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This contribution attempts to (i) critically evaluate the precision and continuity with which metamorphic \u003Cjats:italic>P–T\u003C\u002Fjats:italic> histories are retrieved today and (ii) discuss implications for regional‐scale accretionary processes in subduction zones, through application to the Schistes Lustrés complex (Haute Maurienne, W. Alps). \u003Cjats:italic>P–T\u003C\u002Fjats:italic> estimates are compared and combined using several independent approaches: (i) from minerals assumed to be in textural equilibrium; (ii) from electron microprobe compositional maps; and (iii) from pseudosection modelling predictions. Multi‐equilibrium calculations were performed with tweequ and thermocalc, and pseudosections were built with Perple_X and Theriak\u002FDomino. These \u003Cjats:italic>P–T\u003C\u002Fjats:italic> estimates were also compared with maximum temperatures (\u003Cjats:italic>T\u003C\u002Fjats:italic>\u003Cjats:sub>max\u003C\u002Fjats:sub>) deduced from the Raman spectroscopy of carbonaceous matter. The different methods used here yield the peak of pressure for the lower structural unit of the Schistes Lustrés at 480 °C and 23 kbar and document the retrograde path for both the Median and Lower Units. The results show that \u003Cjats:italic>P–T\u003C\u002Fjats:italic> conditions are recorded almost continuously and can be determined with a precision of ±1 kbar and ±30 °C at best. This study underlines the complementarity of the various thermobarometric methods and demonstrates that precision could be increased by improving solid solution models for chlorite. Observed tectonic patterns, major lithological boundaries, pressure–temperature and \u003Cjats:italic>T\u003C\u002Fjats:italic>\u003Cjats:sub>max\u003C\u002Fjats:sub> data suggest that underplating processes and early structural development played a key role in the Schistes Lustrés accretionary complex.\u003C\u002Fjats:p>",{"EN":109},"How continuous and precise is the record of \u003Ci>P–T\u003C\u002Fi> paths? Insights from combined thermobarometry and thermodynamic modelling into subduction dynamics (Schistes Lustrés, W. 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franco‐italiennes septentrionales): aspects lithostratigraphiques, paléogéographiques et géodynamiques, Comptes Rendus de l’Académie des Sciences de Paris, 305, 467",{},{"id":24,"text":427,"url":24,"identifiers":428},"Fudral S., 1994, Notice Explicative de la Carte Géologique de France (1\u002F50000), Feuille Lanslebourg‐Mont D’Ambin(776)",{},{"id":24,"text":430,"url":24,"identifiers":431},"10.1111\u002Fj.1365-3121.2008.00849.x",{"doi":430},{"id":24,"text":433,"url":24,"identifiers":434},"10.1016\u002Fj.lithos.2008.12.008",{"doi":433},{"id":24,"text":436,"url":24,"identifiers":437},"10.1016\u002Fj.lithos.2009.11.009",{"doi":436},{"id":24,"text":439,"url":24,"identifiers":440},"10.1111\u002Fj.1525-1314.2010.00904.x",{"doi":439},{"id":24,"text":442,"url":24,"identifiers":443},"10.1016\u002F0012-821X(84)90166-3",{"doi":442},{"id":24,"text":445,"url":24,"identifiers":446},"Goffé B., 1973, Sur la présence d’une variété magnésienne de ferro‐ carpholite en Vanoise (Alpes Françaises) Sa signification probable dans le métamorphisme alpin, Comptes Rendus de l’Académie des Sciences, 227, 1965",{},{"id":24,"text":448,"url":24,"identifiers":449},"10.1093\u002Fpetrology\u002Fegq065",{"doi":448},{"id":24,"text":451,"url":24,"identifiers":452},"10.1016\u002FS0191-8141(97)00096-5",{"doi":451},{"id":24,"text":454,"url":24,"identifiers":455},"10.1111\u002Fj.1525-1314.1990.tb00458.x",{"doi":454},{"id":24,"text":457,"url":24,"identifiers":458},"10.1111\u002Fj.1525-1314.1998.00140.x",{"doi":457},{"id":24,"text":460,"url":24,"identifiers":461},"10.1127\u002Fejm\u002F10\u002F3\u002F0395",{"doi":460},{"id":24,"text":463,"url":24,"identifiers":464},"Hyndman R., 1996, Giant earthquakes beneath Canada’s West coast, Geoscience Canada, 23, 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909",{},{"id":24,"text":487,"url":24,"identifiers":488},"10.1016\u002FS0012-821X(03)00455-2",{"doi":487},{"id":24,"text":490,"url":24,"identifiers":491},"10.1130\u002FSPE218-p111",{"doi":490},{"id":24,"text":493,"url":24,"identifiers":494},"Lemoine M., 1986, Les Schistes Lustrés piémontais des Alpes Occidentales: approche stratigraphique, structurale et sédimentologique, Eclogae Geologicae Helvetiae, 79, 271",{},{"id":24,"text":496,"url":24,"identifiers":497},"Lemoine M., 1984, Découverte de foraminifères planctoniques du Crétacé supérieur dans les Schistes Lustrés du Queyras (Alpes Occidentales). Conséquences paléogéographiques et tectoniques, Comptes Rendus de l’Académie des Sciences de Paris, 299, 727",{},{"id":24,"text":499,"url":24,"identifiers":500},"10.1016\u002F0264-8172(86)90044-9",{"doi":499},{"id":24,"text":502,"url":24,"identifiers":503},"10.1180\u002Fminmag.1980.043.332.04",{"doi":502},{"id":24,"text":505,"url":24,"identifiers":506},"Michard A., 1996, Did the Western Alps develop through an Oman‐type stage? The geotectonic setting of high pressure metamorphism in two contrasting Thethyan transects, Eclogae Geologicae Helvetiae, 89, 43",{},{"id":24,"text":508,"url":24,"identifiers":509},"10.1029\u002F2006GC001381",{"doi":508},{"id":24,"text":511,"url":24,"identifiers":512},"Oberhänsli R., 2004, Metamorphic structure of the Alps (1\u002F1000000)",{},{"id":24,"text":514,"url":24,"identifiers":515},"10.1016\u002FS0040-1951(97)00275-8",{"doi":514},{"id":24,"text":517,"url":24,"identifiers":518},"10.1007\u002Fs00410-002-0373-6",{"doi":517},{"id":24,"text":520,"url":24,"identifiers":521},"10.1111\u002Fj.1525-1314.1991.tb00501.x",{"doi":520},{"id":24,"text":523,"url":24,"identifiers":524},"Polino R., 1984, Les séries océaniques du Haut val de Suse (Alpes Cottiennes): analyse des couvertures sédimentaires, Ofioliti, 9, 547",{},{"id":24,"text":526,"url":24,"identifiers":527},"Powell R., 1994, Optimal geothermometry and geobarometry, American Mineralogist, 79, 120",{},{"id":24,"text":529,"url":24,"identifiers":530},"10.1144\u002FGSL.SP.1999.154.01.03",{"doi":529},{"id":24,"text":532,"url":24,"identifiers":533},"Rolland Y., 2000, Extension syn‐convergence, poin connement vertical et unités métamorphiques contrastées en bordure ouest du grand paradis (alpes franco‐italiennes), Geodinamica Acta, 13, 133",{},{"id":24,"text":535,"url":24,"identifiers":536},"10.1016\u002Fj.earscirev.2004.10.001",{"doi":535},{"id":24,"text":538,"url":24,"identifiers":539},"10.1130\u002F0091-7613(2001)029\u003C0003:EAFAS>2.0.CO;2",{"doi":538},{"id":24,"text":541,"url":24,"identifiers":542},"10.1016\u002FS0985-3111(00)00112-1",{"doi":541},{"id":24,"text":544,"url":24,"identifiers":545},"Schwartz S., 2000, La zone d’Acceglio (alpes cottiennes): un nouvel exemple de croûte continentale éclogitisée dans les alpes occidentales. The Acceglio zone (cottian alps): a new example of eclogitized continental crust in the Western Alps, Comptes Rendus de L’Académie des Sciences, 330, 859",{},{"id":24,"text":547,"url":24,"identifiers":548},"10.1007\u002Fs00531-004-0444-1",{"doi":547},{"id":24,"text":550,"url":24,"identifiers":551},"10.1180\u002F002646199548844",{"doi":550},{"id":24,"text":553,"url":24,"identifiers":554},"10.1029\u002FJB091iB10p10229",{"doi":553},{"id":24,"text":556,"url":24,"identifiers":557},"10.1016\u002FS0040-1951(98)00142-5",{"doi":556},{"id":24,"text":559,"url":24,"identifiers":560},"10.1002\u002Fgj.856",{"doi":559},{"id":24,"text":562,"url":24,"identifiers":563},"10.2475\u002Fajs.301.6.557",{"doi":562},{"id":24,"text":565,"url":24,"identifiers":566},"10.1111\u002Fj.1525-1314.2006.00661.x",{"doi":565},{"id":24,"text":568,"url":24,"identifiers":569},"10.1016\u002Fj.epsl.2007.11.025",{"doi":568},{"id":24,"text":571,"url":24,"identifiers":572},"10.1029\u002F2006JB004441",{"doi":571},{"id":24,"text":574,"url":24,"identifiers":575},"10.1111\u002Fj.1525-1314.2007.00722.x",{"doi":574},false,{"id":578,"createTime":579,"updateTime":580,"relativeEntities":581,"slug":582,"properties":583,"entityType":114,"verifyStatus":115,"verifyTime":596,"verifyNote":116,"languages":597,"translateLanguages":24,"viewCount":25,"primaryUrl":598,"fullTextUrl":24,"authors":599,"publicationType":228,"publisherRelationship":665,"citationCount":715,"citationInfo":716,"publishDate":720,"publishYear":717,"citationAnalyzeStatus":23,"lastCitationAnalyze":721,"indexDatabases":722,"openAccess":24,"references":723,"isForceReanalyzing":576},"966c4221-8af0-4281-8061-a0629ab5f917","2024-11-29T04:56:11.760+00:00","2025-07-25T06:17:54.508+00:00",[],"Fluid-inclusions-in-coesite-bearing-eclogites-and-jadeite-quartzite-at-Shuanghe-Dabie-Shan-China-",{"openalex":584,"mag":586,"abstract":588,"title":590,"gsPaper":592,"doi":594},{"VOID":585},"W1990060235",{"VOID":587},"1990060235",{"EN":589},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>Fluid inclusions in coesite‐bearing eclogites and jadeite quartzite at Shuanghe in Dabie Shan, East‐central China, have preserved remnants of early, prograde and\u002For peak metamorphic fluids, reset during post‐UHP (ultrahigh‐pressure) metamorphic uplift. Inclusions occur in several minerals (e.g. omphacite & epidote), notably as isolated, primary inclusions in quartz included in various host minerals. Two major fluid types have been identified: non‐polar fluid species (N\u003Cjats:sub>2\u003C\u002Fjats:sub> or CO\u003Cjats:sub>2\u003C\u002Fjats:sub>) and aqueous, the latter is by far the most predominant. Aqueous fluids cover a wide range of salinity, from halite‐bearing brines to low salinity fluids. For non‐polar fluids, few N\u003Cjats:sub>2\u003C\u002Fjats:sub> inclusions occur in undeformed eclogite, whereas a number of CO\u003Cjats:sub>2\u003C\u002Fjats:sub>‐rich inclusions have been found in microshear zones of eclogite or jadeite quartzite in close proximity to marble occurrences.\u003C\u002Fjats:p>\u003Cjats:p>The primary character of N\u003Cjats:sub>2\u003C\u002Fjats:sub> and high‐salinity aqueous inclusions indicates that they are remnants from UHP metamorphic fluids and for some there is the distinct possibility that they are ultimately derived from pre‐metamorphic fluids. This conclusion is supported by the preservation, in some samples, of microdomains containing synchronous inclusions of variable salinities, which tend to relate to the chemical composition of the host crystal. Carbonic fluids may be derived from neighbouring rocks, notably marble and carbonate‐bearing metasediments, during post‐metamorphic uplift. During post‐UHP exhumation, a limited decrease of the fluid density has occurred, with formation of new sets of fluid inclusions. Fluid movements, however, remained exceedingly limited, at the scale of the enclosing crystal.