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100%;"><div class="u-taCenter"></div><div class="profile--tab_content_container js-tab-pane tab-pane active" id="all"><div class="profile--tab_heading_container js-section-heading" data-section="Papers" id="Papers"><h3 class="profile--tab_heading_container">Papers by Trevor Falloon</h3></div><div class="js-work-strip profile--work_container" data-work-id="123791022"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/123791022/Experimental_constraints_on_near_solidus_melts_from_lherzolite_and_on_melt_segregation_and_transport_in_the_mantle"><img alt="Research paper thumbnail of Experimental constraints on near-solidus melts from lherzolite and on melt segregation and transport in the mantle" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/123791022/Experimental_constraints_on_near_solidus_melts_from_lherzolite_and_on_melt_segregation_and_transport_in_the_mantle">Experimental constraints on near-solidus melts from lherzolite and on melt segregation and transport in the mantle</a></div><div class="wp-workCard_item"><span>EGS - AGU - EUG Joint Assembly</span><span>, Apr 1, 2003</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="123791022"><a class="js-profile-work-strip-edit-button" 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class="js-work-strip profile--work_container" data-work-id="123791021"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/123791021/The_mantle_origins_of_Karoo_picrites"><img alt="Research paper thumbnail of The mantle origins of Karoo picrites" class="work-thumbnail" src="https://attachments.academia-assets.com/118141487/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/123791021/The_mantle_origins_of_Karoo_picrites">The mantle origins of Karoo picrites</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, Nov 1, 1991</span></div><div class="wp-workCard_item wp-workCard--actions"><span 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picrites","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_title_tag":"Mantle Sources and Segregation Depths of Karoo Picrites","grobid_abstract":"Karoo plcrltes are divided into d volumetrically dominant high TI-Zr (HTZ) group and a less abundant low Tl-Zr (LTZ) group Distinguished in this way, it is then possible to use the comparison of major element compositions with those of experimentally determined partial melts of mantle perldOtltes to constrain the depth of segregation for each magma type This approach also identifies the nature of source and residual mantle materials lrom which such magma segregation may have occurred The LTZ group show uniformly shallow pressures (ca 13-15 kb) of magma segregation and the HTZ group show a range of pressures (10 kb to \u003e 30 kb) of segregation In the HTZ group a range of K20, TIO 2 and Zr contents is observed, with greater concentrations in plcrltes which have segregated at higher pressures (hlgh-NaK# HTZ plcrltes) relative to a low-NaK# HTZ plcrlte group (NaK# = [Na20 + K20]/[Na20 + K20 + CaO]) If we measure the refractory character of a mantle source perldOtlte by ItS CaO and AI20 ~ content then it is shown that the LTZ plcrltes have segregated trom sources which are more refractory than MORB or OIB sources and which lack the strong K, TI and Zr enrichments of HTZ sources Mixing of at least two mantle components is required to fully explain the major element and isotopic data in the HTZ group and is combined with variations in composition produced by different depths of magma segregation Consideration of the major element phase relations coupled with trace element abundances and isotope data leads us to suggest that one component is the Kaapvaal hthospherlc mantle (incompatible element enriched but relatively refractory with respect to basaltic components) and the other is asthenospherlc mantle This hthospherlc mantle component is most evident in the hlgh-NaK# HTZ plcrlte end-member which has segregated at a greater depth (ca 18-32 kb) The asthenospherlc component is most closely represented by the low-NaK# HTZ plcrltes which have segregated at pressures o1 10 22 kb The LTZ source, more refractory mantle than MORB, is inferred to be the shallow sub-continental hthospherlc mantle which may also be the source of the low-MgO tholelltes related to these plcrltes, and therefore the source for the main phase of Karoo basaltic eruptions","publication_date":{"day":1,"month":11,"year":1991,"errors":{}},"publication_name":"Earth and Planetary Science 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Pyrolite: A Ringwood Concept and Its Current Expression DAVID H. GREEN and TREVOR J. FA...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Page 341. Pyrolite: A Ringwood Concept and Its Current Expression DAVID H. GREEN and TREVOR J. FALLOON 7.1. 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We also present peridotite melting ex-The experimental determination of liquid compositions in lherzolite periments using the mineral mix KLB-1 at 1•0 GPa. Our results as functions of pressure and temperature provides constraints on demonstrate that the mineral mix KLB-1 fails to equilibrate even mantle dynamics and magma genesis. In this paper, we present a after~340 h at temperatures of 1280-1300°C. We present detailed evaluation of the use of natural mineral mixes as starting reversals of the 1•0 GPa peridotite melting experiments of Hirose material in peridotite melting studies at 1•0 GPa. As an example \u0026 Kushiro (1993, Earth and Planetary Science Letters we have chosen to test the data obtained by Baker \u0026 Stolper (1994, 114, 477-489). Our reversals demonstrate that the mineral Geochimica et Cosmochimica Acta 58, 2811-2827) on mix-diamond aggregate trap technique used by Hirose \u0026 Kushiro a lherzolite composition (MM-3) presented as a potential source has also failed to produce equilibrium melts of a mantle peridotite for mid-ocean ridge basalts (MORB). That study is the most fully composition. It is recommended that data from peridotite melting documented published melting study using natural mineral mixes. studies utilizing natural mineral mixes be used with reservation We have tested the Baker \u0026 Stolper data in three ways: (1) we and that natural mineral mixes are not a suitable starting material have defined the liquidus phases and conditions of the partial melt for such studies. The use of diamond aggregate for separation and compositions obtained by Baker \u0026 Stolper; (2) we have reacted trapping of the melt phase compounds rather than solves the problems these partial melt compositions with a fine-grained synthetic starting inherent in the use of natural mineral mixes. mix of MM-3 composition; (3) we have performed additional melting experiments at 1•0 and 1•5 GPa using the synthetic mix of peridotite MM-3. Our results demonstrate that only the highest temperature experiment of Baker \u0026 Stolper, performed at 1390°C, approached an equilibrium melt of peridotite MM-3 composition KEY WORDS: anhydrous peridotite melting; sandwich experiments; natural mineral mix; diamond aggregate entrapment; batch melting; dynamic melting and that lower temperature experiments have not reached equilibrium, retaining residual unreacted minerals and metastable melt compositions. The degree of disequilibrium increases progressively with lower temperature. 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the Origin of Olivine-phyric Volcanic Rocks","translated_title":"","metadata":{"publisher":"Oxford University Press","grobid_abstract":"changes that cannot be reversed. Short residence times also imply A technique is described for determining the cooling history of olivine that large unzoned cores of high-Fo phenocrysts cannot reflect diffusive phenocrysts. The technique is based on the analysis of the diffusive re-equilibration of originally zoned phenocrysts. The unzoned cores re-equilibration of melt inclusions trapped by olivine phenocrysts are a result of fast efficient accumulation of olivines from the during crystallization. The mechanism of re-equilibration involves crystallizing magma, i.e. olivines are separated from the magma diffusion of Fe from and Mg into the initial volume of the inclusion. faster than melt changes its composition. Thus, the main source of The technique applies to a single crystal, and thus the cooling high-Fo crystals in the erupted magmas is the cumulate layers of history of different phenocrysts in a single erupted magma can be the magmatic system. In other words, olivine-phyric rocks represent established. We show that melt inclusions in high-Fo olivine mixtures of an evolved transporting magma (which forms the phenocrysts from mantle-derived magmas are typically partially regroundmass of the rock) with crystals that were formed during equilibrated with their hosts at temperatures below trapping. Our crystallization of more primitive melt(s). Unlike high-Fo olivine analysis demonstrates that at a reasonable combination of factors phenocrysts, the evolved magma may reside in the magmatic system such as (1) cooling interval before eruption (\u003c350°C), (2) eruption for a long time. This reconciles long magma residence times estimated temperatures (\u003e1000°C), and (3) inclusion size (\u003c70 m in from the compositions of rocks with short residence times of highradius), partial re-equilibration of up to 85% occurs within Fo olivine phenocrysts. 3-5 months, corresponding to cooling rates faster than 1-2°/day. Short residence times of high-Fo phenocrysts suggest that if eruption does not happen within a few months after a primitive magma begins cooling and crystallization, olivines that crystallize from it KEY WORDS: melt inclusions; olivine; picrites; residence time; diffusion are unlikely to be erupted as phenocrysts. This can be explained by efficient separation of olivine crystals from the melt, and their rapid incorporation into the cumulate layer of the chamber. 