":"Low-grade metamorphism","url":"https://www.academia.edu/Documents/in/Low-grade_metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="920668" href="https://www.academia.edu/Documents/in/Contact_Metamorphism">Contact Metamorphism</a><script data-card-contents-for-ri="920668" type="text/json">{"id":920668,"name":"Contact Metamorphism","url":"https://www.academia.edu/Documents/in/Contact_Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=74483174]'), work: {"id":74483174,"title":"Metamorphism of the Dizi Series Rocks (the Greater Caucasus): Petrography, Mineralogy and Evolution of Metamorphic Assemblages","created_at":"2022-03-24T11:38:26.241-07:00","url":"https://www.academia.edu/74483174/Metamorphism_of_the_Dizi_Series_Rocks_the_Greater_Caucasus_Petrography_Mineralogy_and_Evolution_of_Metamorphic_Assemblages?f_ri=172299","dom_id":"work_74483174","summary":"The Dizi Series is exposed within the Southern Slope zone of the Greater Caucasus, in the core of the Svaneti anticlinorium. It is mainly composed of terrigenous, volcanogenic and carbonate rocks faunistically dated from the Devonian to the Triassic inclusive. Regional and contact metamorphism of the Dizi Series rocks was studied. It is stated that the degree of regional metamorphism corresponds to the chlorite-sericite subfacies of the greenschist facies, occurring at a temperature of 300–350°C and a pressure of 1.5–2.3 kbar. As a result of the action of the Middle Jurassic intrusive rock bodies, the regionally metamorphosed rocks of the Dizi Series underwent contact metamorphism. Three zones of contact metamorphism were distinguished corresponding to albite-epidote-hornfels, andalusite-biotite-muscovite-chlorite-hornfels and andalusite-biotite-muscovite-hornfels subfacies. Contact metamorphism took place at a significantly higher temperature and lower pressure than the preceding regional metamorphism. The maximum temperature of the contact metamorphism reached ≈ 570°С, while pressure varied within the range of ≈ 0.3–0.8 kbar. The evolution of rock associations of regional and contact metamorphism of the Dizi Series was studied. The fields of facies and subfacies of regional and contact metamorphism are shown in the Ps-T diagram. Three age populations of zircons were identified using U-Pb LA-ICP-MS dating of the diorite-porphyrite intrusion in the Dizi Series: Zrn1 (ca. 2200 Ma) and Zrn2 (458 ± 29 Ma) that were captured by the diorite-porphyrite magma from the ancient magmatic and metamorphic rocks of the crystalline basement, and Zrn3 (166.5 ± 4.6 Ma) that corresponds to the age of diorite-porphyrite crystallization.","downloadable_attachments":[{"id":82620269,"asset_id":74483174,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":218666021,"first_name":"Irakli","last_name":"Javakhishvili","domain_name":"independent","page_name":"JavakhishviliI","display_name":"Irakli Javakhishvili","profile_url":"https://independent.academia.edu/JavakhishviliI?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":94129,"name":"High-Temperature Metamorphism","url":"https://www.academia.edu/Documents/in/High-Temperature_Metamorphism?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":669455,"name":"Low-grade metamorphism","url":"https://www.academia.edu/Documents/in/Low-grade_metamorphism?f_ri=172299","nofollow":false},{"id":920668,"name":"Contact Metamorphism","url":"https://www.academia.edu/Documents/in/Contact_Metamorphism?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_11196736" data-work_id="11196736" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/11196736/40Ar_39Ar_age_petrography_and_geochemistry_of_the_Yoncayolu_Metamorphic_Rocks_NE_Turkey_Subduction_related_metamorphism_under_greenschist_facies_conditions">40Ar-39Ar age, petrography and geochemistry of the Yoncayolu Metamorphic Rocks (NE Turkey): Subduction-related metamorphism under greenschist facies conditions</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Yoncayolu Metamorphic Rocks (YMR), exposed in the Sakarya zone (Erzincan, NE Turkey), consists mainly of greenschist rocks which are chlorite schists, muscovite-chlorite schists, metabasic rocks and lesser extent of pyhllites and... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_11196736" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Yoncayolu Metamorphic Rocks (YMR), exposed in the Sakarya zone (Erzincan, NE Turkey), consists mainly of greenschist rocks which are chlorite schists, muscovite-chlorite schists, metabasic rocks and lesser extent of pyhllites and calc-schists. All YMR are fine-grained, weakly foliated and often cut by quartz veins. The common mineral assemblage is chlorite+albite+epidote+quartz ± clinozoisite ± actinolite ± opaques. Geochemically, protoliths of the YMR resemble calc-alkaline volcanic arc rocks. The YMR have high contents of large ion lithophile elements (LILEs) and low contents of high field strength elements (HFSEs) similar to mid-ocean ridge basalt (MORB). (La/Lu)CN values are between 0.26 and 6.16. The REE patterns show slight or no Eu anomalies (EuCN/Eu* of 0.48 to 1.13), suggesting minor plagioglase fractionation. 40Ar-39Ar dating on plagioclases from the metabasic samples of the YMR gave ages of 100.8 ± 3.4 Ma (Albian) and 94.1 ± 3.3 Ma (Cenomanian), suggesting that metamorphism was related to the closure of the Neo-Tethyan Ocean. Metamorphism took place during subduction of the Neo- Tethyan Ocean between ~ 90 –70 Ma. Chlorite geothermometry yielded a temperature of 320 – 350 °C and a pressure around 4 kbar. All these findings lend support for greenschist facies metamorphic conditions during the formation of the YMR. <br /> <br />Key words: Yoncayolu Metamorphic Rocks, NE Turkey, 40Ar-39Ar age, greenschist facies, chlorite thermobarometry.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/11196736" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="8c63e65a87a184fb99eafd3ba523ab4a" rel="nofollow" data-download="{"attachment_id":36823782,"asset_id":11196736,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/36823782/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="3727428" href="https://gumushane.academia.edu/MehmetAliG%C3%BCcer">Mehmet Ali Gücer</a><script data-card-contents-for-user="3727428" type="text/json">{"id":3727428,"first_name":"Mehmet Ali","last_name":"Gücer","domain_name":"gumushane","page_name":"MehmetAliGücer","display_name":"Mehmet Ali Gücer","profile_url":"https://gumushane.academia.edu/MehmetAliG%C3%BCcer?f_ri=172299","photo":"https://0.academia-photos.com/3727428/1336180/146910014/s65_mehmet_ali.g_cer.jpg"}</script></span></span></li><li class="js-paper-rank-work_11196736 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="11196736"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 11196736, container: ".js-paper-rank-work_11196736", }); });</script></li><li class="js-percentile-work_11196736 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 11196736; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_11196736"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_11196736 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="11196736"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 11196736; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=11196736]").text(description); $(".js-view-count-work_11196736").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_11196736").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="11196736"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">4</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="16713" href="https://www.academia.edu/Documents/in/Argon_Geochronology">Argon Geochronology</a>, <script data-card-contents-for-ri="16713" type="text/json">{"id":16713,"name":"Argon Geochronology","url":"https://www.academia.edu/Documents/in/Argon_Geochronology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="103767" href="https://www.academia.edu/Documents/in/Petrography">Petrography</a>, <script data-card-contents-for-ri="103767" type="text/json">{"id":103767,"name":"Petrography","url":"https://www.academia.edu/Documents/in/Petrography?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a>, <script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="442449" href="https://www.academia.edu/Documents/in/Geochemsitry">Geochemsitry</a><script data-card-contents-for-ri="442449" type="text/json">{"id":442449,"name":"Geochemsitry","url":"https://www.academia.edu/Documents/in/Geochemsitry?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=11196736]'), work: {"id":11196736,"title":"40Ar-39Ar age, petrography and geochemistry of the Yoncayolu Metamorphic Rocks (NE Turkey): Subduction-related metamorphism under greenschist facies conditions","created_at":"2015-03-02T01:28:17.013-08:00","url":"https://www.academia.edu/11196736/40Ar_39Ar_age_petrography_and_geochemistry_of_the_Yoncayolu_Metamorphic_Rocks_NE_Turkey_Subduction_related_metamorphism_under_greenschist_facies_conditions?f_ri=172299","dom_id":"work_11196736","summary":"The Yoncayolu Metamorphic Rocks (YMR), exposed in the Sakarya zone (Erzincan, NE Turkey), consists mainly of greenschist rocks which are chlorite schists, muscovite-chlorite schists, metabasic rocks and lesser extent of pyhllites and calc-schists. All YMR are fine-grained, weakly foliated and often cut by quartz veins. The common mineral assemblage is chlorite+albite+epidote+quartz ± clinozoisite ± actinolite ± opaques. Geochemically, protoliths of the YMR resemble calc-alkaline volcanic arc rocks. The YMR have high contents of large ion lithophile elements (LILEs) and low contents of high field strength elements (HFSEs) similar to mid-ocean ridge basalt (MORB). (La/Lu)CN values are between 0.26 and 6.16. The REE patterns show slight or no Eu anomalies (EuCN/Eu* of 0.48 to 1.13), suggesting minor plagioglase fractionation. 40Ar-39Ar dating on plagioclases from the metabasic samples of the YMR gave ages of 100.8 ± 3.4 Ma (Albian) and 94.1 ± 3.3 Ma (Cenomanian), suggesting that metamorphism was related to the closure of the Neo-Tethyan Ocean. Metamorphism took place during subduction of the Neo- Tethyan Ocean between ~ 90 –70 Ma. Chlorite geothermometry yielded a temperature of 320 – 350 °C and a pressure around 4 kbar. All these findings lend support for greenschist facies metamorphic conditions during the formation of the YMR.\r\n\r\nKey words: Yoncayolu Metamorphic Rocks, NE Turkey, 40Ar-39Ar age, greenschist facies, chlorite thermobarometry.","downloadable_attachments":[{"id":36823782,"asset_id":11196736,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":3727428,"first_name":"Mehmet Ali","last_name":"Gücer","domain_name":"gumushane","page_name":"MehmetAliGücer","display_name":"Mehmet Ali Gücer","profile_url":"https://gumushane.academia.edu/MehmetAliG%C3%BCcer?f_ri=172299","photo":"https://0.academia-photos.com/3727428/1336180/146910014/s65_mehmet_ali.g_cer.jpg"}],"research_interests":[{"id":16713,"name":"Argon Geochronology","url":"https://www.academia.edu/Documents/in/Argon_Geochronology?f_ri=172299","nofollow":false},{"id":103767,"name":"Petrography","url":"https://www.academia.edu/Documents/in/Petrography?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":442449,"name":"Geochemsitry","url":"https://www.academia.edu/Documents/in/Geochemsitry?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_39936722" data-work_id="39936722" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/39936722/An_experimental_study_on_K_and_Na_incorporation_in_dravitic_tourmaline_and_insight_into_the_origin_of_diamondiferous_tourmaline_from_the_Kokchetav_Massif_Kazakhstan">An experimental study on K and Na incorporation in dravitic tourmaline and insight into the origin of diamondiferous tourmaline from the Kokchetav Massif, Kazakhstan</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/39936722" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="ed70a4111652cc34c11dcf59f64cc83b" rel="nofollow" data-download="{"attachment_id":60123781,"asset_id":39936722,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/60123781/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="2758656" href="https://nrcan-gc.academia.edu/EleanorBerryman">Eleanor Berryman</a><script data-card-contents-for-user="2758656" type="text/json">{"id":2758656,"first_name":"Eleanor","last_name":"Berryman","domain_name":"nrcan-gc","page_name":"EleanorBerryman","display_name":"Eleanor Berryman","profile_url":"https://nrcan-gc.academia.edu/EleanorBerryman?f_ri=172299","photo":"https://0.academia-photos.com/2758656/896252/19636887/s65_eleanor.berryman.jpg"}</script></span></span></li><li class="js-paper-rank-work_39936722 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="39936722"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 39936722, container: ".js-paper-rank-work_39936722", }); 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$(".js-view-count[data-work-id=39936722]").text(description); $(".js-view-count-work_39936722").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_39936722").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="39936722"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="414" href="https://www.academia.edu/Documents/in/Mineralogy">Mineralogy</a>, <script data-card-contents-for-ri="414" type="text/json">{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="54669" href="https://www.academia.edu/Documents/in/Metasomatism">Metasomatism</a>, <script data-card-contents-for-ri="54669" type="text/json">{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="163951" href="https://www.academia.edu/Documents/in/Tourmaline">Tourmaline</a>, <script data-card-contents-for-ri="163951" type="text/json">{"id":163951,"name":"Tourmaline","url":"https://www.academia.edu/Documents/in/Tourmaline?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=39936722]'), work: {"id":39936722,"title":"An experimental study on K and Na incorporation in dravitic tourmaline and insight into the origin of diamondiferous tourmaline from the Kokchetav Massif, Kazakhstan","created_at":"2019-07-26T08:03:13.187-07:00","url":"https://www.academia.edu/39936722/An_experimental_study_on_K_and_Na_incorporation_in_dravitic_tourmaline_and_insight_into_the_origin_of_diamondiferous_tourmaline_from_the_Kokchetav_Massif_Kazakhstan?f_ri=172299","dom_id":"work_39936722","summary":null,"downloadable_attachments":[{"id":60123781,"asset_id":39936722,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":2758656,"first_name":"Eleanor","last_name":"Berryman","domain_name":"nrcan-gc","page_name":"EleanorBerryman","display_name":"Eleanor Berryman","profile_url":"https://nrcan-gc.academia.edu/EleanorBerryman?f_ri=172299","photo":"https://0.academia-photos.com/2758656/896252/19636887/s65_eleanor.berryman.jpg"}],"research_interests":[{"id":414,"name":"Mineralogy","url":"https://www.academia.edu/Documents/in/Mineralogy?f_ri=172299","nofollow":false},{"id":54669,"name":"Metasomatism","url":"https://www.academia.edu/Documents/in/Metasomatism?f_ri=172299","nofollow":false},{"id":163951,"name":"Tourmaline","url":"https://www.academia.edu/Documents/in/Tourmaline?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":3041449,"name":"Structural transitions in elemental tin at ultra high pressures up to 230 GPa","url":"https://www.academia.edu/Documents/in/Structural_transitions_in_elemental_tin_at_ultra_high_pressures_up_to_230_GPa?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_6839670" data-work_id="6839670" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/6839670/Lextraction_de_mat%C3%A9riaux_argileux_%C3%A0_l%C3%A9poque_protohistorique_lexemple_du_site_arch%C3%A9ologique_de_La_Goulti%C3%A8re_%C3%A0_Chateaubourg_Ille_et_Vilaine_par_Sicard_S_Deloze_V_Morzadec_H_Nicolas_T_Seignac_H">L'extraction de matériaux argileux à l'époque protohistorique : l'exemple du site archéologique de "La Goultière" à Chateaubourg (Ille-et-Vilaine). par Sicard S., Deloze V., Morzadec H., Nicolas T., Seignac H.</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">La fouille du site a permis de caractériser une activité originale d'extraction d'argile datée du 6ème siècle ou début du 7ème siècle avant notre ère. Elle était implantée sur un point haut correspondant à un affleurement de dolérite et... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_6839670" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">La fouille du site a permis de caractériser une activité originale d'extraction d'argile datée du 6ème siècle ou début du 7ème siècle avant notre ère. Elle était implantée sur un point haut correspondant à un affleurement de dolérite et au versant sud d'une plateau s'inclinant en double pente légère, du nord vers le sud de l'emprise mais aussi de l'ouest vers l'est. <br />L'extraction de 2 types d'argile liés aux auréoles de métamorphisme qui encadrent le filon de dolérite a servi essentiellement à la fabrication de céramique, certaines ayant été rejetées après utilisation, dans les fosses utilisées secondairement comme fosses dépotoir. <br />L'intérêt de la fouille réside dans la mise en évidence d'une activité d'extraction artisanale et des techniques mises en oeuvre du fait de la spécificité du substrat géologique local.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/6839670" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="b68007b99ebdf68932837408ca01c4da" rel="nofollow" data-download="{"attachment_id":33536317,"asset_id":6839670,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/33536317/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="5014724" href="https://inrap.academia.edu/valeriedeloze">valerie deloze</a><script data-card-contents-for-user="5014724" type="text/json">{"id":5014724,"first_name":"valerie","last_name":"deloze","domain_name":"inrap","page_name":"valeriedeloze","display_name":"valerie deloze","profile_url":"https://inrap.academia.edu/valeriedeloze?f_ri=172299","photo":"https://0.academia-photos.com/5014724/2177996/18508325/s65_valerie.deloze.jpg"}</script></span></span></li><li class="js-paper-rank-work_6839670 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="6839670"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 6839670, container: ".js-paper-rank-work_6839670", }); });</script></li><li class="js-percentile-work_6839670 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 6839670; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_6839670"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_6839670 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="6839670"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 6839670; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=6839670]").text(description); $(".js-view-count-work_6839670").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_6839670").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="6839670"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="42197" href="https://www.academia.edu/Documents/in/Iron_Age">Iron Age</a>, <script data-card-contents-for-ri="42197" type="text/json">{"id":42197,"name":"Iron Age","url":"https://www.academia.edu/Documents/in/Iron_Age?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a>, <script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="237329" href="https://www.academia.edu/Documents/in/Extraction_Techniques">Extraction Techniques</a>, <script data-card-contents-for-ri="237329" type="text/json">{"id":237329,"name":"Extraction Techniques","url":"https://www.academia.edu/Documents/in/Extraction_Techniques?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="1205716" href="https://www.academia.edu/Documents/in/Clay_Quarry">Clay Quarry</a><script data-card-contents-for-ri="1205716" type="text/json">{"id":1205716,"name":"Clay Quarry","url":"https://www.academia.edu/Documents/in/Clay_Quarry?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=6839670]'), work: {"id":6839670,"title":"L'extraction de matériaux argileux à l'époque protohistorique : l'exemple du site archéologique de \"La Goultière\" à Chateaubourg (Ille-et-Vilaine). par Sicard S., Deloze V., Morzadec H., Nicolas T., Seignac H.","created_at":"2014-04-22T19:24:03.395-07:00","url":"https://www.academia.edu/6839670/Lextraction_de_mat%C3%A9riaux_argileux_%C3%A0_l%C3%A9poque_protohistorique_lexemple_du_site_arch%C3%A9ologique_de_La_Goulti%C3%A8re_%C3%A0_Chateaubourg_Ille_et_Vilaine_par_Sicard_S_Deloze_V_Morzadec_H_Nicolas_T_Seignac_H?f_ri=172299","dom_id":"work_6839670","summary":"La fouille du site a permis de caractériser une activité originale d'extraction d'argile datée du 6ème siècle ou début du 7ème siècle avant notre ère. Elle était implantée sur un point haut correspondant à un affleurement de dolérite et au versant sud d'une plateau s'inclinant en double pente légère, du nord vers le sud de l'emprise mais aussi de l'ouest vers l'est.\r\nL'extraction de 2 types d'argile liés aux auréoles de métamorphisme qui encadrent le filon de dolérite a servi essentiellement à la fabrication de céramique, certaines ayant été rejetées après utilisation, dans les fosses utilisées secondairement comme fosses dépotoir.