\u003C\u002Fjats:p>",{"EN":591},"Fluid inclusions in coesite‐bearing eclogites and jadeite quartzite at Shuanghe, Dabie Shan (China)",{"VOID":593},"[\"15405154273559620908\"]",{"VOID":595},"10.1046\u002Fj.0263-4929.2001.00327.x","2024-11-29T04:56:11.759+00:00",[118],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1046\u002Fj.0263-4929.2001.00327.x",[600,629,646],{"id":601,"sortIndex":25,"researcher":24,"roles":602,"affiliations":603,"properties":620,"displayName":624,"givenName":24,"familyName":24},"c203cf8c-c007-4bb2-9163-808159b8c901",[],[604,612],{"id":605,"sortIndex":25,"affiliation":606,"properties":24},"94d275f9-26b2-42ac-a964-d604fda18459",{"id":605,"createTime":24,"updateTime":24,"relativeEntities":607,"slug":24,"properties":608,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":611,"statistic":24},[],{"title":609},{"VI":610},"Department of Earth and Space Sciences, University of Science and Technology of China, Hefei, 230026, P.R. China",[],{"id":613,"sortIndex":135,"affiliation":614,"properties":24},"84e5319d-284b-497c-8611-b03059c87b9d",{"id":613,"createTime":24,"updateTime":24,"relativeEntities":615,"slug":24,"properties":616,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":619,"statistic":24},[],{"title":617},{"VI":618},"Department of Petrology, Faculty of Earth Sciences, Vrije Universiteit Amsterdam, De Boelelaan 1085, NL-1081 HV Amsterdam, The Netherlands",[],{"orcid":621,"title":623,"gsAuthor":625,"openalex":627},{"VOID":622},"https:\u002F\u002Forcid.org\u002F0000-0002-6266-8415",{"EN":624},"Bin 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V., 1999, Multi‐chronometric study of the country gneisses of UHP eclogites of Dabieshan: evidence for ‘in‐situ’ tectonic relationship, Journal of Conference Abstracts (EUG-10), 4, 102",{},{"id":24,"text":767,"url":24,"identifiers":768},"Cong Y., 1993, Fluid inclusions in eclogites from Dabie Mountains, eastern China, Terra Abstracts, 5, 475",{},{"id":24,"text":770,"url":24,"identifiers":771},"10.1127\u002Fejm\u002F7\u002F1\u002F0119",{"doi":770},{"id":24,"text":773,"url":24,"identifiers":774},"Crawford M. L., 1981, Short Course in Fluid Inclusions: Applications to Petrology, 75–100",{},{"id":24,"text":776,"url":24,"identifiers":777},"10.1127\u002Fejm\u002F1\u002F4\u002F0517",{"doi":776},{"id":24,"text":779,"url":24,"identifiers":780},"10.1007\u002Fs004100050468",{"doi":779},{"id":24,"text":782,"url":24,"identifiers":783},"10.1007\u002FBF00310869",{"doi":782},{"id":24,"text":785,"url":24,"identifiers":786},"10.1029\u002F97GL03309",{"doi":785},{"id":24,"text":788,"url":24,"identifiers":789},"10.1016\u002FS0012-821X(98)00152-6",{"doi":788},{"id":24,"text":791,"url":24,"identifiers":792},"10.2475\u002Fajs.271.2.97",{"doi":791},{"id":24,"text":794,"url":24,"identifiers":795},"Holland T. 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C., 1985, Microcharacterization of fluid inclusions in minerals by Raman microprobe, Scanning Electron Microscopy, 1985, 103",{},{"id":24,"text":896,"url":24,"identifiers":897},"Touret J. L. R., 1981, Short Course in Fluid Inclusions: Applications to Petrology, 182",{},{"id":24,"text":899,"url":24,"identifiers":900},"10.1016\u002Fs0024-4937(00)00036-0",{"doi":899},{"id":24,"text":902,"url":24,"identifiers":903},"10.1016\u002Fs0024-4937(96)00012-6",{"doi":902},{"id":24,"text":905,"url":24,"identifiers":906},"Van den Kerkhof A. M., 1988, Phase transitions and molar Volumes of CO2‐CH4‐N2 inclusions, Bulletin de Minéralogie, 111, 257, 10.3406\u002Fbulmi.1988.8046",{"doi":907},"10.3406\u002Fbulmi.1988.8046",{"id":24,"text":909,"url":24,"identifiers":910},"10.1007\u002FBF00285936",{"doi":909},{"id":24,"text":912,"url":24,"identifiers":913},"10.1130\u002F0091-7613(1991)019\u003C0933:RUPCBE>2.3.CO;2",{"doi":912},{"id":24,"text":915,"url":24,"identifiers":916},"10.1130\u002F0091-7613(1989)017\u003C1085:CBEFTD>2.3.CO;2",{"doi":915},{"id":24,"text":918,"url":24,"identifiers":919},"10.1086\u002F629585",{"doi":918},{"id":24,"text":921,"url":24,"identifiers":922},"10.1007\u002Fs004100050570",{"doi":921},{"id":24,"text":924,"url":24,"identifiers":925},"10.1126\u002Fscience.256.5053.80",{"doi":924},{"id":24,"text":927,"url":24,"identifiers":928},"10.1016\u002F0040-1951(87)90342-8",{"doi":927},{"id":24,"text":930,"url":24,"identifiers":931},"10.1127\u002Fejm\u002F10\u002F5\u002F0969",{"doi":930},{"id":24,"text":933,"url":24,"identifiers":934},"You Z. Han Y. Yang W. Zhang Z. Wei B. Liu R. 1996. The High‐Pressure and Ultrahigh‐Pressure Metamorphic Belt in the East Qinling and Dabie Mountains China.China University of Geosciences Press Wuhan.",{},{"id":24,"text":936,"url":24,"identifiers":937},"10.1016\u002Fs0009-2541(96)00153-2",{"doi":936},{"id":24,"text":939,"url":24,"identifiers":940},"10.1016\u002F0016-7037(95)00161-r",{"doi":939},{"id":24,"text":942,"url":24,"identifiers":943},"10.1016\u002F0743-9547(94)00036-E",{"doi":942},{"id":24,"text":945,"url":24,"identifiers":946},"10.1016\u002F0009-2541(87)90012-X",{"doi":945},{"id":24,"text":948,"url":24,"identifiers":949},"10.1093\u002Fpetrology\u002F36.4.1011",{"doi":948},{"id":24,"text":951,"url":24,"identifiers":952},"10.1111\u002Fj.1525-1314.1996.00319.x",{"doi":951},{"id":24,"text":954,"url":24,"identifiers":955},"10.1016\u002Fs0009-2541(98)00051-5",{"doi":954},{"id":24,"text":957,"url":24,"identifiers":958},"10.1127\u002Fejm\u002F8\u002F2\u002F0317",{"doi":957},{"id":24,"text":960,"url":24,"identifiers":961},"10.1016\u002Fs0012-821x(97)00203-3",{"doi":960},{"id":24,"text":963,"url":24,"identifiers":964},"10.1016\u002Fs0024-4937(98)00090-5",{"doi":963},{"id":24,"text":966,"url":24,"identifiers":967},"10.1016\u002Fs0009-2541(00)00199-6",{"doi":966},{"id":969,"createTime":970,"updateTime":970,"relativeEntities":971,"slug":972,"properties":973,"entityType":114,"verifyStatus":115,"verifyTime":970,"verifyNote":116,"languages":984,"translateLanguages":24,"viewCount":25,"primaryUrl":985,"fullTextUrl":24,"authors":986,"publicationType":228,"publisherRelationship":1055,"citationCount":1104,"citationInfo":1105,"publishDate":1108,"publishYear":1106,"citationAnalyzeStatus":23,"lastCitationAnalyze":24,"indexDatabases":1109,"openAccess":24,"references":1110,"isForceReanalyzing":576},"a6bd7eab-3412-44bc-99a8-079e98c992e6","2025-02-07T12:40:39.550+00:00",[],"Strain-related-differences-in-the-crystal-growth-of-white-mica-and-chlorite-a-TEM-and-XRD-study-of-the-development-of-metapelitic-microfabrics-in-the-Southern-Uplands-thrust-terrane-Scotland",{"openalex":974,"mag":976,"abstract":978,"title":980,"doi":982},{"VOID":975},"W2055071952",{"VOID":977},"2055071952",{"EN":979},"\u003Cjats:p>\u003Cjats:bold>Abstract\n\t\t\t\t\t\u003C\u002Fjats:bold> TEM and XRD techniques were used to study crystal growth characteristics of the fabric‐forming phyllosilicates which developed in response to low‐grade metamorphism and tectonic imbrication in part of the Southern Uplands thrust terrane. Prograde regional metamorphism, ranging from late diagenesis through the anchizone to the epizone, was accompanied by the development of a slaty cleavage which is commonly bedding‐parallel. TEM‐measured mean thicknesses of white mica and chlorite crystallite populations increase with advancing grade and correlate with XRD‐measured crystallinity indices. Analytical TEM data show that prograde changes in composition lead to a net loss of Si, Ca and minor Fe from the fabric‐forming phyllosilicates. White micas are paragonite‐poor phengites with a mean \u003Cjats:italic>b\u003C\u002Fjats:italic> lattice parameter of 9.037 Å, and indicate an intermediate pressure series of metamorphism with a field gradient of <25° C km\u003Cjats:sup>‐1\u003C\u002Fjats:sup>. Chlorite compositions evolved from diabantite (with intergrown corrensite) to ripidolite over an estimated temperature range of 150–320° C. Field gradient and temperature estimates suggest that crystal growth and fabric development occurred at burial depths ranging from 6 km to at least 13 km in the thrust terrane. During late diagenesis, crystal growth of white mica and chlorite was predominantly a consequence of polytypic and phase transitions, and resulted in similar size distributions which resemble typical Ostwald ripening curves. Under anchizonal and epizonal conditions, white mica grew more rapidly than chlorite because of its greater ability to store strain energy and recover from subgrain development; as a result crystal thickness distributions are not typical of Ostwald ripening. In contrast, chlorite crystals which grew under these conditions developed subgrain boundaries at high strain rates which were only partially recovered at low strain rates; these retained dislocations reduce the crystallite thicknesses detected by TEM and XRD, compared with those of white mica. These differences in strain‐induced crystal growth indicate that white mica (illite) and chlorite crystallinity indices are likely to show significant differences where low‐grade metamorphism is closely associated with tectonic fabric development.\u003C\u002Fjats:p>",{"EN":981},"Strain‐related differences in the crystal growth of white mica and chlorite: a TEM and XRD study of the development of metapelitic microfabrics in the Southern Uplands thrust terrane, Scotland",{"VOID":983},"10.1111\u002Fj.1525-1314.1995.tb00243.x",[118],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1111\u002Fj.1525-1314.1995.tb00243.x",[987,1004,1023,1040],{"id":988,"sortIndex":25,"researcher":24,"roles":989,"affiliations":990,"properties":999,"displayName":1001,"givenName":24,"familyName":24},"b3e4c68d-511f-4a1a-99c8-73bf0cae199c",[],[991],{"id":992,"sortIndex":25,"affiliation":993,"properties":24},"f7848752-e9e8-40cd-99df-1e601a781fae",{"id":992,"createTime":24,"updateTime":24,"relativeEntities":994,"slug":24,"properties":995,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":998,"statistic":24},[],{"title":996},{"EN":997},"British Geological Survey, Keyworth, Nottingham NG12 5GG, UK (email: k_rjm@ua.mkw.ac.uk)",[],{"title":1000,"openalex":1002},{"EN":1001},"R. 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J., 1987, Low Temperature Metamorphism, 227",{},{"id":24,"text":1206,"url":24,"identifiers":1207},"10.1111\u002Fj.1525-1314.1991.tb00556.x",{"doi":1206},{"id":24,"text":1209,"url":24,"identifiers":1210},"10.1016\u002F0040-1951(81)90016-0",{"doi":1209},{"id":24,"text":1212,"url":24,"identifiers":1213},"Laird J., 1988, Chlorites: metamorphic petrology, Mineralogical Society of America, Reviews in Mineralogy, 19, 405",{},{"id":24,"text":1215,"url":24,"identifiers":1216},"10.1144\u002Fgsjgs.136.6.0755",{"doi":1215},{"id":24,"text":1218,"url":24,"identifiers":1219},"10.1346\u002FCCMN.1994.0420401",{"doi":1218},{"id":24,"text":1221,"url":24,"identifiers":1222},"Lorimer G. W., 1976, Electron Microscopy in Mineralogy, 501",{},{"id":24,"text":1224,"url":24,"identifiers":1225},"10.1130\u002F0091-7613(1989)017\u003C0630:LVITLP>2.3.CO;2",{"doi":1224},{"id":24,"text":1227,"url":24,"identifiers":1228},"10.1144\u002Fgsjgs.144.5.0735",{"doi":1227},{"id":24,"text":1230,"url":24,"identifiers":1231},"10.1038\u002F267237a0",{"doi":1230},{"id":24,"text":1233,"url":24,"identifiers":1234},"Meike A., 1989, In situ deformation of micas: a high‐voltage electron‐microscope study, American Mineralogist, 74, 780",{},{"id":24,"text":1236,"url":24,"identifiers":1237},"Merriman R. J.