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data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/120545648/Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges"><img alt="Research paper thumbnail of Mantle-derived magmas: intraplate, hot-spots and mid-ocean ridges" class="work-thumbnail" src="https://attachments.academia-assets.com/115660062/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/120545648/Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges">Mantle-derived magmas: intraplate, hot-spots and mid-ocean ridges</a></div><div class="wp-workCard_item"><span>Science Bulletin</span><span>, Nov 1, 2015</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="dcbbd157499f6bfebbd7caffaad59ba8" 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});</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "dcbbd157499f6bfebbd7caffaad59ba8" } } $('.js-work-strip[data-work-id=120545648]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":120545648,"title":"Mantle-derived magmas: intraplate, hot-spots and mid-ocean ridges","translated_title":"","metadata":{"publisher":"Springer Nature","grobid_abstract":"Primary or parental magmas act as probes to infer eruption and source temperatures for both mid-ocean ridge (MOR) and 'hot-spot' magmas (tholeiitic picrites). The experimental petrogenetic constraints ('inverse' experiments) argue for no significant temperature differences between them. However, there are differences in major, minor and trace elements which characterise geochemical, not thermal, anomalies beneath 'hot-spots'. We suggest that diapiric upwelling from interfaces (redox contrasts) between old subducted slab and normal MOR basalt source mantle is the major reason for the observed characteristics of island chain or 'hot-spot' volcanism. Intraplate basalts also include widely distributed volcanic centres containing lherzolite xenoliths, i.e. mantle-derived magmas. Inverse experiments on olivine basalt, alkali olivine basalt, olivine basanite, olivine nephelinite, olivine melilitite and olivine leucitite (lamproite) determined liquidus phases as a function of pressure, initially under anhydrous and CO 2-absent conditions. Under C-and H-absent conditions, only tholeiites to alkali olivine basalts had Ol ? Opx ± Cpx as high-pressure liquidus phases. Addition of H 2 O accessed olivine basanites at 2.5-3 GPa, *1,200°C, but both CO 2 and H 2 O were necessary to obtain saturation with Ol, Opx, Cpx and Ga at 2.5-3.5 GPa for olivine nephelinite and olivine melilitite. The forward and inverse experimental studies are combined to formulate a petrogenetic grid for intraplate, 'hot-spot' and MOR magmatism within the plate tectonics paradigm. The asthenosphere is geochemically zoned by slow upward migration of incipient melt. The solidus and phase stabilities of lherzolite with very small water contents (\\3,000 ppm) determine the thin plate behaviour of the oceanic lithosphere and thus the Earth's convection in the form of plate tectonics. There is no evidence from the parental magmas of MOR and 'hot-spots' to support the 'deep mantle thermal plume' hypothesis. The preferred alternative is the presence of old subducted slabs, relatively buoyant and oxidised with respect to MORB source mantle and suspended or upwelling in or below the lower asthenosphere (and thus detached from overlying plate movement). Keywords Mantle-derived magmas Á High-pressure experiments Á C-H-O Á Asthenosphere Á Hot-spots Á Plate tectonics","publication_date":{"day":1,"month":11,"year":2015,"errors":{}},"publication_name":"Science Bulletin","grobid_abstract_attachment_id":115660062},"translated_abstract":null,"internal_url":"https://www.academia.edu/120545648/Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges","translated_internal_url":"","created_at":"2024-06-04T14:05:00.271-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":11983682,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":115660062,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115660062/thumbnails/1.jpg","file_name":"2733abafa84c4c06b6ae3978cf024007.pdf","download_url":"https://www.academia.edu/attachments/115660062/download_file?st=MTczMzM1MDI2Miw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Mantle_derived_magmas_intraplate_hot_spo.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115660062/2733abafa84c4c06b6ae3978cf024007-libre.pdf?1717538217=\u0026response-content-disposition=attachment%3B+filename%3DMantle_derived_magmas_intraplate_hot_spo.pdf\u0026Expires=1733342023\u0026Signature=LOtEIdKLmmlQ0ITO9rZ21GoIx88rPYvVDfXElV63sH98fsQoA1gzULtA0bsJlgtPx7WhL36dc1bcHyq0FoEWKQr-CTJxcR4xrRMI0DGEOls9SSk7OoVTQM2MSaY2bpPwcMjC3INQnjWO6pdEq3KZ5NFgpO2xt2QrJsFCI7011tpfOt35-kzhY2twlSrVOgEN5Ue16HupAatz2UucEmkbEA36DSV5hJIQMj~yPSjG2FfMmCVhzruHj-j-0Yc7IBbKAMc1fpL8f-McnkMFOGOLpgPCvCbVc6u6rnmbq3aWOyl5C4GFS2Dn1reEiCrTuErpqS2LtpwFtH38sq6CgpYWEg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges","translated_slug":"","page_count":29,"language":"en","content_type":"Work","owner":{"id":11983682,"first_name":"Trevor","middle_initials":null,"last_name":"Falloon","page_name":"TrevorFalloon","domain_name":"utas","created_at":"2014-05-12T17:48:17.009-07:00","display_name":"Trevor Falloon","url":"https://utas.academia.edu/TrevorFalloon"},"attachments":[{"id":115660062,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115660062/thumbnails/1.jpg","file_name":"2733abafa84c4c06b6ae3978cf024007.pdf","download_url":"https://www.academia.edu/attachments/115660062/download_file?st=MTczMzM1MDI2Miw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Mantle_derived_magmas_intraplate_hot_spo.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115660062/2733abafa84c4c06b6ae3978cf024007-libre.pdf?1717538217=\u0026response-content-disposition=attachment%3B+filename%3DMantle_derived_magmas_intraplate_hot_spo.pdf\u0026Expires=1733342023\u0026Signature=LOtEIdKLmmlQ0ITO9rZ21GoIx88rPYvVDfXElV63sH98fsQoA1gzULtA0bsJlgtPx7WhL36dc1bcHyq0FoEWKQr-CTJxcR4xrRMI0DGEOls9SSk7OoVTQM2MSaY2bpPwcMjC3INQnjWO6pdEq3KZ5NFgpO2xt2QrJsFCI7011tpfOt35-kzhY2twlSrVOgEN5Ue16HupAatz2UucEmkbEA36DSV5hJIQMj~yPSjG2FfMmCVhzruHj-j-0Yc7IBbKAMc1fpL8f-McnkMFOGOLpgPCvCbVc6u6rnmbq3aWOyl5C4GFS2Dn1reEiCrTuErpqS2LtpwFtH38sq6CgpYWEg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":70919,"name":"Mid Ocean Ridge","url":"https://www.academia.edu/Documents/in/Mid_Ocean_Ridge"}],"urls":[{"id":42650235,"url":"https://doi.org/10.1007/s11434-015-0920-y"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="120545647"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/120545647/Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji"><img alt="Research paper thumbnail of Evolution processes of primitive adakite magmas revealed by melt inclusions in olivine phenocrysts from Kadavu adakites, Fiji" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/120545647/Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji">Evolution processes of primitive adakite magmas revealed by melt inclusions in olivine phenocrysts from Kadavu adakites, Fiji</a></div><div class="wp-workCard_item"><span>AGU Fall Meeting Abstracts</span><span>, Dec 1, 2008</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains p...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains primitive high-Mg lavas [1]. These lavas have two distinctive compositions, both strongly enriched in Sr and La, with high Sr/Y (&amp;gt;120) and La/Yb (&amp;gt;30) values. The east Kadavu high-Mg adakite is relatively enriched in K2O and depleted in TiO2 and Nb, compared to the Ngaloa high-Mg adakite. The east Kadavu primitive lavas contain phenocrysts of magnesian olivine (Fo 93-84) and clinopyroxene (Mg# 92-86). We present here the results of experimental study of primary melt inclusions in olivine phenocrysts from the east Kandavu adakites. Olivine grains with melt inclusions have been experimentally reheated in a Vernadsky-type heating stage under visual control and inclusions quenched to glass and exposed for chemical analysis. Inclusions, their host olivines and clinopyroxene phenocrysts were analysed by electron microprobe and LA-ICPMS for major and trace elements. The trace element compositions of clinopyroxene indicate that they crystallised from an adakite melt and are not xenocrystic. The major and trace element compositions of melt inclusions in olivine also have typical adakite compositions demonstrating that olivine is not xenocrystic either. The results show that the extent of the adakite geochemical signature (eg, Sr/Y values) is the highest in the most magnesian compositions (300) and continuously decreases in more evolved compositions (100). This effect cannot result from olivine+clinopyroxene crystallisation. The major element compositions of melt inclusions are also inconsistent with primitive melts that evolved to typical Kadavu adakites via olivine+clinopyroxene crystallisation. The results suggest that the primitive Kadavu adakite melts studied evolved via the dissolution-reaction-mixing processes [2] within the Kadavu volcanic plumbing system. These processes are likely to occur at the margins of primitive magma bodies, where magma is in contact with cooler semi-solidified more evolved adakitic crystal mush zones The existence of such processes is confirmed by the common presence of primitive enclaves in more evolved adakite lavas. [1] Danyushevsky L.V., Falloon T.J., Crawford A.J., Tetroeva S.A., Leslie R., Verbeeten A. (2008) Geology 36, 499-502. [2] Danyushevsky L.V., Leslie R., Crawford A.J.,.Durance P. (2004) JPetrology, 45, 2531-2553.