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| 1 | Charnockites and charnockites显示文摘1.Introduction The continental crust,covering nearly a third of the Earth's surface,is dominantly made up of granites and granodiorites(Rudnick and Gao, 2003).Although the vast majority of these granitoids are amphiboleand /or biotite-bearing,orthopyroxene-bearing granitoids form a minor but important component of the lower continental crust in many high-grade terrains(e.g.,Bohlender et al.,1992;Kilpatrick and Ellis,1992;Sheraton et al.,1992;Berger et al.,1995;Zhou et al., 1995;Peucat et al.,1996;Duchesne and Wilmart,1997;Hughes et al.,1997;Prame.1997;Frost et al.,2000;Janasi,2002; | H.M.Rajesh M.Santosh | 2012 | Geoscience Frontiers2012，3，6： | 4 |
| 2 | Deciphering fluid inclusions in high-grade rocks显示文摘The study of fluid inclusions in high-grade rocks is especially challenging as the host minerals have been normally subjected to deformation,recrystallization and fluid-rock interaction so that primary inclusions,formed at the peak of metamorphism are rare.The larger part of the fluid inclusions found in metamorphic minerals is typically modified during uplift.These late processes may strongly disguise the characteristics of the 'original' peak metamorphic fluid.A detailed miciostructural analysis of the host minerals,notably quartz,is therefore indispensable for a proper interpretation of fluid inclusions.Cathodoluminescence(CL) techniques combined with trace element analysis of quartz(EPMA.LAICPMS) have shown to be very helpful in deciphering the rock-fluid evolution.Whereas high-grade metamorphic quartz may have relatively high contents of trace elements like Ti and Al,lowtemperature re-equilibrated quartz typically shows reduced trace element concentrations.The resulting microstructures in Cl.can be basically distinguished in diffusion patterns(along microfractures and grain boundaries).and secondary quartz formed by dissolution-reprecipilation.Most of these textures are formed during retrograde fluid-controlled processes between ca.220 and 500 C,i.e.the range of semi-brittle deformation(greenschist-lacies) and can be correlated with the fluid inclusions.In this way modified and re-trapped fluids can be identified.even when there are no optical features observed under the microscope. | Alfons van den Kerkhof Andreas Kronz Klaus Simon | 2014 | Geoscience Frontiers2014，5，5： | 3 |
| 3 | Norite and charnockites from the Venda Nova Pluton,SE Brazil:Intensive parameters and some petrogenetic constraints显示文摘Venda 新星 Pluton (VNP ) 是在 Neoproterozoic Ara 的南部的部分的 zoned 戒指结构 emplaced ? uai 带,在 Esp ? 瀠牥污浵湩畯 ?? 洠瑥污浵湩畯 ??? 映牥潲湡吗?? | Julio Cezar Mendes Cristina M.P.De Campos | 2012 | Geoscience Frontiers2012，3，6： | 1 |
| 4 | 华南云开高州紫苏花岗岩及其两类石榴石的成因:岩石学和锆石U-Pb年代学证据显示文摘云开地块早古生代的构造背景至今仍存有争论。对云炉-龙修一带出露的含石榴石紫苏花岗岩进行研究可为该区构造-变质演化提供重要制约。详细的岩相学研究表明紫苏花岗岩中存在两种成因的石榴石(石榴石Ⅰ和石榴石Ⅱ),并识别出该岩石保留了三阶段演化的矿物组合(M1-M3)。峰期前矿物组合(M1)由紫苏辉石变斑晶中的包裹体矿物石榴石+黑云母+斜长石+钛铁矿+石英组成。峰期变质-深熔矿物组合(M2)由基质中平衡共生的斑晶矿物石榴石Ⅰ+紫苏辉石+黑云母+石英+斜长石+钛铁矿构成。退变质矿物组合(M3)以紫苏辉石和黑云母以及钛铁矿边部降温生成石榴石Ⅱ+石英冠状体('红眼圈')和黑云母+石英后成合晶为特征。传统地质温压计、平均温压法及在NCKFMASHTO模式体系下的相平衡模拟结果表明,紫苏花岗岩峰期前矿物组合形成条件为720℃/7.0kbar(M1),峰期变质-深熔结晶条件为835~810℃/6.5~5.8kbar(M2),退变质条件为740℃/5.6kbar(M3)。岩相观察和P-T计算结果表明紫苏花岗岩的形成可能反映了一条顺时针的P-T轨迹,且以峰期前略微减压并伴随明显的升温和峰期后具有近等压冷却(IBC)过程为特征。LA-ICP-MS锆石U-Pb年代学结果显示锆石核部加权平均年龄为~431Ma,锆石边部加权平均年龄为~243Ma。我们认为峰期深熔作用和岩浆结晶石榴石Ⅰ的形成可能发生于早古生代(加里东期),而晚期退变质作用和变质重结晶石榴石Ⅱ的形成可能发生在早中生代(印支期)。本研究也表明云开地区含石榴石紫苏花岗岩的形成与早古生代扬子和华夏陆块碰撞后抬升过程有紧密联系,并遭受了早中生代印支期构造热事件的明显叠加。 | 李超 仝来喜 刘兆 黄小龙 | 2020 | 岩石学报2020，36，3： | 1 |
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