&Roberts B. 1993.The low grade metamorphism of Lower Palaeozoic strata on the Rhins of Galloway SW Scotland.Technical Report of the British Geological Survey WG\u002F92\u002F40.",{},{"id":24,"text":1239,"url":24,"identifiers":1240},"10.1007\u002FBF00306406",{"doi":1239},{"id":24,"text":1242,"url":24,"identifiers":1243},"10.1144\u002Fgsjgs.150.2.0341",{"doi":1242},{"id":24,"text":1245,"url":24,"identifiers":1246},"Oliver G. J. H., 1984, Early Palaeozoic metamorphic history of the Midland Valley, the Southern Uplands‐Longford‐Down massif and the Lake District, British Isles, Transactions of the Royal Society of Edinburgh: Earth Science, 75, 259",{},{"id":24,"text":1248,"url":24,"identifiers":1249},"10.1017\u002FS0263593300013602",{"doi":1248},{"id":24,"text":1251,"url":24,"identifiers":1252},"Ostwald W., 1900, Über die vermeintliche Isomeric des roten und gelben Quecksilberoxyds und die Oberflächenspannung fester Körper, Zeitschrift für physikalische Chemie Stochiometrie und Verwandtschaftslehre, 34, 495, 10.1515\u002Fzpch-1900-3431",{"doi":1253},"10.1515\u002Fzpch-1900-3431",{"id":24,"text":1255,"url":24,"identifiers":1256},"10.1007\u002FBF00376965",{"doi":1255},{"id":24,"text":1258,"url":24,"identifiers":1259},"Peacor D. R., 1992, Diagenesis and low‐grade metamorphism of shales and slates, Mineralogical Society of America Reviews in Mineralogy, 27, 335",{},{"id":24,"text":1261,"url":24,"identifiers":1262},"10.1016\u002F0024-4937(77)90038-X",{"doi":1261},{"id":24,"text":1264,"url":24,"identifiers":1265},"10.1144\u002Fgsjgs.147.2.0271",{"doi":1264},{"id":24,"text":1267,"url":24,"identifiers":1268},"10.1017\u002FS0016756800019737",{"doi":1267},{"id":24,"text":1270,"url":24,"identifiers":1271},"10.1007\u002FBF00371166",{"doi":1270},{"id":24,"text":1273,"url":24,"identifiers":1274},"10.1007\u002FBF00678980",{"doi":1273},{"id":24,"text":1276,"url":24,"identifiers":1277},"10.1007\u002FBF00324564",{"doi":1276},{"id":24,"text":1279,"url":24,"identifiers":1280},"Sorby H. C., 1853, On the origin of slaty cleavage, New Philosophical Journal (Edinburgh), 55, 137",{},{"id":24,"text":1282,"url":24,"identifiers":1283},"Stone P., 1995, Memoir of the British Geological Survey Sheet 1+3 (Scotland)",{},{"id":24,"text":1285,"url":24,"identifiers":1286},"Urai J. L. Means W. D.&Lister G. S. 1986.Dynamic recrystallization of minerals. In:Mineral and Rock Deformation: Laboratory Studies(edsHobbs B. E.&Heard H. C.) The Paterson Volume. Geophysical Monograph 36 161–199.",{"doi":1287},"10.1029\u002FGM036p0161",{"id":24,"text":1289,"url":24,"identifiers":1290},"10.2475\u002Fajs.263.10.886",{"doi":1289},{"id":24,"text":1292,"url":24,"identifiers":1293},"10.1111\u002Fj.1525-1314.1994.tb00010.x",{"doi":1292},{"id":24,"text":1295,"url":24,"identifiers":1296},"10.1007\u002FBF00372155",{"doi":1295},{"id":24,"text":1298,"url":24,"identifiers":1299},"10.1016\u002F0040-1951(79)90328-7",{"doi":1298},{"id":1301,"createTime":1302,"updateTime":1302,"relativeEntities":1303,"slug":1304,"properties":1305,"entityType":114,"verifyStatus":115,"verifyTime":1302,"verifyNote":116,"languages":1316,"translateLanguages":24,"viewCount":25,"primaryUrl":1317,"fullTextUrl":24,"authors":1318,"publicationType":228,"publisherRelationship":1353,"citationCount":1403,"citationInfo":1404,"publishDate":1415,"publishYear":1405,"citationAnalyzeStatus":23,"lastCitationAnalyze":24,"indexDatabases":1416,"openAccess":24,"references":1417,"isForceReanalyzing":576},"ec8b6447-5661-487c-b9e3-19cd430b0e80","2025-02-06T14:43:41.766+00:00",[],"An-automated-strategy-for-calculation-of-phase-diagram-sections-and-retrieval-of-rock-properties-as-a-function-of-physical-conditions",{"openalex":1306,"mag":1308,"abstract":1310,"title":1312,"doi":1314},{"VOID":1307},"W2145525590",{"VOID":1309},"2145525590",{"EN":1311},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>We formulate an algorithm for the calculation of stable phase relations of a system with constrained bulk composition as a function of its environmental variables. The basis of this algorithm is the approximate representation of the free energy composition surfaces of solution phases by inscribed polyhedra. This representation leads to discretization of high variance phase fields into a continuous mesh of smaller polygonal fields within which the composition and physical properties of the phases are uniquely determined. The resulting phase diagram sections are useful for understanding the phase relations of complex metamorphic systems and for applications in which it is necessary to establish the variations in rock properties such as density, seismic velocities and volatile‐content through a metamorphic cycle. The algorithm has been implemented within a computer program that is general with respect to both the choice of variables and the number of components and phases possible in a system, and is independent of the structure of the equations of state used to describe the phases of the system.\u003C\u002Fjats:p>",{"EN":1313},"An automated strategy for calculation of phase diagram sections and retrieval of rock properties as a function of physical conditions",{"VOID":1315},"10.1046\u002Fj.1525-1314.2002.00398.x",[118],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1046\u002Fj.1525-1314.2002.00398.x",[1319,1338],{"id":1320,"sortIndex":25,"researcher":24,"roles":1321,"affiliations":1322,"properties":1331,"displayName":1335,"givenName":24,"familyName":24},"a84ee3af-1e5c-46c7-ad9c-b94aa17fc753",[],[1323],{"id":1324,"sortIndex":25,"affiliation":1325,"properties":24},"4397720e-b9cc-4097-b180-472e8ce0ed0e",{"id":1324,"createTime":24,"updateTime":24,"relativeEntities":1326,"slug":24,"properties":1327,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1330,"statistic":24},[],{"title":1328},{"EN":1329},"Earth Sciences Department, Swiss Federal Institute of Technology, 8092 Zurich, Switzerland (james.connolly@erdw.ethz.ch)",[],{"orcid":1332,"title":1334,"openalex":1336},{"VOID":1333},"https:\u002F\u002Forcid.org\u002F0000-0001-5060-4281",{"EN":1335},"J. A. D. Connolly",{"VOID":1337},"A5020644677",{"id":1339,"sortIndex":135,"researcher":24,"roles":1340,"affiliations":1341,"properties":1348,"displayName":1350,"givenName":24,"familyName":24},"c534e90e-621c-47b4-9214-e645077d3ecf",[],[1342],{"id":1324,"sortIndex":25,"affiliation":1343,"properties":24},{"id":1324,"createTime":24,"updateTime":24,"relativeEntities":1344,"slug":24,"properties":1345,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1347,"statistic":24},[],{"title":1346},{"EN":1329},[],{"title":1349,"openalex":1351},{"EN":1350},"K. 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D., 1975, A thermodynamic study of the pseudo‐binary join muscovite‐paragonite in the system KAlSi3O8‐NaAlSi3O8‐Al2O3‐SiO2‐H2O, American Mineralogist, 60, 985",{},{"id":24,"text":1437,"url":24,"identifiers":1438},"10.2475\u002Fajs.290.6.666",{"doi":1437},{"id":24,"text":1440,"url":24,"identifiers":1441},"10.1029\u002F97JB00731",{"doi":1440},{"id":24,"text":1443,"url":24,"identifiers":1444},"10.1111\u002Fj.1525-1314.1993.tb00155.x",{"doi":1443},{"id":24,"text":379,"url":24,"identifiers":1446},{"doi":379},{"id":24,"text":1448,"url":24,"identifiers":1449},"Connolly J. A. D., 1994, Forward modeling of calc‐silicate microinclusions and fluid evolution in a graphitic metapelite (NE Sardinia), American Mineralogist, 79, 960",{},{"id":24,"text":349,"url":24,"identifiers":1451},{"doi":349},{"id":24,"text":1453,"url":24,"identifiers":1454},"10.1007\u002FBF00310886",{"doi":1453},{"id":24,"text":1456,"url":24,"identifiers":1457},"10.1007\u002FBF02670272",{"doi":1456},{"id":24,"text":1459,"url":24,"identifiers":1460},"10.1007\u002FBF00381556",{"doi":1459},{"id":24,"text":1462,"url":24,"identifiers":1463},"10.1127\u002Fejm\u002F9\u002F1\u002F0175",{"doi":1462},{"id":24,"text":1465,"url":24,"identifiers":1466},"10.1016\u002F0895-7177(88)90082-9",{"doi":1465},{"id":24,"text":1468,"url":24,"identifiers":1469},"10.1016\u002F0012-821X(94)90053-1",{"doi":1468},{"id":24,"text":1471,"url":24,"identifiers":1472},"10.1046\u002Fj.0263-4929.2001.00320.x",{"doi":1471},{"id":24,"text":1474,"url":24,"identifiers":1475},"10.1007\u002FBF02868269",{"doi":1474},{"id":24,"text":1477,"url":24,"identifiers":1478},"Hillert M., 1985, A review of phase diagram principles, International Metallurgical Reviews, 30, 45, 10.1179\u002Fimr.1985.30.1.45",{"doi":1479},"10.1179\u002Fimr.1985.30.1.45",{"id":24,"text":460,"url":24,"identifiers":1481},{"doi":460},{"id":24,"text":457,"url":24,"identifiers":1483},{"doi":457},{"id":24,"text":1485,"url":24,"identifiers":1486},"10.1016\u002F0098-3004(92)90029-Q",{"doi":1485},{"id":24,"text":1488,"url":24,"identifiers":1489},"10.1029\u002F2000JB900357",{"doi":1488},{"id":24,"text":1491,"url":24,"identifiers":1492},"10.1130\u002F0091-7613(1998)026\u003C0375:SOOARO>2.3.CO;2",{"doi":1491},{"id":24,"text":1494,"url":24,"identifiers":1495},"10.1038\u002F35077056",{"doi":1494},{"id":24,"text":1497,"url":24,"identifiers":1498},"10.1016\u002FS0012-821X(01)00347-8",{"doi":1497},{"id":24,"text":818,"url":24,"identifiers":1500},{},{"id":24,"text":1502,"url":24,"identifiers":1503},"10.1016\u002FS0040-1951(01)00188-3",{"doi":1502},{"id":24,"text":1505,"url":24,"identifiers":1506},"10.1007\u002Fs004100100266",{"doi":1505},{"id":24,"text":1508,"url":24,"identifiers":1509},"10.1016\u002F0016-7037(80)90283-5",{"doi":1508},{"id":24,"text":1511,"url":24,"identifiers":1512},"Palatnik L. S., 1964, Phase Equilibria in Multicomponent Systems",{},{"id":24,"text":1514,"url":24,"identifiers":1515},"10.1046\u002Fj.1365-3121.2001.00371.x",{"doi":1514},{"id":24,"text":1517,"url":24,"identifiers":1518},"Powell R., 1978, Equilibrium Thermodynamics in Petrology: an Introduction",{},{"id":24,"text":1520,"url":24,"identifiers":1521},"10.1111\u002Fj.1525-1314.1988.tb00415.x",{"doi":1520},{"id":24,"text":1523,"url":24,"identifiers":1524},"10.1111\u002Fj.1525-1314.1998.00157.x",{"doi":1523},{"id":24,"text":1526,"url":24,"identifiers":1527},"10.1093\u002Fpetrology\u002F24.4.538",{"doi":1526},{"id":24,"text":1529,"url":24,"identifiers":1530},"Schmalzreid V. H., 1973, Zur geometrischen Darstellung von Phasengleichgewichten, Bunsengesellschaft Fuer Physikalische Chemie, 77, 90, 10.1002\u002Fbbpc.19730770207",{"doi":1531},"10.1002\u002Fbbpc.19730770207",{"id":24,"text":1533,"url":24,"identifiers":1534},"10.1130\u002F0016-7606(1956)67[919:GOPRPI]2.0.CO;2",{"doi":1533},{"id":24,"text":1536,"url":24,"identifiers":1537},"10.1007\u002FBF00690173",{"doi":1536},{"id":24,"text":1539,"url":24,"identifiers":1540},"10.1007\u002FBF00371465",{"doi":1539},{"id":24,"text":1542,"url":24,"identifiers":1543},"Spear F. S., 1999, Geological Materials Research, 1",{},{"id":24,"text":1545,"url":24,"identifiers":1546},"10.1007\u002Fs004100050322",{"doi":1545},{"id":24,"text":1548,"url":24,"identifiers":1549},"10.1007\u002FBF00310719",{"doi":1548},{"id":24,"text":1551,"url":24,"identifiers":1552},"Stuewe K., 1997, Reaction enthalpies of subsolidus equilibria in pelitic rocks. Magnitude and influence on Cretaceous Metamorphism of the Koralm Complex, Eastern Alps, Mitteilungen Des Naturwissentschaftlichen Vereins der Steirmark, 127, 45",{},{"id":24,"text":1554,"url":24,"identifiers":1555},"Thompson J. B., 1957, The graphical analysis of mineral assemblages in pelitic