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545647"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545647"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545647; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=120545647]").text(description); $(".js-view-count[data-work-id=120545647]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 120545647; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='120545647']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 120545647, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=120545647]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":120545647,"title":"Evolution processes of primitive adakite magmas revealed by melt inclusions in olivine phenocrysts from Kadavu adakites, Fiji","translated_title":"","metadata":{"abstract":"ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains primitive high-Mg lavas [1]. These lavas have two distinctive compositions, both strongly enriched in Sr and La, with high Sr/Y (\u0026amp;gt;120) and La/Yb (\u0026amp;gt;30) values. The east Kadavu high-Mg adakite is relatively enriched in K2O and depleted in TiO2 and Nb, compared to the Ngaloa high-Mg adakite. The east Kadavu primitive lavas contain phenocrysts of magnesian olivine (Fo 93-84) and clinopyroxene (Mg# 92-86). We present here the results of experimental study of primary melt inclusions in olivine phenocrysts from the east Kandavu adakites. Olivine grains with melt inclusions have been experimentally reheated in a Vernadsky-type heating stage under visual control and inclusions quenched to glass and exposed for chemical analysis. Inclusions, their host olivines and clinopyroxene phenocrysts were analysed by electron microprobe and LA-ICPMS for major and trace elements. The trace element compositions of clinopyroxene indicate that they crystallised from an adakite melt and are not xenocrystic. The major and trace element compositions of melt inclusions in olivine also have typical adakite compositions demonstrating that olivine is not xenocrystic either. The results show that the extent of the adakite geochemical signature (eg, Sr/Y values) is the highest in the most magnesian compositions (300) and continuously decreases in more evolved compositions (100). This effect cannot result from olivine+clinopyroxene crystallisation. The major element compositions of melt inclusions are also inconsistent with primitive melts that evolved to typical Kadavu adakites via olivine+clinopyroxene crystallisation. The results suggest that the primitive Kadavu adakite melts studied evolved via the dissolution-reaction-mixing processes [2] within the Kadavu volcanic plumbing system. These processes are likely to occur at the margins of primitive magma bodies, where magma is in contact with cooler semi-solidified more evolved adakitic crystal mush zones The existence of such processes is confirmed by the common presence of primitive enclaves in more evolved adakite lavas. [1] Danyushevsky L.V., Falloon T.J., Crawford A.J., Tetroeva S.A., Leslie R., Verbeeten A. (2008) Geology 36, 499-502. [2] Danyushevsky L.V., Leslie R., Crawford A.J.,.Durance P. (2004) JPetrology, 45, 2531-2553.","publication_date":{"day":1,"month":12,"year":2008,"errors":{}},"publication_name":"AGU Fall Meeting Abstracts"},"translated_abstract":"ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains primitive high-Mg lavas [1]. These lavas have two distinctive compositions, both strongly enriched in Sr and La, with high Sr/Y (\u0026amp;gt;120) and La/Yb (\u0026amp;gt;30) values. The east Kadavu high-Mg adakite is relatively enriched in K2O and depleted in TiO2 and Nb, compared to the Ngaloa high-Mg adakite. The east Kadavu primitive lavas contain phenocrysts of magnesian olivine (Fo 93-84) and clinopyroxene (Mg# 92-86). We present here the results of experimental study of primary melt inclusions in olivine phenocrysts from the east Kandavu adakites. Olivine grains with melt inclusions have been experimentally reheated in a Vernadsky-type heating stage under visual control and inclusions quenched to glass and exposed for chemical analysis. Inclusions, their host olivines and clinopyroxene phenocrysts were analysed by electron microprobe and LA-ICPMS for major and trace elements. The trace element compositions of clinopyroxene indicate that they crystallised from an adakite melt and are not xenocrystic. The major and trace element compositions of melt inclusions in olivine also have typical adakite compositions demonstrating that olivine is not xenocrystic either. The results show that the extent of the adakite geochemical signature (eg, Sr/Y values) is the highest in the most magnesian compositions (300) and continuously decreases in more evolved compositions (100). This effect cannot result from olivine+clinopyroxene crystallisation. The major element compositions of melt inclusions are also inconsistent with primitive melts that evolved to typical Kadavu adakites via olivine+clinopyroxene crystallisation. The results suggest that the primitive Kadavu adakite melts studied evolved via the dissolution-reaction-mixing processes [2] within the Kadavu volcanic plumbing system. These processes are likely to occur at the margins of primitive magma bodies, where magma is in contact with cooler semi-solidified more evolved adakitic crystal mush zones The existence of such processes is confirmed by the common presence of primitive enclaves in more evolved adakite lavas. [1] Danyushevsky L.V., Falloon T.J., Crawford A.J., Tetroeva S.A., Leslie R., Verbeeten A. (2008) Geology 36, 499-502. [2] Danyushevsky L.V., Leslie R., Crawford A.J.,.Durance P. (2004) JPetrology, 45, 2531-2553.","internal_url":"https://www.academia.edu/120545647/Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji","translated_internal_url":"","created_at":"2024-06-04T14:04:59.875-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":11983682,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":11983682,"first_name":"Trevor","middle_initials":null,"last_name":"Falloon","page_name":"TrevorFalloon","domain_name":"utas","created_at":"2014-05-12T17:48:17.009-07:00","display_name":"Trevor Falloon","url":"https://utas.academia.edu/TrevorFalloon"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":415323,"name":"Phenocryst","url":"https://www.academia.edu/Documents/in/Phenocryst"},{"id":642278,"name":"Adakite","url":"https://www.academia.edu/Documents/in/Adakite"}],"urls":[{"id":42650234,"url":"https://ui.adsabs.harvard.edu/abs/2008AGUFM.V21A2083D/abstract"}]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="120545645"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/120545645/Melt_flow_and_hypersolidus_deformation_in_the_lower_ocean_crust_Preliminary_observations_from_IODP_Leg_345"><img alt="Research paper thumbnail of Melt flow and hypersolidus deformation in the lower ocean crust: Preliminary observations from IODP Leg 345" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/120545645/Melt_flow_and_hypersolidus_deformation_in_the_lower_ocean_crust_Preliminary_observations_from_IODP_Leg_345">Melt flow and hypersolidus deformation in the lower ocean crust: Preliminary observations from IODP Leg 345</a></div><div class="wp-workCard_item"><span>AGUFM</span><span>, Dec 1, 2013</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545645"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545645"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545645; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="120545644"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/120545644/Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_"><img alt="Research paper thumbnail of Plate Tectonics Constrained by Evidence-Based Magmatic Temperatures and Phase Relations of Fertile Lherzolite (Invited)" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/120545644/Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_">Plate Tectonics Constrained by Evidence-Based Magmatic Temperatures and Phase Relations of Fertile Lherzolite (Invited)</a></div><div class="wp-workCard_item"><span>AGU Fall Meeting Abstracts</span><span>, Dec 1, 2010</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">In order to understand Earth&#x27;s plate tectonics we must interpret the most direct probes for ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">In order to understand Earth&#x27;s plate tectonics we must interpret the most direct probes for mantle composition and temperature distribution i.e. the primitive basaltic magmas and peridotites representing partial melts and mantle residues. An evidence-based approach to identification of parental magmas and determination of their temperatures requires glass and phenocryst compositions and experimentally calibrated Fe/Mg partitioning between olivine and melt. We have compared magmatic crystallization temperatures between `hot-spot&#x27;(proposed to be plume-related) and normal mid-ocean ridge basalt (MORB) parental liquids, by examining three representative magmatic suites from both ocean island (Hawaii, Iceland, and Réunion) and mid-ocean ridge settings (Cocos-Nazca, East Pacific Rise, and Mid-Atlantic Ridge). We have glass and olivine phenocryst compositions, including volatile (H2O) contents, and have calculated parental liquid compositions at 0.2GPa by incrementally adding olivine back into the glass compositions until a liquid in equilibrium with the most-magnesian olivine phenocryst composition is obtained. The results of these calculations demonstrate that there is very little difference (maximum of ~20°C) between the ranges of crystallization temperatures of the parental liquids (MORB:1243-1351°C versus OIB:1286-1372°C) when volatile contents are taken into account. However while lacking temperature contrast, the source regions for `hot-spot&#x27; parental magmas contain geochemical signatures of old subducted crust/lithosphere. The mantle depths of origin determined for both the MORB and OIB suites are similar (MORB:1-2 GPa; OIB:1-2.5 GPa). Calculations of mantle potential temperatures (Tp) are model dependent, particularly to melt fraction from an inferred source. Assuming similar fertile lherzolite sources, the differences in Tp values between the hottest MORB and the hottest ocean island tholeiite sources are ~80°C. These differences disappear if the hotspot magmas are derived by smaller melt fraction from a refertilized refractory source. In the plate tectonics paradigm, intraplate volcanic chains associated with broad swells are due to upper mantle compositional heterogeneity and consequent buoyancy contrasts and are not a consequence of deep mantle thermal plumes A new experimental study has determined the solidus and melting behaviour of model fertile lherzolite (MORB source) between 1.5 and 6 GPa, and with water contents from ~500 ppm to 14.5 wt % H2O, i.e. from water in nominally anhydrous minerals (NAMs) to vapour-leaching conditions. The lithosphere/asthenosphere boundary is attributed to a change in the water-storage capacity of fertile lherzolite from 2000-4000 ppm at 3 GPa, due to the high pressure instability of pargasite. The consequent appearance of silicate melt along an oceanic geotherm at depths &gt;3GPa causes the rheological change characterising thin plate tectonics. The upper asthenosphere becomes chemically enriched (intraplate magma source) and lower asthenosphere depleted in incompatible elements (MORB source, including ~200 ppm H2O in NAMs) by movement of an incipient melt fraction at the water-saturated solidus.