\r\nL'intérêt de la fouille réside dans la mise en évidence d'une activité d'extraction artisanale et des techniques mises en oeuvre du fait de la spécificité du substrat géologique local.\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n\r\n","downloadable_attachments":[{"id":33536317,"asset_id":6839670,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":5014724,"first_name":"valerie","last_name":"deloze","domain_name":"inrap","page_name":"valeriedeloze","display_name":"valerie deloze","profile_url":"https://inrap.academia.edu/valeriedeloze?f_ri=172299","photo":"https://0.academia-photos.com/5014724/2177996/18508325/s65_valerie.deloze.jpg"}],"research_interests":[{"id":42197,"name":"Iron Age","url":"https://www.academia.edu/Documents/in/Iron_Age?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":237329,"name":"Extraction Techniques","url":"https://www.academia.edu/Documents/in/Extraction_Techniques?f_ri=172299","nofollow":false},{"id":1205716,"name":"Clay Quarry","url":"https://www.academia.edu/Documents/in/Clay_Quarry?f_ri=172299","nofollow":false},{"id":1306201,"name":"Dolérite","url":"https://www.academia.edu/Documents/in/Dolerite?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_11258536" data-work_id="11258536" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/11258536/Synoblique_convergent_and_extensional_deformation_and_metamorphism_in_the_Neoproterozoic_rocks_along_Wadi_Fatira_shear_zone_Northern_Eastern_Desert_Egypt">Synoblique convergent and extensional deformation and metamorphism in the Neoproterozoic rocks along Wadi Fatira shear zone, Northern Eastern Desert, Egypt</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Wadi Fatira area occurs at the southern margin of the Northern Eastern Desert (NED) of Egypt and is occupied by highly sheared metavolcanics tectonically alternated with banded iron formations and intruded by Barud... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_11258536" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Wadi Fatira area occurs at the southern margin of the Northern Eastern Desert (NED) of Egypt and is occupied by highly sheared metavolcanics tectonically alternated with banded iron formations and intruded by Barud tonalite–granodiorite, post-tectonic gabbroic and granitic intrusions. Detailed structural investigation showed that the schists and migmatitic amphibolites are formed by shearing in metavolcanics and syntectonic Barud tonalite–granodiorite due to movement along the Wadi Fatira shear zone (WFSZ). This shear zone starts as a NW–SE striking fault along Wadi Barud Al Azraq and the Eastern part of Wadi Fatira and turns to a E–W trending fault to the north of Wadi Fatira. Microstructural shear sense indicators such as asymmetric geometry of porphyroclasts such as σ-type and asymmetric folds deforming fine-grained bands which are frequently found around porphyroclasts indicate sinistral sense of shearing along the WFSZ. This shear zone is characterized by transitions from local convergence to local extension along their E–W and NW–SE trending parts, respectively. The NW–SE part of the WFSZ is of about 200 m in width and characterized by synmagmatic extensional features such as intrusion of synkinematic tonalite, creation of NE–SE trending normal faults, and formation of migmatitic amphibolites and schlieric tonalites. This part of the shear zone is metamorphosed under synthermal peak metamorphic conditions (725°C at 2–4 kbar). The E–W compressional part of the WFSZ is up to 3 km in width and composed of hornblende, chlorite, actinolite, and biotite schists together with sheared intermediate and acidic metatuffs. Contractional and transpressional structures in this part of the WFSZ include E–W trending major asymmetrical anticline and syncline, nearly vertical foliation and steeply pitching stretching lineations, NNE dipping minor thrusts, and minor intrafolial folds with their hinges parallel to the stretching lineation. P–T estimates using mineral analyses of plagioclase and hornblende from schists and foliated metavolcanics indicate prograde metamorphism under medium-grade amphibolite facies (500–600°C at 3–7 kbar) retrogressed to low-grade greenschist facies (227–317°C). The foliation in Barud tonalite–granodiorite close to the E–W part of the WFSZ runs parallel to the plane of shearing and the tonalite show numerous magmatic flow structures overprinted by folding and ductile shearing. The WFSZ is similar to structures resulted from combined simple shear and orthogonal shortening of oblique transpressive shear zones and their sense of movement is comparable with the characteristics of the Najd Fault System. تقع منطقة وادى فطيرة على الحافة الجنوبية للجزء الشمالي من الصحراء الشرقية المصرية، والمنطقة يتواجد بها صخور البركانيات المتحولة يصاحبها رقائق من تكوينات الحديد ويتداخل فى هذه الصخور جرانيت وادى بارود المصاحب للحركة التكتونية وكذلك بعض من متداخلات مابعد الحركة التكتونية من الجرانيت والجابرو. الدراسة التركيبية التفصيلية للمنطقة أثبتت ان الشيست والأمفيبولايت الميجماتى تكونا نتيجة التشوة والتحول اللذان حدثا للصخور البركانية وتوناليت-جرانودايورايت وادى بارود وذلك كنتيجة للحركة على نطاق تشوه وادى فطيرة وأثناء تداخل جرانيت وادى بارود. نطاق تشوه وادى فطيرة بدأ كصدع يتجة شمال غربى-جنوب شرقى عبر وادى بارود الأزرق والجزء الشرقى من وادى فطيرة ثم تغير مساره الى صدع يتجه شرق-غرب وذلك الى الشمال من وادى فطيرة. أدلة الحركة مثل تواجد البروفيروبلاست فى شكل سيجما، تواجد الطيات الدقيقة الغير متماثلة والتى تشوه الأشرطة الدقيقة الموجودة حول البروفيروبلاست، هذه الأدلة أكدت أن الحركة يسارية عبر نطاق تشوه وادى فطيرة. يتميز نطاق تشوه وادى فطيرة بالانتقال من مرحلة التشوة المصاحب للتقارب المائل الى التشوه المصاحب للبسط والإطالة. يتكون نطاق بتر وادى فطيرة من جزأين، الجزء الأول يتجه شمال غرب – جنوب شرق وهذا اتساعه حوالى 200 متر ويتميز بتواجد الظواهر المصاحبة لتشوه البسط والصخور فى الحالة المجماتية، ومن أمثلة هذا الظواهر تداخل جرانيت وادى بارود، الصدوع التى تتجة شمال شرق-جنوب غرب، وتكوين الأمفيبولايت الميجماتى والتونالايت ذو الأشرطة. وجد أن ظروف التحول فى هذا الجزء من نطاق التشوه وصلت الى قمة الحرارة حيث تم تسجيل حرارة تصل الى 725 درجة مئوية وضغط يتراوح بين 2 الى 4 كليوبار. أما الجزء الثانى من نطاق تشوه وادى فطيرة فإنه يتجه شرق-غرب واتساعه حوالى 3 كيلومتر ويتكون من أنواع مختلفة من صخر الشيست بالإضافة الى صخور بركانية متوسطة التشوه. ويميز هذا الجزء من نطاق تشوه وادى فطيرة التراكيب المصاحبة للتضاغط والتقارب والتى تشمل التحدبات والتقعرات الغير متماثلة والتى تتجه شرق-غرب، التورق الشبة رأسى واستطالة المعادن شديدة الغطس، الدسور المائلة فى اتجاه شمال الشمال الشرقى، والطيات الصغيرة التى تتوازى اتجاهات محاورها مع الاتجاهات التى تميز استطالة المعادن. وجد ان الصخور فى هذا الجزء من نطاق التشوة تحولت تحت ظروف من الضغط ودرجة الحرارة تتوافق مع سحنة الأمفيبولايت (500-600 درجة مئوية، 3-7 كيلوبار) ثم حدث تراجع حتى وصلت الى سحنة الشيست الأخضر (227-317 درجة مئوية). التورق الذى يميز صخور التوناليت والجرانودايورايت فى متداخل جرانيت وادى بارود يتوازى مع مستوى التشوه فى هذا الجزء من نطاق تشوه وادى فطيرة. أخيرا، ان نطاق تشوه وادى فطيرة يشبه التراكيب التى تنتج من تأثير simple shear والتقصير المتعامد المصاحب لنطاقات التشوة والعقص المائلة هذا يجعله مشابه لنطاقات التشوه التى تميز نظام صدوع النجد. للمراسلة: د/ محمد احمد عبد الواحد</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" 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type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="1419" href="https://www.academia.edu/Documents/in/Structural_Geology">Structural Geology</a>, <script data-card-contents-for-ri="1419" type="text/json">{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="158597" href="https://www.academia.edu/Documents/in/Iron">Iron</a>, <script data-card-contents-for-ri="158597" type="text/json">{"id":158597,"name":"Iron","url":"https://www.academia.edu/Documents/in/Iron?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" 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post-tectonic gabbroic and granitic intrusions. Detailed structural investigation showed that the schists and migmatitic amphibolites are formed by shearing in metavolcanics and syntectonic Barud tonalite–granodiorite due to movement along the Wadi Fatira shear zone (WFSZ). This shear zone starts as a NW–SE striking fault along Wadi Barud Al Azraq and the Eastern part of Wadi Fatira and turns to a E–W trending fault to the north of Wadi Fatira. Microstructural shear sense indicators such as asymmetric geometry of porphyroclasts such as σ-type and asymmetric folds deforming fine-grained bands which are frequently found around porphyroclasts indicate sinistral sense of shearing along the WFSZ. This shear zone is characterized by transitions from local convergence to local extension along their E–W and NW–SE trending parts, respectively. The NW–SE part of the WFSZ is of about 200 m in width and characterized by synmagmatic extensional features such as intrusion of synkinematic tonalite, creation of NE–SE trending normal faults, and formation of migmatitic amphibolites and schlieric tonalites. This part of the shear zone is metamorphosed under synthermal peak metamorphic conditions (725°C at 2–4 kbar). The E–W compressional part of the WFSZ is up to 3 km in width and composed of hornblende, chlorite, actinolite, and biotite schists together with sheared intermediate and acidic metatuffs. Contractional and transpressional structures in this part of the WFSZ include E–W trending major asymmetrical anticline and syncline, nearly vertical foliation and steeply pitching stretching lineations, NNE dipping minor thrusts, and minor intrafolial folds with their hinges parallel to the stretching lineation. P–T estimates using mineral analyses of plagioclase and hornblende from schists and foliated metavolcanics indicate prograde metamorphism under medium-grade amphibolite facies (500–600°C at 3–7 kbar) retrogressed to low-grade greenschist facies (227–317°C). The foliation in Barud tonalite–granodiorite close to the E–W part of the WFSZ runs parallel to the plane of shearing and the tonalite show numerous magmatic flow structures overprinted by folding and ductile shearing. The WFSZ is similar to structures resulted from combined simple shear and orthogonal shortening of oblique transpressive shear zones and their sense of movement is comparable with the characteristics of the Najd Fault System. تقع منطقة وادى فطيرة على الحافة الجنوبية للجزء الشمالي من الصحراء الشرقية المصرية، والمنطقة يتواجد بها صخور البركانيات المتحولة يصاحبها رقائق من تكوينات الحديد ويتداخل فى هذه الصخور جرانيت وادى بارود المصاحب للحركة التكتونية وكذلك بعض من متداخلات مابعد الحركة التكتونية من الجرانيت والجابرو. الدراسة التركيبية التفصيلية للمنطقة أثبتت ان الشيست والأمفيبولايت الميجماتى تكونا نتيجة التشوة والتحول اللذان حدثا للصخور البركانية وتوناليت-جرانودايورايت وادى بارود وذلك كنتيجة للحركة على نطاق تشوه وادى فطيرة وأثناء تداخل جرانيت وادى بارود. نطاق تشوه وادى فطيرة بدأ كصدع يتجة شمال غربى-جنوب شرقى عبر وادى بارود الأزرق والجزء الشرقى من وادى فطيرة ثم تغير مساره الى صدع يتجه شرق-غرب وذلك الى الشمال من وادى فطيرة. أدلة الحركة مثل تواجد البروفيروبلاست فى شكل سيجما، تواجد الطيات الدقيقة الغير متماثلة والتى تشوه الأشرطة الدقيقة الموجودة حول البروفيروبلاست، هذه الأدلة أكدت أن الحركة يسارية عبر نطاق تشوه وادى فطيرة. يتميز نطاق تشوه وادى فطيرة بالانتقال من مرحلة التشوة المصاحب للتقارب المائل الى التشوه المصاحب للبسط والإطالة. يتكون نطاق بتر وادى فطيرة من جزأين، الجزء الأول يتجه شمال غرب – جنوب شرق وهذا اتساعه حوالى 200 متر ويتميز بتواجد الظواهر المصاحبة لتشوه البسط والصخور فى الحالة المجماتية، ومن أمثلة هذا الظواهر تداخل جرانيت وادى بارود، الصدوع التى تتجة شمال شرق-جنوب غرب، وتكوين الأمفيبولايت الميجماتى والتونالايت ذو الأشرطة. وجد أن ظروف التحول فى هذا الجزء من نطاق التشوه وصلت الى قمة الحرارة حيث تم تسجيل حرارة تصل الى 725 درجة مئوية وضغط يتراوح بين 2 الى 4 كليوبار. أما الجزء الثانى من نطاق تشوه وادى فطيرة فإنه يتجه شرق-غرب واتساعه حوالى 3 كيلومتر ويتكون من أنواع مختلفة من صخر الشيست بالإضافة الى صخور بركانية متوسطة التشوه. ويميز هذا الجزء من نطاق تشوه وادى فطيرة التراكيب المصاحبة للتضاغط والتقارب والتى تشمل التحدبات والتقعرات الغير متماثلة والتى تتجه شرق-غرب، التورق الشبة رأسى واستطالة المعادن شديدة الغطس، الدسور المائلة فى اتجاه شمال الشمال الشرقى، والطيات الصغيرة التى تتوازى اتجاهات محاورها مع الاتجاهات التى تميز استطالة المعادن. وجد ان الصخور فى هذا الجزء من نطاق التشوة تحولت تحت ظروف من الضغط ودرجة الحرارة تتوافق مع سحنة الأمفيبولايت (500-600 درجة مئوية، 3-7 كيلوبار) ثم حدث تراجع حتى وصلت الى سحنة الشيست الأخضر (227-317 درجة مئوية). التورق الذى يميز صخور التوناليت والجرانودايورايت فى متداخل جرانيت وادى بارود يتوازى مع مستوى التشوه فى هذا الجزء من نطاق تشوه وادى فطيرة. أخيرا، ان نطاق تشوه وادى فطيرة يشبه التراكيب التى تنتج من تأثير simple shear والتقصير المتعامد المصاحب لنطاقات التشوة والعقص المائلة هذا يجعله مشابه لنطاقات التشوه التى تميز نظام صدوع النجد. للمراسلة: د/ محمد احمد عبد الواحد","downloadable_attachments":[{"id":48905205,"asset_id":11258536,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":27194743,"first_name":"Mohamed","last_name":"Abd El-Wahed","domain_name":"tanta","page_name":"MAbdElWahed","display_name":"Mohamed Abd El-Wahed","profile_url":"https://tanta.academia.edu/MAbdElWahed?f_ri=172299","photo":"https://0.academia-photos.com/27194743/7829160/12282632/s65_mohamed.abd_el-wahed.png"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=172299","nofollow":false},{"id":158597,"name":"Iron","url":"https://www.academia.edu/Documents/in/Iron?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":179580,"name":"Banded Iron Formation","url":"https://www.academia.edu/Documents/in/Banded_Iron_Formation?f_ri=172299"},{"id":284025,"name":"Shear Zone","url":"https://www.academia.edu/Documents/in/Shear_Zone?f_ri=172299"},{"id":473797,"name":"Microstructures","url":"https://www.academia.edu/Documents/in/Microstructures?f_ri=172299"},{"id":959838,"name":"Arabian Journal of Geosciences","url":"https://www.academia.edu/Documents/in/Arabian_Journal_of_Geosciences?f_ri=172299"},{"id":1908713,"name":"Local Convergence","url":"https://www.academia.edu/Documents/in/Local_Convergence?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_17180255" data-work_id="17180255" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/17180255/Intrabed_Andalusite_variation_pattern_as_an_indicator_of_graded_beds_at_Kuala_Kemasik_Trengganu">Intrabed Andalusite variation pattern as 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and Bell, T.H., 1996. Microstructural controls on sites of metamorphic reaction: a case study of the inter-relationship between deformation and metamorphism</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/5768832" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2377cfbc814e170d8be37c27c4b0b3af" rel="nofollow" data-download="{"attachment_id":32793673,"asset_id":5768832,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/32793673/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="8413622" href="https://jamescook.academia.edu/THBell">TH (Tim) Bell</a><script data-card-contents-for-user="8413622" type="text/json">{"id":8413622,"first_name":"TH (Tim)","last_name":"Bell","domain_name":"jamescook","page_name":"THBell","display_name":"TH (Tim) Bell","profile_url":"https://jamescook.academia.edu/THBell?f_ri=172299","photo":"https://0.academia-photos.com/8413622/2940587/3450308/s65_th_tim_.bell.jpg"}</script></span></span></li><li class="js-paper-rank-work_5768832 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="5768832"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 5768832, container: ".js-paper-rank-work_5768832", }); 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$(".js-view-count[data-work-id=5768832]").text(description); $(".js-view-count-work_5768832").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_5768832").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="5768832"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="10769" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="126340" href="https://www.academia.edu/Documents/in/Deformation">Deformation</a>, <script data-card-contents-for-ri="126340" type="text/json">{"id":126340,"name":"Deformation","url":"https://www.academia.edu/Documents/in/Deformation?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a>, <script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="473797" href="https://www.academia.edu/Documents/in/Microstructures">Microstructures</a><script data-card-contents-for-ri="473797" type="text/json">{"id":473797,"name":"Microstructures","url":"https://www.academia.edu/Documents/in/Microstructures?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=5768832]'), work: {"id":5768832,"title":"Spiess, R. and Bell, T.H., 1996. Microstructural controls on sites of metamorphic reaction: a case study of the inter-relationship between deformation and metamorphism","created_at":"2014-01-19T06:19:33.964-08:00","url":"https://www.academia.edu/5768832/Spiess_R_and_Bell_T_H_1996_Microstructural_controls_on_sites_of_metamorphic_reaction_a_case_study_of_the_inter_relationship_between_deformation_and_metamorphism?f_ri=172299","dom_id":"work_5768832","summary":null,"downloadable_attachments":[{"id":32793673,"asset_id":5768832,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":8413622,"first_name":"TH (Tim)","last_name":"Bell","domain_name":"jamescook","page_name":"THBell","display_name":"TH (Tim) Bell","profile_url":"https://jamescook.academia.edu/THBell?f_ri=172299","photo":"https://0.academia-photos.com/8413622/2940587/3450308/s65_th_tim_.bell.jpg"}],"research_interests":[{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":126340,"name":"Deformation","url":"https://www.academia.edu/Documents/in/Deformation?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":473797,"name":"Microstructures","url":"https://www.academia.edu/Documents/in/Microstructures?f_ri=172299","nofollow":false},{"id":1230710,"name":"Reactions","url":"https://www.academia.edu/Documents/in/Reactions?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_80056198" data-work_id="80056198" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/80056198/Greenschist_metamorphism_of_volcanic_rocks_Stocking_Lake_area_Ladysmith_BC">Greenschist metamorphism of volcanic rocks, Stocking Lake area, Ladysmith, BC</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest">This poster presents petrography and major oxide geochemistry from metavolcanic rocks found at Stocking Lake, Ladysmith, British Columbia. The intent of the research is to show that metamorphism is regional-style and of greenschist grade.</div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/80056198" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="627057f960fccd27d12b9a79a8553eb5" rel="nofollow" data-download="{"attachment_id":86564827,"asset_id":80056198,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/86564827/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="106164254" href="https://viu.academia.edu/SpencerWoodward">Spencer Woodward</a><script data-card-contents-for-user="106164254" type="text/json">{"id":106164254,"first_name":"Spencer","last_name":"Woodward","domain_name":"viu","page_name":"SpencerWoodward","display_name":"Spencer Woodward","profile_url":"https://viu.academia.edu/SpencerWoodward?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_80056198 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="80056198"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 80056198, container: ".js-paper-rank-work_80056198", }); 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The intent of the research is to show that metamorphism is regional-style and of greenschist grade.","downloadable_attachments":[{"id":86564827,"asset_id":80056198,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":106164254,"first_name":"Spencer","last_name":"Woodward","domain_name":"viu","page_name":"SpencerWoodward","display_name":"Spencer Woodward","profile_url":"https://viu.academia.edu/SpencerWoodward?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_10904335 coauthored" data-work_id="10904335" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/10904335/The_effect_of_Alpine_metamorphism_on_an_oceanic_Cu_Fe_sulfide_ore_the_Herin_deposit_Western_Alps_Italy">The effect of Alpine metamorphism on an oceanic Cu-Fe sulfide ore: the Herin deposit, Western Alps, Italy</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Herin mine (Champdepraz, Aosta, Italy), located in Aosta Valley, approximately between 1600 and 1800 m a.s.l., was exploited for at least 250 years for its Cu-Fe sulfide ore. The deposit host rocks belong to the metaophiolitic Zermatt-... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_10904335" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Herin mine (Champdepraz, Aosta, Italy), located in Aosta Valley, approximately between 1600 and 1800 m a.s.l., was exploited for at least 250 years for its Cu-Fe sulfide ore. The deposit host rocks belong to the metaophiolitic Zermatt- Saas unit, the eclogitic lower portion<br />of the Piedmont Western Alpine Nappe. The ore mineral association mainly comprises pyrite and chalcopyrite, along with other sulfides such as pyrrhotite, sphalerite, cubanite and oxides (magnetite, rutile, ilmenite). The deposit occurs within lenticular massive bodies and thin<br />layers hosted in various greenschist-facies metamorphosed lithotypes. New data on geometric features, mineralogy, mineral chemistry, petrography, minerography were collected and compared with the existing models for massive-sulfide mineral deposits. We suggest a hydrothermal-volcanogenic primary origin of the mineralization with original characteristics<br />largely obliterated by subsequent metamorphic history. On the basis of studies and our results, we identified two parameters as driving criteria for a comprehension of the multistage process that led to the present configuration of the ore: (a) textural characters of pyrite and (b) distribution of selected trace elements (Co, Ni, As) in sulfides. Spot analyses and atomic maps obtained by electron microprobe provided an integration of these two sets of data. Trace elements, in fact, show a zoned distribution, in particular in pyrite, that can be related to specific textural styles. We selected cobalt as a useful trace element, due to its high concentration and wide range in pyrite (270 -22200 ppm). We determined a critical concentration value for cobalt at 3160 ppm, useful as a discriminate between two generations of pyrite. This led to the delineation of a series of dissolution and crystallization events that describe the metamorphic history of the sulfide ore.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/10904335" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="0b1ffe55e833d639380fc06292c5a53b" rel="nofollow" data-download="{"attachment_id":36684133,"asset_id":10904335,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/36684133/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="21860943" href="https://unimi.academia.edu/IreneFantone">Irene Fantone</a><script data-card-contents-for-user="21860943" type="text/json">{"id":21860943,"first_name":"Irene","last_name":"Fantone","domain_name":"unimi","page_name":"IreneFantone","display_name":"Irene Fantone","profile_url":"https://unimi.academia.edu/IreneFantone?f_ri=172299","photo":"https://0.academia-photos.com/21860943/7831741/33868169/s65_irene.fantone.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-10904335">+1</span><div class="hidden js-additional-users-10904335"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://independent.academia.edu/AndreaStrini">Andrea Strini</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-10904335'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-10904335').html(); 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container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_10904335 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="10904335"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 10904335; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=10904335]").text(description); $(".js-view-count-work_10904335").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_10904335").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="10904335"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">7</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="8116" href="https://www.academia.edu/Documents/in/Trace_element_Geochemistry">Trace element Geochemistry</a>, <script data-card-contents-for-ri="8116" type="text/json">{"id":8116,"name":"Trace element Geochemistry","url":"https://www.academia.edu/Documents/in/Trace_element_Geochemistry?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="146671" href="https://www.academia.edu/Documents/in/Mineral_Resources">Mineral Resources</a>, <script data-card-contents-for-ri="146671" type="text/json">{"id":146671,"name":"Mineral Resources","url":"https://www.academia.edu/Documents/in/Mineral_Resources?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="156636" href="https://www.academia.edu/Documents/in/Pyrite">Pyrite</a>, <script data-card-contents-for-ri="156636" type="text/json">{"id":156636,"name":"Pyrite","url":"https://www.academia.edu/Documents/in/Pyrite?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=10904335]'), work: {"id":10904335,"title":"The effect of Alpine metamorphism on an oceanic Cu-Fe sulfide ore: the Herin deposit, Western Alps, Italy","created_at":"2015-02-18T10:12:39.370-08:00","url":"https://www.academia.edu/10904335/The_effect_of_Alpine_metamorphism_on_an_oceanic_Cu_Fe_sulfide_ore_the_Herin_deposit_Western_Alps_Italy?f_ri=172299","dom_id":"work_10904335","summary":"Herin mine (Champdepraz, Aosta, Italy), located in Aosta Valley, approximately between 1600 and 1800 m a.s.l., was exploited for at least 250 years for its Cu-Fe sulfide ore. The deposit host rocks belong to the metaophiolitic Zermatt- Saas unit, the eclogitic lower portion\nof the Piedmont Western Alpine Nappe. The ore mineral association mainly comprises pyrite and chalcopyrite, along with other sulfides such as pyrrhotite, sphalerite, cubanite and oxides (magnetite, rutile, ilmenite). The deposit occurs within lenticular massive bodies and thin\nlayers hosted in various greenschist-facies metamorphosed lithotypes. New data on geometric features, mineralogy, mineral chemistry, petrography, minerography were collected and compared with the existing models for massive-sulfide mineral deposits. We suggest a hydrothermal-volcanogenic primary origin of the mineralization with original characteristics\nlargely obliterated by subsequent metamorphic history. On the basis of studies and our results, we identified two parameters as driving criteria for a comprehension of the multistage process that led to the present configuration of the ore: (a) textural characters of pyrite and (b) distribution of selected trace elements (Co, Ni, As) in sulfides. Spot analyses and atomic maps obtained by electron microprobe provided an integration of these two sets of data. Trace elements, in fact, show a zoned distribution, in particular in pyrite, that can be related to specific textural styles. We selected cobalt as a useful trace element, due to its high concentration and wide range in pyrite (270 -22200 ppm). We determined a critical concentration value for cobalt at 3160 ppm, useful as a discriminate between two generations of pyrite. This led to the delineation of a series of dissolution and crystallization events that describe the metamorphic history of the sulfide ore. ","downloadable_attachments":[{"id":36684133,"asset_id":10904335,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":21860943,"first_name":"Irene","last_name":"Fantone","domain_name":"unimi","page_name":"IreneFantone","display_name":"Irene Fantone","profile_url":"https://unimi.academia.edu/IreneFantone?f_ri=172299","photo":"https://0.academia-photos.com/21860943/7831741/33868169/s65_irene.fantone.jpg"},{"id":26561997,"first_name":"Andrea","last_name":"Strini","domain_name":"independent","page_name":"AndreaStrini","display_name":"Andrea Strini","profile_url":"https://independent.academia.edu/AndreaStrini?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":8116,"name":"Trace element Geochemistry","url":"https://www.academia.edu/Documents/in/Trace_element_Geochemistry?f_ri=172299","nofollow":false},{"id":146671,"name":"Mineral Resources","url":"https://www.academia.edu/Documents/in/Mineral_Resources?f_ri=172299","nofollow":false},{"id":156636,"name":"Pyrite","url":"https://www.academia.edu/Documents/in/Pyrite?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":224577,"name":"Trace Elements","url":"https://www.academia.edu/Documents/in/Trace_Elements?f_ri=172299"},{"id":362708,"name":"Abandoned Mines","url":"https://www.academia.edu/Documents/in/Abandoned_Mines?f_ri=172299"},{"id":895636,"name":"Massive Sulphide","url":"https://www.academia.edu/Documents/in/Massive_Sulphide?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_35336314" data-work_id="35336314" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/35336314/Metamorphic_history_of_the_South_Tibetan_Detachment_System_Mt_Everest_region_revealed_by_RSCM_thermometry_and_phase_equilibria_modelling">Metamorphic history of the South Tibetan Detachment System, Mt. Everest region, revealed by RSCM thermometry and phase equilibria modelling</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/35336314" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="3742facb56844eb7ee7613b03089a9b5" rel="nofollow" data-download="{"attachment_id":55197292,"asset_id":35336314,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/55197292/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="191944" href="https://oxford.academia.edu/DaveWaters">Dave Waters</a><script data-card-contents-for-user="191944" type="text/json">{"id":191944,"first_name":"Dave","last_name":"Waters","domain_name":"oxford","page_name":"DaveWaters","display_name":"Dave Waters","profile_url":"https://oxford.academia.edu/DaveWaters?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_35336314 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="35336314"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 35336314, container: ".js-paper-rank-work_35336314", }); 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Everest region, revealed by RSCM thermometry and phase equilibria modelling","created_at":"2017-12-04T11:11:53.133-08:00","url":"https://www.academia.edu/35336314/Metamorphic_history_of_the_South_Tibetan_Detachment_System_Mt_Everest_region_revealed_by_RSCM_thermometry_and_phase_equilibria_modelling?f_ri=172299","dom_id":"work_35336314","summary":null,"downloadable_attachments":[{"id":55197292,"asset_id":35336314,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":191944,"first_name":"Dave","last_name":"Waters","domain_name":"oxford","page_name":"DaveWaters","display_name":"Dave Waters","profile_url":"https://oxford.academia.edu/DaveWaters?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":14228,"name":"Geochronology","url":"https://www.academia.edu/Documents/in/Geochronology?f_ri=172299","nofollow":false},{"id":19524,"name":"Mountain Building","url":"https://www.academia.edu/Documents/in/Mountain_Building?f_ri=172299","nofollow":false},{"id":22594,"name":"Himalayan Tectonics","url":"https://www.academia.edu/Documents/in/Himalayan_Tectonics?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":251912,"name":"Erosion and climate","url":"https://www.academia.edu/Documents/in/Erosion_and_climate?f_ri=172299"},{"id":531715,"name":"Metamorphic Geology","url":"https://www.academia.edu/Documents/in/Metamorphic_Geology?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_15062130 coauthored" data-work_id="15062130" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/15062130/Pressure_temperature_time_evolution_of_high_pressure_rocks_of_the_Acatl%C3%A1n_Complex_southern_Mexico_Implications_for_the_evolution_of_the_Iapetus_and_Rheic_Oceans_Comment">Pressure-temperature-time evolution of high-pressure rocks of the Acatlán Complex (southern Mexico): Implications for the evolution of the Iapetus and Rheic Oceans: Comment</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/15062130" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="b96890cd105a393fc69a783d878e4788" rel="nofollow" data-download="{"attachment_id":38528364,"asset_id":15062130,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/38528364/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="33255192" href="https://smu-ca.academia.edu/JDostal">Jaroslav Dostal</a><script data-card-contents-for-user="33255192" type="text/json">{"id":33255192,"first_name":"Jaroslav","last_name":"Dostal","domain_name":"smu-ca","page_name":"JDostal","display_name":"Jaroslav Dostal","profile_url":"https://smu-ca.academia.edu/JDostal?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-15062130">+6</span><div class="hidden js-additional-users-15062130"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://ohio.academia.edu/DamianNance">R. Damian Nance</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://smu-ca.academia.edu/jaroslavdostal">jaroslav dostal</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://independent.academia.edu/BMurphy1">B. Murphy</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://independent.academia.edu/MarcoL%C3%B3peztorres">Marco López-torres</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://unam.academia.edu/AOrtegarivera">A. Ortega-Rivera</a></span></div><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://uson.academia.edu/RicardoVega">Ricardo Vega</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-15062130'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-15062130').html(); } } new HoverPopover(popoverSettings); })();</script></li><li class="js-paper-rank-work_15062130 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="15062130"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 15062130, container: ".js-paper-rank-work_15062130", }); });</script></li><li class="js-percentile-work_15062130 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 15062130; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_15062130"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_15062130 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="15062130"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 15062130; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=15062130]").text(description); $(".js-view-count-work_15062130").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_15062130").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="15062130"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">3</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="10769" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="89567" href="https://www.academia.edu/Documents/in/Tectonics_and_Structural_Geology_Metamorphic_Petrology_Tectonic_Geomorphology">Tectonics and Structural Geology, Metamorphic Petrology, Tectonic Geomorphology</a>, <script data-card-contents-for-ri="89567" type="text/json">{"id":89567,"name":"Tectonics and Structural Geology, Metamorphic Petrology, Tectonic Geomorphology","url":"https://www.academia.edu/Documents/in/Tectonics_and_Structural_Geology_Metamorphic_Petrology_Tectonic_Geomorphology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=15062130]'), work: {"id":15062130,"title":"Pressure-temperature-time evolution of high-pressure rocks of the Acatlán Complex (southern Mexico): Implications for the evolution of the Iapetus and Rheic Oceans: Comment","created_at":"2015-08-20T13:45:24.000-07:00","url":"https://www.academia.edu/15062130/Pressure_temperature_time_evolution_of_high_pressure_rocks_of_the_Acatl%C3%A1n_Complex_southern_Mexico_Implications_for_the_evolution_of_the_Iapetus_and_Rheic_Oceans_Comment?f_ri=172299","dom_id":"work_15062130","summary":null,"downloadable_attachments":[{"id":38528364,"asset_id":15062130,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":33255192,"first_name":"Jaroslav","last_name":"Dostal","domain_name":"smu-ca","page_name":"JDostal","display_name":"Jaroslav Dostal","profile_url":"https://smu-ca.academia.edu/JDostal?f_ri=172299","photo":"/images/s65_no_pic.png"},{"id":393523,"first_name":"R. 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Ortega-Rivera","profile_url":"https://unam.academia.edu/AOrtegarivera?f_ri=172299","photo":"/images/s65_no_pic.png"},{"id":2306996,"first_name":"Ricardo","last_name":"Vega","domain_name":"uson","page_name":"RicardoVega","display_name":"Ricardo Vega","profile_url":"https://uson.academia.edu/RicardoVega?f_ri=172299","photo":"https://0.academia-photos.com/2306996/2446636/2844367/s65_ricardo.vega.jpg"}],"research_interests":[{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":89567,"name":"Tectonics and Structural Geology, Metamorphic Petrology, Tectonic Geomorphology","url":"https://www.academia.edu/Documents/in/Tectonics_and_Structural_Geology_Metamorphic_Petrology_Tectonic_Geomorphology?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_15060579" data-work_id="15060579" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/15060579/433_Eros_Problems_with_the_meteorite_magnetism_record_in_attempting_an_asteroid_match">433 Eros: Problems with the meteorite magnetism record in attempting an asteroid match</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The magnetometer experiment (MAG) onboard the Near-Earth Asteroid Rendezvous (NEAR)-Shoemaker spacecraft detected no global scale magnetization and established a maximum magnetization of 2.1 x 10(-6) Am-2 kg(-1) for asteroid 433 Eros.... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_15060579" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The magnetometer experiment (MAG) onboard the Near-Earth Asteroid Rendezvous (NEAR)-Shoemaker spacecraft detected no global scale magnetization and established a maximum magnetization of 2.1 x 10(-6) Am-2 kg(-1) for asteroid 433 Eros. This is in sharp contrast with the estimated magnetization of other S-class asteroids (Gaspra, similar to2.4 x 10(-2) Amt(2) kg(-1); Braille, similar to2.8 x 10(-2) Am-2 kg(-1)) and is below published values for all types of ordinary chondrites. This includes the L/LL types considered to most closely match 433 Eros based on preliminary interpretations of NEAR remote geochemical experiments. <br /><br />The ordinary chondrite meteorite magnetization intensity data was reviewed in order to assess the reasonableness of an asteroid-meteorite match based on magnetic property measurements. Natural remanent magnetization (NRM) intensities for the ordinary chondrite meteorites show at least a 2 order of magnitude range within each of the H, L, and LL groups, all well above the 2.1 x 10(-6) Amt(2) kg(-1) level for 433 Eros. The REM values (ratio of the NRM to the SIRM (saturation remanent magnetization)) range over 3 orders of magnitude for all chondrite groups indicating no clear relationship between NRM and the amount of magnetic material. Levels of magnetic noise in chondrite meteorites can be as much as 70% or more of the NRM. Consequently, published values of the NRM should be considered suspect unless careful evaluation of the noise sources is done. NASA Goddard SFC studies of per unit mass intensities in large (>10 000 g) and small (down to <1 g) samples from the same meteorite demonstrate magnetic intensity decreases as size increases. This would appear to be explained by demagnetization due to magnetic vector randomness at unknown scale sizes in the larger samples. This would then argue for some level of demagnetization of large objects such as an asteroid. The possibility that 433 Eros is an LL chondrite cannot be discounted.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/15060579" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="50c73300ae808ff36207ae15cda96c92" rel="nofollow" data-download="{"attachment_id":38527328,"asset_id":15060579,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/38527328/download_file?st=MTczMjQ0NDI2NCw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="33099665" href="https://cuni.academia.edu/GuntherKletetschka">Gunther Kletetschka</a><script data-card-contents-for-user="33099665" type="text/json">{"id":33099665,"first_name":"Gunther","last_name":"Kletetschka","domain_name":"cuni","page_name":"GuntherKletetschka","display_name":"Gunther Kletetschka","profile_url":"https://cuni.academia.edu/GuntherKletetschka?f_ri=172299","photo":"https://0.academia-photos.com/33099665/10004870/11158721/s65_gunther.kletetschka.jpg"}</script></span></span></li><li class="js-paper-rank-work_15060579 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="15060579"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 15060579, container: ".js-paper-rank-work_15060579", }); 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This is in sharp contrast with the estimated magnetization of other S-class asteroids (Gaspra, similar to2.4 x 10(-2) Amt(2) kg(-1); Braille, similar to2.8 x 10(-2) Am-2 kg(-1)) and is below published values for all types of ordinary chondrites. This includes the L/LL types considered to most closely match 433 Eros based on preliminary interpretations of NEAR remote geochemical experiments. \n\nThe ordinary chondrite meteorite magnetization intensity data was reviewed in order to assess the reasonableness of an asteroid-meteorite match based on magnetic property measurements. Natural remanent magnetization (NRM) intensities for the ordinary chondrite meteorites show at least a 2 order of magnitude range within each of the H, L, and LL groups, all well above the 2.1 x 10(-6) Amt(2) kg(-1) level for 433 Eros. The REM values (ratio of the NRM to the SIRM (saturation remanent magnetization)) range over 3 orders of magnitude for all chondrite groups indicating no clear relationship between NRM and the amount of magnetic material. Levels of magnetic noise in chondrite meteorites can be as much as 70% or more of the NRM. Consequently, published values of the NRM should be considered suspect unless careful evaluation of the noise sources is done. NASA Goddard SFC studies of per unit mass intensities in large (\u003e10 000 g) and small (down to \u003c1 g) samples from the same meteorite demonstrate magnetic intensity decreases as size increases. This would appear to be explained by demagnetization due to magnetic vector randomness at unknown scale sizes in the larger samples. This would then argue for some level of demagnetization of large objects such as an asteroid. The possibility that 433 Eros is an LL chondrite cannot be discounted.","downloadable_attachments":[{"id":38527328,"asset_id":15060579,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":33099665,"first_name":"Gunther","last_name":"Kletetschka","domain_name":"cuni","page_name":"GuntherKletetschka","display_name":"Gunther Kletetschka","profile_url":"https://cuni.academia.edu/GuntherKletetschka?f_ri=172299","photo":"https://0.academia-photos.com/33099665/10004870/11158721/s65_gunther.kletetschka.jpg"}],"research_interests":[{"id":51654,"name":"Phases","url":"https://www.academia.edu/Documents/in/Phases?f_ri=172299","nofollow":false},{"id":158597,"name":"Iron","url":"https://www.academia.edu/Documents/in/Iron?