schists, American Mineralogist, 42, 842",{},{"id":24,"text":1557,"url":24,"identifiers":1558},"Thompson J. B., 1969, Mixing properties of sanidine crystalline solutions. IV. Phase diagrams from equations of state, American Mineralogist, 76, 493",{},{"id":24,"text":1560,"url":24,"identifiers":1561},"Trommsdorff V., 1996, The ultramafic contact aureole about the Bregaglia (Bergell) Tonalite: isograds and a thermal model, Schweizerische Mineralogische Petrographische Mitteilungen, 76, 537",{},{"id":24,"text":1563,"url":24,"identifiers":1564},"10.1016\u002F0016-7037(84)90358-2",{"doi":1563},{"id":24,"text":1566,"url":24,"identifiers":1567},"10.1111\u002Fj.1525-1314.1994.tb00006.x",{"doi":1566},{"id":1569,"createTime":1570,"updateTime":1571,"relativeEntities":1572,"slug":1573,"properties":1574,"entityType":114,"verifyStatus":115,"verifyTime":1570,"verifyNote":116,"languages":1589,"translateLanguages":1590,"viewCount":25,"primaryUrl":1592,"fullTextUrl":24,"authors":1593,"publicationType":228,"publisherRelationship":1651,"citationCount":1701,"citationInfo":1702,"publishDate":1711,"publishYear":1703,"citationAnalyzeStatus":23,"lastCitationAnalyze":24,"indexDatabases":1712,"openAccess":24,"references":1713,"isForceReanalyzing":576},"2cc7c0ba-c694-4376-b33a-ed74331687c0","2024-11-29T04:55:57.197+00:00","2025-01-21T11:26:03.751+00:00",[],"An-extended-episode-of-early-Mesoproterozoic-metamorphic-fluid-flow-in-the-Reynolds-Range-central-Australia-",{"openalex":1575,"mag":1577,"abstract":1579,"title":1582,"keywords":1585,"doi":1587},{"VOID":1576},"W2048731492",{"VOID":1578},"2048731492",{"EN":1580,"VI":1581},"\u003Cjats:p>\u003Cjats:bold>ABSTRACT\u003C\u002Fjats:bold> The products of metamorphic fluid flow are preserved in zones within the marbles and metamorphosed semipelites of the Upper Calcsilicate Unit in the granulite portion of the Late Palaeoproterozoic Reynolds Range Group, northern Arunta Block, central Australia. The zones of retrogression, characterized by minerals such as wollastonite, grossular and clinohumite, local resetting of oxygen isotopic compositions and local major element metasomatism, were channelways for water‐rich fluids derived from granulite facies metapelites. U–Th–Pb isotopic ages measured by the SHRIMP ion microprobe on zircon and monazite from a granulite facies semipelite, an early semiconcordant aluminous quartz‐rich fluid‐flow segregation and a late discordant quartz‐rich segregation record some of the extended thermal history of the area. Zircon cores from the semipelite show its likely protolith to be an igneous rock 1812 ± 11 Ma old, itself derived from a source containing zircon as old as 2.2 Ga. Low‐Th\u002FU overgrowths on the zircon grew during granulite facies metamorphism at 1594 ± 6 Ma. Monazite cooled to its blocking temperature at 1576 ± 8 Ma. Zircon cores from the semiconcordant segregation are dominantly >2.3 Ga old, indicating that the source of the fluids was not the particular metamorphosed semipelite studied. Two generations of low‐Th\u002FU overgrowths on the zircon give indistinguishable ages for the older and younger of 1589 ± 8 and 1582 ± 8 Ma, respectively. The monazite age is the same, 1576 ± 12 Ma. Zircon from the late discordant segregation gave 1568 ± 4 Ma. Fluid flow occurred for at least 18 ± 3 (σ) Ma and ended 26 ± 3 (σ) Ma after the peak of metamorphism, suggesting a very slow cooling rate of ∼3°C Ma\u003Cjats:sup>–1\u003C\u002Fjats:sup>. The last regional high‐grade metamorphism in the Reynolds Range occurred at ∼1.6 Ga, not ∼1.78 Ga as previously thought. The high‐grade event at ∼1.78 Ga is a separate event that affected only the basement to the Reynolds Range Group.\u003C\u002Fjats:p>","\u003Cjats:p>\u003Cjats:bold>TÓM TẮT\u003C\u002Fjats:bold> Các sản phẩm của dòng chảy chất lỏng biến chất được bảo tồn trong các vùng trong đá cẩm thạch và đá bán điển hình đã biến chất của Đơn vị Calcsilicate trên cùng trong phần granulite của Nhóm Reynolds Range thuộc kỷ Palaeoproterozoic muộn, phía bắc khối Arunta, Trung Australia. Các vùng tái phát triển, đặc trưng bởi các khoáng vật như wollastonite, grossular và clinohumite, tái thiết lập cục bộ các thành phần đồng vị oxy và sự biến chất của các nguyên tố chính tại chỗ, đã là những kênh dẫn cho các chất lỏng giàu nước có nguồn gốc từ các đá metapelites thuộc facies granulite. Tuổi đồng vị U–Th–Pb được đo bằng thiết bị SHRIMP trên zircon và monazite từ một đá bán điển hình thuộc facies granulite, một phân loại chất lỏng giàu nhôm-quartz sơ bộ nửa đồng nhất và một phân loại quartz giàu muộn không đồng nhất ghi lại một phần lịch sử nhiệt độ kéo dài của khu vực. Nhân zircon từ đá bán điển hình cho thấy một tiền thể có thể là một loại đá magma có tuổi 1812 ± 11 Ma, bản thân nó có nguồn gốc từ một nguồn chứa zircon có tuổi lên tới 2.2 Ga. Các lớp phủ Low-Th\u002FU trên zircon phát triển trong quá trình biến chất facies granulite ở 1594 ± 6 Ma. Monazite làm mát xuống nhiệt độ chặn của nó ở 1576 ± 8 Ma. Nhân zircon từ phân loại nửa đồng nhất chủ yếu có tuổi >2.3 Ga, cho thấy nguồn của các chất lỏng không phải là đá bán điển hình biến chất cụ thể được nghiên cứu. Hai thế hệ lớp phủ Low-Th\u002FU trên zircon có tuổi không phân biệt cho thế hệ cũ và trẻ là 1589 ± 8 và 1582 ± 8 Ma, tương ứng. Tuổi monazite là giống nhau, 1576 ± 12 Ma. Zircon từ phân loại không đồng nhất muộn cho kết quả 1568 ± 4 Ma. Dòng chảy chất lỏng xảy ra ít nhất 18 ± 3 (σ) Ma và kết thúc 26 ± 3 (σ) Ma sau đỉnh điểm của biến chất, gợi ý về một tỷ lệ làm mát rất chậm khoảng 3°C Ma\u003Cjats:sup>–1\u003C\u002Fjats:sup>. Giai đoạn biến chất cao cấp cuối cùng ở Dãy Reynolds xảy ra vào khoảng 1.6 Ga, không phải khoảng 1.78 Ga như đã từng được nghĩ. Sự kiện biến chất cao cấp ở 1.78 Ga là một sự kiện riêng biệt chỉ ảnh hưởng đến tầng đá gốc của Nhóm Reynolds Range.\u003C\u002Fjats:p>",{"EN":1583,"VI":1584},"An extended episode of early Mesoproterozoic metamorphic fluid flow in the Reynolds Range, central Australia*","Một giai đoạn kéo dài của dòng chảy chất lỏng biến chất đầu kỷ Mesoproterozoic ở dãy Reynolds, Trung Australia*",{"VI":1586},"",{"VOID":1588},"10.1111\u002Fj.1525-1314.1996.00029.x",[118],[1591],"VI","https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1111\u002Fj.1525-1314.1996.00029.x",[1594,1613,1632],{"id":1595,"sortIndex":25,"researcher":24,"roles":1596,"affiliations":1597,"properties":1606,"displayName":1610,"givenName":24,"familyName":24},"46e0031b-0eb8-458a-a3af-282029a688b0",[],[1598],{"id":1599,"sortIndex":25,"affiliation":1600,"properties":24},"65c21e28-064b-4b34-9436-c664520fafc4",{"id":1599,"createTime":24,"updateTime":24,"relativeEntities":1601,"slug":24,"properties":1602,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1605,"statistic":24},[],{"title":1603},{"EN":1604},"Research School of Earth Sciences, Australian National University, Canberra, ACT 0200, Australia (email: ian.williams@anu.edu.au)",[],{"orcid":1607,"title":1609,"openalex":1611},{"VOID":1608},"https:\u002F\u002Forcid.org\u002F0000-0003-4465-6493",{"EN":1610},"Ian S. Williams",{"VOID":1612},"A5085825108",{"id":1614,"sortIndex":135,"researcher":24,"roles":1615,"affiliations":1616,"properties":1625,"displayName":1629,"givenName":24,"familyName":24},"24d2b963-b299-4a6b-8d8a-95104a11f0a6",[],[1617],{"id":1618,"sortIndex":25,"affiliation":1619,"properties":24},"06f11c1d-7813-46cc-a82a-04a2fd13f9f1",{"id":1618,"createTime":24,"updateTime":24,"relativeEntities":1620,"slug":24,"properties":1621,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1624,"statistic":24},[],{"title":1622},{"VI":1623},"School of Earth Sciences, La Trobe University, Bundoora, Victoria, 3083, Australia",[],{"orcid":1626,"title":1628,"openalex":1630},{"VOID":1627},"https:\u002F\u002Forcid.org\u002F0000-0003-0217-3522",{"EN":1629},"I. S. Buick",{"VOID":1631},"A5004126395",{"id":1633,"sortIndex":170,"researcher":24,"roles":1634,"affiliations":1635,"properties":1644,"displayName":1648,"givenName":24,"familyName":24},"ec345b53-c0a1-42c4-bc8e-240e8c499ff4",[],[1636],{"id":1637,"sortIndex":25,"affiliation":1638,"properties":24},"7a48bec6-e376-4f40-b30f-07b17efd59a9",{"id":1637,"createTime":24,"updateTime":24,"relativeEntities":1639,"slug":24,"properties":1640,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1643,"statistic":24},[],{"title":1641},{"EN":1642},"Dept. of Earth Sciences, Monash Univ., Clayton, Victoria, 3168, Australia",[],{"orcid":1645,"title":1647,"openalex":1649},{"VOID":1646},"https:\u002F\u002Forcid.org\u002F0000-0001-5300-4716",{"EN":1648},"Ian Cartwright",{"VOID":1650},"A5019537260",{"url":24,"publisher":1652,"properties":1694},{"id":6,"createTime":7,"updateTime":8,"relativeEntities":1653,"slug":10,"properties":1654,"entityType":22,"verifyStatus":23,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":25,"subjectFields":1659,"manageAffiliations":1668,"indexDatabases":1679,"url":90,"thumbnailPath":24,"statistic":24,"gsStatistic":24,"type":24,"analyzePriority":24},[],{"country":1655,"eissn":1656,"issn":1657,"title":1658},{"VOID":13},{"VOID":15},{"VOID":17},{"EN":19},[1660,1664],{"id":28,"createTime":24,"updateTime":24,"relativeEntities":1661,"label":1662,"description":1663,"parentId":24,"standard":24,"scholarHubFieldId":24},[],{"EN":31},{},{"id":34,"createTime":24,"updateTime":24,"relativeEntities":1665,"label":1666,"description":1667,"parentId":24,"standard":24,"scholarHubFieldId":24},[],{"EN":37},{},[1669,1674],{"id":41,"createTime":24,"updateTime":24,"relativeEntities":1670,"slug":24,"properties":1671,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1673,"statistic":24},[],{"title":1672},{"EN":45},[],{"id":48,"createTime":24,"updateTime":24,"relativeEntities":1675,"slug":24,"properties":1676,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1678,"statistic":24},[],{"title":1677},{"EN":52},[],[1680,1687],{"id":56,"indexDatabase":1681,"url":69,"indexYears":24,"academicFieldIds":1686,"indexDatabaseRanking":24},{"id":58,"createTime":24,"updateTime":24,"relativeEntities":1682,"label":1683,"description":1684,"key":65,"publicationTags":1685,"standard":24},[],{"EN":61,"VI":61},{"EN":63,"VI":64},[67,68],[71],{"id":73,"indexDatabase":1688,"url":84,"indexYears":85,"academicFieldIds":1693,"indexDatabaseRanking":89},{"id":75,"createTime":24,"updateTime":24,"relativeEntities":1689,"label":1690,"description":1691,"key":81,"publicationTags":1692,"standard":24},[],{"EN":78,"VI":78},{"EN":78,"VI":80},[83],[87,88],{"issue":1695,"pages":1697,"volume":1699},{"VOID":1696},"1",{"VOID":1698},"29-47",{"VOID":1700},"14",510,{"total":1701,"publishYear":1703,"statisticByYear":1704},1996,{"2012":286,"2013":1705,"2014":1407,"2015":1706,"2016":1706,"2017":1707,"2018":1708,"2019":1408,"2020":1709,"2021":1710,"2022":283,"2023":719,"2024":284},21,27,28,25,14,24,"1996-01-01",[67,89],[1714,1717,1720,1723,1726,1729,1732,1735,1738,1741,1744,1747,1751,1754,1757,1760,1763,1766,1769,1772,1775,1778,1781,1784,1787,1790,1793,1796,1799,1802,1805,1807,1810,1813,1816,1819,1822,1825,1828,1831,1834,1837,1840,1843,1846,1849,1852,1855,1858,1861,1864,1867,1870,1873,1876,1879,1882,1885,1888,1891,1894,1897,1900,1903],{"id":24,"text":1715,"url":24,"identifiers":1716},"10.1007\u002FBF00373680",{"doi":1715},{"id":24,"text":1718,"url":24,"identifiers":1719},"10.1016\u002F0301-9268(90)90009-F",{"doi":1718},{"id":24,"text":1721,"url":24,"identifiers":1722},"10.1007\u002FBF00371371",{"doi":1721},{"id":24,"text":1724,"url":24,"identifiers":1725},"10.1080\u002F08120099208728012",{"doi":1724},{"id":24,"text":1727,"url":24,"identifiers":1728},"Black L. P., 1983, Rb–Sr geochronology of Proterozoic events in the Arunta Inlier, central Australia, Bureau of Mineral Resources Journal of Australian Geology and Geophysics, 8, 129",{},{"id":24,"text":1730,"url":24,"identifiers":1731},"10.2475\u002Fajs.294.1.1",{"doi":1730},{"id":24,"text":1733,"url":24,"identifiers":1734},"Buick I. S., 1994, Mineralogical Magazine, 130",{},{"id":24,"text":1736,"url":24,"identifiers":1737},"10.1029\u002F94JB01147",{"doi":1736},{"id":24,"text":1739,"url":24,"identifiers":1740},"10.1111\u002Fj.1525-1314.1988.tb00409.x",{"doi":1739},{"id":24,"text":1742,"url":24,"identifiers":1743},"10.1144\u002Fgsjgs.151.4.0583",{"doi":1742},{"id":24,"text":1745,"url":24,"identifiers":1746},"10.1111\u002Fj.1525-1314.1995.tb00228.x",{"doi":1745},{"id":24,"text":1748,"url":24,"identifiers":1749},"Cartwright I. Buick I. S.