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545644"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545644"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545644; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=120545644]").text(description); $(".js-view-count[data-work-id=120545644]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 120545644; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='120545644']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 120545644, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=120545644]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":120545644,"title":"Plate Tectonics Constrained by Evidence-Based Magmatic Temperatures and Phase Relations of Fertile Lherzolite (Invited)","translated_title":"","metadata":{"abstract":"In order to understand Earth\u0026#x27;s plate tectonics we must interpret the most direct probes for mantle composition and temperature distribution i.e. the primitive basaltic magmas and peridotites representing partial melts and mantle residues. An evidence-based approach to identification of parental magmas and determination of their temperatures requires glass and phenocryst compositions and experimentally calibrated Fe/Mg partitioning between olivine and melt. We have compared magmatic crystallization temperatures between `hot-spot\u0026#x27;(proposed to be plume-related) and normal mid-ocean ridge basalt (MORB) parental liquids, by examining three representative magmatic suites from both ocean island (Hawaii, Iceland, and Réunion) and mid-ocean ridge settings (Cocos-Nazca, East Pacific Rise, and Mid-Atlantic Ridge). We have glass and olivine phenocryst compositions, including volatile (H2O) contents, and have calculated parental liquid compositions at 0.2GPa by incrementally adding olivine back into the glass compositions until a liquid in equilibrium with the most-magnesian olivine phenocryst composition is obtained. The results of these calculations demonstrate that there is very little difference (maximum of ~20°C) between the ranges of crystallization temperatures of the parental liquids (MORB:1243-1351°C versus OIB:1286-1372°C) when volatile contents are taken into account. However while lacking temperature contrast, the source regions for `hot-spot\u0026#x27; parental magmas contain geochemical signatures of old subducted crust/lithosphere. The mantle depths of origin determined for both the MORB and OIB suites are similar (MORB:1-2 GPa; OIB:1-2.5 GPa). Calculations of mantle potential temperatures (Tp) are model dependent, particularly to melt fraction from an inferred source. Assuming similar fertile lherzolite sources, the differences in Tp values between the hottest MORB and the hottest ocean island tholeiite sources are ~80°C. These differences disappear if the hotspot magmas are derived by smaller melt fraction from a refertilized refractory source. In the plate tectonics paradigm, intraplate volcanic chains associated with broad swells are due to upper mantle compositional heterogeneity and consequent buoyancy contrasts and are not a consequence of deep mantle thermal plumes A new experimental study has determined the solidus and melting behaviour of model fertile lherzolite (MORB source) between 1.5 and 6 GPa, and with water contents from ~500 ppm to 14.5 wt % H2O, i.e. from water in nominally anhydrous minerals (NAMs) to vapour-leaching conditions. The lithosphere/asthenosphere boundary is attributed to a change in the water-storage capacity of fertile lherzolite from 2000-4000 ppm at 3 GPa, due to the high pressure instability of pargasite. The consequent appearance of silicate melt along an oceanic geotherm at depths \u0026gt;3GPa causes the rheological change characterising thin plate tectonics. The upper asthenosphere becomes chemically enriched (intraplate magma source) and lower asthenosphere depleted in incompatible elements (MORB source, including ~200 ppm H2O in NAMs) by movement of an incipient melt fraction at the water-saturated solidus.","publication_date":{"day":1,"month":12,"year":2010,"errors":{}},"publication_name":"AGU Fall Meeting Abstracts"},"translated_abstract":"In order to understand Earth\u0026#x27;s plate tectonics we must interpret the most direct probes for mantle composition and temperature distribution i.e. the primitive basaltic magmas and peridotites representing partial melts and mantle residues. An evidence-based approach to identification of parental magmas and determination of their temperatures requires glass and phenocryst compositions and experimentally calibrated Fe/Mg partitioning between olivine and melt. We have compared magmatic crystallization temperatures between `hot-spot\u0026#x27;(proposed to be plume-related) and normal mid-ocean ridge basalt (MORB) parental liquids, by examining three representative magmatic suites from both ocean island (Hawaii, Iceland, and Réunion) and mid-ocean ridge settings (Cocos-Nazca, East Pacific Rise, and Mid-Atlantic Ridge). We have glass and olivine phenocryst compositions, including volatile (H2O) contents, and have calculated parental liquid compositions at 0.2GPa by incrementally adding olivine back into the glass compositions until a liquid in equilibrium with the most-magnesian olivine phenocryst composition is obtained. The results of these calculations demonstrate that there is very little difference (maximum of ~20°C) between the ranges of crystallization temperatures of the parental liquids (MORB:1243-1351°C versus OIB:1286-1372°C) when volatile contents are taken into account. However while lacking temperature contrast, the source regions for `hot-spot\u0026#x27; parental magmas contain geochemical signatures of old subducted crust/lithosphere. The mantle depths of origin determined for both the MORB and OIB suites are similar (MORB:1-2 GPa; OIB:1-2.5 GPa). Calculations of mantle potential temperatures (Tp) are model dependent, particularly to melt fraction from an inferred source. Assuming similar fertile lherzolite sources, the differences in Tp values between the hottest MORB and the hottest ocean island tholeiite sources are ~80°C. These differences disappear if the hotspot magmas are derived by smaller melt fraction from a refertilized refractory source. In the plate tectonics paradigm, intraplate volcanic chains associated with broad swells are due to upper mantle compositional heterogeneity and consequent buoyancy contrasts and are not a consequence of deep mantle thermal plumes A new experimental study has determined the solidus and melting behaviour of model fertile lherzolite (MORB source) between 1.5 and 6 GPa, and with water contents from ~500 ppm to 14.5 wt % H2O, i.e. from water in nominally anhydrous minerals (NAMs) to vapour-leaching conditions. The lithosphere/asthenosphere boundary is attributed to a change in the water-storage capacity of fertile lherzolite from 2000-4000 ppm at 3 GPa, due to the high pressure instability of pargasite. The consequent appearance of silicate melt along an oceanic geotherm at depths \u0026gt;3GPa causes the rheological change characterising thin plate tectonics. The upper asthenosphere becomes chemically enriched (intraplate magma source) and lower asthenosphere depleted in incompatible elements (MORB source, including ~200 ppm H2O in NAMs) by movement of an incipient melt fraction at the water-saturated solidus.","internal_url":"https://www.academia.edu/120545644/Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_","translated_internal_url":"","created_at":"2024-06-04T14:04:58.763-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":11983682,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":11983682,"first_name":"Trevor","middle_initials":null,"last_name":"Falloon","page_name":"TrevorFalloon","domain_name":"utas","created_at":"2014-05-12T17:48:17.009-07:00","display_name":"Trevor Falloon","url":"https://utas.academia.edu/TrevorFalloon"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":4107,"name":"High Pressure","url":"https://www.academia.edu/Documents/in/High_Pressure"},{"id":44747,"name":"Plate Tectonics","url":"https://www.academia.edu/Documents/in/Plate_Tectonics"},{"id":70919,"name":"Mid Ocean Ridge","url":"https://www.academia.edu/Documents/in/Mid_Ocean_Ridge"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":215075,"name":"Experimental Study","url":"https://www.academia.edu/Documents/in/Experimental_Study"},{"id":235663,"name":"Temperature Distribution","url":"https://www.academia.edu/Documents/in/Temperature_Distribution"},{"id":814934,"name":"Plate tectonic","url":"https://www.academia.edu/Documents/in/Plate_tectonic"},{"id":845678,"name":"Water Content","url":"https://www.academia.edu/Documents/in/Water_Content"}],"urls":[{"id":42650231,"url":"http://ui.adsabs.harvard.edu/abs/2010AGUFM.V21A2320G/abstract"}]}, dispatcherData: dispatcherData }); 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This model is based on experimental studies of various primitive magmas and of peridotite + (C-H-O), including melting and phase relationships under variable oxygen fugacities (fO 2). The deep mantle plume hypothesis requires a large potential temperature difference (DT p 200-250 °C) between the upwelling plume and normal ambient mantle as sampled by mid-ocean ridge upwelling and by nonplume intraplate basalts. 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Part I: Incompatible Behaviour, Implications for Mantle Storage, and Origin of Regional Variations</a></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, Aug 1, 2000</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2efab5007445611bae99e905b801541a" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":115660048,"asset_id":120545640,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/115660048/download_file?st=MTczMzM1MDI2Miw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545640"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545640"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545640; 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Regional variations in from the Northern East Pacific Rise (EPR, 9-11°N) and the relative H 2 O contents in EMORB that have more radiogenic Sr, South East Indian Ridge (SEIR, 127-129°E). Exactly the same Nd and Pb isotopes might be explained by differences in the nature region of the glass samples has been analysed for these components of enriched components recycled via subduction processes. However, using microbeam techniques. Our data allow examination of the when EMORB have the same radiogenic isotope compositions as fine details of H 2 O geochemical behaviour during MORB genesis. NMORB within a segment, relative H 2 O contents in EMORB We demonstrate that relative H 2 O contents [i.e. H 2 O/(another probably reflect local processes that lead to enrichment in incompatible incompatible element)] vary systematically with increasing (La/ elements. Regional differences in relative H 2 O contents of NMORB Sm) N in MORB glasses from both the EPR and SEIR. This may reflect either initial variations in the Earth's mantle or inindicates that H 2 O behaves like other incompatible (in peridotite homogeneities left after formation of the continental crust. mineralogies) elements during MORB petrogenesis, and is primarily controlled by solid-melt partitioning. However, the relative H 2 O contents of MORB glasses from the SEIR are higher than in glasses from the EPR at a given (La/Sm) N , demonstrating global KEY WORDS: glass; geochemistry; H 2 O; MORB; petrology variations in the H 2 O contents of MORB. Despite regional differences in relative H 2 O contents, the incompatible behaviour of H 2 O is similar in both studied regions. 