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":188706,"name":"Metal","url":"https://www.academia.edu/Documents/in/Metal?f_ri=172299","nofollow":false},{"id":192783,"name":"Field","url":"https://www.academia.edu/Documents/in/Field?f_ri=172299"},{"id":309434,"name":"Solar System","url":"https://www.academia.edu/Documents/in/Solar_System?f_ri=172299"},{"id":2049776,"name":"Ordinary Chondrites","url":"https://www.academia.edu/Documents/in/Ordinary_Chondrites?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_12045538 coauthored" data-work_id="12045538" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/12045538/Protomylonite_evolution_potentially_revealed_by_the_3D_depiction_and_fractal_analysis_of_chemical_data_from_a_feldspar">Protomylonite evolution potentially revealed by the 3D depiction and fractal analysis of chemical data from a feldspar</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/12045538" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="bec50200b52fd53fba7fb07a61f88450" rel="nofollow" data-download="{"attachment_id":37373968,"asset_id":12045538,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/37373968/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="29596928" href="https://pan-pl.academia.edu/ESlaby">E. 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Slaby","profile_url":"https://pan-pl.academia.edu/ESlaby?f_ri=172299","photo":"https://0.academia-photos.com/29596928/8663294/9676210/s65_e..slaby.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-12045538">+1</span><div class="hidden js-additional-users-12045538"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://fuw.academia.edu/Pawe%C5%82Rydelek">Paweł Rydelek</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-12045538'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-12045538').html(); } } new HoverPopover(popoverSettings); })();</script></li><li class="js-paper-rank-work_12045538 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="12045538"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 12045538, container: ".js-paper-rank-work_12045538", }); 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$(".js-view-count[data-work-id=12045538]").text(description); $(".js-view-count-work_12045538").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_12045538").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="12045538"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">4</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="16937" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry">Petrology and Geochemistry</a>, <script data-card-contents-for-ri="16937" type="text/json">{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a>, <script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="730238" href="https://www.academia.edu/Documents/in/Fractals_and_Chaos">Fractals and Chaos</a>, <script data-card-contents-for-ri="730238" type="text/json">{"id":730238,"name":"Fractals and Chaos","url":"https://www.academia.edu/Documents/in/Fractals_and_Chaos?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="1028570" href="https://www.academia.edu/Documents/in/Feldspar">Feldspar</a><script data-card-contents-for-ri="1028570" type="text/json">{"id":1028570,"name":"Feldspar","url":"https://www.academia.edu/Documents/in/Feldspar?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=12045538]'), work: {"id":12045538,"title":"Protomylonite evolution potentially revealed by the 3D depiction and fractal analysis of chemical data from a feldspar","created_at":"2015-04-21T05:14:36.861-07:00","url":"https://www.academia.edu/12045538/Protomylonite_evolution_potentially_revealed_by_the_3D_depiction_and_fractal_analysis_of_chemical_data_from_a_feldspar?f_ri=172299","dom_id":"work_12045538","summary":null,"downloadable_attachments":[{"id":37373968,"asset_id":12045538,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":29596928,"first_name":"E.","last_name":"Slaby","domain_name":"pan-pl","page_name":"ESlaby","display_name":"E. Slaby","profile_url":"https://pan-pl.academia.edu/ESlaby?f_ri=172299","photo":"https://0.academia-photos.com/29596928/8663294/9676210/s65_e..slaby.jpg"},{"id":41692738,"first_name":"Paweł","last_name":"Rydelek","domain_name":"fuw","page_name":"PawełRydelek","display_name":"Paweł Rydelek","profile_url":"https://fuw.academia.edu/Pawe%C5%82Rydelek?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":730238,"name":"Fractals and Chaos","url":"https://www.academia.edu/Documents/in/Fractals_and_Chaos?f_ri=172299","nofollow":false},{"id":1028570,"name":"Feldspar","url":"https://www.academia.edu/Documents/in/Feldspar?f_ri=172299","nofollow":false}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_40407068 coauthored" data-work_id="40407068" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/40407068/Multi_stage_metamorphic_evolution_and_protolith_reconstruction_of_spinel_bearing_and_symplectite_bearing_ultramafic_rocks_in_the_Zheltau_massif_Southern_Kazakhstan_Central_Asian_Orogenic_Belt">Multi-stage metamorphic evolution and protolith reconstruction of spinel-bearing and symplectite-bearing ultramafic rocks in the Zheltau massif, Southern Kazakhstan (Central Asian Orogenic Belt</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Spinel-bearing ultramafic rocks, metamorphosed in high-pressure conditions, are described from the metamor-phic complexes of the western part of the Central Asian Orogenic Belt (CAOB) in the Chu-Yili region in Southern Kazakhstan. They... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_40407068" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Spinel-bearing ultramafic rocks, metamorphosed in high-pressure conditions, are described from the metamor-phic complexes of the western part of the Central Asian Orogenic Belt (CAOB) in the Chu-Yili region in Southern Kazakhstan. They comprise small bodies of magnetite-bearing serpentinites, Cr-spinel-bearing serpentinized and amphibolitized dunites and peridotites enclosed by strongly retrogressed kyanite-bearing paragneisses. Apart from serpentinization, the ultramafic rocks were also overprinted by later rodingitization expressed in the development of the index-minerals hydrogrossular, prehnite and vuagnatite. Cr-spinel-bearing peridotites are characterized by extensive development of symplectitic and coronitic microtextures, which are interpreted to have been formed after garnet breakdown during decompression (i.e. exhumation). Calculated pressure (P) and temperature (T) obtained by phase diagram modeling and conventional geothermobarometry for the symplectites were P 11.5-14.5 kbar for a wide temperature range of T 600-850 °C, which followed the transition from garnet to spinel peridotite. Major and trace element whole-rock geochemical characteristics of the spinel-bearing ultra-mafic rocks as well as their structurally close relations indicate their mutual origin as parts of an oceanic cumulate complex of an arc-basin system. The protoliths were probably plagioclase-bearing (thus shallow, crustal) ultra-mafic rocks and troctolites, subducted to eclogite facies conditions and then exhumed along with other metamor-phic complexes of the Zheltau massif. These spinel-bearing ultramafic rocks could be classified as crustal formations in accordance with the inferred depths of their origin (b5 kbar), in common with many HP ultra-mafic/mafic complexes in the CAOB. However, strongly depleted geochemical signatures of the rocks, together with the distinctive microtextural features observed in the spinel peridotites, are unique, and their occurrence in the western CAOB is described here for the first time.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/40407068" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="4f299292940f96e767f328320dedab1e" rel="nofollow" data-download="{"attachment_id":60660742,"asset_id":40407068,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/60660742/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="3625605" href="https://independent.academia.edu/TayaAlifirova">Taisia Alifirova</a><script data-card-contents-for-user="3625605" type="text/json">{"id":3625605,"first_name":"Taisia","last_name":"Alifirova","domain_name":"independent","page_name":"TayaAlifirova","display_name":"Taisia Alifirova","profile_url":"https://independent.academia.edu/TayaAlifirova?f_ri=172299","photo":"https://0.academia-photos.com/3625605/1270868/16399508/s65_taya.alifirova.jpg"}</script></span></span><span class="u-displayInlineBlock InlineList-item-text"> and <span class="u-textDecorationUnderline u-clickable InlineList-item-text js-work-more-authors-40407068">+1</span><div class="hidden js-additional-users-40407068"><div><span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a href="https://independent.academia.edu/AnfisaPilitsyna">Anfisa Pilitsyna</a></span></div></div></span><script>(function(){ var popoverSettings = { el: $('.js-work-more-authors-40407068'), placement: 'bottom', hide_delay: 200, html: true, content: function(){ return $('.js-additional-users-40407068').html(); } } new HoverPopover(popoverSettings); })();</script></li><li class="js-paper-rank-work_40407068 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="40407068"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 40407068, container: ".js-paper-rank-work_40407068", }); });</script></li><li class="js-percentile-work_40407068 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 40407068; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_40407068"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_40407068 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="40407068"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 40407068; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=40407068]").text(description); $(".js-view-count-work_40407068").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_40407068").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="40407068"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">5</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="2635" href="https://www.academia.edu/Documents/in/Metamorphic_Petrology">Metamorphic Petrology</a>, <script data-card-contents-for-ri="2635" type="text/json">{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="16937" href="https://www.academia.edu/Documents/in/Petrology_and_Geochemistry">Petrology and Geochemistry</a>, <script data-card-contents-for-ri="16937" type="text/json">{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="54668" href="https://www.academia.edu/Documents/in/Peridotite">Peridotite</a>, <script data-card-contents-for-ri="54668" type="text/json">{"id":54668,"name":"Peridotite","url":"https://www.academia.edu/Documents/in/Peridotite?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=40407068]'), work: {"id":40407068,"title":"Multi-stage metamorphic evolution and protolith reconstruction of spinel-bearing and symplectite-bearing ultramafic rocks in the Zheltau massif, Southern Kazakhstan (Central Asian Orogenic Belt","created_at":"2019-09-21T02:42:13.547-07:00","url":"https://www.academia.edu/40407068/Multi_stage_metamorphic_evolution_and_protolith_reconstruction_of_spinel_bearing_and_symplectite_bearing_ultramafic_rocks_in_the_Zheltau_massif_Southern_Kazakhstan_Central_Asian_Orogenic_Belt?f_ri=172299","dom_id":"work_40407068","summary":"Spinel-bearing ultramafic rocks, metamorphosed in high-pressure conditions, are described from the metamor-phic complexes of the western part of the Central Asian Orogenic Belt (CAOB) in the Chu-Yili region in Southern Kazakhstan. They comprise small bodies of magnetite-bearing serpentinites, Cr-spinel-bearing serpentinized and amphibolitized dunites and peridotites enclosed by strongly retrogressed kyanite-bearing paragneisses. Apart from serpentinization, the ultramafic rocks were also overprinted by later rodingitization expressed in the development of the index-minerals hydrogrossular, prehnite and vuagnatite. Cr-spinel-bearing peridotites are characterized by extensive development of symplectitic and coronitic microtextures, which are interpreted to have been formed after garnet breakdown during decompression (i.e. exhumation). Calculated pressure (P) and temperature (T) obtained by phase diagram modeling and conventional geothermobarometry for the symplectites were P 11.5-14.5 kbar for a wide temperature range of T 600-850 °C, which followed the transition from garnet to spinel peridotite. Major and trace element whole-rock geochemical characteristics of the spinel-bearing ultra-mafic rocks as well as their structurally close relations indicate their mutual origin as parts of an oceanic cumulate complex of an arc-basin system. The protoliths were probably plagioclase-bearing (thus shallow, crustal) ultra-mafic rocks and troctolites, subducted to eclogite facies conditions and then exhumed along with other metamor-phic complexes of the Zheltau massif. These spinel-bearing ultramafic rocks could be classified as crustal formations in accordance with the inferred depths of their origin (b5 kbar), in common with many HP ultra-mafic/mafic complexes in the CAOB. However, strongly depleted geochemical signatures of the rocks, together with the distinctive microtextural features observed in the spinel peridotites, are unique, and their occurrence in the western CAOB is described here for the first time.","downloadable_attachments":[{"id":60660742,"asset_id":40407068,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":3625605,"first_name":"Taisia","last_name":"Alifirova","domain_name":"independent","page_name":"TayaAlifirova","display_name":"Taisia Alifirova","profile_url":"https://independent.academia.edu/TayaAlifirova?f_ri=172299","photo":"https://0.academia-photos.com/3625605/1270868/16399508/s65_taya.alifirova.jpg"},{"id":28460253,"first_name":"Anfisa","last_name":"Pilitsyna","domain_name":"independent","page_name":"AnfisaPilitsyna","display_name":"Anfisa Pilitsyna","profile_url":"https://independent.academia.edu/AnfisaPilitsyna?f_ri=172299","photo":"https://0.academia-photos.com/28460253/12881500/28029158/s65_anfisa.pilitsyna.jpg"}],"research_interests":[{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=172299","nofollow":false},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299","nofollow":false},{"id":54668,"name":"Peridotite","url":"https://www.academia.edu/Documents/in/Peridotite?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":191925,"name":"Symplectites","url":"https://www.academia.edu/Documents/in/Symplectites?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_30375599" data-work_id="30375599" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/30375599/CONSIDERACIONES_SOBRE_EL_METAMORFISMO_Y_LA_MICROTECT%C3%93NICA_DE_LOS_M%C3%81RMOLES_DE_POLANCO">CONSIDERACIONES SOBRE EL METAMORFISMO Y LA MICROTECTÓNICA DE LOS MÁRMOLES DE POLANCO</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">RESUMEN Los mármoles que afloran extensamente entre las localidades de Polanco y Manguera Azul presentan una serie de estructuras meso a microscópicas, así como una asociación mineral de metamorfismo dinamotérmico, de grado bajo (facies... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_30375599" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">RESUMEN Los mármoles que afloran extensamente entre las localidades de Polanco y Manguera Azul presentan una serie de estructuras meso a microscópicas, así como una asociación mineral de metamorfismo dinamotérmico, de grado bajo (facies esquistos verdes). El presente trabajo aborda algunos aspectos históricos, petrográficos (mineralógicos y microestructurales) y de campo sobre el metamorfismo de los mismos, tema sobre el cual varios autores reseñan diferentes aspectos. Se presentan aquí los resultados de observaciones de campo y petrografía en lámina delgada de muestras colectadas entre las localidades de Manguera Azul, Polanco y Barriga Negra.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/30375599" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2d3eca6b7b8a6b9bc854dc53c5252469" rel="nofollow" data-download="{"attachment_id":50825462,"asset_id":30375599,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/50825462/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="10868200" href="https://independent.academia.edu/HernanSilva1">Hernan Silva</a><script data-card-contents-for-user="10868200" type="text/json">{"id":10868200,"first_name":"Hernan","last_name":"Silva","domain_name":"independent","page_name":"HernanSilva1","display_name":"Hernan Silva","profile_url":"https://independent.academia.edu/HernanSilva1?f_ri=172299","photo":"https://0.academia-photos.com/10868200/4376306/5079797/s65_hernan.silva.jpg_oh_62b22dd84386dd64cb9ccd4908fc5c31_oe_54939619___gda___1415315798_bbd7e803a2f81f4725f3c80f6bcf3f3d"}</script></span></span></li><li class="js-paper-rank-work_30375599 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="30375599"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 30375599, container: ".js-paper-rank-work_30375599", }); 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El presente trabajo aborda algunos aspectos históricos, petrográficos (mineralógicos y microestructurales) y de campo sobre el metamorfismo de los mismos, tema sobre el cual varios autores reseñan diferentes aspectos. Se presentan aquí los resultados de observaciones de campo y petrografía en lámina delgada de muestras colectadas entre las localidades de Manguera Azul, Polanco y Barriga Negra.","downloadable_attachments":[{"id":50825462,"asset_id":30375599,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":10868200,"first_name":"Hernan","last_name":"Silva","domain_name":"independent","page_name":"HernanSilva1","display_name":"Hernan Silva","profile_url":"https://independent.academia.edu/HernanSilva1?f_ri=172299","photo":"https://0.academia-photos.com/10868200/4376306/5079797/s65_hernan.silva.jpg_oh_62b22dd84386dd64cb9ccd4908fc5c31_oe_54939619___gda___1415315798_bbd7e803a2f81f4725f3c80f6bcf3f3d"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=172299","nofollow":false},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":30029,"name":"Uruguay","url":"https://www.academia.edu/Documents/in/Uruguay?f_ri=172299","nofollow":false},{"id":71503,"name":"Marbles","url":"https://www.academia.edu/Documents/in/Marbles?f_ri=172299"},{"id":147519,"name":"Geologia","url":"https://www.academia.edu/Documents/in/Geologia?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":358945,"name":"Tectonica","url":"https://www.academia.edu/Documents/in/Tectonica?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_26524997" data-work_id="26524997" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/26524997/Isotope_and_trace_element_heterogeneities_in_high_grade_basic_metamorphic_rocks_of_Marvejols_Tectonic_implications_for_the_hercynian_suture_zone_of_the_French_Massif_Central">Isotope and trace-element heterogeneities in high-grade basic metamorphic rocks of Marvejols: Tectonic implications for the hercynian suture zone of the French Massif Central</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/26524997" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li 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href="https://shef.academia.edu/JeanLouisBodinier">Jean-Louis Bodinier</a><script data-card-contents-for-user="50493172" type="text/json">{"id":50493172,"first_name":"Jean-Louis","last_name":"Bodinier","domain_name":"shef","page_name":"JeanLouisBodinier","display_name":"Jean-Louis Bodinier","profile_url":"https://shef.academia.edu/JeanLouisBodinier?