&Vry J. K. 1995.Polyphase metamorphic fluid flow in the Lower Calcsilicate Unit Reynolds Range central Australia.Precambrian Research in press.",{"doi":1750},"10.1016\u002F0301-9268(95)00055-0",{"id":24,"text":1752,"url":24,"identifiers":1753},"10.1007\u002FBF00310607",{"doi":1752},{"id":24,"text":1755,"url":24,"identifiers":1756},"Claoué‐Long J. C. Compston W. Roberts J.&Fanning C. M. 1995.Two Carboniferous ages: a comparison of SHRIMP zircon dating with conventional zircon ages and40Ar\u002F39Ar analysis.SEPM Special Publication in press.",{},{"id":24,"text":1758,"url":24,"identifiers":1759},"10.1111\u002Fj.1525-1314.1993.tb00141.x",{"doi":1758},{"id":24,"text":1761,"url":24,"identifiers":1762},"10.1016\u002F0191-8141(91)90075-T",{"doi":1761},{"id":24,"text":1764,"url":24,"identifiers":1765},"10.1016\u002F0301-9268(94)00067-2",{"doi":1764},{"id":24,"text":1767,"url":24,"identifiers":1768},"10.1130\u002F0091-7613(1993)021\u003C0953:HWEIIC>2.3.CO;2",{"doi":1767},{"id":24,"text":1770,"url":24,"identifiers":1771},"10.1016\u002F0301-9268(94)00056-W",{"doi":1770},{"id":24,"text":1773,"url":24,"identifiers":1774},"10.1016\u002F0012-821X(86)90020-8",{"doi":1773},{"id":24,"text":1776,"url":24,"identifiers":1777},"10.1029\u002FJB089iS02p0B525",{"doi":1776},{"id":24,"text":1779,"url":24,"identifiers":1780},"Cooper J. A., 1988, Rate of Arunta Inlier evolution at the eastern margin of the Entia dome, central Australia, Precambrian Research, 4041, 251",{},{"id":24,"text":1782,"url":24,"identifiers":1783},"10.1016\u002F0024-4937(81)90037-2",{"doi":1782},{"id":24,"text":1785,"url":24,"identifiers":1786},"10.1016\u002F0016-7037(92)90397-2",{"doi":1785},{"id":24,"text":1788,"url":24,"identifiers":1789},"10.1080\u002F08120099008727941",{"doi":1788},{"id":24,"text":1791,"url":24,"identifiers":1792},"10.1111\u002Fj.1525-1314.1991.tb00514.x",{"doi":1791},{"id":24,"text":1794,"url":24,"identifiers":1795},"10.1111\u002Fj.1525-1314.1991.tb00553.x",{"doi":1794},{"id":24,"text":1797,"url":24,"identifiers":1798},"10.1016\u002F0191-8141(90)90080-I",{"doi":1797},{"id":24,"text":1800,"url":24,"identifiers":1801},"10.1007\u002FBF00371145",{"doi":1800},{"id":24,"text":1803,"url":24,"identifiers":1804},"10.1111\u002Fj.1365-2818.1991.tb03197.x",{"doi":1803},{"id":24,"text":1736,"url":24,"identifiers":1806},{"doi":1736},{"id":24,"text":1808,"url":24,"identifiers":1809},"10.1130\u002F0091-7613(1991)019\u003C0211:FFMRAM>2.3.CO;2",{"doi":1808},{"id":24,"text":1811,"url":24,"identifiers":1812},"10.1016\u002F0009-2541(93)90244-D",{"doi":1811},{"id":24,"text":1814,"url":24,"identifiers":1815},"10.1016\u002F0191-8141(92)90159-T",{"doi":1814},{"id":24,"text":1817,"url":24,"identifiers":1818},"10.1130\u002F0091-7613(1992)020\u003C0649:HWEIIC>2.3.CO;2",{"doi":1817},{"id":24,"text":1820,"url":24,"identifiers":1821},"10.1130\u002F0091-7613(1993)021\u003C0955:SAWCCI>2.3.CO;2",{"doi":1820},{"id":24,"text":1823,"url":24,"identifiers":1824},"10.1111\u002Fj.1525-1314.1994.tb00042.x",{"doi":1823},{"id":24,"text":1826,"url":24,"identifiers":1827},"10.1180\u002Fminmag.1994.58A.1.196",{"doi":1826},{"id":24,"text":1829,"url":24,"identifiers":1830},"Hensen B. J., 1984, Fluid evolution in granulites from the Arunta Block, central Australia, Geological Society of Australia Abstracts Volume, 12, 235",{},{"id":24,"text":1832,"url":24,"identifiers":1833},"10.1180\u002Fminmag.1984.048.349.05",{"doi":1832},{"id":24,"text":1835,"url":24,"identifiers":1836},"10.1086\u002F628165",{"doi":1835},{"id":24,"text":1838,"url":24,"identifiers":1839},"10.1111\u002Fj.1365-2818.1993.tb03379.x",{"doi":1838},{"id":24,"text":1841,"url":24,"identifiers":1842},"10.1086\u002F648243",{"doi":1841},{"id":24,"text":1844,"url":24,"identifiers":1845},"10.1130\u002F0091-7613(1993)021\u003C0607:PATOOM>2.3.CO;2",{"doi":1844},{"id":24,"text":1847,"url":24,"identifiers":1848},"10.1016\u002F0016-7037(94)90521-5",{"doi":1847},{"id":24,"text":1850,"url":24,"identifiers":1851},"10.1139\u002Fe90-152",{"doi":1850},{"id":24,"text":1853,"url":24,"identifiers":1854},"10.1111\u002Fj.1525-1314.1991.tb00527.x",{"doi":1853},{"id":24,"text":1856,"url":24,"identifiers":1857},"10.1080\u002F08120098408729305",{"doi":1856},{"id":24,"text":1859,"url":24,"identifiers":1860},"Smith H. A., 1994, 204Pb tracer diffusion in monazite and implications for U–Pb closer temperatures, EOS, 75, 692",{},{"id":24,"text":1862,"url":24,"identifiers":1863},"Sommerauer J., 1974, Trace element distribution patterns and the mineralogical stability of zircon ‐ an application for combined electron microprobe techniques, Proceedings of the Electron Microscopy Society of South Africa, 4, 71",{},{"id":24,"text":1865,"url":24,"identifiers":1866},"10.1016\u002F0012-821X(77)90060-7",{"doi":1865},{"id":24,"text":1868,"url":24,"identifiers":1869},"10.1080\u002F08120098408729304",{"doi":1868},{"id":24,"text":1871,"url":24,"identifiers":1872},"10.1093\u002Fpetrology\u002F31.3.555",{"doi":1871},{"id":24,"text":1874,"url":24,"identifiers":1875},"10.1016\u002F0012-821X(92)90155-O",{"doi":1874},{"id":24,"text":1877,"url":24,"identifiers":1878},"Reenen D. D., 1986, Hydration of cordierite and hypersthene and a description of the retrograde orthoamphibole isograd, American Mineralogist, 71, 900",{},{"id":24,"text":1880,"url":24,"identifiers":1881},"10.1007\u002FBF00306410",{"doi":1880},{"id":24,"text":1883,"url":24,"identifiers":1884},"10.1007\u002FBF00310691",{"doi":1883},{"id":24,"text":1886,"url":24,"identifiers":1887},"10.1007\u002FBF00371240",{"doi":1886},{"id":24,"text":1889,"url":24,"identifiers":1890},"10.1007\u002FBF00371438",{"doi":1889},{"id":24,"text":1892,"url":24,"identifiers":1893},"10.1016\u002F0301-9268(94)00055-V",{"doi":1892},{"id":24,"text":1895,"url":24,"identifiers":1896},"10.1130\u002F0091-7613(1990)018\u003C0626:IMDOZF>2.3.CO;2",{"doi":1895},{"id":24,"text":1898,"url":24,"identifiers":1899},"10.1029\u002F91TC00168",{"doi":1898},{"id":24,"text":1901,"url":24,"identifiers":1902},"10.1016\u002F0016-7037(93)90042-U",{"doi":1901},{"id":24,"text":1904,"url":24,"identifiers":1905},"10.1016\u002F0301-9268(94)00054-U",{"doi":1904},{"id":1907,"createTime":1908,"updateTime":1908,"relativeEntities":1909,"slug":1910,"properties":1911,"entityType":114,"verifyStatus":115,"verifyTime":1908,"verifyNote":116,"languages":1922,"translateLanguages":24,"viewCount":25,"primaryUrl":1923,"fullTextUrl":24,"authors":1924,"publicationType":228,"publisherRelationship":2006,"citationCount":2055,"citationInfo":2056,"publishDate":2059,"publishYear":2057,"citationAnalyzeStatus":23,"lastCitationAnalyze":24,"indexDatabases":2060,"openAccess":24,"references":2061,"isForceReanalyzing":576},"ef8d109f-a87f-4dc0-8281-08c7233259ca","2024-12-29T01:46:09.442+00:00",[],"The-metamorphic-signature-of-contemporaneous-extension-and-shortening-in-the-central-Himalayan-orogen-data-from-the-Nyalam-transect-southern-Tibet",{"openalex":1912,"mag":1914,"abstract":1916,"title":1918,"doi":1920},{"VOID":1913},"W2036725830",{"VOID":1915},"2036725830",{"EN":1917},"\u003Cjats:p>\u003Cjats:bold>Abstract\n\t\t\t\t\t\u003C\u002Fjats:bold> Geological relationships and geochronological data suggest that in Miocene time the metamorphic core of the central Himalayan orogen was a wedge‐shaped body bounded below by the N‐dipping Main Central thrust system and above the N‐dipping South Tibetan detachment system. We infer that synchronous movement on these fault systems expelled the metamorphic core southward toward the Indian foreland, thereby moderating the extreme topographic gradient at the southern margin of the Tibetan Plateau. Reaction textures, thermobarometric data and thermodynamic modelling of pelitic schists and gneisses from the Nyalam transect in southern Tibet (28°N, 86°E) imply that gravitational collapse of the orogen produced a complex thermal structure in the metamorphic core. Amphibolite facies metamorphism and anatexis at temperatures of 950 K and depths of at least 30 km accompanied the early stages of displacement on the Main Central thrust system. Our findings suggest that the late metamorphic history of these rocks was characterized by high‐\u003Cjats:italic>T\u003C\u002Fjats:italic> decompression associated with roughly 15 km of unroofing by movement on the South Tibetan detachment system. In the middle of the metamorphic core, roughly 7–8 km below the basal detachment of the South Tibetan system, the decompression was essentially isothermal. Near the base of the metamorphic core, roughly 4–6 km above the Main Central thrust, the decompression was accompanied by about 150 K of cooling. We attribute the disparity between the \u003Cjats:italic>P–T\u003C\u002Fjats:italic> paths of these two structural levels to cooling of the lower part of the metamorphic core as a consequence of continued (and probably accelerated) underthrusting of cooler rocks in the footwall of the Main Central thrust at the same time as movement on the South Tibetan detachment system.\u003C\u002Fjats:p>",{"EN":1919},"The metamorphic signature of contemporaneous extension and shortening in the central Himalayan orogen: data from the Nyalam transect, southern Tibet",{"VOID":1921},"10.1111\u002Fj.1525-1314.1993.tb00183.x",[118],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1111\u002Fj.1525-1314.1993.tb00183.x",[1925,1944,1959,1974,1991],{"id":1926,"sortIndex":25,"researcher":24,"roles":1927,"affiliations":1928,"properties":1937,"displayName":1941,"givenName":24,"familyName":24},"553e30e5-4898-4306-90fe-ab43cd4b621a",[],[1929],{"id":1930,"sortIndex":25,"affiliation":1931,"properties":24},"31e33e9e-dc20-4c8a-92d1-505540519808",{"id":1930,"createTime":24,"updateTime":24,"relativeEntities":1932,"slug":24,"properties":1933,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":1936,"statistic":24},[],{"title":1934},{"VI":1935},"Department of Earth, Atmospheric and Planetary Sciences, Massachusetts Institute of Technology, Cambridge MA 02139, USA, ",[],{"orcid":1938,"title":1940,"openalex":1942},{"VOID":1939},"https:\u002F\u002Forcid.org\u002F0000-0003-2805-8899",{"EN":1941},"K. 