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picrites","translated_title":"","metadata":{"publisher":"Elsevier BV","ai_title_tag":"Mantle Sources and Segregation Depths of Karoo Picrites","grobid_abstract":"Karoo plcrltes are divided into d volumetrically dominant high TI-Zr (HTZ) group and a less abundant low Tl-Zr (LTZ) group Distinguished in this way, it is then possible to use the comparison of major element compositions with those of experimentally determined partial melts of mantle perldOtltes to constrain the depth of segregation for each magma type This approach also identifies the nature of source and residual mantle materials lrom which such magma segregation may have occurred The LTZ group show uniformly shallow pressures (ca 13-15 kb) of magma segregation and the HTZ group show a range of pressures (10 kb to \u003e 30 kb) of segregation In the HTZ group a range of K20, TIO 2 and Zr contents is observed, with greater concentrations in plcrltes which have segregated at higher pressures (hlgh-NaK# HTZ plcrltes) relative to a low-NaK# HTZ plcrlte group (NaK# = [Na20 + K20]/[Na20 + K20 + CaO]) If we measure the refractory character of a mantle source perldOtlte by ItS CaO and AI20 ~ content then it is shown that the LTZ plcrltes have segregated trom sources which are more refractory than MORB or OIB sources and which lack the strong K, TI and Zr enrichments of HTZ sources Mixing of at least two mantle components is required to fully explain the major element and isotopic data in the HTZ group and is combined with variations in composition produced by different depths of magma segregation Consideration of the major element phase relations coupled with trace element abundances and isotope data leads us to suggest that one component is the Kaapvaal hthospherlc mantle (incompatible element enriched but relatively refractory with respect to basaltic components) and the other is asthenospherlc mantle This hthospherlc mantle component is most evident in the hlgh-NaK# HTZ plcrlte end-member which has segregated at a greater depth (ca 18-32 kb) The asthenospherlc component is most closely represented by the low-NaK# HTZ plcrltes which have segregated at pressures o1 10 22 kb The LTZ source, more refractory mantle than MORB, is inferred to be the shallow sub-continental hthospherlc mantle which may also be the source of the low-MgO tholelltes related to these plcrltes, and therefore the source for the main phase of Karoo basaltic eruptions","publication_date":{"day":1,"month":11,"year":1991,"errors":{}},"publication_name":"Earth and Planetary Science 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Pyrolite: A Ringwood Concept and Its Current Expression DAVID H. GREEN and TREVOR J. FA...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Page 341. Pyrolite: A Ringwood Concept and Its Current Expression DAVID H. GREEN and TREVOR J. FALLOON 7.1. 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We also present peridotite melting ex-The experimental determination of liquid compositions in lherzolite periments using the mineral mix KLB-1 at 1•0 GPa. Our results as functions of pressure and temperature provides constraints on demonstrate that the mineral mix KLB-1 fails to equilibrate even mantle dynamics and magma genesis. In this paper, we present a after~340 h at temperatures of 1280-1300°C. We present detailed evaluation of the use of natural mineral mixes as starting reversals of the 1•0 GPa peridotite melting experiments of Hirose material in peridotite melting studies at 1•0 GPa. As an example \u0026 Kushiro (1993, Earth and Planetary Science Letters we have chosen to test the data obtained by Baker \u0026 Stolper (1994, 114, 477-489). Our reversals demonstrate that the mineral Geochimica et Cosmochimica Acta 58, 2811-2827) on mix-diamond aggregate trap technique used by Hirose \u0026 Kushiro a lherzolite composition (MM-3) presented as a potential source has also failed to produce equilibrium melts of a mantle peridotite for mid-ocean ridge basalts (MORB). That study is the most fully composition. It is recommended that data from peridotite melting documented published melting study using natural mineral mixes. studies utilizing natural mineral mixes be used with reservation We have tested the Baker \u0026 Stolper data in three ways: (1) we and that natural mineral mixes are not a suitable starting material have defined the liquidus phases and conditions of the partial melt for such studies. The use of diamond aggregate for separation and compositions obtained by Baker \u0026 Stolper; (2) we have reacted trapping of the melt phase compounds rather than solves the problems these partial melt compositions with a fine-grained synthetic starting inherent in the use of natural mineral mixes. mix of MM-3 composition; (3) we have performed additional melting experiments at 1•0 and 1•5 GPa using the synthetic mix of peridotite MM-3. Our results demonstrate that only the highest temperature experiment of Baker \u0026 Stolper, performed at 1390°C, approached an equilibrium melt of peridotite MM-3 composition KEY WORDS: anhydrous peridotite melting; sandwich experiments; natural mineral mix; diamond aggregate entrapment; batch melting; dynamic melting and that lower temperature experiments have not reached equilibrium, retaining residual unreacted minerals and metastable melt compositions. The degree of disequilibrium increases progressively with lower temperature. 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the Origin of Olivine-phyric Volcanic Rocks","translated_title":"","metadata":{"publisher":"Oxford University Press","grobid_abstract":"changes that cannot be reversed. Short residence times also imply A technique is described for determining the cooling history of olivine that large unzoned cores of high-Fo phenocrysts cannot reflect diffusive phenocrysts. The technique is based on the analysis of the diffusive re-equilibration of originally zoned phenocrysts. The unzoned cores re-equilibration of melt inclusions trapped by olivine phenocrysts are a result of fast efficient accumulation of olivines from the during crystallization. The mechanism of re-equilibration involves crystallizing magma, i.e. olivines are separated from the magma diffusion of Fe from and Mg into the initial volume of the inclusion. faster than melt changes its composition. Thus, the main source of The technique applies to a single crystal, and thus the cooling high-Fo crystals in the erupted magmas is the cumulate layers of history of different phenocrysts in a single erupted magma can be the magmatic system. In other words, olivine-phyric rocks represent established. We show that melt inclusions in high-Fo olivine mixtures of an evolved transporting magma (which forms the phenocrysts from mantle-derived magmas are typically partially regroundmass of the rock) with crystals that were formed during equilibrated with their hosts at temperatures below trapping. Our crystallization of more primitive melt(s). Unlike high-Fo olivine analysis demonstrates that at a reasonable combination of factors phenocrysts, the evolved magma may reside in the magmatic system such as (1) cooling interval before eruption (\u003c350°C), (2) eruption for a long time. This reconciles long magma residence times estimated temperatures (\u003e1000°C), and (3) inclusion size (\u003c70 m in from the compositions of rocks with short residence times of highradius), partial re-equilibration of up to 85% occurs within Fo olivine phenocrysts. 3-5 months, corresponding to cooling rates faster than 1-2°/day. Short residence times of high-Fo phenocrysts suggest that if eruption does not happen within a few months after a primitive magma begins cooling and crystallization, olivines that crystallize from it KEY WORDS: melt inclusions; olivine; picrites; residence time; diffusion are unlikely to be erupted as phenocrysts. This can be explained by efficient separation of olivine crystals from the melt, and their rapid incorporation into the cumulate layer of the chamber. 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data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/120545648/Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges"><img alt="Research paper thumbnail of Mantle-derived magmas: intraplate, hot-spots and mid-ocean ridges" class="work-thumbnail" src="https://attachments.academia-assets.com/115660062/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/120545648/Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges">Mantle-derived magmas: intraplate, hot-spots and mid-ocean ridges</a></div><div class="wp-workCard_item"><span>Science Bulletin</span><span>, Nov 1, 2015</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="dcbbd157499f6bfebbd7caffaad59ba8" 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});</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "dcbbd157499f6bfebbd7caffaad59ba8" } } $('.js-work-strip[data-work-id=120545648]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":120545648,"title":"Mantle-derived magmas: intraplate, hot-spots and mid-ocean ridges","translated_title":"","metadata":{"publisher":"Springer Nature","grobid_abstract":"Primary or parental magmas act as probes to infer eruption and source temperatures for both mid-ocean ridge (MOR) and 'hot-spot' magmas (tholeiitic picrites). The experimental petrogenetic constraints ('inverse' experiments) argue for no significant temperature differences between them. However, there are differences in major, minor and trace elements which characterise geochemical, not thermal, anomalies beneath 'hot-spots'. We suggest that diapiric upwelling from interfaces (redox contrasts) between old subducted slab and normal MOR basalt source mantle is the major