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_26524997 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="26524997"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 26524997, container: ".js-paper-rank-work_26524997", }); });</script></li><li class="js-percentile-work_26524997 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" 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type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="409" href="https://www.academia.edu/Documents/in/Geophysics">Geophysics</a>, <script data-card-contents-for-ri="409" type="text/json">{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="10769" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a><script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=26524997]'), work: {"id":26524997,"title":"Isotope and trace-element heterogeneities in high-grade basic metamorphic rocks of Marvejols: Tectonic implications for the hercynian suture zone of the French Massif Central","created_at":"2016-06-27T00:04:16.808-07:00","url":"https://www.academia.edu/26524997/Isotope_and_trace_element_heterogeneities_in_high_grade_basic_metamorphic_rocks_of_Marvejols_Tectonic_implications_for_the_hercynian_suture_zone_of_the_French_Massif_Central?f_ri=172299","dom_id":"work_26524997","summary":null,"downloadable_attachments":[{"id":46821122,"asset_id":26524997,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":50493172,"first_name":"Jean-Louis","last_name":"Bodinier","domain_name":"shef","page_name":"JeanLouisBodinier","display_name":"Jean-Louis Bodinier","profile_url":"https://shef.academia.edu/JeanLouisBodinier?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=172299","nofollow":false},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_18744425" data-work_id="18744425" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/18744425/Hypersaline_fluids_generated_by_high_grade_metamorphism_of_evaporites_Fluid_inclusion_study_of_uranium_occurrences_in_the_Western_Zambian_Copperbelt">Hypersaline fluids generated by high-grade metamorphism of evaporites: Fluid inclusion study of uranium occurrences in the Western Zambian Copperbelt</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">In the Pan-African Lufilian belt (Western Zambian Copperbelt), uranium mineralizations, preferentially scattered in kyanite ± talc micaschists (metamorphosed evaporitic sediments) or concentrated along transposed quartz veins provide an... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_18744425" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">In the Pan-African Lufilian belt (Western Zambian Copperbelt), uranium mineralizations, preferentially scattered in kyanite ± talc micaschists (metamorphosed evaporitic sediments) or concentrated along transposed quartz veins provide an opportunity to (1) understand the time/space relationship between the ore minerals and the deformation of the host rocks, (2) identify the different fluid events associated with specific stages of quartz deformation and (3) characterize the ore fluid geochemistry in terms of fluid origin and fluid/rock interactions. In the U occurrences studied in Lolwa and Mitukuluku (Domes region, Western Zambian Copperbelt), two mineralizing stages are described. The first generation of ore fluids (53–59 wt% CaCl2, 13–15 wt% NaCl; N2–H2 in the gas phase of fluid inclusions) circulated during the high-temperature quartz recrystallization, at 500–700 °C. This temperature is in agreement with the P–T conditions recorded during the crustal thickening related to continental collision at ca. 530 Ma. LA-ICPMS analyses show the presence of uranium within this fluid, with a concentration mode around 20 ppm. The second generation of ore fluid (21–32 wt% NaCl, 19–21 wt% CaCl2; CO2–CO in the gas phase of fluid inclusions) percolated at lower temperature conditions, at the brittle–ductile transition, between 200 and 300 °C. This temperature could be related to the exhumation of the high-grade metamorphic rocks at ca. 500 Ma. The formation of H2 and CO is interpreted as the result of radiolysis in the presence of dissolved uranium in the aqueous phase of these fluid inclusions. Finally, a late fluid (14–16 wt% NaClequiv) circulated in the brittle domain but seems unrelated to U (re-)mobilization event.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/18744425" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="399ae177b33a1c6b627828d3f2258035" rel="nofollow" data-download="{"attachment_id":40231774,"asset_id":18744425,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/40231774/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="36621028" href="https://univ-lorraine.academia.edu/AntoninRichard">Antonin Richard</a><script data-card-contents-for-user="36621028" type="text/json">{"id":36621028,"first_name":"Antonin","last_name":"Richard","domain_name":"univ-lorraine","page_name":"AntoninRichard","display_name":"Antonin Richard","profile_url":"https://univ-lorraine.academia.edu/AntoninRichard?f_ri=172299","photo":"https://0.academia-photos.com/36621028/10755556/12005903/s65_antonin.richard.jpg"}</script></span></span></li><li class="js-paper-rank-work_18744425 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="18744425"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 18744425, container: ".js-paper-rank-work_18744425", }); 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In the U occurrences studied in Lolwa and Mitukuluku (Domes region, Western Zambian Copperbelt), two mineralizing stages are described. The first generation of ore fluids (53–59 wt% CaCl2, 13–15 wt% NaCl; N2–H2 in the gas phase of fluid inclusions) circulated during the high-temperature quartz recrystallization, at 500–700 °C. This temperature is in agreement with the P–T conditions recorded during the crustal thickening related to continental collision at ca. 530 Ma. LA-ICPMS analyses show the presence of uranium within this fluid, with a concentration mode around 20 ppm. The second generation of ore fluid (21–32 wt% NaCl, 19–21 wt% CaCl2; CO2–CO in the gas phase of fluid inclusions) percolated at lower temperature conditions, at the brittle–ductile transition, between 200 and 300 °C. This temperature could be related to the exhumation of the high-grade metamorphic rocks at ca. 500 Ma. The formation of H2 and CO is interpreted as the result of radiolysis in the presence of dissolved uranium in the aqueous phase of these fluid inclusions. Finally, a late fluid (14–16 wt% NaClequiv) circulated in the brittle domain but seems unrelated to U (re-)mobilization event.","downloadable_attachments":[{"id":40231774,"asset_id":18744425,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":36621028,"first_name":"Antonin","last_name":"Richard","domain_name":"univ-lorraine","page_name":"AntoninRichard","display_name":"Antonin Richard","profile_url":"https://univ-lorraine.academia.edu/AntoninRichard?f_ri=172299","photo":"https://0.academia-photos.com/36621028/10755556/12005903/s65_antonin.richard.jpg"}],"research_interests":[{"id":2406,"name":"Economic Geology","url":"https://www.academia.edu/Documents/in/Economic_Geology?f_ri=172299","nofollow":false},{"id":82911,"name":"fluid Inclusions","url":"https://www.academia.edu/Documents/in/fluid_Inclusions?f_ri=172299","nofollow":false},{"id":83556,"name":"Evaporites","url":"https://www.academia.edu/Documents/in/Evaporites?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":644878,"name":"Copperbelt","url":"https://www.academia.edu/Documents/in/Copperbelt?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_2127284" data-work_id="2127284" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/2127284/A_geochemical_study_of_aluminous_granulites_from_the_high_grade_metamorphic_terrain_of_southern_Karnataka_India">A geochemical study of aluminous granulites from the high-grade metamorphic terrain of southern Karnataka, India</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/2127284" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2a944649824be153a54a3e3e77a4225d" rel="nofollow" data-download="{"attachment_id":30185810,"asset_id":2127284,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" 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href="https://www.academia.edu/Documents/in/Petrology">Petrology</a>, <script data-card-contents-for-ri="2404" type="text/json">{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="2635" href="https://www.academia.edu/Documents/in/Metamorphic_Petrology">Metamorphic Petrology</a><script data-card-contents-for-ri="2635" type="text/json">{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=2127284]'), work: {"id":2127284,"title":"A geochemical study of aluminous granulites from the high-grade metamorphic terrain of southern Karnataka, India","created_at":"2012-11-13T02:18:44.268-08:00","url":"https://www.academia.edu/2127284/A_geochemical_study_of_aluminous_granulites_from_the_high_grade_metamorphic_terrain_of_southern_Karnataka_India?f_ri=172299","dom_id":"work_2127284","summary":null,"downloadable_attachments":[{"id":30185810,"asset_id":2127284,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":2456695,"first_name":"Tejaswi","last_name":"Lakkundi","domain_name":"kud-in","page_name":"TejaswaiL","display_name":"Tejaswi Lakkundi","profile_url":"https://kud-in.academia.edu/TejaswaiL?f_ri=172299","photo":"https://0.academia-photos.com/2456695/769371/1120592/s65_tejaswai.l.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":2404,"name":"Petrology","url":"https://www.academia.edu/Documents/in/Petrology?f_ri=172299","nofollow":false},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=172299","nofollow":false},{"id":8116,"name":"Trace element Geochemistry","url":"https://www.academia.edu/Documents/in/Trace_element_Geochemistry?f_ri=172299"},{"id":15941,"name":"Microtectonics And Metamorphic Geology","url":"https://www.academia.edu/Documents/in/Microtectonics_And_Metamorphic_Geology?f_ri=172299"},{"id":16070,"name":"Petrologic Geochemistry","url":"https://www.academia.edu/Documents/in/Petrologic_Geochemistry?f_ri=172299"},{"id":16741,"name":"Geological Processes, Geochemistry","url":"https://www.academia.edu/Documents/in/Geological_Processes_Geochemistry?f_ri=172299"},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299"},{"id":20824,"name":"Thermodynamics in metamorphic petrology","url":"https://www.academia.edu/Documents/in/Thermodynamics_in_metamorphic_petrology?f_ri=172299"},{"id":22416,"name":"Granulites","url":"https://www.academia.edu/Documents/in/Granulites?f_ri=172299"},{"id":89567,"name":"Tectonics and Structural Geology, Metamorphic Petrology, Tectonic Geomorphology","url":"https://www.academia.edu/Documents/in/Tectonics_and_Structural_Geology_Metamorphic_Petrology_Tectonic_Geomorphology?f_ri=172299"},{"id":94129,"name":"High-Temperature Metamorphism","url":"https://www.academia.edu/Documents/in/High-Temperature_Metamorphism?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":215805,"name":"High Grade Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/High_Grade_Metamorphic_Petrology?f_ri=172299"},{"id":219290,"name":"Metamorphic Rocks Geochemistry","url":"https://www.academia.edu/Documents/in/Metamorphic_Rocks_Geochemistry?f_ri=172299"},{"id":255222,"name":"Igneous and Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Igneous_and_Metamorphic_Petrology?f_ri=172299"},{"id":621417,"name":"HT/HP Metamorphism and Crustal Anatexis","url":"https://www.academia.edu/Documents/in/HT_HP_Metamorphism_and_Crustal_Anatexis?f_ri=172299"},{"id":708388,"name":"Aluminous granulites","url":"https://www.academia.edu/Documents/in/Aluminous_granulites?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div 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type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="407" href="https://www.academia.edu/Documents/in/Geochemistry">Geochemistry</a>, <script data-card-contents-for-ri="407" type="text/json">{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="409" href="https://www.academia.edu/Documents/in/Geophysics">Geophysics</a>, <script data-card-contents-for-ri="409" type="text/json">{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="2635" href="https://www.academia.edu/Documents/in/Metamorphic_Petrology">Metamorphic Petrology</a><script data-card-contents-for-ri="2635" 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Belt)","created_at":"2022-04-01T04:35:24.180-07:00","url":"https://www.academia.edu/75143634/Multi_stage_metamorphic_evolution_and_protolith_reconstruction_of_spinel_bearing_and_symplectite_bearing_ultramafic_rocks_in_the_Zheltau_massif_Southern_Kazakhstan_Central_Asian_Orogenic_Belt_?f_ri=172299","dom_id":"work_75143634","summary":null,"downloadable_attachments":[{"id":83031258,"asset_id":75143634,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":3625605,"first_name":"Taisia","last_name":"Alifirova","domain_name":"independent","page_name":"TayaAlifirova","display_name":"Taisia Alifirova","profile_url":"https://independent.academia.edu/TayaAlifirova?f_ri=172299","photo":"https://0.academia-photos.com/3625605/1270868/16399508/s65_taya.alifirova.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=172299","nofollow":false},{"id":2635,"name":"Metamorphic Petrology","url":"https://www.academia.edu/Documents/in/Metamorphic_Petrology?f_ri=172299","nofollow":false},{"id":16937,"name":"Petrology and Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299"},{"id":54668,"name":"Peridotite","url":"https://www.academia.edu/Documents/in/Peridotite?f_ri=172299"},{"id":78133,"name":"Gondwana","url":"https://www.academia.edu/Documents/in/Gondwana?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":191925,"name":"Symplectites","url":"https://www.academia.edu/Documents/in/Symplectites?f_ri=172299"},{"id":897823,"name":"Elsevier","url":"https://www.academia.edu/Documents/in/Elsevier?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_14284392" data-work_id="14284392" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/14284392/Devonian_and_Carboniferous_conodonts_from_the_Kanthan_Limestone_Peninsular_Malaysia_and_their_stratigraphic_and_tectonic_implications">Devonian and Carboniferous conodonts from the Kanthan Limestone, Peninsular Malaysia and their stratigraphic and tectonic implications.</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Bedded pale-grey limestones, siliceous limestones and thinly interbedded dark-grey to black limestones and shales of the Kanthan Limestone have yielded Lower-Middle Devonian (Polygnathus costatus patulus, Polygnathus costatus costatus and... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_14284392" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Bedded pale-grey limestones, siliceous limestones and thinly interbedded dark-grey to black limestones and shales of the Kanthan Limestone have yielded Lower-Middle Devonian (Polygnathus costatus patulus, Polygnathus costatus costatus and Tortodus kockelianus conodont Zones) and mixed Devonian and Carboniferous (Scaliognathus anchoralis, Paragnathodus commutatus and Gnathodus bilineatus Zones with reworked Devonian conodonts) faunas. The presence of two disconformities in the sequence is revealed, separating Lower-Middle Devonian from overlying Upper Tournaisian (Tn3c, Scaliognathus anchoralis Zone), and one separating the Upper Tournaisian (Tn3c) from the Lower Visean (Arundian-Brigantian Paragnathodus commutatus and Gnathodus bilineatus Zones). The Upper Tournaisian and Lower Visean limestones also contain Devonian, Lower Tournaisian and basal Visean conodonts interpreted as reworked.  The Kanthan Limestone was deposited on the Sibumasu continental lithospheric block when it was still attached to and forming part of the NW Australian margin of Gondwanaland. The presence of the eastern Australian endemic genus Montognathus at Gunong Kanthan suggests close proximity of the Sibumasu terrane to Australia in the Carboniferous. In addition, the presence of Mestognathus in the Kanthan Limestone provides a biogeographic link with Gondwanaland and Laurentia in the Lower Carboniferous. The two observed disconformities are interpreted as possibly related to the rifting and separation of Chinese-SE Asian continental blocks from Gondwanaland in the Devonian-Carboniferous-Permian. Conodonts exhibit CAIs of 5 to 6 indicating that they have been heated to between 300oC and 500oC. The conodonts also include tectonically folded elements and show textural alteration interpreted as due to regional metamorphism.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/14284392" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="deb50f66fb8346e4c739179947966134" rel="nofollow" data-download="{"attachment_id":38256836,"asset_id":14284392,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/38256836/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="25161326" href="https://une-au.academia.edu/IanMetcalfe">Ian Metcalfe</a><script data-card-contents-for-user="25161326" type="text/json">{"id":25161326,"first_name":"Ian","last_name":"Metcalfe","domain_name":"une-au","page_name":"IanMetcalfe","display_name":"Ian Metcalfe","profile_url":"https://une-au.academia.edu/IanMetcalfe?f_ri=172299","photo":"https://0.academia-photos.com/25161326/6873491/7756375/s65_ian.metcalfe.jpg"}</script></span></span></li><li class="js-paper-rank-work_14284392 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="14284392"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 14284392, container: ".js-paper-rank-work_14284392", }); 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$(".js-view-count[data-work-id=14284392]").text(description); $(".js-view-count-work_14284392").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_14284392").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="14284392"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">6</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="10769" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="76748" href="https://www.academia.edu/Documents/in/Devonian">Devonian</a>, <script data-card-contents-for-ri="76748" type="text/json">{"id":76748,"name":"Devonian","url":"https://www.academia.edu/Documents/in/Devonian?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="96185" href="https://www.academia.edu/Documents/in/Carboniferous">Carboniferous</a>, <script data-card-contents-for-ri="96185" type="text/json">{"id":96185,"name":"Carboniferous","url":"https://www.academia.edu/Documents/in/Carboniferous?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=14284392]'), work: {"id":14284392,"title":"Devonian and Carboniferous conodonts from the Kanthan Limestone, Peninsular Malaysia and their stratigraphic and tectonic implications.","created_at":"2015-07-22T03:03:26.780-07:00","url":"https://www.academia.edu/14284392/Devonian_and_Carboniferous_conodonts_from_the_Kanthan_Limestone_Peninsular_Malaysia_and_their_stratigraphic_and_tectonic_implications?f_ri=172299","dom_id":"work_14284392","summary":"Bedded pale-grey limestones, siliceous limestones and thinly interbedded dark-grey to black limestones and shales of the Kanthan Limestone have yielded Lower-Middle Devonian (Polygnathus costatus patulus, Polygnathus costatus costatus and Tortodus kockelianus conodont Zones) and mixed Devonian and Carboniferous (Scaliognathus anchoralis, Paragnathodus commutatus and Gnathodus bilineatus Zones with reworked Devonian conodonts) faunas. The presence of two disconformities in the sequence is revealed, separating Lower-Middle Devonian from overlying Upper Tournaisian (Tn3c, Scaliognathus anchoralis Zone), and one separating the Upper Tournaisian (Tn3c) from the Lower Visean (Arundian-Brigantian Paragnathodus commutatus and Gnathodus bilineatus Zones). The Upper Tournaisian and Lower Visean limestones also contain Devonian, Lower Tournaisian and basal Visean conodonts interpreted as reworked. The Kanthan Limestone was deposited on the Sibumasu continental lithospheric block when it was still attached to and forming part of the NW Australian margin of Gondwanaland. The presence of the eastern Australian endemic genus Montognathus at Gunong Kanthan suggests close proximity of the Sibumasu terrane to Australia in the Carboniferous. In addition, the presence of Mestognathus in the Kanthan Limestone provides a biogeographic link with Gondwanaland and Laurentia in the Lower Carboniferous. The two observed disconformities are interpreted as possibly related to the rifting and separation of Chinese-SE Asian continental blocks from Gondwanaland in the Devonian-Carboniferous-Permian. Conodonts exhibit CAIs of 5 to 6 indicating that they have been heated to between 300oC and 500oC. The conodonts also include tectonically folded elements and show textural alteration interpreted as due to regional metamorphism.","downloadable_attachments":[{"id":38256836,"asset_id":14284392,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":25161326,"first_name":"Ian","last_name":"Metcalfe","domain_name":"une-au","page_name":"IanMetcalfe","display_name":"Ian Metcalfe","profile_url":"https://une-au.academia.edu/IanMetcalfe?f_ri=172299","photo":"https://0.academia-photos.com/25161326/6873491/7756375/s65_ian.metcalfe.jpg"}],"research_interests":[{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":76748,"name":"Devonian","url":"https://www.academia.edu/Documents/in/Devonian?f_ri=172299","nofollow":false},{"id":96185,"name":"Carboniferous","url":"https://www.academia.edu/Documents/in/Carboniferous?