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D., 1975, A thermodynamic study of the pseudobinary join muscovite–paragonite in the system KAlSi2O8–Al2O3–SiO2–H2O, American Mineralogist, 60, 985",{},{"id":24,"text":2092,"url":24,"identifiers":2093},"Clarke D. B., 1981, The mineralogy of peraluminous granites: a review, Canadian Mineralogist, 19, 3",{},{"id":24,"text":2095,"url":24,"identifiers":2096},"Clemens J. D., 1981, Origin and crystallization of some peraluminous (S‐type) granitic magmas, Canadian Mineralogist, 19, 111",{},{"id":24,"text":2098,"url":24,"identifiers":2099},"10.1016\u002F0377-0273(90)90010-D",{"doi":2098},{"id":24,"text":2101,"url":24,"identifiers":2102},"Elkins L. 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W., 1988, Accuracy versus precision in locating reaction boundaries: implications for the garnet–plagioclase–aluminum silicate–quartz geobarometer, American Mineralogist, 73, 1205",{},{"id":24,"text":2187,"url":24,"identifiers":2188},"10.1029\u002FJB095iB04p04833",{"doi":2187},{"id":24,"text":2190,"url":24,"identifiers":2191},"Parrish R. R., 1992, 7th Himalaya–Tibet–Karakoram Workshop Abstracts, 67",{},{"id":24,"text":2193,"url":24,"identifiers":2194},"10.1029\u002F90TC02655",{"doi":2193},{"id":24,"text":2196,"url":24,"identifiers":2197},"10.1007\u002FBF00371485",{"doi":2196},{"id":24,"text":2199,"url":24,"identifiers":2200},"Ruppel C. D. 1986.Thermal‐modelling of extensional tectonics.Unpubl. PhD Thesis Massachusetts Institute of Technology.",{},{"id":24,"text":2202,"url":24,"identifiers":2203},"10.1029\u002FTC007i005p00947",{"doi":2202},{"id":24,"text":2205,"url":24,"identifiers":2206},"10.1016\u002F0012-821X(83)90115-2",{"doi":2205},{"id":24,"text":2208,"url":24,"identifiers":2209},"10.1016\u002F0012-821X(86)90130-5",{"doi":2208},{"id":24,"text":2211,"url":24,"identifiers":2212},"10.1130\u002FSPE232-p47",{"doi":2211},{"id":24,"text":2214,"url":24,"identifiers":2215},"10.1016\u002F0191-8141(81)90060-2",{"doi":2214},{"id":24,"text":2217,"url":24,"identifiers":2218},"10.1144\u002FGSL.SP.1989.043.01.04",{"doi":2217},{"id":24,"text":2220,"url":24,"identifiers":2221},"10.1111\u002Fj.1525-1314.1991.tb00533.x",{"doi":2220},{"id":24,"text":2223,"url":24,"identifiers":2224},"10.1029\u002FSC007",{"doi":2223},{"id":24,"text":2226,"url":24,"identifiers":2227},"10.1007\u002FBF00371203",{"doi":2226},{"id":24,"text":2229,"url":24,"identifiers":2230},"10.1007\u002FBF00375530",{"doi":2229},{"id":24,"text":2232,"url":24,"identifiers":2233},"10.2475\u002Fajs.282.10.1567",{"doi":2232},{"id":24,"text":2235,"url":24,"identifiers":2236},"10.1007\u002FBF00371049",{"doi":2235},{"id":24,"text":2238,"url":24,"identifiers":2239},"10.1515\u002F9781501508172-013",{"doi":2238},{"id":24,"text":2241,"url":24,"identifiers":2242},"10.1007\u002FBF00375178",{"doi":2241},{"id":24,"text":2244,"url":24,"identifiers":2245},"Xizang Team of Scientific Exploration, 1974, Report of Scientific Exploration in Qomolangma (1966–1968): Geology",{},{"id":2247,"createTime":2248,"updateTime":2248,"relativeEntities":2249,"slug":2250,"properties":2251,"entityType":114,"verifyStatus":115,"verifyTime":2248,"verifyNote":116,"languages":2262,"translateLanguages":24,"viewCount":25,"primaryUrl":2263,"fullTextUrl":24,"authors":2264,"publicationType":228,"publisherRelationship":2360,"citationCount":1709,"citationInfo":2409,"publishDate":2412,"publishYear":2410,"citationAnalyzeStatus":23,"lastCitationAnalyze":24,"indexDatabases":2413,"openAccess":24,"references":2414,"isForceReanalyzing":576},"8420cc86-51ee-4ea3-9dd7-e45aa645303d","2024-12-17T08:16:41.610+00:00",[],"Metamorphic-evolution-and-SIMS-U-Pb-geochronology-of-orthopyroxene-bearing-high-i-P-i-semipelitic-granulite-in-the-Fuping-area-middle-Trans-North-China-Orogen",{"openalex":2252,"mag":2254,"abstract":2256,"title":2258,"doi":2260},{"VOID":2253},"W3096050769",{"VOID":2255},"3096050769",{"EN":2257},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>The Fuping area lies in the middle part of the Trans‐North China Orogen, which is a critical region for understanding the metamorphic–tectonic evolution of this orogenic belt in the Precambrian. The newly discovered orthopyroxene‐bearing semipelitic granulite in this area is a coherent stratigraphic unit, among which three generations of metamorphic mineral assemblages (peak, post‐peak and cooling retrograde) have been identified based on petrographic observation and mineral chemical analysis. The peak metamorphic mineral assemblage mainly consists of porphyroblastic garnet plus matrix minerals including biotite, plagioclase, orthopyroxene, quartz as well as accessory minerals including pyrite, monazite, zircon and apatite. Geothermobarometry calculations and phase equilibria modelling confirm that the representative samples record different\u003Cjats:italic>P–T\u003C\u002Fjats:italic>conditions and metamorphic stages due to retrogressive metamorphism, with the highest\u003Cjats:italic>P–T\u003C\u002Fjats:italic>conditions reaching high‐\u003Cjats:italic>P\u003C\u002Fjats:italic>granulite facies. The retrieved clockwise metamorphic\u003Cjats:italic>P\u003C\u002Fjats:italic>–\u003Cjats:italic>T\u003C\u002Fjats:italic>paths pass from 12.5 to 13.5 kbar\u002F855–880℃ (peak stage) through 8.5–11 kbar\u002F850–886℃ (post‐peak stage) and to a speculative cooling phase (retrograde stage), reflecting near isothermal decompression (ITD) followed by near isobaric cooling (IBC). This\u003Cjats:italic>P–T\u003C\u002Fjats:italic>path is interpreted to reflect a subduction and\u002For collision event followed by a rapid exhumation. Secondary ion mass spectrometry (SIMS) U–Pb dating on metamorphic monazite and zircon yielded metamorphic ages ranging from 1,825 to 1,815 Ma, possibly constraining a retrograde metamorphic age. 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A. Wilde P. A. Cawood K. Y. Wang X. L. Qian Z. D. You H. C. Halls The relationship and timing of granitoid evolution with respect to felsic volcanism in the Wutai Complex North China Craton 75 88",{},{"id":24,"text":2704,"url":24,"identifiers":2705},"10.1016\u002Fj.jseaes.2003.11.006",{"doi":2704},{"id":24,"text":2707,"url":24,"identifiers":2708},"10.1144\u002FGSL.SP.2004.226.01.02",{"doi":2707},{"id":24,"text":2710,"url":24,"identifiers":2711},"10.1007\u002FBF02901747",{"doi":2710},{"id":24,"text":2713,"url":24,"identifiers":2714},"Williams I. 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H., 1995, A geochronological study of the Longquanguan ductile shear zone, Quaternary Sciences, 4, 332",{},{"id":24,"text":2737,"url":24,"identifiers":2738},"10.2475\u002F09.2015.03",{"doi":2737},{"id":24,"text":2740,"url":24,"identifiers":2741},"10.1016\u002Fj.precamres.2013.12.025",{"doi":2740},{"id":24,"text":2743,"url":24,"identifiers":2744},"Zhai M. G., 1995, Discovery of retrograded eclogites in North China Craton and its implications, Chinese Science Bulletin, 40, 1590",{},{"id":24,"text":2746,"url":24,"identifiers":2747},"Zhai M. G., 1992, Discovery and preliminary study of the Archean high‐pressure granulites in the North China, Science in China, 12, 1325",{},{"id":24,"text":2749,"url":24,"identifiers":2750},"10.1016\u002Fj.precamres.2016.04.009",{"doi":2749},{"id":24,"text":2752,"url":24,"identifiers":2753},"Zhang J., 2006, Structures of syn‐deformational granites in the Longquanguan shear zone and their monazite electronic microprobe dating, Acta Geologica Sinica‐English Edition, 80, 864, 10.1111\u002Fj.1755-6724.2006.tb00308.x",{"doi":2754},"10.1111\u002Fj.1755-6724.2006.tb00308.x",{"id":24,"text":2756,"url":24,"identifiers":2757},"10.1016\u002Fj.lithos.2020.105434",{"doi":2756},{"id":24,"text":2759,"url":24,"identifiers":2760},"10.1016\u002Fj.precamres.2018.04.022",{"doi":2759},{"id":24,"text":2762,"url":24,"identifiers":2763},"10.1016\u002FS0301-9268(98)00090-4",{"doi":2762},{"id":24,"text":2765,"url":24,"identifiers":2766},"10.1017\u002FS001675689900254X",{"doi":2765},{"id":24,"text":2768,"url":24,"identifiers":2769},"10.1093\u002Fpetrology\u002F42.6.1141",{"doi":2768},{"id":24,"text":2771,"url":24,"identifiers":2772},"10.1016\u002FS0301-9268(00)00154-6",{"doi":2771},{"id":24,"text":2774,"url":24,"identifiers":2775},"10.1016\u002Fj.precamres.2004.10.002",{"doi":2774},{"id":24,"text":2777,"url":24,"identifiers":2778},"10.1080\u002F00206819809465233",{"doi":2777},{"id":24,"text":2780,"url":24,"identifiers":2781},"10.1046\u002Fj.1525-1314.2000.00264.x",{"doi":2780},{"id":24,"text":2783,"url":24,"identifiers":2784},"10.2475\u002Fajs.302.3.191",{"doi":2783},{"id":24,"text":2786,"url":24,"identifiers":2787},"10.2475\u002F10.2010.10",{"doi":2786},{"id":24,"text":2789,"url":24,"identifiers":2790},"10.1016\u002Fj.gr.2012.08.016",{"doi":2789},{"id":24,"text":2792,"url":24,"identifiers":2793},"10.1016\u002Fj.precamres.2017.07.010",{"doi":2792},{"id":2795,"createTime":2796,"updateTime":2796,"relativeEntities":2797,"slug":2798,"properties":2799,"entityType":114,"verifyStatus":115,"verifyTime":2796,"verifyNote":116,"languages":2810,"translateLanguages":24,"viewCount":25,"primaryUrl":2811,"fullTextUrl":24,"authors":2812,"publicationType":228,"publisherRelationship":2857,"citationCount":2906,"citationInfo":2907,"publishDate":2911,"publishYear":2908,"citationAnalyzeStatus":23,"lastCitationAnalyze":24,"indexDatabases":2912,"openAccess":24,"references":2913,"isForceReanalyzing":576},"a4296ac6-82ec-461b-9716-c05b37d83fef","2024-12-17T08:16:40.141+00:00",[],"-i-P-T-t-i-evolution-of-garnet-amphibolites-in-the-Wutai-Hengshan-area-North-China-Craton-insights-from-phase-equilibria-and-geochronology",{"openalex":2800,"mag":2802,"abstract":2804,"title":2806,"doi":2808},{"VOID":2801},"W2253875564",{"VOID":2803},"2253875564",{"EN":2805},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>Garnet amphibolites can provide valuable insights into geological processes of orogenic belts, but their metamorphic evolution is still poorly constrained. Garnet amphibolites from the Wutai–Hengshan area of the North China Craton mainly consist of garnet, hornblende, plagioclase, quartz, rutile and ilmenite, with or without titanite and epidote. Four samples selected in a south–north profile were studied by the pseudosection approach in order to elucidate the characteristics of their metamorphic evolution, and to better reveal the northwards prograde change in \u003Cjats:italic>P–T\u003C\u002Fjats:italic> conditions as established previously. For the sample from the lower Wutai Subgroup, garnet exhibits obvious two‐substage growth zoning characteristic of pyrope (\u003Cjats:italic>X\u003C\u002Fjats:italic>\u003Cjats:sub>py\u003C\u002Fjats:sub>) increasing but grossular (\u003Cjats:italic>X\u003C\u002Fjats:italic>\u003Cjats:sub>gr\u003C\u002Fjats:sub>) decreasing outwards in the core, and both \u003Cjats:italic>X\u003C\u002Fjats:italic>\u003Cjats:sub>py\u003C\u002Fjats:sub> and \u003Cjats:italic>X\u003C\u002Fjats:italic>\u003Cjats:sub>gr\u003C\u002Fjats:sub> increasing outwards in the rim. Phase modelling using \u003Cjats:sc>thermocalc\u003C\u002Fjats:sc> suggests that the garnet cores were formed by chlorite breakdown over 7–9 kbar at 530–600 °C, and rims grew from hornblende and epidote breakdown over 9.5–11.5 kbar at 600–670 °C. The isopleths of the minimum An in plagioclase and maximum \u003Cjats:italic>X\u003C\u002Fjats:italic>\u003Cjats:sub>py\u003C\u002Fjats:sub> in garnet were used to constrain the peak \u003Cjats:italic>P–T\u003C\u002Fjats:italic> conditions of ~11.5 kbar\u002F670 °C. The modelled peak assemblage garnet + hornblende + epidote+ plagioclase + rutile + quartz matches well the observed one. Plagioclase–hornblende coronae around garnet indicate post‐peak decompression and fluid ingress. For the samples from the south Hengshan Complex, the garnet zoning weaken gradually, reflecting modifications during decompression of the rocks. Using the same approach, the rocks are inferred to have suprasolidus peak conditions, increasing northwards from 11.5 kbar\u002F745 °C, 12.5 kbar\u002F780 °C to 13 kbar\u002F800 °C. Their modelled peak assemblages involve diopside, garnet, hornblende, plagioclase, rutile and quartz, yet diopside is not observed petrographically. The post‐peak decompression is characterized by diopside + garnet + quartz + melt = hornblende + plagioclase, causing the diopside consumption and garnet compositions to be largely modified. Thus, the pesudosection approach is expected to provide better pressure results than conventional thermobarometry, because the later approach cannot be applied with confidence to rocks with multi‐generation assemblages. U–Pb dating of zircon in the Wutai sample records a protolith age of \u003Cjats:italic>c\u003C\u002Fjats:italic>. 2.50 Ga, and a metamorphic age of \u003Cjats:italic>c\u003C\u002Fjats:italic>. 1.95 Ga, while zircon in the Hengshan samples records metamorphic ages of \u003Cjats:italic>c\u003C\u002Fjats:italic>. 1.92 Ga. The \u003Cjats:italic>c\u003C\u002Fjats:italic>. 1.95 Ga is interpreted to represent the pre‐peak or peak metamorphic stages, and the ages of \u003Cjats:italic>c\u003C\u002Fjats:italic>. 1.92 Ga are assigned to represent the cooling stages. All rocks in the Wutai–Hengshan area share similar clockwise \u003Cjats:italic>P–T\u003C\u002Fjats:italic> morphologies. They may represent metamorphic products at different crustal depths in one orogenic event, which included a main thickening stage at \u003Cjats:italic>c\u003C\u002Fjats:italic>. 1.95 Ga followed by a prolonged uplift and cooling after 1.92 Ga.\u003C\u002Fjats:p>",{"EN":2807},"\u003Ci>P–T–t\u003C\u002Fi> evolution of garnet amphibolites in the Wutai–Hengshan area, North China Craton: insights from phase equilibria and 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the age and stratigraphic subdivision of the Hutuo Group in the Wutai Mountains area, North China Craton: evidence from geology and zircon U\u002FPb geochronology, Acta Petrologica Sinica, 27, 1037",{},{"id":24,"text":2952,"url":24,"identifiers":2953},"10.1016\u002Fj.jseaes.2012.11.040",{"doi":2952},{"id":24,"text":2472,"url":24,"identifiers":2955},{"doi":2472},{"id":24,"text":2957,"url":24,"identifiers":2958},"Faure M., 2007, Polyorogenic evolution of the Paleoproterozoic Trans‐North China Belt, new insights from the Lüliangshan–Hengshan–Wutaishan and Fuping massifs, Episodes, 30, 1, 10.18814\u002Fepiiugs\u002F2007\u002Fv30i2\u002F004",{"doi":2959},"10.18814\u002Fepiiugs\u002F2007\u002Fv30i2\u002F004",{"id":24,"text":2961,"url":24,"identifiers":2962},"10.1111\u002Fjmg.12108",{"doi":2961},{"id":24,"text":2964,"url":24,"identifiers":2965},"10.1111\u002Fj.1525-1314.1984.tb00282.x",{"doi":2964},{"id":24,"text":2483,"url":24,"identifiers":2967},{"doi":2483},{"id":24,"text":2969,"url":24,"identifiers":2970},"Guo J.H., 1999, Metamorphism, PT paths and tectonic significance of garnet amphibolite and granulite from Hengshan, North China Craton, Scientia Geologica Sinica, 34, 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PhD Thesis.Peking University Beijing(in Chinese with English abstract).",{},{"id":24,"text":3140,"url":24,"identifiers":3141},"10.1016\u002Fj.jsg.2007.02.013",{"doi":3140},{"id":24,"text":3143,"url":24,"identifiers":3144},"10.1007\u002Fs11434-013-5993-x",{"doi":3143},{"id":24,"text":2762,"url":24,"identifiers":3146},{"doi":2762},{"id":24,"text":2768,"url":24,"identifiers":3148},{"doi":2768},{"id":24,"text":2783,"url":24,"identifiers":3150},{"doi":2783},{"id":24,"text":2774,"url":24,"identifiers":3152},{"doi":2774},{"id":24,"text":3154,"url":24,"identifiers":3155},"10.1017\u002FS0016756807003561",{"doi":3154},{"id":24,"text":3157,"url":24,"identifiers":3158},"Zhao R.F., 2011, 2.1 Ga crustal remelting event in Hengshan Complex: evidence from zircon U‐Pb dating and Hf–Nd isotopic study on potassic granites, Acta Petrologica Sinca, 27, 1607",{},{"id":24,"text":3160,"url":24,"identifiers":3161},"10.1016\u002Fj.precamres.2012.09.016",{"doi":3160},{"id":3163,"createTime":3164,"updateTime":3164,"relativeEntities":3165,"slug":3166,"properties":3167,"entityType":114,"verifyStatus":115,"verifyTime":3164,"verifyNote":116,"languages":3177,"translateLanguages":24,"viewCount":25,"primaryUrl":3178,"fullTextUrl":24,"authors":3179,"publicationType":228,"publisherRelationship":3304,"citationCount":3353,"citationInfo":3354,"publishDate":3358,"publishYear":3355,"citationAnalyzeStatus":23,"lastCitationAnalyze":24,"indexDatabases":3359,"openAccess":24,"references":3360,"isForceReanalyzing":576},"abecfb02-6f0c-4a11-946c-15b24cd1a4ad","2024-12-17T08:16:18.608+00:00",[],"Petrology-phase-equilibria-modelling-and-zircon-U-Pb-geochronology-of-Paleoproterozoic-mafic-granulites-from-the-Fuping-Complex-North-China-Craton",{"openalex":3168,"mag":3170,"abstract":3172,"title":3174,"doi":3176},{"VOID":3169},"W2569644591",{"VOID":3171},"2569644591",{"EN":3173},"\u003Cjats:title>Abstract\u003C\u002Fjats:title>\u003Cjats:p>The Fuping Complex is one of the important basement terranes within the central segment of the Trans‐North China Orogen (TNCO) where mafic granulites are exposed as boudins within tonalite–trondhjemite–granodiorite (\u003Cjats:styled-content style=\"fixed-case\">TTG\u003C\u002Fjats:styled-content>) gneisses. Garnet in these granulites shows compositional zoning with homogeneous cores formed in the peak metamorphic stage, surrounded by thin rims with an increase in almandine and decrease in grossular contents suggesting retrograde decompression and cooling. Petrological and phase equilibria studies including pseudosection calculation using \u003Cjats:sc>thermocalc\u003C\u002Fjats:sc> define a clockwise \u003Cjats:italic>P–T\u003C\u002Fjats:italic> path. The peak mineral assemblages comprise garnet+clinopyroxene+amphibole+quartz+plagioclase+K‐feldspar+ilmenite±orthopyroxene±magnetite, with metamorphic \u003Cjats:italic>P–T\u003C\u002Fjats:italic> conditions estimated at 8.2–9.2 kbar, 870–882 °C (15\u003Cjats:styled-content style=\"fixed-case\">FP\u003C\u002Fjats:styled-content>‐02), 9.6–11.3 kbar, 855–870 °C (15\u003Cjats:styled-content style=\"fixed-case\">FP\u003C\u002Fjats:styled-content>‐03) and 9.7–10.5 kbar, 880–900 °C (15\u003Cjats:styled-content style=\"fixed-case\">FP\u003C\u002Fjats:styled-content>‐06) respectively. The pseudosections for the subsequent retrograde stages based on relatively higher H\u003Cjats:sub>2\u003C\u002Fjats:sub>O contents from \u003Cjats:italic>P\u002FT–M\u003C\u002Fjats:italic>(H\u003Cjats:sub>2\u003C\u002Fjats:sub>O) diagrams define the retrograde \u003Cjats:italic>P–T\u003C\u002Fjats:italic> conditions of <6.1 kbar, <795 °C (15\u003Cjats:styled-content style=\"fixed-case\">FP\u003C\u002Fjats:styled-content>‐02), 5.6–5.8 kbar, <795 °C (15\u003Cjats:styled-content style=\"fixed-case\">FP\u003C\u002Fjats:styled-content>‐03), and <9 kbar, <865 °C (15\u003Cjats:styled-content style=\"fixed-case\">FP\u003C\u002Fjats:styled-content>‐06) respectively. Data from \u003Cjats:styled-content style=\"fixed-case\">LA\u003C\u002Fjats:styled-content>‐\u003Cjats:styled-content style=\"fixed-case\">ICP\u003C\u002Fjats:styled-content>‐\u003Cjats:styled-content style=\"fixed-case\">MS\u003C\u002Fjats:styled-content> zircon U–Pb dating show that the mafic dyke protoliths of the granulite were emplaced at \u003Cjats:italic>c\u003C\u002Fjats:italic>. 2327 Ma. The metamorphic zircon shows two groups of ages at 1.96–1.90 Ga (peak at 1.93–1.92 Ga) and 1.89–1.80 Ga (peak at 1.86–1.83 Ga), consistent with the two metamorphic events widely reported from different segments of the TNCO. The 1.93–1.92 Ga ages are considered to date the peak granulite facies metamorphism, whereas the 1.86–1.83 Ga ages are correlated with the retrograde event. Thus, the collisional assembly of the major crustal blocks in the North China Craton (NCC) might have occurred during 1.93–1.90 Ga, marking the final cratonization of the NCC.\u003C\u002Fjats:p>",{"EN":3175},"Petrology, phase equilibria modelling and zircon U–Pb geochronology of Paleoproterozoic mafic granulites from the Fuping Complex, North China Craton",{"VOID":2659},[118],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1111\u002Fjmg.12243",[3180,3207,3232,3257,3272,3289],{"id":3181,"sortIndex":25,"researcher":24,"roles":3182,"affiliations":3183,"properties":3200,"displayName":3204,"givenName":24,"familyName":24},"c911f2ca-117d-45df-becd-0e1d897e1efb",[],[3184,3192],{"id":3185,"sortIndex":25,"affiliation":3186,"properties":24},"62d071e5-1016-4eef-9ffe-27f434a0dcd1",{"id":3185,"createTime":24,"updateTime":24,"relativeEntities":3187,"slug":24,"properties":3188,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":3191,"statistic":24},[],{"title":3189},{"VI":3190},"Graduate School of Life and Environmental Sciences, University of Tsukuba, Ibaraki 305-8572, Japan",[],{"id":3193,"sortIndex":135,"affiliation":3194,"properties":24},"b543dd1e-c193-4bc6-85cd-27026503ab92",{"id":3193,"createTime":24,"updateTime":24,"relativeEntities":3195,"slug":24,"properties":3196,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":3199,"statistic":24},[],{"title":3197},{"VI":3198},"School of Earth Sciences and Resources, China University of Geosciences (Beijing), 29 Xueyuan Road, Beijing 100083, China",[],{"orcid":3201,"title":3203,"openalex":3205},{"VOID":3202},"https:\u002F\u002Forcid.org\u002F0000-0001-8311-2507",{"EN":3204},"Li Tang",{"VOID":3206},"A5067142616",{"id":3208,"sortIndex":135,"researcher":24,"roles":3209,"affiliations":3210,"properties":3225,"displayName":3229,"givenName":24,"familyName":24},"ad0de7ed-2067-400a-90ad-1a4dddf4b971",[],[3211,3219],{"id":3212,"sortIndex":25,"affiliation":3213,"properties":24},"2878af21-999a-49a6-ad05-e01d3733258a",{"id":3212,"createTime":24,"updateTime":24,"relativeEntities":3214,"slug":24,"properties":3215,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":3218,"statistic":24},[],{"title":3216},{"VI":3217},"Centre for Tectonics, Exploration and Research, University of Adelaide, Adelaide, SA 5005, Australia",[],{"id":3193,"sortIndex":135,"affiliation":3220,"properties":24},{"id":3193,"createTime":24,"updateTime":24,"relativeEntities":3221,"slug":24,"properties":3222,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":3224,"statistic":24},[],{"title":3223},{"VI":3198},[],{"orcid":3226,"title":3228,"openalex":3230},{"VOID":3227},"https:\u002F\u002Forcid.org\u002F0000-0002-1073-8477",{"EN":3229},"M. 