reason for the observed characteristics of island chain or 'hot-spot' volcanism. Intraplate basalts also include widely distributed volcanic centres containing lherzolite xenoliths, i.e. mantle-derived magmas. Inverse experiments on olivine basalt, alkali olivine basalt, olivine basanite, olivine nephelinite, olivine melilitite and olivine leucitite (lamproite) determined liquidus phases as a function of pressure, initially under anhydrous and CO 2-absent conditions. Under C-and H-absent conditions, only tholeiites to alkali olivine basalts had Ol ? Opx ± Cpx as high-pressure liquidus phases. Addition of H 2 O accessed olivine basanites at 2.5-3 GPa, *1,200°C, but both CO 2 and H 2 O were necessary to obtain saturation with Ol, Opx, Cpx and Ga at 2.5-3.5 GPa for olivine nephelinite and olivine melilitite. The forward and inverse experimental studies are combined to formulate a petrogenetic grid for intraplate, 'hot-spot' and MOR magmatism within the plate tectonics paradigm. The asthenosphere is geochemically zoned by slow upward migration of incipient melt. The solidus and phase stabilities of lherzolite with very small water contents (\\3,000 ppm) determine the thin plate behaviour of the oceanic lithosphere and thus the Earth's convection in the form of plate tectonics. There is no evidence from the parental magmas of MOR and 'hot-spots' to support the 'deep mantle thermal plume' hypothesis. The preferred alternative is the presence of old subducted slabs, relatively buoyant and oxidised with respect to MORB source mantle and suspended or upwelling in or below the lower asthenosphere (and thus detached from overlying plate movement). Keywords Mantle-derived magmas Á High-pressure experiments Á C-H-O Á Asthenosphere Á Hot-spots Á Plate tectonics","publication_date":{"day":1,"month":11,"year":2015,"errors":{}},"publication_name":"Science Bulletin","grobid_abstract_attachment_id":115660062},"translated_abstract":null,"internal_url":"https://www.academia.edu/120545648/Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges","translated_internal_url":"","created_at":"2024-06-04T14:05:00.271-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":11983682,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":115660062,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115660062/thumbnails/1.jpg","file_name":"2733abafa84c4c06b6ae3978cf024007.pdf","download_url":"https://www.academia.edu/attachments/115660062/download_file?st=MTczMzM1MDI2Miw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Mantle_derived_magmas_intraplate_hot_spo.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115660062/2733abafa84c4c06b6ae3978cf024007-libre.pdf?1717538217=\u0026response-content-disposition=attachment%3B+filename%3DMantle_derived_magmas_intraplate_hot_spo.pdf\u0026Expires=1733342023\u0026Signature=LOtEIdKLmmlQ0ITO9rZ21GoIx88rPYvVDfXElV63sH98fsQoA1gzULtA0bsJlgtPx7WhL36dc1bcHyq0FoEWKQr-CTJxcR4xrRMI0DGEOls9SSk7OoVTQM2MSaY2bpPwcMjC3INQnjWO6pdEq3KZ5NFgpO2xt2QrJsFCI7011tpfOt35-kzhY2twlSrVOgEN5Ue16HupAatz2UucEmkbEA36DSV5hJIQMj~yPSjG2FfMmCVhzruHj-j-0Yc7IBbKAMc1fpL8f-McnkMFOGOLpgPCvCbVc6u6rnmbq3aWOyl5C4GFS2Dn1reEiCrTuErpqS2LtpwFtH38sq6CgpYWEg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Mantle_derived_magmas_intraplate_hot_spots_and_mid_ocean_ridges","translated_slug":"","page_count":29,"language":"en","content_type":"Work","owner":{"id":11983682,"first_name":"Trevor","middle_initials":null,"last_name":"Falloon","page_name":"TrevorFalloon","domain_name":"utas","created_at":"2014-05-12T17:48:17.009-07:00","display_name":"Trevor Falloon","url":"https://utas.academia.edu/TrevorFalloon"},"attachments":[{"id":115660062,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/115660062/thumbnails/1.jpg","file_name":"2733abafa84c4c06b6ae3978cf024007.pdf","download_url":"https://www.academia.edu/attachments/115660062/download_file?st=MTczMzM1MDI2Miw4LjIyMi4yMDguMTQ2&","bulk_download_file_name":"Mantle_derived_magmas_intraplate_hot_spo.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/115660062/2733abafa84c4c06b6ae3978cf024007-libre.pdf?1717538217=\u0026response-content-disposition=attachment%3B+filename%3DMantle_derived_magmas_intraplate_hot_spo.pdf\u0026Expires=1733342023\u0026Signature=LOtEIdKLmmlQ0ITO9rZ21GoIx88rPYvVDfXElV63sH98fsQoA1gzULtA0bsJlgtPx7WhL36dc1bcHyq0FoEWKQr-CTJxcR4xrRMI0DGEOls9SSk7OoVTQM2MSaY2bpPwcMjC3INQnjWO6pdEq3KZ5NFgpO2xt2QrJsFCI7011tpfOt35-kzhY2twlSrVOgEN5Ue16HupAatz2UucEmkbEA36DSV5hJIQMj~yPSjG2FfMmCVhzruHj-j-0Yc7IBbKAMc1fpL8f-McnkMFOGOLpgPCvCbVc6u6rnmbq3aWOyl5C4GFS2Dn1reEiCrTuErpqS2LtpwFtH38sq6CgpYWEg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":70919,"name":"Mid Ocean Ridge","url":"https://www.academia.edu/Documents/in/Mid_Ocean_Ridge"}],"urls":[{"id":42650235,"url":"https://doi.org/10.1007/s11434-015-0920-y"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="120545647"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/120545647/Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji"><img alt="Research paper thumbnail of Evolution processes of primitive adakite magmas revealed by melt inclusions in olivine phenocrysts from Kadavu adakites, Fiji" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/120545647/Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji">Evolution processes of primitive adakite magmas revealed by melt inclusions in olivine phenocrysts from Kadavu adakites, Fiji</a></div><div class="wp-workCard_item"><span>AGU Fall Meeting Abstracts</span><span>, Dec 1, 2008</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains p...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains primitive high-Mg lavas [1]. These lavas have two distinctive compositions, both strongly enriched in Sr and La, with high Sr/Y (&amp;gt;120) and La/Yb (&amp;gt;30) values. The east Kadavu high-Mg adakite is relatively enriched in K2O and depleted in TiO2 and Nb, compared to the Ngaloa high-Mg adakite. The east Kadavu primitive lavas contain phenocrysts of magnesian olivine (Fo 93-84) and clinopyroxene (Mg# 92-86). We present here the results of experimental study of primary melt inclusions in olivine phenocrysts from the east Kandavu adakites. Olivine grains with melt inclusions have been experimentally reheated in a Vernadsky-type heating stage under visual control and inclusions quenched to glass and exposed for chemical analysis. Inclusions, their host olivines and clinopyroxene phenocrysts were analysed by electron microprobe and LA-ICPMS for major and trace elements. The trace element compositions of clinopyroxene indicate that they crystallised from an adakite melt and are not xenocrystic. The major and trace element compositions of melt inclusions in olivine also have typical adakite compositions demonstrating that olivine is not xenocrystic either. The results show that the extent of the adakite geochemical signature (eg, Sr/Y values) is the highest in the most magnesian compositions (300) and continuously decreases in more evolved compositions (100). This effect cannot result from olivine+clinopyroxene crystallisation. The major element compositions of melt inclusions are also inconsistent with primitive melts that evolved to typical Kadavu adakites via olivine+clinopyroxene crystallisation. The results suggest that the primitive Kadavu adakite melts studied evolved via the dissolution-reaction-mixing processes [2] within the Kadavu volcanic plumbing system. These processes are likely to occur at the margins of primitive magma bodies, where magma is in contact with cooler semi-solidified more evolved adakitic crystal mush zones The existence of such processes is confirmed by the common presence of primitive enclaves in more evolved adakite lavas. [1] Danyushevsky L.V., Falloon T.J., Crawford A.J., Tetroeva S.A., Leslie R., Verbeeten A. (2008) Geology 36, 499-502. [2] Danyushevsky L.V., Leslie R., Crawford A.J.,.Durance P. (2004) JPetrology, 45, 2531-2553.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545647"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545647"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545647; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=120545647]").text(description); $(".js-view-count[data-work-id=120545647]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 120545647; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='120545647']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 120545647, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=120545647]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":120545647,"title":"Evolution processes of primitive adakite magmas revealed by melt inclusions in olivine phenocrysts from Kadavu adakites, Fiji","translated_title":"","metadata":{"abstract":"ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains primitive high-Mg lavas [1]. These lavas have two distinctive compositions, both strongly enriched in Sr and La, with high Sr/Y (\u0026amp;gt;120) and La/Yb (\u0026amp;gt;30) values. The east Kadavu high-Mg adakite is relatively enriched in K2O and depleted in TiO2 and Nb, compared to the Ngaloa high-Mg adakite. The east Kadavu primitive lavas contain phenocrysts of magnesian olivine (Fo 93-84) and clinopyroxene (Mg# 92-86). We present here the results of experimental study of primary melt inclusions in olivine phenocrysts from the east Kandavu adakites. Olivine grains with melt inclusions have been experimentally reheated in a Vernadsky-type heating stage under visual control and inclusions quenched to glass and exposed for chemical analysis. Inclusions, their host olivines and clinopyroxene phenocrysts were analysed by electron microprobe and LA-ICPMS for major and trace elements. The trace element compositions of clinopyroxene indicate that they crystallised from an adakite melt and are not xenocrystic. The major and trace element compositions of melt inclusions in olivine also have typical adakite compositions demonstrating that olivine is not xenocrystic either. The results show that the extent of the adakite geochemical signature (eg, Sr/Y values) is the highest in the most magnesian compositions (300) and continuously decreases in more evolved compositions (100). This effect cannot result from olivine+clinopyroxene crystallisation. The major element compositions of melt inclusions are also inconsistent with primitive melts that evolved to typical Kadavu adakites via olivine+clinopyroxene crystallisation. The results suggest that the primitive Kadavu adakite melts studied evolved via the