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":456389,"name":"Peninsular Malaysia","url":"https://www.academia.edu/Documents/in/Peninsular_Malaysia?f_ri=172299"},{"id":981386,"name":"Conodont Biostratigraphy","url":"https://www.academia.edu/Documents/in/Conodont_Biostratigraphy?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_14284246" data-work_id="14284246" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/14284246/Colour_and_textural_alteration_of_Palaeozoic_and_Triassic_conodonts_from_Peninsular_Malaysia_implications_for_tectonic_evolution_and_hydrocarbon_generation">Colour and textural alteration of Palaeozoic and Triassic conodonts from Peninsular Malaysia: implications for tectonic evolution and hydrocarbon generation. </a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Colour Alteration Indices (CAIs) of conodonts in Peninsular Malaysia range in value from 1.5 to 8 (Figure 1). The lowest values are found in Triassic limestones in northwest Peninsular Malaysia and the highest values occur in Palaeozoic... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_14284246" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Colour Alteration Indices (CAIs) of conodonts in Peninsular Malaysia range in value from 1.5 to 8 (Figure 1).  The lowest values are found in Triassic limestones in northwest Peninsular Malaysia and the highest values occur in Palaeozoic strata within or close to zones of deformation or to intrusives. Palaeozoic conodonts from the Sibumasu Block (Western Belt of Peninsular Malaysia) show a background value of CAI 5, all conodonts of Ordovician to Middle Permian age showing CAIs of at least 5 and locally up to 8. Palaeozoic conodonts of Sibumasu exhibit textural alteration interpreted as due to regional metamorphism, whereas Triassic conodonts exhibit little textural alteration. The disparity between CAIs and textural alteration of Palaeozoic vs. Triassic conodonts of Sibumasu suggests regional metamorphism of these rocks around the Palaeozoic/Mesozoic boundary which is consistent with the previously suggested timing for initial collision between the Sibumasu and Indochina blocks. Upper Palaeozoic conodonts from the Indochina Block (Central and Eastern Belts), however, are more variable.  Late Lower Carboniferous (Namurian) conodonts from the Panching Limestone in the Eastern Belt exhibit a CAI of 3 and appear to have escaped the effects of the regional metamorphism that affected the coeval rocks on the Sibumasu Block.  Permian conodonts from limestones along the western margin of the Central Belt have an anomalously high CAI of 5, probably caused by the heating effect of the Main Range Granitoids. <br />Triassic conodont CAIs for Peninsular Malaysia show an overall range of 1.5 to 5.  The lower values of 1.5-2.5 are found in conodonts from the Kodiang and Chuping limestones of northwest Peninsular Malaysia and indicate that these sediments fall within the mature liquid hydrocarbon window. This indicates that these, and similar early Mesozoic sediments buried beneath offshore Cenozoic sediments, may have acted as source rocks for hydrocarbons now trapped in Mesozoic and Cenozoic sedimentary basins of the region.  Conodonts from the Lower-Middle Triassic of Gunong Keriang, south of the main Kodiang limestone, appears to be anomalous with CAIs of 3-4.  These higher values are unlikely to be caused by extra overburden but could be due to the presence of a subsurface intrusion.  Gravity data from the area, however, suggests that this is not the case and that migration of hydrothermal fluids may be the cause.  High Triassic values of CAI 5 are recorded from Lower-Middle Triassic limestones along the western margin of the Central Belt and are probably the result of heating by the Main Range Granitoids of latest Triassic-Early Jurassic age.  Values of CAI 5 are also recorded from Middle Triassic pelagic limestones associated with cherts of the Semanggol Formation in Kedah.  This CAI value implies an overburden of 7,500-10,000 metres if the CAI is due solely to burial but the estimated maximum overburden is only 3,500 mtres indicating that the CAI is anomalously high.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/14284246" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="3e902d16a9fe13a9c6d21f0827f16a48" rel="nofollow" data-download="{"attachment_id":38256729,"asset_id":14284246,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/38256729/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="25161326" href="https://une-au.academia.edu/IanMetcalfe">Ian Metcalfe</a><script data-card-contents-for-user="25161326" type="text/json">{"id":25161326,"first_name":"Ian","last_name":"Metcalfe","domain_name":"une-au","page_name":"IanMetcalfe","display_name":"Ian Metcalfe","profile_url":"https://une-au.academia.edu/IanMetcalfe?f_ri=172299","photo":"https://0.academia-photos.com/25161326/6873491/7756375/s65_ian.metcalfe.jpg"}</script></span></span></li><li class="js-paper-rank-work_14284246 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="14284246"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 14284246, container: ".js-paper-rank-work_14284246", }); 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$(".js-view-count[data-work-id=14284246]").text(description); $(".js-view-count-work_14284246").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_14284246").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="14284246"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">9</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="6818" href="https://www.academia.edu/Documents/in/Malaysia">Malaysia</a>, <script data-card-contents-for-ri="6818" type="text/json">{"id":6818,"name":"Malaysia","url":"https://www.academia.edu/Documents/in/Malaysia?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="10769" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="42008" href="https://www.academia.edu/Documents/in/Thermal_alteration">Thermal alteration</a>, <script data-card-contents-for-ri="42008" type="text/json">{"id":42008,"name":"Thermal alteration","url":"https://www.academia.edu/Documents/in/Thermal_alteration?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="70354" href="https://www.academia.edu/Documents/in/Mesozoic">Mesozoic</a><script data-card-contents-for-ri="70354" type="text/json">{"id":70354,"name":"Mesozoic","url":"https://www.academia.edu/Documents/in/Mesozoic?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=14284246]'), work: {"id":14284246,"title":"Colour and textural alteration of Palaeozoic and Triassic conodonts from Peninsular Malaysia: implications for tectonic evolution and hydrocarbon generation. ","created_at":"2015-07-22T02:54:23.103-07:00","url":"https://www.academia.edu/14284246/Colour_and_textural_alteration_of_Palaeozoic_and_Triassic_conodonts_from_Peninsular_Malaysia_implications_for_tectonic_evolution_and_hydrocarbon_generation?f_ri=172299","dom_id":"work_14284246","summary":"Colour Alteration Indices (CAIs) of conodonts in Peninsular Malaysia range in value from 1.5 to 8 (Figure 1). The lowest values are found in Triassic limestones in northwest Peninsular Malaysia and the highest values occur in Palaeozoic strata within or close to zones of deformation or to intrusives. Palaeozoic conodonts from the Sibumasu Block (Western Belt of Peninsular Malaysia) show a background value of CAI 5, all conodonts of Ordovician to Middle Permian age showing CAIs of at least 5 and locally up to 8. Palaeozoic conodonts of Sibumasu exhibit textural alteration interpreted as due to regional metamorphism, whereas Triassic conodonts exhibit little textural alteration. The disparity between CAIs and textural alteration of Palaeozoic vs. Triassic conodonts of Sibumasu suggests regional metamorphism of these rocks around the Palaeozoic/Mesozoic boundary which is consistent with the previously suggested timing for initial collision between the Sibumasu and Indochina blocks. Upper Palaeozoic conodonts from the Indochina Block (Central and Eastern Belts), however, are more variable. Late Lower Carboniferous (Namurian) conodonts from the Panching Limestone in the Eastern Belt exhibit a CAI of 3 and appear to have escaped the effects of the regional metamorphism that affected the coeval rocks on the Sibumasu Block. Permian conodonts from limestones along the western margin of the Central Belt have an anomalously high CAI of 5, probably caused by the heating effect of the Main Range Granitoids. \nTriassic conodont CAIs for Peninsular Malaysia show an overall range of 1.5 to 5. The lower values of 1.5-2.5 are found in conodonts from the Kodiang and Chuping limestones of northwest Peninsular Malaysia and indicate that these sediments fall within the mature liquid hydrocarbon window. This indicates that these, and similar early Mesozoic sediments buried beneath offshore Cenozoic sediments, may have acted as source rocks for hydrocarbons now trapped in Mesozoic and Cenozoic sedimentary basins of the region. Conodonts from the Lower-Middle Triassic of Gunong Keriang, south of the main Kodiang limestone, appears to be anomalous with CAIs of 3-4. These higher values are unlikely to be caused by extra overburden but could be due to the presence of a subsurface intrusion. Gravity data from the area, however, suggests that this is not the case and that migration of hydrothermal fluids may be the cause. High Triassic values of CAI 5 are recorded from Lower-Middle Triassic limestones along the western margin of the Central Belt and are probably the result of heating by the Main Range Granitoids of latest Triassic-Early Jurassic age. Values of CAI 5 are also recorded from Middle Triassic pelagic limestones associated with cherts of the Semanggol Formation in Kedah. This CAI value implies an overburden of 7,500-10,000 metres if the CAI is due solely to burial but the estimated maximum overburden is only 3,500 mtres indicating that the CAI is anomalously high.","downloadable_attachments":[{"id":38256729,"asset_id":14284246,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":25161326,"first_name":"Ian","last_name":"Metcalfe","domain_name":"une-au","page_name":"IanMetcalfe","display_name":"Ian Metcalfe","profile_url":"https://une-au.academia.edu/IanMetcalfe?f_ri=172299","photo":"https://0.academia-photos.com/25161326/6873491/7756375/s65_ian.metcalfe.jpg"}],"research_interests":[{"id":6818,"name":"Malaysia","url":"https://www.academia.edu/Documents/in/Malaysia?f_ri=172299","nofollow":false},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":42008,"name":"Thermal alteration","url":"https://www.academia.edu/Documents/in/Thermal_alteration?f_ri=172299","nofollow":false},{"id":70354,"name":"Mesozoic","url":"https://www.academia.edu/Documents/in/Mesozoic?f_ri=172299","nofollow":false},{"id":72541,"name":"Conodonts","url":"https://www.academia.edu/Documents/in/Conodonts?f_ri=172299"},{"id":171492,"name":"Paleozoic","url":"https://www.academia.edu/Documents/in/Paleozoic?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":270438,"name":"HYDROCARBONS","url":"https://www.academia.edu/Documents/in/HYDROCARBONS?f_ri=172299"},{"id":697809,"name":"Conodont Colour Alteration Index, CAI","url":"https://www.academia.edu/Documents/in/Conodont_Colour_Alteration_Index_CAI?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_647302" data-work_id="647302" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/647302/Metamorphic_history_of_the_South_Tibetan_Detachment_System_Mt_Everest_region_revealed_by_RSCM_thermometry_and_phase_equilibria_modelling">Metamorphic history of the South Tibetan Detachment System, Mt. Everest region, revealed by RSCM thermometry and phase equilibria modelling</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">This study combines microstructural observations with Raman spectroscopy on carbonaceous material (RSCM), phase equilibria modelling and U–Pb dating of titanite to delineate the metamorphic history of a well-exposed section through the... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_647302" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">This study combines microstructural observations with Raman spectroscopy on carbonaceous material (RSCM), phase equilibria modelling and U–Pb dating of titanite to delineate the metamorphic history of a well-exposed section through the South Tibetan Detachment System (STDS) in the Dzakaa Chu valley of Southern Tibet. In the hanging wall of the STDS, undeformed Tibetan Sedimentary Series rocks consistently record peak metamorphic temperatures of ∼340 °C. Temperatures increase down-section, reaching ∼650 °C at the base of the shear zone, defining an apparent metamorphic field gradient of ∼310 °C km−1 across the entire structure. U–Th–Pb geochronological data indicate that metamorphism and deformation at high temperatures occurred over a protracted period from at least 20 to 13 Ma. Deformation within this 1-km-thick zone of distributed top-down-to-the-northeast ductile shear included a strong component of vertical shortening and was responsible for significant condensing of palaeo-isotherms along the upper margin of the Greater Himalayan Series (GHS). We interpret the preservation of such a high metamorphic gradient to be the result of a progressive up-section migration in the locus of deformation within the zone. This segment of the STDS provides a detailed thermal and kinematic record of the exhumation of footwall GHS rocks from beneath the southern margin of the Tibetan plateau.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/647302" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="117229" href="https://ucsb.academia.edu/JohnCottle">John Cottle</a><script data-card-contents-for-user="117229" type="text/json">{"id":117229,"first_name":"John","last_name":"Cottle","domain_name":"ucsb","page_name":"JohnCottle","display_name":"John Cottle","profile_url":"https://ucsb.academia.edu/JohnCottle?f_ri=172299","photo":"https://0.academia-photos.com/117229/31517/28965/s65_john.cottle.jpg"}</script></span></span></li><li class="js-paper-rank-work_647302 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="647302"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 647302, container: ".js-paper-rank-work_647302", }); });</script></li><li class="js-percentile-work_647302 InlineList-item InlineList-item--bordered hidden u-tcGrayDark"><span class="percentile-widget hidden"><span class="u-mr2x percentile-widget" style="display: none">•</span><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 647302; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-percentile-work_647302"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></li><li class="js-view-count-work_647302 InlineList-item InlineList-item--bordered hidden"><div><span><span class="js-view-count view-count u-mr2x" data-work-id="647302"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 647302; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=647302]").text(description); $(".js-view-count-work_647302").attr('title', description).tooltip(); }); });</script></span><script>$(function() { $(".js-view-count-work_647302").removeClass('hidden') })</script></div></li><li class="InlineList-item u-positionRelative" style="max-width: 250px"><div class="u-positionAbsolute" data-has-card-for-ri-list="647302"><i class="fa fa-tag InlineList-item-icon u-positionRelative"></i>  <a class="InlineList-item-text u-positionRelative">6</a>  </div><span class="InlineList-item-text u-textTruncate u-pl9x"><a class="InlineList-item-text" data-has-card-for-ri="10769" href="https://www.academia.edu/Documents/in/Tectonics">Tectonics</a>, <script data-card-contents-for-ri="10769" type="text/json">{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="14228" href="https://www.academia.edu/Documents/in/Geochronology">Geochronology</a>, <script data-card-contents-for-ri="14228" type="text/json">{"id":14228,"name":"Geochronology","url":"https://www.academia.edu/Documents/in/Geochronology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="19524" href="https://www.academia.edu/Documents/in/Mountain_Building">Mountain Building</a>, <script data-card-contents-for-ri="19524" type="text/json">{"id":19524,"name":"Mountain Building","url":"https://www.academia.edu/Documents/in/Mountain_Building?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="22594" href="https://www.academia.edu/Documents/in/Himalayan_Tectonics">Himalayan Tectonics</a><script data-card-contents-for-ri="22594" type="text/json">{"id":22594,"name":"Himalayan Tectonics","url":"https://www.academia.edu/Documents/in/Himalayan_Tectonics?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=647302]'), work: {"id":647302,"title":"Metamorphic history of the South Tibetan Detachment System, Mt. Everest region, revealed by RSCM thermometry and phase equilibria modelling","created_at":"2011-06-06T06:28:25.386-07:00","url":"https://www.academia.edu/647302/Metamorphic_history_of_the_South_Tibetan_Detachment_System_Mt_Everest_region_revealed_by_RSCM_thermometry_and_phase_equilibria_modelling?f_ri=172299","dom_id":"work_647302","summary":"This study combines microstructural observations with Raman spectroscopy on carbonaceous material (RSCM), phase equilibria modelling and U–Pb dating of titanite to delineate the metamorphic history of a well-exposed section through the South Tibetan Detachment System (STDS) in the Dzakaa Chu valley of Southern Tibet. In the hanging wall of the STDS, undeformed Tibetan Sedimentary Series rocks consistently record peak metamorphic temperatures of ∼340 °C. Temperatures increase down-section, reaching ∼650 °C at the base of the shear zone, defining an apparent metamorphic field gradient of ∼310 °C km−1 across the entire structure. U–Th–Pb geochronological data indicate that metamorphism and deformation at high temperatures occurred over a protracted period from at least 20 to 13 Ma. Deformation within this 1-km-thick zone of distributed top-down-to-the-northeast ductile shear included a strong component of vertical shortening and was responsible for significant condensing of palaeo-isotherms along the upper margin of the Greater Himalayan Series (GHS). We interpret the preservation of such a high metamorphic gradient to be the result of a progressive up-section migration in the locus of deformation within the zone. This segment of the STDS provides a detailed thermal and kinematic record of the exhumation of footwall GHS rocks from beneath the southern margin of the Tibetan plateau.","downloadable_attachments":[],"ordered_authors":[{"id":117229,"first_name":"John","last_name":"Cottle","domain_name":"ucsb","page_name":"JohnCottle","display_name":"John Cottle","profile_url":"https://ucsb.academia.edu/JohnCottle?f_ri=172299","photo":"https://0.academia-photos.com/117229/31517/28965/s65_john.cottle.jpg"}],"research_interests":[{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299","nofollow":false},{"id":14228,"name":"Geochronology","url":"https://www.academia.edu/Documents/in/Geochronology?f_ri=172299","nofollow":false},{"id":19524,"name":"Mountain Building","url":"https://www.academia.edu/Documents/in/Mountain_Building?f_ri=172299","nofollow":false},{"id":22594,"name":"Himalayan Tectonics","url":"https://www.academia.edu/Documents/in/Himalayan_Tectonics?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":1006049,"name":"Erosion and Climate)","url":"https://www.academia.edu/Documents/in/Erosion_and_Climate_?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_77399332" data-work_id="77399332" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/77399332/Metamorphism_of_metasediments_at_the_scale_of_an_orogen_a_key_to_the_Tertiary_geodynamic_evolution_of_the_Alps">Metamorphism of metasediments at the scale of an orogen: a key to the Tertiary geodynamic evolution of the Alps</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Major discoveries in metamorphic petrology, as well as other geological disciplines, have been made in the Alps. The regional distribution of Late Cretaceous–Tertiary metamorphic conditions, documented in post-Hercynian metasediments... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_77399332" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Major discoveries in metamorphic petrology, as well as other geological disciplines, have been made in the Alps. The regional distribution of Late Cretaceous–Tertiary metamorphic conditions, documented in post-Hercynian metasediments across the entire Alpine belt from Corsica–Tuscany in the west to Vienna in the east, is presented in this paper. In view of the uneven distribution of information, we concentrate on type and grade of metamorphism; and we elected to distinguish between metamorphic paths where either pressure and temperature peaked simultaneously, or where the maximum temperature was reached at lower pressures, after a significant temperature increase on the decompression path.The results show which types of process caused the main metamorphic imprint: a subduction process in the western Alps, a collision process in the central Alps, and complex metamorphic structures in the eastern Alps, owing to a complex geodynamic and metamorphic history involving the succession of t...</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/77399332" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="dffa93a2eb15c277397cc1591d6605eb" rel="nofollow" data-download="{"attachment_id":84882773,"asset_id":77399332,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/84882773/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="109469929" href="https://independent.academia.edu/MariaedUARDAGOMESREIS">Maria edUARDA GOMES REIS</a><script data-card-contents-for-user="109469929" type="text/json">{"id":109469929,"first_name":"Maria edUARDA GOMES","last_name":"REIS","domain_name":"independent","page_name":"MariaedUARDAGOMESREIS","display_name":"Maria edUARDA GOMES REIS","profile_url":"https://independent.academia.edu/MariaedUARDAGOMESREIS?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_77399332 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="77399332"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 77399332, container: ".js-paper-rank-work_77399332", }); 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The regional distribution of Late Cretaceous–Tertiary metamorphic conditions, documented in post-Hercynian metasediments across the entire Alpine belt from Corsica–Tuscany in the west to Vienna in the east, is presented in this paper. In view of the uneven distribution of information, we concentrate on type and grade of metamorphism; and we elected to distinguish between metamorphic paths where either pressure and temperature peaked simultaneously, or where the maximum temperature was reached at lower pressures, after a significant temperature increase on the decompression path.The results show which types of process caused the main metamorphic imprint: a subduction process in the western Alps, a collision process in the central Alps, and complex metamorphic structures in the eastern Alps, owing to a complex geodynamic and metamorphic history involving the succession of t...","downloadable_attachments":[{"id":84882773,"asset_id":77399332,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":109469929,"first_name":"Maria edUARDA GOMES","last_name":"REIS","domain_name":"independent","page_name":"MariaedUARDAGOMESREIS","display_name":"Maria edUARDA GOMES REIS","profile_url":"https://independent.academia.edu/MariaedUARDAGOMESREIS?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=172299","nofollow":false},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":4107,"name":"High Pressure","url":"https://www.academia.edu/Documents/in/High_Pressure?f_ri=172299","nofollow":false},{"id":148652,"name":"Late Cretaceous","url":"https://www.academia.edu/Documents/in/Late_Cretaceous?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":926279,"name":"GEological Society of London","url":"https://www.academia.edu/Documents/in/GEological_Society_of_London?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_75823805" data-work_id="75823805" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/75823805/First_report_on_Mesozoic_eclogite_facies_metamorphism_preceding_Barrovian_overprint_from_the_western_Rhodope_Chalkidiki_northern_Greece_">First-report on Mesozoic eclogite-facies metamorphism preceding Barrovian overprint from the western Rhodope (Chalkidiki, northern Greece)</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Chalkidiki block in Northern Greece represents the southwesternmost piece of the ultrahigh-pressure Rhodope and has played an important role in the evolution of the North Aegean. The eastern part of the Chalkidiki block is a basement... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_75823805" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Chalkidiki block in Northern Greece represents the southwesternmost piece of the ultrahigh-pressure Rhodope and has played an important role in the evolution of the North Aegean. The eastern part of the Chalkidiki block is a basement complex (Vertiskos Unit) that is made largely of Palaeozoic granitoids and clastic sediments that metamorphosed during the Mesozoic. This basement is traditionally considered as part of the Rhodopean hanging-wall, an assignment mainly supported by the absence of high-pressure mineral indicators and the presence of a regional medium-pressure/medium-temperature amphibolite-facies Barrovian metamorphic imprint. Toward the west, the basement is juxtaposed with meta-sedimentary (Circum-Rhodope belt) and arc units (Chortiatis Magmatic Suite) that carry evidence of a Mesozoic high-pressure/low-temperature event. In this study, garnet–staurolite-mica schists from the eastern part of the basement were examined by means of micro-textures, mineral chemistry an...</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/75823805" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="9586269102fbe8054d1da6cfa2b5bffd" rel="nofollow" data-download="{"attachment_id":83461622,"asset_id":75823805,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/83461622/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="67085045" href="https://independent.academia.edu/KonstantinosKydonakis">Konstantinos Kydonakis</a><script data-card-contents-for-user="67085045" type="text/json">{"id":67085045,"first_name":"Konstantinos","last_name":"Kydonakis","domain_name":"independent","page_name":"KonstantinosKydonakis","display_name":"Konstantinos Kydonakis","profile_url":"https://independent.academia.edu/KonstantinosKydonakis?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_75823805 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="75823805"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 75823805, container: ".js-paper-rank-work_75823805", }); 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The eastern part of the Chalkidiki block is a basement complex (Vertiskos Unit) that is made largely of Palaeozoic granitoids and clastic sediments that metamorphosed during the Mesozoic. This basement is traditionally considered as part of the Rhodopean hanging-wall, an assignment mainly supported by the absence of high-pressure mineral indicators and the presence of a regional medium-pressure/medium-temperature amphibolite-facies Barrovian metamorphic imprint. Toward the west, the basement is juxtaposed with meta-sedimentary (Circum-Rhodope belt) and arc units (Chortiatis Magmatic Suite) that carry evidence of a Mesozoic high-pressure/low-temperature event. In this study, garnet–staurolite-mica schists from the eastern part of the basement were examined by means of micro-textures, mineral chemistry an...","downloadable_attachments":[{"id":83461622,"asset_id":75823805,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":67085045,"first_name":"Konstantinos","last_name":"Kydonakis","domain_name":"independent","page_name":"KonstantinosKydonakis","display_name":"Konstantinos 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and Eclogites in Kaghan-Naran Valley, Pakistan Himalaya","created_at":"2022-03-29T16:49:35.934-07:00","url":"https://www.academia.edu/74920519/Contrasting_Pressure_Temperature_Evolution_of_Pelitic_Schists_Gneisses_and_Eclogites_in_Kaghan_Naran_Valley_Pakistan_Himalaya?f_ri=172299","dom_id":"work_74920519","summary":null,"downloadable_attachments":[{"id":83585403,"asset_id":74920519,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":5323850,"first_name":"Hafiz","last_name":"Rehman","domain_name":"independent","page_name":"HafizRehman","display_name":"Hafiz 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js-work-card work_74686241" data-work_id="74686241" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/74686241/Geochronology_of_high_grade_metamorphism_in_the_Sveconorwegian_belt_S_Norway_U_Pb_Th_Pb_and_Re_Os_data">Geochronology of high-grade metamorphism in the Sveconorwegian belt, S. Norway: U-Pb, Th-Pb and Re-Os data</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Mesoproterozoic crust in the southwest part of the Fennoscandian Shield was reworked during the Sveconorwegian orogeny (Pasteels & Michot 1975; Berthelsen 1980; Demaiffe & Michot 1985; Falkum 1985). Though this idea has been well... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_74686241" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Mesoproterozoic crust in the southwest part of the Fennoscandian Shield was reworked during the Sveconorwegian orogeny (Pasteels & Michot 1975; Berthelsen 1980; Demaiffe & Michot 1985; Falkum 1985). Though this idea has been well established in the literature for decades, it is not until recently that the Sveconorwegian age of high-grade metamorphism was established in all lithotectonic units of the Sveconorwegian orogenic belt. Especially controversial was the timing of granulitefacies metamorphism in the Bamble Terrane in south Norway (Kullerud & Dahlgren 1993) and the Eastern Segment in southwestern Sweden (Johansson et al. 1991). Today, the objective is to improve the chronologic and tectonic model for the Sveconorwegian orogenic event itself. In this paper, monazite, zircon and titanite U-Pb data and molybdenite Re-Os data are reported from metamorphic rocks to date high-grade metamorphism in the four main lithotectonic units in south Norway. A pressure-temperature estimate...</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/74686241" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="f19fd5c1cdfc01d901da3b64bab4ea02" rel="nofollow" data-download="{"attachment_id":82748280,"asset_id":74686241,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/82748280/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="122566336" href="https://independent.academia.edu/%C3%98ysteinNordgulen">Øystein Nordgulen</a><script data-card-contents-for-user="122566336" type="text/json">{"id":122566336,"first_name":"Øystein","last_name":"Nordgulen","domain_name":"independent","page_name":"ØysteinNordgulen","display_name":"Øystein Nordgulen","profile_url":"https://independent.academia.edu/%C3%98ysteinNordgulen?f_ri=172299","photo":"https://0.academia-photos.com/122566336/30717065/28435491/s65__ystein.nordgulen.jpg"}</script></span></span></li><li class="js-paper-rank-work_74686241 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="74686241"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 74686241, container: ".js-paper-rank-work_74686241", }); 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Norway: U-Pb, Th-Pb and Re-Os data","created_at":"2022-03-27T05:18:01.826-07:00","url":"https://www.academia.edu/74686241/Geochronology_of_high_grade_metamorphism_in_the_Sveconorwegian_belt_S_Norway_U_Pb_Th_Pb_and_Re_Os_data?f_ri=172299","dom_id":"work_74686241","summary":"The Mesoproterozoic crust in the southwest part of the Fennoscandian Shield was reworked during the Sveconorwegian orogeny (Pasteels \u0026 Michot 1975; Berthelsen 1980; Demaiffe \u0026 Michot 1985; Falkum 1985). Though this idea has been well established in the literature for decades, it is not until recently that the Sveconorwegian age of high-grade metamorphism was established in all lithotectonic units of the Sveconorwegian orogenic belt. Especially controversial was the timing of granulitefacies metamorphism in the Bamble Terrane in south Norway (Kullerud \u0026 Dahlgren 1993) and the Eastern Segment in southwestern Sweden (Johansson et al. 1991). Today, the objective is to improve the chronologic and tectonic model for the Sveconorwegian orogenic event itself. In this paper, monazite, zircon and titanite U-Pb data and molybdenite Re-Os data are reported from metamorphic rocks to date high-grade metamorphism in the four main lithotectonic units in south Norway. A pressure-temperature estimate...","downloadable_attachments":[{"id":82748280,"asset_id":74686241,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":122566336,"first_name":"Øystein","last_name":"Nordgulen","domain_name":"independent","page_name":"ØysteinNordgulen","display_name":"Øystein 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Geochemistry","url":"https://www.academia.edu/Documents/in/Petrology_and_Geochemistry?f_ri=172299"},{"id":54668,"name":"Peridotite","url":"https://www.academia.edu/Documents/in/Peridotite?f_ri=172299"},{"id":78133,"name":"Gondwana","url":"https://www.academia.edu/Documents/in/Gondwana?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"},{"id":191925,"name":"Symplectites","url":"https://www.academia.edu/Documents/in/Symplectites?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_54068122" data-work_id="54068122" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/54068122/Pressure_temperature_time_evolution_of_high_pressure_rocks_of_the_Acatl%C3%A1n_Complex_southern_Mexico_Implications_for_the_evolution_of_the_Iapetus_and_Rheic_Oceans_Comment">Pressure-temperature-time evolution of high-pressure rocks of the Acatlán Complex (southern Mexico): Implications for the evolution of the Iapetus and Rheic Oceans: Comment</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">Vega-Granillo et al.(2007) are to be congratulated for publishing high-quality, pressure-temperature-time (PTt) data on the high-pressure (HP) rocks within the Acatlán Complex (Fig. 1); these data expand on previously published PT data of... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_54068122" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">Vega-Granillo et al.(2007) are to be congratulated for publishing high-quality, pressure-temperature-time (PTt) data on the high-pressure (HP) rocks within the Acatlán Complex (Fig. 1); these data expand on previously published PT data of Meza-Figueroa et al.(2005). The evolution of this complex and its Paleozoic oceanic assemblage are central to resolving the Paleozoic tectonothermal history of Mexico and its role in the understanding of the Appalachian-Ouachita orogeny and the assembly of Pangea. Although we welcome their ...</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/54068122" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="e7472fcbe30e5e8ad1b9f5773e45cb56" rel="nofollow" data-download="{"attachment_id":70611013,"asset_id":54068122,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" href="https://www.academia.edu/attachments/70611013/download_file?st=MTczMjQ0NDI2NSw4LjIyMi4yMDguMTQ2&s=work_strip"><i class="fa fa-arrow-circle-o-down fa-lg"></i><span class="u-textUppercase u-ml1x" data-content="button_text">Download</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="33255192" href="https://smu-ca.academia.edu/JDostal">Jaroslav Dostal</a><script data-card-contents-for-user="33255192" type="text/json">{"id":33255192,"first_name":"Jaroslav","last_name":"Dostal","domain_name":"smu-ca","page_name":"JDostal","display_name":"Jaroslav Dostal","profile_url":"https://smu-ca.academia.edu/JDostal?f_ri=172299","photo":"/images/s65_no_pic.png"}</script></span></span></li><li class="js-paper-rank-work_54068122 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="54068122"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 54068122, container: ".js-paper-rank-work_54068122", }); 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these data expand on previously published PT data of Meza-Figueroa et al.(2005). The evolution of this complex and its Paleozoic oceanic assemblage are central to resolving the Paleozoic tectonothermal history of Mexico and its role in the understanding of the Appalachian-Ouachita orogeny and the assembly of Pangea. Although we welcome their ...","downloadable_attachments":[{"id":70611013,"asset_id":54068122,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":33255192,"first_name":"Jaroslav","last_name":"Dostal","domain_name":"smu-ca","page_name":"JDostal","display_name":"Jaroslav Dostal","profile_url":"https://smu-ca.academia.edu/JDostal?f_ri=172299","photo":"/images/s65_no_pic.png"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=172299","nofollow":false},{"id":4107,"name":"High 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Implications for the evolution of the Iapetus and Rheic Oceans: Comment</a></div></div><div class="u-pb4x u-mt3x"></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/50138820" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><div class="download"><a id="2c6c2abc95b90316407aa2688a514dde" rel="nofollow" data-download="{"attachment_id":68236778,"asset_id":50138820,"asset_type":"Work","always_allow_download":false,"track":null,"button_location":"work_strip","source":null,"hide_modal":null}" class="Button Button--sm Button--inverseGreen js-download-button prompt_button doc_download" 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Comment","created_at":"2021-07-21T13:30:49.515-07:00","url":"https://www.academia.edu/50138820/Pressure_temperature_time_evolution_of_high_pressure_rocks_of_the_Acatlan_Complex_southern_Mexico_Implications_for_the_evolution_of_the_Iapetus_and_Rheic_Oceans_Comment?f_ri=172299","dom_id":"work_50138820","summary":null,"downloadable_attachments":[{"id":68236778,"asset_id":50138820,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":108893627,"first_name":"Duncan","last_name":"Keppie","domain_name":"independent","page_name":"DuncanKeppie","display_name":"Duncan 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Murphy","profile_url":"https://independent.academia.edu/BMurphy1?f_ri=172299","photo":"/images/s65_no_pic.png"},{"id":7164451,"first_name":"Amabel","last_name":"Ortega-Rivera","domain_name":"unam","page_name":"AmabelOrtegaRivera","display_name":"Amabel Ortega-Rivera","profile_url":"https://unam.academia.edu/AmabelOrtegaRivera?f_ri=172299","photo":"https://0.academia-photos.com/7164451/13938303/14994268/s65_amabel.ortega-rivera.png"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences?f_ri=172299","nofollow":false},{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=172299","nofollow":false},{"id":4107,"name":"High Pressure","url":"https://www.academia.edu/Documents/in/High_Pressure?f_ri=172299"},{"id":10769,"name":"Tectonics","url":"https://www.academia.edu/Documents/in/Tectonics?f_ri=172299"},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_6178908" data-work_id="6178908" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/6178908/Synoblique_convergent_and_extensional_deformation_and_metamorphism_in_the_Neoproterozoic_rocks_along_Wadi_Fatira_shear_zone_Northern_Eastern_Desert_Egypt">Synoblique convergent and extensional deformation and metamorphism in the Neoproterozoic rocks along Wadi Fatira shear zone, Northern Eastern Desert, Egypt</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The Wadi Fatira area occurs at the southern margin of the Northern Eastern Desert (NED) of Egypt and is occupied by highly sheared metavolcanics tectonically alternated with banded iron formations and intruded by Barud... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_6178908" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The Wadi Fatira area occurs at the southern margin of the Northern Eastern Desert (NED) of Egypt and is occupied by highly sheared metavolcanics tectonically alternated with banded iron formations and intruded by Barud tonalite–granodiorite, post-tectonic gabbroic and granitic intrusions. Detailed structural investigation showed that the schists and migmatitic amphibolites are formed by shearing in metavolcanics and syntectonic Barud tonalite–granodiorite due to movement along the Wadi Fatira shear zone (WFSZ). This shear zone starts as a NW–SE striking fault along Wadi Barud Al Azraq and the Eastern part of Wadi Fatira and turns to a E–W trending fault to the north of Wadi Fatira. Microstructural shear sense indicators such as asymmetric geometry of porphyroclasts such as σ-type and asymmetric folds deforming fine-grained bands which are frequently found around porphyroclasts indicate sinistral sense of shearing along the WFSZ. This shear zone is characterized by transitions from local convergence to local extension along their E–W and NW–SE trending parts, respectively. The NW–SE part of the WFSZ is of about 200 m in width and characterized by synmagmatic extensional features such as intrusion of synkinematic tonalite, creation of NE–SE trending normal faults, and formation of migmatitic amphibolites and schlieric tonalites. This part of the shear zone is metamorphosed under synthermal peak metamorphic conditions (725°C at 2–4 kbar). The E–W compressional part of the WFSZ is up to 3 km in width and composed of hornblende, chlorite, actinolite, and biotite schists together with sheared intermediate and acidic metatuffs. Contractional and transpressional structures in this part of the WFSZ include E–W trending major asymmetrical anticline and syncline, nearly vertical foliation and steeply pitching stretching lineations, NNE dipping minor thrusts, and minor intrafolial folds with their hinges parallel to the stretching lineation. P–T estimates using mineral analyses of plagioclase and hornblende from schists and foliated metavolcanics indicate prograde metamorphism under medium-grade amphibolite facies (500–600°C at 3–7 kbar) retrogressed to low-grade greenschist facies (227–317°C). The foliation in Barud tonalite–granodiorite close to the E–W part of the WFSZ runs parallel to the plane of shearing and the tonalite show numerous magmatic flow structures overprinted by folding and ductile shearing. The WFSZ is similar to structures resulted from combined simple shear and orthogonal shortening of oblique transpressive shear zones and their sense of movement is comparable with the characteristics of the Najd Fault System. تقع منطقة وادى فطيرة على الحافة الجنوبية للجزء الشمالي من الصحراء الشرقية المصرية، والمنطقة يتواجد بها صخور البركانيات المتحولة يصاحبها رقائق من تكوينات الحديد ويتداخل فى هذه الصخور جرانيت وادى بارود المصاحب للحركة التكتونية وكذلك بعض من متداخلات مابعد الحركة التكتونية من الجرانيت والجابرو. الدراسة التركيبية التفصيلية للمنطقة أثبتت ان الشيست والأمفيبولايت الميجماتى تكونا نتيجة التشوة والتحول اللذان حدثا للصخور البركانية وتوناليت-جرانودايورايت وادى بارود وذلك كنتيجة للحركة على نطاق تشوه وادى فطيرة وأثناء تداخل جرانيت وادى بارود. نطاق تشوه وادى فطيرة بدأ كصدع يتجة شمال غربى-جنوب شرقى عبر وادى بارود الأزرق والجزء الشرقى من وادى فطيرة ثم تغير مساره الى صدع يتجه شرق-غرب وذلك الى الشمال من وادى فطيرة. أدلة الحركة مثل تواجد البروفيروبلاست فى شكل سيجما، تواجد الطيات الدقيقة الغير متماثلة والتى تشوه الأشرطة الدقيقة الموجودة حول البروفيروبلاست، هذه الأدلة أكدت أن الحركة يسارية عبر نطاق تشوه وادى فطيرة. يتميز نطاق تشوه وادى فطيرة بالانتقال من مرحلة التشوة المصاحب للتقارب المائل الى التشوه المصاحب للبسط والإطالة. يتكون نطاق بتر وادى فطيرة من جزأين، الجزء الأول يتجه شمال غرب – جنوب شرق وهذا اتساعه حوالى 200 متر ويتميز بتواجد الظواهر المصاحبة لتشوه البسط والصخور فى الحالة المجماتية، ومن أمثلة هذا الظواهر تداخل جرانيت وادى بارود، الصدوع التى تتجة شمال شرق-جنوب غرب، وتكوين الأمفيبولايت الميجماتى والتونالايت ذو الأشرطة. وجد أن ظروف التحول فى هذا الجزء من نطاق التشوه وصلت الى قمة الحرارة حيث تم تسجيل حرارة تصل الى 725 درجة مئوية وضغط يتراوح بين 2 الى 4 كليوبار. أما الجزء الثانى من نطاق تشوه وادى فطيرة فإنه يتجه شرق-غرب واتساعه حوالى 3 كيلومتر ويتكون من أنواع مختلفة من صخر الشيست بالإضافة الى صخور بركانية متوسطة التشوه. ويميز هذا الجزء من نطاق تشوه وادى فطيرة التراكيب المصاحبة للتضاغط والتقارب والتى تشمل التحدبات والتقعرات الغير متماثلة والتى تتجه شرق-غرب، التورق الشبة رأسى واستطالة المعادن شديدة الغطس، الدسور المائلة فى اتجاه شمال الشمال الشرقى، والطيات الصغيرة التى تتوازى اتجاهات محاورها مع الاتجاهات التى تميز استطالة المعادن. وجد ان الصخور فى هذا الجزء من نطاق التشوة تحولت تحت ظروف من الضغط ودرجة الحرارة تتوافق مع سحنة الأمفيبولايت (500-600 درجة مئوية، 3-7 كيلوبار) ثم حدث تراجع حتى وصلت الى سحنة الشيست الأخضر (227-317 درجة مئوية). التورق الذى يميز صخور التوناليت والجرانودايورايت فى متداخل جرانيت وادى بارود يتوازى مع مستوى التشوه فى هذا الجزء من نطاق تشوه وادى فطيرة. أخيرا، ان نطاق تشوه وادى فطيرة يشبه التراكيب التى تنتج من تأثير simple shear والتقصير المتعامد المصاحب لنطاقات التشوة والعقص المائلة هذا يجعله مشابه لنطاقات التشوه التى تميز نظام صدوع النجد. للمراسلة: د/ محمد احمد عبد الواحد</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" 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type="text/json">{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="1419" href="https://www.academia.edu/Documents/in/Structural_Geology">Structural Geology</a>, <script data-card-contents-for-ri="1419" type="text/json">{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="158597" href="https://www.academia.edu/Documents/in/Iron">Iron</a>, <script data-card-contents-for-ri="158597" type="text/json">{"id":158597,"name":"Iron","url":"https://www.academia.edu/Documents/in/Iron?f_ri=172299","nofollow":false}</script><a class="InlineList-item-text" data-has-card-for-ri="172299" href="https://www.academia.edu/Documents/in/Metamorphism">Metamorphism</a><script data-card-contents-for-ri="172299" type="text/json">{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false}</script></span></li><script>(function(){ if (true) { new Aedu.ResearchInterestListCard({ el: $('*[data-has-card-for-ri-list=6178908]'), work: {"id":6178908,"title":"Synoblique convergent and extensional deformation and metamorphism in the Neoproterozoic rocks along Wadi Fatira shear zone, Northern Eastern Desert, Egypt","created_at":"2014-02-23T06:14:43.754-08:00","url":"https://www.academia.edu/6178908/Synoblique_convergent_and_extensional_deformation_and_metamorphism_in_the_Neoproterozoic_rocks_along_Wadi_Fatira_shear_zone_Northern_Eastern_Desert_Egypt?f_ri=172299","dom_id":"work_6178908","summary":"The Wadi Fatira area occurs at the southern margin of the Northern Eastern Desert (NED) of Egypt and is occupied by highly sheared metavolcanics tectonically alternated with banded iron formations and intruded by Barud tonalite–granodiorite, post-tectonic gabbroic and granitic intrusions. Detailed structural investigation showed that the schists and migmatitic amphibolites are formed by shearing in metavolcanics and syntectonic Barud tonalite–granodiorite due to movement along the Wadi Fatira shear zone (WFSZ). This shear zone starts as a NW–SE striking fault along Wadi Barud Al Azraq and the Eastern part of Wadi Fatira and turns to a E–W trending fault to the north of Wadi Fatira. Microstructural shear sense indicators such as asymmetric geometry of porphyroclasts such as σ-type and asymmetric folds deforming fine-grained bands which are frequently found around porphyroclasts indicate sinistral sense of shearing along the WFSZ. This shear zone is characterized by transitions from local convergence to local extension along their E–W and NW–SE trending parts, respectively. The NW–SE part of the WFSZ is of about 200 m in width and characterized by synmagmatic extensional features such as intrusion of synkinematic tonalite, creation of NE–SE trending normal faults, and formation of migmatitic amphibolites and schlieric tonalites. This part of the shear zone is metamorphosed under synthermal peak metamorphic conditions (725°C at 2–4 kbar). The E–W compressional part of the WFSZ is up to 3 km in width and composed of hornblende, chlorite, actinolite, and biotite schists together with sheared intermediate and acidic metatuffs. Contractional and transpressional structures in this part of the WFSZ include E–W trending major asymmetrical anticline and syncline, nearly vertical foliation and steeply pitching stretching lineations, NNE dipping minor thrusts, and minor intrafolial folds with their hinges parallel to the stretching lineation. P–T estimates using mineral analyses of plagioclase and hornblende from schists and foliated metavolcanics indicate prograde metamorphism under medium-grade amphibolite facies (500–600°C at 3–7 kbar) retrogressed to low-grade greenschist facies (227–317°C). The foliation in Barud tonalite–granodiorite close to the E–W part of the WFSZ runs parallel to the plane of shearing and the tonalite show numerous magmatic flow structures overprinted by folding and ductile shearing. The WFSZ is similar to structures resulted from combined simple shear and orthogonal shortening of oblique transpressive shear zones and their sense of movement is comparable with the characteristics of the Najd Fault System. تقع منطقة وادى فطيرة على الحافة الجنوبية للجزء الشمالي من الصحراء الشرقية المصرية، والمنطقة يتواجد بها صخور البركانيات المتحولة يصاحبها رقائق من تكوينات الحديد ويتداخل فى هذه الصخور جرانيت وادى بارود المصاحب للحركة التكتونية وكذلك بعض من متداخلات مابعد الحركة التكتونية من الجرانيت والجابرو. الدراسة التركيبية التفصيلية للمنطقة أثبتت ان الشيست والأمفيبولايت الميجماتى تكونا نتيجة التشوة والتحول اللذان حدثا للصخور البركانية وتوناليت-جرانودايورايت وادى بارود وذلك كنتيجة للحركة على نطاق تشوه وادى فطيرة وأثناء تداخل جرانيت وادى بارود. نطاق تشوه وادى فطيرة بدأ كصدع يتجة شمال غربى-جنوب شرقى عبر وادى بارود الأزرق والجزء الشرقى من وادى فطيرة ثم تغير مساره الى صدع يتجه شرق-غرب وذلك الى الشمال من وادى فطيرة. أدلة الحركة مثل تواجد البروفيروبلاست فى شكل سيجما، تواجد الطيات الدقيقة الغير متماثلة والتى تشوه الأشرطة الدقيقة الموجودة حول البروفيروبلاست، هذه الأدلة أكدت أن الحركة يسارية عبر نطاق تشوه وادى فطيرة. يتميز نطاق تشوه وادى فطيرة بالانتقال من مرحلة التشوة المصاحب للتقارب المائل الى التشوه المصاحب للبسط والإطالة. يتكون نطاق بتر وادى فطيرة من جزأين، الجزء الأول يتجه شمال غرب – جنوب شرق وهذا اتساعه حوالى 200 متر ويتميز بتواجد الظواهر المصاحبة لتشوه البسط والصخور فى الحالة المجماتية، ومن أمثلة هذا الظواهر تداخل جرانيت وادى بارود، الصدوع التى تتجة شمال شرق-جنوب غرب، وتكوين الأمفيبولايت الميجماتى والتونالايت ذو الأشرطة. وجد أن ظروف التحول فى هذا الجزء من نطاق التشوه وصلت الى قمة الحرارة حيث تم تسجيل حرارة تصل الى 725 درجة مئوية وضغط يتراوح بين 2 الى 4 كليوبار. أما الجزء الثانى من نطاق تشوه وادى فطيرة فإنه يتجه شرق-غرب واتساعه حوالى 3 كيلومتر ويتكون من أنواع مختلفة من صخر الشيست بالإضافة الى صخور بركانية متوسطة التشوه. ويميز هذا الجزء من نطاق تشوه وادى فطيرة التراكيب المصاحبة للتضاغط والتقارب والتى تشمل التحدبات والتقعرات الغير متماثلة والتى تتجه شرق-غرب، التورق الشبة رأسى واستطالة المعادن شديدة الغطس، الدسور المائلة فى اتجاه شمال الشمال الشرقى، والطيات الصغيرة التى تتوازى اتجاهات محاورها مع الاتجاهات التى تميز استطالة المعادن. وجد ان الصخور فى هذا الجزء من نطاق التشوة تحولت تحت ظروف من الضغط ودرجة الحرارة تتوافق مع سحنة الأمفيبولايت (500-600 درجة مئوية، 3-7 كيلوبار) ثم حدث تراجع حتى وصلت الى سحنة الشيست الأخضر (227-317 درجة مئوية). التورق الذى يميز صخور التوناليت والجرانودايورايت فى متداخل جرانيت وادى بارود يتوازى مع مستوى التشوه فى هذا الجزء من نطاق تشوه وادى فطيرة. أخيرا، ان نطاق تشوه وادى فطيرة يشبه التراكيب التى تنتج من تأثير simple shear والتقصير المتعامد المصاحب لنطاقات التشوة والعقص المائلة هذا يجعله مشابه لنطاقات التشوه التى تميز نظام صدوع النجد. للمراسلة: د/ محمد احمد عبد الواحد","downloadable_attachments":[{"id":48981769,"asset_id":6178908,"asset_type":"Work","always_allow_download":false}],"ordered_authors":[{"id":9418047,"first_name":"Mohamed","last_name":"Abd El-Wahed","domain_name":"tanta","page_name":"MohamedAbdElWahed","display_name":"Mohamed Abd El-Wahed","profile_url":"https://tanta.academia.edu/MohamedAbdElWahed?f_ri=172299","photo":"https://0.academia-photos.com/9418047/2999663/3522203/s65_mohamed.abd_el-wahed.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":1419,"name":"Structural Geology","url":"https://www.academia.edu/Documents/in/Structural_Geology?f_ri=172299","nofollow":false},{"id":158597,"name":"Iron","url":"https://www.academia.edu/Documents/in/Iron?f_ri=172299","nofollow":false},{"id":172299,"name":"Metamorphism","url":"https://www.academia.edu/Documents/in/Metamorphism?f_ri=172299","nofollow":false},{"id":179580,"name":"Banded Iron Formation","url":"https://www.academia.edu/Documents/in/Banded_Iron_Formation?f_ri=172299"},{"id":284025,"name":"Shear Zone","url":"https://www.academia.edu/Documents/in/Shear_Zone?f_ri=172299"},{"id":473797,"name":"Microstructures","url":"https://www.academia.edu/Documents/in/Microstructures?f_ri=172299"},{"id":959838,"name":"Arabian Journal of Geosciences","url":"https://www.academia.edu/Documents/in/Arabian_Journal_of_Geosciences?f_ri=172299"},{"id":959840,"name":"(Arab J Geosci","url":"https://www.academia.edu/Documents/in/_Arab_J_Geosci?f_ri=172299"},{"id":1908713,"name":"Local Convergence","url":"https://www.academia.edu/Documents/in/Local_Convergence?f_ri=172299"}]}, }) } })();</script></ul></li></ul></div></div><div class="u-borderBottom1 u-borderColorGrayLighter"><div class="clearfix u-pv7x u-mb0x js-work-card work_24066123 coauthored" data-work_id="24066123" itemscope="itemscope" itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" 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Bogdanova","profile_url":"https://independent.academia.edu/SvetlanaBogdanova?f_ri=172299","photo":"/images/s65_no_pic.png"},{"id":9522969,"first_name":"Bogusław","last_name":"Bagiński","domain_name":"uw","page_name":"BogusławBagiński","display_name":"Bogusław Bagiński","profile_url":"https://uw.academia.edu/Bogus%C5%82awBagi%C5%84ski?f_ri=172299","photo":"https://0.academia-photos.com/9522969/7972452/8930117/s65_bogus_aw.bagi_ski.jpg_oh_af7d5425344221101506f1b028f8ae8d_oe_55b706d0___gda___1433446589_9255c5bdbb3c647fcb313113813d12da"},{"id":36986895,"first_name":"Svetlana","last_name":"Bogdanova","domain_name":"independent","page_name":"SBogdanova","display_name":"Svetlana 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itemtype="https://schema.org/ScholarlyArticle"><div class="header"><div class="title u-fontSerif u-fs22 u-lineHeight1_3"><a class="u-tcGrayDarkest js-work-link" href="https://www.academia.edu/82236759/Radiogeochemistry_uranium_migration_and_radiogenic_heat_of_the_granite_gneisses_in_parts_of_the_southwestern_Basement_Complex_of_Nigeria">Radiogeochemistry, uranium migration, and radiogenic heat of the granite gneisses in parts of the southwestern Basement Complex of Nigeria</a></div></div><div class="u-pb4x u-mt3x"><div class="summary u-fs14 u-fw300 u-lineHeight1_5 u-tcGrayDarkest"><div class="summarized">The radiogeochemistry of granite gneisses in Akunu-Akoko (AK) and Ayere (AY) areas of the southwestern Basement Complex of Nigeria was studied using gamma-ray spectrometry and statistical analyses and modelling. This study was aimed at... <a class="more_link u-tcGrayDark u-linkUnstyled" data-container=".work_82236759" data-show=".complete" data-hide=".summarized" data-more-link-behavior="true" href="#">more</a></div><div class="complete hidden">The radiogeochemistry of granite gneisses in Akunu-Akoko (AK) and Ayere (AY) areas of the southwestern Basement Complex of Nigeria was studied using gamma-ray spectrometry and statistical analyses and modelling. This study was aimed at determining the radionuclides concentration in these rocks, as well as alteration scenarios, nature and rates of uranium migration (UM), levels of radiological hazards, and rate of radiogenic heat production (RHP). The interquartile () elemental concentrations for 40 K, 238 U and 232 Th were 0.23&amp;lt;3.75&amp;lt;4.06%; 1.00&amp;lt;4.20&amp;lt;5.40 ppm; and 4.10&amp;lt;16.10&amp;lt;30.20 ppm, respectively, within the minimum and maximum limits of BDL (below detection limit)-5.23%, BDL-9.70 ppm, and 0.40-60.20 ppm. The average activity concentrations of 40 K, 238 U and 232 Th with values of 629.28, 38.58, and 49.96 , respectively, were above their crustal averages in the order of AK3&amp;lt;AK2&amp;lt;AK3&amp;lt;AY3&amp;lt;AY1&amp;lt;AY2. Variability in K-eU-eTh content and alteration in the rocks were affirmed by radioelement ratios and F-parameter. The high radionuclide concentrations could be due to high levels of radioactive-bearing materials, as well as trace and rare earth elements. Low radionuclides concentration in the rocks may have resulted through weathering, metamorphism, and 12-86% outward UM. The absorbed dose rate (ADR) average of 75.09 was within the allowable range, with the Square R prediction rates of 25-92% from the radionuclides. The average radium activity was below the permissible limit of 370 , and the annual effective doses, hazard indices, gamma activity, and activity utilization index were all far below the safe limit of 1. However, gonad equivalent and excess lifetime cancer risk were above their permissible limits. RHP average of 1.89 above the crustal range of 0.8-1.2 may have considerably contributed to the heat flux in the areas. Square R analysis also predicted that 36-86% of RHP rates in the rocks are achievable from the radionuclides. Reduction in the usage of granite gneisses as a sole raw 2 material for constructions is advised due to the increase in radionuclides and some radiological indicators exceeding world allowed limits.</div></div></div><ul class="InlineList u-ph0x u-fs13"><li class="InlineList-item logged_in_only"><div class="share_on_academia_work_button"><a class="academia_share Button Button--inverseBlue Button--sm js-bookmark-button" data-academia-share="Work/82236759" data-share-source="work_strip" data-spinner="small_white_hide_contents"><i class="fa fa-plus"></i><span class="work-strip-link-text u-ml1x" data-content="button_text">Bookmark</span></a></div></li><li class="InlineList-item"><ul class="InlineList InlineList--bordered u-ph0x"><li class="InlineList-item InlineList-item--bordered"><span class="InlineList-item-text">by <span itemscope="itemscope" itemprop="author" itemtype="https://schema.org/Person"><a class="u-tcGrayDark u-fw700" data-has-card-for-user="26829177" href="https://ajasin.academia.edu/cyrilokpoli">cyril okpoli</a><script data-card-contents-for-user="26829177" type="text/json">{"id":26829177,"first_name":"cyril","last_name":"okpoli","domain_name":"ajasin","page_name":"cyrilokpoli","display_name":"cyril okpoli","profile_url":"https://ajasin.academia.edu/cyrilokpoli?f_ri=172299","photo":"https://0.academia-photos.com/26829177/7492915/18543208/s65_cyril.okpoli.jpg"}</script></span></span></li><li class="js-paper-rank-work_82236759 InlineList-item InlineList-item--bordered hidden"><span class="js-paper-rank-view hidden u-tcGrayDark" data-paper-rank-work-id="82236759"><i class="u-m1x fa fa-bar-chart"></i><strong class="js-paper-rank"></strong></span><script>$(function() { new Works.PaperRankView({ workId: 82236759, container: ".js-paper-rank-work_82236759", }); 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This study was aimed at determining the radionuclides concentration in these rocks, as well as alteration scenarios, nature and rates of uranium migration (UM), levels of radiological hazards, and rate of radiogenic heat production (RHP). The interquartile () elemental concentrations for 40 K, 238 U and 232 Th were 0.23\u0026amp;lt;3.75\u0026amp;lt;4.06%; 1.00\u0026amp;lt;4.20\u0026amp;lt;5.40 ppm; and 4.10\u0026amp;lt;16.10\u0026amp;lt;30.20 ppm, respectively, within the minimum and maximum limits of BDL (below detection limit)-5.23%, BDL-9.70 ppm, and 0.40-60.20 ppm. The average activity concentrations of 40 K, 238 U and 232 Th with values of 629.28, 38.58, and 49.96 , respectively, were above their crustal averages in the order of AK3\u0026amp;lt;AK2\u0026amp;lt;AK3\u0026amp;lt;AY3\u0026amp;lt;AY1\u0026amp;lt;AY2. Variability in K-eU-eTh content and alteration in the rocks were affirmed by radioelement ratios and F-parameter. The high radionuclide concentrations could be due to high levels of radioactive-bearing materials, as well as trace and rare earth elements. Low radionuclides concentration in the rocks may have resulted through weathering, metamorphism, and 12-86% outward UM. The absorbed dose rate (ADR) average of 75.09 was within the allowable range, with the Square R prediction rates of 25-92% from the radionuclides. The average radium activity was below the permissible limit of 370 , and the annual effective doses, hazard indices, gamma activity, and activity utilization index were all far below the safe limit of 1. However, gonad equivalent and excess lifetime cancer risk were above their permissible limits. RHP average of 1.89 above the crustal range of 0.8-1.2 may have considerably contributed to the heat flux in the areas. Square R analysis also predicted that 36-86% of RHP rates in the rocks are achievable from the radionuclides. Reduction in the usage of granite gneisses as a sole raw 2 material for constructions is advised due to the increase in radionuclides and some radiological indicators exceeding world allowed limits.","downloadable_attachments":[],"ordered_authors":[{"id":26829177,"first_name":"cyril","last_name":"okpoli","domain_name":"ajasin","page_name":"cyrilokpoli","display_name":"cyril okpoli","profile_url":"https://ajasin.academia.edu/cyrilokpoli?f_ri=172299","photo":"https://0.academia-photos.com/26829177/7492915/18543208/s65_cyril.okpoli.jpg"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology?f_ri=172299","nofollow":false},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry?f_ri=172299","nofollow":false},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics?f_ri=172299","nofollow":false},{"id":1419,"name":"Structural 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