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basic granulites are widely distributed as enclaves and sheet‐like blocks in the Huaian TTG gneiss terrane in the Sanggan area of the Central Zone of the North China craton. Four stages of the metamorphic history have been recognised in mineral assemblages based on inclusion, exsolution and reaction textures integrated with garnet zonation patterns as revealed by compositional maps and compositional profiles. The \u003Cjats:italic>P–T\u003C\u002Fjats:italic> conditions for each metamorphic stage were obtained using thermodynamically and experimentally calibrated geothermobarometers. The low‐Ca core of growth‐zoned garnet, along with inclusion minerals, defines a prograde assemblage (M1) of garnet + clinopyroxene + plagioclase + quartz, yielding 700 °C and 10 kbar. The peak of metamorphism at about 750–870 °C and 11–14.5 kbar (M2) is defined by high‐Ca domains in garnet interiors and inclusion minerals of clinopyroxene, plagioclase and quartz. Kelyphites or coronas of orthopyroxene + plagioclase ± magnetite around garnet porphyroblasts indicate garnet breakdown reactions (M3) at conditions around 770–830 °C and 8.5–10.5 kbar. Garnet exsolution lamellae in clinopyroxene and kelyphites of amphibole + plagioclase around garnet formed during the cooling process at about 500–650 °C and 5.5–8 kbar (M4). These results help define a sequential \u003Cjats:italic>P–T\u003C\u002Fjats:italic> path containing prograde, near‐isothermal decompression (ITD) and near‐isobaric cooling (IBC) stages.\u003C\u002Fjats:p>\u003Cjats:p>The clockwise hybrid ITD and IBC \u003Cjats:italic>P–T\u003C\u002Fjats:italic> paths of the H\u003Cjats:italic>P\u003C\u002Fjats:italic> granulites in the Sanggan area imply a model of thickening followed by extension in a collisional environment. Furthermore, the relatively high‐pressures (6–14.5 kbar) of the four metamorphic stages and the geometry of the \u003Cjats:italic>P–T\u003C\u002Fjats:italic> paths suggest that the H\u003Cjats:italic>P\u003C\u002Fjats:italic> granulites, together with their host Huaian TTG gneisses, represent the lower plate in a crust thickened during collision. The corresponding upper‐plate might be the tectonically overlying Khondalite series, which was subjected to medium‐ to low‐pressure (M\u003Cjats:italic>P\u003C\u002Fjats:italic>\u002FL\u003Cjats:italic>P\u003C\u002Fjats:italic>: 7–4 kbar) granulite facies metamorphism with a clockwise \u003Cjats:italic>P–T\u003C\u002Fjats:italic> path including an ITD segment. Both the H\u003Cjats:italic>P\u003C\u002Fjats:italic> and the M\u003Cjats:italic>P\u003C\u002Fjats:italic>\u002FL\u003Cjats:italic>P\u003C\u002Fjats:italic> granulite facies events occurred contemporaneously at \u003Cjats:italic>c\u003C\u002Fjats:italic>. 1.90–1.85 Ga in a collisional environment created by the assembly process of the North China craton.\u003C\u002Fjats:p>",{"EN":3759},"High‐pressure granulites in the Sanggan area, North China craton: metamorphic evolution, \u003Ci>P–T\u003C\u002Fi> paths and geotectonic significance",{"VOID":2486},[118],"https:\u002F\u002Fonlinelibrary.wiley.com\u002Fdoi\u002F10.1046\u002Fj.1525-1314.2002.00401.x",[3764,3781,3800],{"id":3765,"sortIndex":25,"researcher":24,"roles":3766,"affiliations":3767,"properties":3776,"displayName":3778,"givenName":24,"familyName":24},"59539b41-7972-4572-9cdf-2f9f32df84f2",[],[3768],{"id":3769,"sortIndex":25,"affiliation":3770,"properties":24},"700b67ff-24d4-4d58-9133-326676a44f81",{"id":3769,"createTime":24,"updateTime":24,"relativeEntities":3771,"slug":24,"properties":3772,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":3775,"statistic":24},[],{"title":3773},{"EN":3774},"Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing, 100029, China (jhguo@mail.igcas.ac.cn)",[],{"title":3777,"openalex":3779},{"EN":3778},"Jinghui Guo",{"VOID":3780},"A5101921374",{"id":3782,"sortIndex":135,"researcher":24,"roles":3783,"affiliations":3784,"properties":3793,"displayName":3797,"givenName":24,"familyName":24},"6cd471cb-7a68-4acc-a7ff-f6a0175cfbf9",[],[3785],{"id":3786,"sortIndex":25,"affiliation":3787,"properties":24},"e4811989-1e15-4691-9366-46ce49b182ad",{"id":3786,"createTime":24,"updateTime":24,"relativeEntities":3788,"slug":24,"properties":3789,"entityType":24,"verifyStatus":24,"verifyTime":24,"verifyNote":24,"languages":24,"translateLanguages":24,"viewCount":24,"url":24,"parentIds":3792,"statistic":24},[],{"title":3790},{"EN":3791},"Institut für Geowissenschaften, Universita¨t Potsdam, Postfach 601553, D‐14415 Potsdam, Germany",[],{"orcid":3794,"title":3796,"openalex":3798},{"VOID":3795},"https:\u002F\u002Forcid.org\u002F0000-0003-0235-9116",{"EN":3797},"Patrick J. 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M., 1991, Al zoning in pyroxene and plagioclase: Window on late prograde to early retrograde P‐T paths in granulite terranes, American Mineralogist, 76, 1328",{},{"id":24,"text":2428,"url":24,"identifiers":3879},{"doi":2428},{"id":24,"text":2431,"url":24,"identifiers":3881},{"doi":2431},{"id":24,"text":2434,"url":24,"identifiers":3883},{"doi":2434},{"id":24,"text":3885,"url":24,"identifiers":3886},"10.1093\u002Fpetrology\u002F34.3.427",{"doi":3885},{"id":24,"text":3888,"url":24,"identifiers":3889},"10.1007\u002F978-94-010-9263-0_4",{"doi":3888},{"id":24,"text":3891,"url":24,"identifiers":3892},"10.1007\u002Fs005310000123",{"doi":3891},{"id":24,"text":3894,"url":24,"identifiers":3895},"10.1046\u002Fj.1525-1314.2000.00273.x",{"doi":3894},{"id":24,"text":3897,"url":24,"identifiers":3898},"10.1007\u002FBF02875243",{"doi":3897},{"id":24,"text":3900,"url":24,"identifiers":3901},"10.1016\u002FS0191-8141(97)00044-8",{"doi":3900},{"id":24,"text":3903,"url":24,"identifiers":3904},"Eckert J. 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S., 1997, Chronological framework of the early Precambrian important events of the north‐western Hebei granulite terrain, Acta Geologie Sinica, 71, 316",{},{"id":24,"text":2964,"url":24,"identifiers":3922},{"doi":2964},{"id":24,"text":3924,"url":24,"identifiers":3925},"10.1016\u002FS0016-7037(67)80031-0",{"doi":3924},{"id":24,"text":3927,"url":24,"identifiers":3928},"Guo J. H., 1999, Pb isotopic composition of feldspar and U‐Pb age of zircon from early Proterozoic granite in Sanggan area, North China craton: Metamorphism, crustal melting and tectono‐thermal event, Acta Petrologica Sinica, 15, 199",{},{"id":24,"text":3930,"url":24,"identifiers":3931},"Guo J. H., 2001, 40Ar‐39Ar age spectra of garnet porphyroblasts: Implications for themetamorphic age of high‐pressure granulites in the North China craton, Acta Petrologia Sinica, 17, 436",{},{"id":24,"text":3933,"url":24,"identifiers":3934},"10.1007\u002FBF03187002",{"doi":3933},{"id":24,"text":3936,"url":24,"identifiers":3937},"Guo J. H., 1994, Geological Evolution of the Granulite Terrane in North Part of the North China Craton, 130",{},{"id":24,"text":3939,"url":24,"identifiers":3940},"Guo J. H., 1998, Contrasing metamorphic P‐T paths of Archaean high‐pressure granulites from the north China craton: metamorphism and tectonic significance, Acta Petrologica Sinica, 14, 430",{},{"id":24,"text":3942,"url":24,"identifiers":3943},"Guo J. H., 1993, Early Precambrian Manjinggou high‐pressure granulite melange belt on the south edge of the Huaian complex, North China craton: geological features, petrology and isotopic geochronology, Acta Petrologica Sinica, 9, 329",{},{"id":24,"text":3945,"url":24,"identifiers":3946},"10.1007\u002FBF01187140",{"doi":3945},{"id":24,"text":2495,"url":24,"identifiers":3948},{"doi":2495},{"id":24,"text":3950,"url":24,"identifiers":3951},"Holland T. J. B., 1980, The reaction albite = jadeite + quartz determined experimentally in the range 600–1200 °C, American Mineralogist, 65, 129",{},{"id":24,"text":3953,"url":24,"identifiers":3954},"10.1007\u002Fs004100050544",{"doi":3953},{"id":24,"text":3956,"url":24,"identifiers":3957},"Kohn M. J., 1990, Two new geobarometers for garnet amphibolites, with applications to southeastern Vermont, American Mineralogist, 75, 89",{},{"id":24,"text":818,"url":24,"identifiers":3959},{},{"id":24,"text":3961,"url":24,"identifiers":3962},"10.1007\u002FBF00399364",{"doi":3961},{"id":24,"text":3964,"url":24,"identifiers":3965},"10.1046\u002Fj.1525-1314.1996.03710.x",{"doi":3964},{"id":24,"text":3967,"url":24,"identifiers":3968},"Li J. H., 1998, The geological occurrence, regional tectonic setting and exhumation of late Archaean high‐pressure granulite with the high‐grade metamorphic terranes, north to central portion of North China craton, Acta Petrologica Sinica, 14, 176",{},{"id":24,"text":3970,"url":24,"identifiers":3971},"Liu D. Y., 1997, Late Archean crustal accretion and reworking in northwest Hebei province: geochronological evidence, Acta Geoscientia Sinica, 18, 226",{},{"id":24,"text":3973,"url":24,"identifiers":3974},"Liu S. W., 1996, Metamorphic evolution of two types of garnet‐granulites in Northwestern Hebei province and analyses by Gibbs method, Acta Petrologica Sinica, 12, 261",{},{"id":24,"text":2577,"url":24,"identifiers":3976},{"doi":2577},{"id":24,"text":3978,"url":24,"identifiers":3979},"10.1111\u002Fj.1525-1314.1993.tb00166.x",{"doi":3978},{"id":24,"text":3981,"url":24,"identifiers":3982},"Mao D. B., 1999, The isotope ages and their geological implications of high‐pressure basic granulites in north region to Chengde, Hebei province, China, Acta Petrologica Sinica, 15, 524",{},{"id":24,"text":3527,"url":24,"identifiers":3984},{"doi":3527},{"id":24,"text":3986,"url":24,"identifiers":3987},"10.1016\u002F0024-4937(86)90021-6",{"doi":3986},{"id":24,"text":3989,"url":24,"identifiers":3990},"Newton R. C., 1982, Thermodynamic calibration of geobarometers based on the assemblages garnet‐plagioclase‐orthopyroxene (clinopyroxene)‐quartz, American Mineralogist, 67, 203",{},{"id":24,"text":3992,"url":24,"identifiers":3993},"10.1016\u002FS0024-4937(97)82008-7",{"doi":3992},{"id":24,"text":3995,"url":24,"identifiers":3996},"O'Brien P. J., 1997, Petrological and isotopic studies on Palaeozoic high pressure granulites, Góry Sowie Mts., Polish Sudetes, Journal of Petrology, 38, 433, 10.1093\u002Fpetroj\u002F38.4.433",{"doi":3997},"10.1093\u002Fpetroj\u002F38.4.433",{"id":24,"text":3542,"url":24,"identifiers":3999},{"doi":3542},{"id":24,"text":4001,"url":24,"identifiers":4002},"10.1111\u002Fj.1525-1314.1985.tb00319.x",{"doi":4001},{"id":24,"text":1520,"url":24,"identifiers":4004},{"doi":1520},{"id":24,"text":4006,"url":24,"identifiers":4007},"Salje E., 1986, Heat capacities and entropies of andalusite and sillimanite. The influence of fibrolitisation on the phase diagram of the Al2SiO5 polymorphs, American Mineralogist, 71, 1366",{},{"id":24,"text":4009,"url":24,"identifiers":4010},"10.1016\u002F0012-821X(86)90048-8",{"doi":4009},{"id":24,"text":4012,"url":24,"identifiers":4013},"Sonder L. 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