dissolution-reaction-mixing processes [2] within the Kadavu volcanic plumbing system. These processes are likely to occur at the margins of primitive magma bodies, where magma is in contact with cooler semi-solidified more evolved adakitic crystal mush zones The existence of such processes is confirmed by the common presence of primitive enclaves in more evolved adakite lavas. [1] Danyushevsky L.V., Falloon T.J., Crawford A.J., Tetroeva S.A., Leslie R., Verbeeten A. (2008) Geology 36, 499-502. [2] Danyushevsky L.V., Leslie R., Crawford A.J.,.Durance P. (2004) JPetrology, 45, 2531-2553.","publication_date":{"day":1,"month":12,"year":2008,"errors":{}},"publication_name":"AGU Fall Meeting Abstracts"},"translated_abstract":"ABSTRACT The 0.5-3.5 Ma adakite magmatic suite forming the Kadavu Island Group., Fiji, contains primitive high-Mg lavas [1]. These lavas have two distinctive compositions, both strongly enriched in Sr and La, with high Sr/Y (\u0026amp;gt;120) and La/Yb (\u0026amp;gt;30) values. The east Kadavu high-Mg adakite is relatively enriched in K2O and depleted in TiO2 and Nb, compared to the Ngaloa high-Mg adakite. The east Kadavu primitive lavas contain phenocrysts of magnesian olivine (Fo 93-84) and clinopyroxene (Mg# 92-86). We present here the results of experimental study of primary melt inclusions in olivine phenocrysts from the east Kandavu adakites. Olivine grains with melt inclusions have been experimentally reheated in a Vernadsky-type heating stage under visual control and inclusions quenched to glass and exposed for chemical analysis. Inclusions, their host olivines and clinopyroxene phenocrysts were analysed by electron microprobe and LA-ICPMS for major and trace elements. The trace element compositions of clinopyroxene indicate that they crystallised from an adakite melt and are not xenocrystic. The major and trace element compositions of melt inclusions in olivine also have typical adakite compositions demonstrating that olivine is not xenocrystic either. The results show that the extent of the adakite geochemical signature (eg, Sr/Y values) is the highest in the most magnesian compositions (300) and continuously decreases in more evolved compositions (100). This effect cannot result from olivine+clinopyroxene crystallisation. The major element compositions of melt inclusions are also inconsistent with primitive melts that evolved to typical Kadavu adakites via olivine+clinopyroxene crystallisation. The results suggest that the primitive Kadavu adakite melts studied evolved via the dissolution-reaction-mixing processes [2] within the Kadavu volcanic plumbing system. These processes are likely to occur at the margins of primitive magma bodies, where magma is in contact with cooler semi-solidified more evolved adakitic crystal mush zones The existence of such processes is confirmed by the common presence of primitive enclaves in more evolved adakite lavas. [1] Danyushevsky L.V., Falloon T.J., Crawford A.J., Tetroeva S.A., Leslie R., Verbeeten A. (2008) Geology 36, 499-502. [2] Danyushevsky L.V., Leslie R., Crawford A.J.,.Durance P. (2004) JPetrology, 45, 2531-2553.","internal_url":"https://www.academia.edu/120545647/Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji","translated_internal_url":"","created_at":"2024-06-04T14:04:59.875-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":11983682,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Evolution_processes_of_primitive_adakite_magmas_revealed_by_melt_inclusions_in_olivine_phenocrysts_from_Kadavu_adakites_Fiji","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":11983682,"first_name":"Trevor","middle_initials":null,"last_name":"Falloon","page_name":"TrevorFalloon","domain_name":"utas","created_at":"2014-05-12T17:48:17.009-07:00","display_name":"Trevor Falloon","url":"https://utas.academia.edu/TrevorFalloon"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":415323,"name":"Phenocryst","url":"https://www.academia.edu/Documents/in/Phenocryst"},{"id":642278,"name":"Adakite","url":"https://www.academia.edu/Documents/in/Adakite"}],"urls":[{"id":42650234,"url":"https://ui.adsabs.harvard.edu/abs/2008AGUFM.V21A2083D/abstract"}]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="120545645"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/120545645/Melt_flow_and_hypersolidus_deformation_in_the_lower_ocean_crust_Preliminary_observations_from_IODP_Leg_345"><img alt="Research paper thumbnail of Melt flow and hypersolidus deformation in the lower ocean crust: Preliminary observations from IODP Leg 345" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/120545645/Melt_flow_and_hypersolidus_deformation_in_the_lower_ocean_crust_Preliminary_observations_from_IODP_Leg_345">Melt flow and hypersolidus deformation in the lower ocean crust: Preliminary observations from IODP Leg 345</a></div><div class="wp-workCard_item"><span>AGUFM</span><span>, Dec 1, 2013</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545645"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545645"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545645; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") }); </script> <div class="js-work-strip profile--work_container" data-work-id="120545644"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/120545644/Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_"><img alt="Research paper thumbnail of Plate Tectonics Constrained by Evidence-Based Magmatic Temperatures and Phase Relations of Fertile Lherzolite (Invited)" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" rel="nofollow" href="https://www.academia.edu/120545644/Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_">Plate Tectonics Constrained by Evidence-Based Magmatic Temperatures and Phase Relations of Fertile Lherzolite (Invited)</a></div><div class="wp-workCard_item"><span>AGU Fall Meeting Abstracts</span><span>, Dec 1, 2010</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">In order to understand Earth&#x27;s plate tectonics we must interpret the most direct probes for ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">In order to understand Earth&#x27;s plate tectonics we must interpret the most direct probes for mantle composition and temperature distribution i.e. the primitive basaltic magmas and peridotites representing partial melts and mantle residues. An evidence-based approach to identification of parental magmas and determination of their temperatures requires glass and phenocryst compositions and experimentally calibrated Fe/Mg partitioning between olivine and melt. We have compared magmatic crystallization temperatures between `hot-spot&#x27;(proposed to be plume-related) and normal mid-ocean ridge basalt (MORB) parental liquids, by examining three representative magmatic suites from both ocean island (Hawaii, Iceland, and Réunion) and mid-ocean ridge settings (Cocos-Nazca, East Pacific Rise, and Mid-Atlantic Ridge). We have glass and olivine phenocryst compositions, including volatile (H2O) contents, and have calculated parental liquid compositions at 0.2GPa by incrementally adding olivine back into the glass compositions until a liquid in equilibrium with the most-magnesian olivine phenocryst composition is obtained. The results of these calculations demonstrate that there is very little difference (maximum of ~20°C) between the ranges of crystallization temperatures of the parental liquids (MORB:1243-1351°C versus OIB:1286-1372°C) when volatile contents are taken into account. However while lacking temperature contrast, the source regions for `hot-spot&#x27; parental magmas contain geochemical signatures of old subducted crust/lithosphere. The mantle depths of origin determined for both the MORB and OIB suites are similar (MORB:1-2 GPa; OIB:1-2.5 GPa). Calculations of mantle potential temperatures (Tp) are model dependent, particularly to melt fraction from an inferred source. Assuming similar fertile lherzolite sources, the differences in Tp values between the hottest MORB and the hottest ocean island tholeiite sources are ~80°C. These differences disappear if the hotspot magmas are derived by smaller melt fraction from a refertilized refractory source. In the plate tectonics paradigm, intraplate volcanic chains associated with broad swells are due to upper mantle compositional heterogeneity and consequent buoyancy contrasts and are not a consequence of deep mantle thermal plumes A new experimental study has determined the solidus and melting behaviour of model fertile lherzolite (MORB source) between 1.5 and 6 GPa, and with water contents from ~500 ppm to 14.5 wt % H2O, i.e. from water in nominally anhydrous minerals (NAMs) to vapour-leaching conditions. The lithosphere/asthenosphere boundary is attributed to a change in the water-storage capacity of fertile lherzolite from 2000-4000 ppm at 3 GPa, due to the high pressure instability of pargasite. The consequent appearance of silicate melt along an oceanic geotherm at depths &gt;3GPa causes the rheological change characterising thin plate tectonics. The upper asthenosphere becomes chemically enriched (intraplate magma source) and lower asthenosphere depleted in incompatible elements (MORB source, including ~200 ppm H2O in NAMs) by movement of an incipient melt fraction at the water-saturated solidus.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545644"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545644"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545644; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=120545644]").text(description); $(".js-view-count[data-work-id=120545644]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 120545644; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='120545644']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span><span><script>$(function() { new Works.PaperRankView({ workId: 120545644, container: "", }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-f77ea15d77ce96025a6048a514272ad8becbad23c641fc2b3bd6e24ca6ff1932.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=120545644]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":120545644,"title":"Plate Tectonics Constrained by Evidence-Based Magmatic Temperatures and Phase Relations of Fertile Lherzolite (Invited)","translated_title":"","metadata":{"abstract":"In order to understand Earth\u0026#x27;s plate tectonics we must interpret the most direct probes for mantle composition and temperature distribution i.e. the primitive basaltic magmas and peridotites representing partial melts and mantle residues. An evidence-based approach to identification of parental magmas and determination of their temperatures requires glass and phenocryst compositions and experimentally calibrated Fe/Mg partitioning between olivine and melt. We have compared magmatic crystallization temperatures between `hot-spot\u0026#x27;(proposed to be plume-related) and normal mid-ocean ridge basalt (MORB) parental liquids, by examining three representative magmatic suites from both ocean island (Hawaii, Iceland, and Réunion) and mid-ocean ridge settings (Cocos-Nazca, East Pacific Rise, and Mid-Atlantic Ridge). We have glass and olivine phenocryst compositions, including volatile (H2O) contents, and have calculated parental liquid compositions at 0.2GPa by incrementally adding olivine back into the glass compositions until a liquid in equilibrium with the most-magnesian olivine phenocryst composition is obtained. The results of these calculations demonstrate that there is very little difference (maximum of ~20°C) between the ranges of crystallization temperatures of the parental liquids (MORB:1243-1351°C versus OIB:1286-1372°C) when volatile contents are taken into account. However while lacking temperature contrast, the source regions for `hot-spot\u0026#x27; parental magmas contain geochemical signatures of old subducted crust/lithosphere. The mantle depths of origin determined for both the MORB and OIB suites are similar (MORB:1-2 GPa; OIB:1-2.5 GPa). Calculations of mantle potential temperatures (Tp) are model dependent, particularly to melt fraction from an inferred source. Assuming similar fertile lherzolite sources, the differences in Tp values between the hottest MORB and the hottest ocean island tholeiite sources are ~80°C. These differences disappear if the hotspot magmas are derived by smaller melt fraction from a refertilized refractory source. In the plate tectonics paradigm, intraplate volcanic chains associated with broad swells are due to upper mantle compositional heterogeneity and consequent buoyancy contrasts and are not a consequence of deep mantle thermal plumes A new experimental study has determined the solidus and melting behaviour of model fertile lherzolite (MORB source) between 1.5 and 6 GPa, and with water contents from ~500 ppm to 14.5 wt % H2O, i.e. from water in nominally anhydrous minerals (NAMs) to vapour-leaching conditions. The lithosphere/asthenosphere boundary is attributed to a change in the water-storage capacity of fertile lherzolite from 2000-4000 ppm at 3 GPa, due to the high pressure instability of pargasite. The consequent appearance of silicate melt along an oceanic geotherm at depths \u0026gt;3GPa causes the rheological change characterising thin plate tectonics. The upper asthenosphere becomes chemically enriched (intraplate magma source) and lower asthenosphere depleted in incompatible elements (MORB source, including ~200 ppm H2O in NAMs) by movement of an incipient melt fraction at the water-saturated solidus.","publication_date":{"day":1,"month":12,"year":2010,"errors":{}},"publication_name":"AGU Fall Meeting Abstracts"},"translated_abstract":"In order to understand Earth\u0026#x27;s plate tectonics we must interpret the most direct probes for mantle composition and temperature distribution i.e. the primitive basaltic magmas and peridotites representing partial melts and mantle residues. An evidence-based approach to identification of parental magmas and determination of their temperatures requires glass and phenocryst compositions and experimentally calibrated Fe/Mg partitioning between olivine and melt. We have compared magmatic crystallization temperatures between `hot-spot\u0026#x27;(proposed to be plume-related) and normal mid-ocean ridge basalt (MORB) parental liquids, by examining three representative magmatic suites from both ocean island (Hawaii, Iceland, and Réunion) and mid-ocean ridge settings (Cocos-Nazca, East Pacific Rise, and Mid-Atlantic Ridge). We have glass and olivine phenocryst compositions, including volatile (H2O) contents, and have calculated parental liquid compositions at 0.2GPa by incrementally adding olivine back into the glass compositions until a liquid in equilibrium with the most-magnesian olivine phenocryst composition is obtained. The results of these calculations demonstrate that there is very little difference (maximum of ~20°C) between the ranges of crystallization temperatures of the parental liquids (MORB:1243-1351°C versus OIB:1286-1372°C) when volatile contents are taken into account. However while lacking temperature contrast, the source regions for `hot-spot\u0026#x27; parental magmas contain geochemical signatures of old subducted crust/lithosphere. The mantle depths of origin determined for both the MORB and OIB suites are similar (MORB:1-2 GPa; OIB:1-2.5 GPa). Calculations of mantle potential temperatures (Tp) are model dependent, particularly to melt fraction from an inferred source. Assuming similar fertile lherzolite sources, the differences in Tp values between the hottest MORB and the hottest ocean island tholeiite sources are ~80°C. These differences disappear if the hotspot magmas are derived by smaller melt fraction from a refertilized refractory source. In the plate tectonics paradigm, intraplate volcanic chains associated with broad swells are due to upper mantle compositional heterogeneity and consequent buoyancy contrasts and are not a consequence of deep mantle thermal plumes A new experimental study has determined the solidus and melting behaviour of model fertile lherzolite (MORB source) between 1.5 and 6 GPa, and with water contents from ~500 ppm to 14.5 wt % H2O, i.e. from water in nominally anhydrous minerals (NAMs) to vapour-leaching conditions. The lithosphere/asthenosphere boundary is attributed to a change in the water-storage capacity of fertile lherzolite from 2000-4000 ppm at 3 GPa, due to the high pressure instability of pargasite. The consequent appearance of silicate melt along an oceanic geotherm at depths \u0026gt;3GPa causes the rheological change characterising thin plate tectonics. The upper asthenosphere becomes chemically enriched (intraplate magma source) and lower asthenosphere depleted in incompatible elements (MORB source, including ~200 ppm H2O in NAMs) by movement of an incipient melt fraction at the water-saturated solidus.","internal_url":"https://www.academia.edu/120545644/Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_","translated_internal_url":"","created_at":"2024-06-04T14:04:58.763-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":11983682,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Plate_Tectonics_Constrained_by_Evidence_Based_Magmatic_Temperatures_and_Phase_Relations_of_Fertile_Lherzolite_Invited_","translated_slug":"","page_count":null,"language":"en","content_type":"Work","owner":{"id":11983682,"first_name":"Trevor","middle_initials":null,"last_name":"Falloon","page_name":"TrevorFalloon","domain_name":"utas","created_at":"2014-05-12T17:48:17.009-07:00","display_name":"Trevor Falloon","url":"https://utas.academia.edu/TrevorFalloon"},"attachments":[],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":4107,"name":"High Pressure","url":"https://www.academia.edu/Documents/in/High_Pressure"},{"id":44747,"name":"Plate Tectonics","url":"https://www.academia.edu/Documents/in/Plate_Tectonics"},{"id":70919,"name":"Mid Ocean Ridge","url":"https://www.academia.edu/Documents/in/Mid_Ocean_Ridge"},{"id":191125,"name":"Partial Melting","url":"https://www.academia.edu/Documents/in/Partial_Melting"},{"id":215075,"name":"Experimental Study","url":"https://www.academia.edu/Documents/in/Experimental_Study"},{"id":235663,"name":"Temperature Distribution","url":"https://www.academia.edu/Documents/in/Temperature_Distribution"},{"id":814934,"name":"Plate tectonic","url":"https://www.academia.edu/Documents/in/Plate_tectonic"},{"id":845678,"name":"Water Content","url":"https://www.academia.edu/Documents/in/Water_Content"}],"urls":[{"id":42650231,"url":"http://ui.adsabs.harvard.edu/abs/2010AGUFM.V21A2320G/abstract"}]}, dispatcherData: dispatcherData }); 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This model is based on experimental studies of various primitive magmas and of peridotite + (C-H-O), including melting and phase relationships under variable oxygen fugacities (fO 2). The deep mantle plume hypothesis requires a large potential temperature difference (DT p 200-250 °C) between the upwelling plume and normal ambient mantle as sampled by mid-ocean ridge upwelling and by nonplume intraplate basalts. 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Part I: Incompatible Behaviour, Implications for Mantle Storage, and Origin of Regional Variations</a></div><div class="wp-workCard_item"><span>Journal of Petrology</span><span>, Aug 1, 2000</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2efab5007445611bae99e905b801541a" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":115660048,"asset_id":120545640,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/115660048/download_file?st=MTczMzM1MDI2Miw4LjIyMi4yMDguMTQ2&s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="120545640"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span><span id="work-strip-rankings-button-container"></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="120545640"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 120545640; 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Regional variations in from the Northern East Pacific Rise (EPR, 9-11°N) and the relative H 2 O contents in EMORB that have more radiogenic Sr, South East Indian Ridge (SEIR, 127-129°E). Exactly the same Nd and Pb isotopes might be explained by differences in the nature region of the glass samples has been analysed for these components of enriched components recycled via subduction processes. However, using microbeam techniques. Our data allow examination of the when EMORB have the same radiogenic isotope compositions as fine details of H 2 O geochemical behaviour during MORB genesis. NMORB within a segment, relative H 2 O contents in EMORB We demonstrate that relative H 2 O contents [i.e. H 2 O/(another probably reflect local processes that lead to enrichment in incompatible incompatible element)] vary systematically with increasing (La/ elements. Regional differences in relative H 2 O contents of NMORB Sm) N in MORB glasses from both the EPR and SEIR. 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