2021, Vol. 37
2. 中国地质科学院矿产资源研究所, 北京 100037
2. Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China
二叠纪-三叠纪这一地质历史时期是地质演化历史中极为重要的一个阶段，表现为古特提斯洋俯冲消减、冈瓦纳大陆裂解、新特提斯洋的开启与扩张，是一个地质构造复杂期。古特提斯洋俯冲到最终关闭在不同地区有着不同的时限(Audley-Charles, 1988; Deng et al., 2014; Cheng et al., 2015; 吴福元等, 2020)，例如在拉萨地块古特提斯洋的最终闭合大约在230Ma(Cheng et al., 2015)，特提斯东段的古特提斯洋在250Ma左右基本关闭(吴福元等, 2020)。根据古地理重建，冈瓦纳大陆初始裂解和新特提斯洋的开启与扩张始于中-晚二叠世(Torsvik et al., 2012, 2014; Svensen et al., 2017)，与地幔柱活动相关，产生了大规模的岩浆作用，其中以溢流玄武岩最为常见(Kent et al., 1992; Courtillot et al., 1999; Lapierre et al., 2004)。此次裂解导致多个微陆块从冈瓦纳大陆北缘裂解，其中喜马拉雅造山带也保存了与此次裂解相关的岩浆作用记录(Acharyya, 1992; Vannay and Spring, 1993; Garzanti, 1993, 1999; Garzanti et al., 1999; Corfield et al., 1999; 曾令森等, 2012)，主要分布在西部的Panjal，中部的吉隆地区和东部的隆子-Abor地区(图 1a)。
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图 1 新特提斯带简要地质图(a)和喜马拉雅地区晚二叠世岩浆作用分布图(b) Fig. 1 Simplified geological map of the Neo-Theyan belt showing the major ophiolite sequences and the Late Permian volcanic rocks (a) and the distribution of Permian magmatism in the Himalayas (b) |
特提斯喜马拉雅带作为冈瓦纳大陆的重要组成部分，位于大印度地块与澳大利亚地块连接的边缘，保存有冈瓦纳大陆多期裂解的记录，吸引了国内外众多学者的关注(Norton and Sclater, 1979; Coffin and Rabinowitz, 1987; Lawver and Scotese, 1987; Storey, 1995; Metcalfe, 1996; Chatterjee et al., 2013; Svensen et al., 2017; Sensarma et al., 2018; 王亚莹等, 2016; Wang et al., 2018, 2020, 2021; Tian et al., 2019; 田怡红, 2019)。揭示这些岩浆作用的时代和地球化学性质是刻画特提斯喜马拉雅构造演化过程的关键，对于深化理解冈瓦纳大陆北缘的构造动力学过程及其深部驱动机制也具有重要意义。另外，了解冈瓦纳大陆和新特提斯洋的形成及演化的过程对重塑地球演化和板块运动过程至关重要(Jokat et al., 2003; Upchurch, 2008; Eagles and König, 2008; Tian et al., 2019; 田怡红, 2019)。
在本次研究中，我们利用特提斯喜马拉雅哲古错地区晚二叠世花岗闪长岩来限定特提斯洋和冈瓦纳大陆的演化阶段。花岗闪长岩成因机制有三种：第一种理论认为长英质熔体来自于地壳部分熔融(Draper, 1991; Borg and Clynne, 1998; He et al., 2011; Tian et al., 2019; 田怡红, 2019)；第二种理论认为酸性岩是由单一地幔岩浆源区经历不同程度的分离结晶而形成(Barker and Arth, 1976; Mccurry et al., 2008)；第三种理论认为它是由长英质熔体和镁铁质熔体混合形成(Vernon, 1990; Bateman, 1995)。本文在详实的野外考察和系统采样的基础上，通过对其中代表性样品(T0919-B)花岗闪长岩进行了野外产出关系、岩相学、U-Pb锆石年代学和地球化学分析，来确定其形成时代和成因机制，探讨晚二叠世新特提斯洋和冈瓦纳大陆的演化历史和地球动力学意义。
1 地质背景和岩相学特征喜马拉雅造山带包括三个北向倾斜的构造单元，即特提斯喜马拉雅沉积岩系(THS)、高喜马拉雅结晶岩系(GHC)和低喜马拉雅序列(LHS)(图 1b, Yin and Harrison, 2000; Yin, 2006; Tian et al., 2019; 田怡红, 2019)。
特提斯喜马拉雅沉积岩系(THS)，位于印度-雅鲁藏布缝合带(ITS)和藏南拆离断层系(STDS)之间，呈东西向弧形带状展布，宽达100~120km(田怡红, 2019)。雅鲁藏布缝合带是青藏高原上最年轻的一条缝合带；藏南拆离断层系是一北倾低角度断层系(Burg and Chen, 1984; Burchfiel et al., 1992)，为特提斯喜马拉雅沉积岩系和高喜马拉雅结晶岩系的分界线。在地层上，特提斯喜马拉雅沉积岩系主要是元古界到始新统(1840~40Ma)的沉积序列，该沉积序列又分成四个主要序列：(1)由横向扩展的岩相单元所组成的元古界到泥盆系的前裂谷序列；(2)从石炭系到下侏罗统的裂谷和后裂谷序列；(3)从侏罗系到白垩系的被动大陆边缘序列；(4)从晚白垩系到始新统的同碰撞序列(Liu and Einsele, 1994; Garzanti, 1999; Yin, 2006; Tian et al., 2019; 田怡红, 2019)。在岩性上，THS由发育于早新生代南上褶皱冲断带上的晚元古代-显生宙(变质)沉积岩和寒武-奥陶纪花岗岩体组成(Gaetani and Garzanti, 1991; Corfield and Searle, 2000; Aikman et al., 2008)。特提斯喜马拉雅沉积岩系的前寒武系结晶基底由以片麻岩和片岩为代表的角闪岩相变质岩、混合岩、中新元古代片麻岩和古元古代花岗片麻岩组成(Liao et al., 2008; 田怡红, 2019)，出露于北喜马拉雅穹隆中。
在特提斯喜马拉雅哲古错地区，通过野外观测，我们识别出一套花岗闪长岩，命名为哲古错花岗闪长岩。该花岗闪长岩侵入特提斯喜马拉雅沉积岩系砂岩和页岩中，同时，该岩体又被时代为~146Ma的闪长岩(T0919-A，图 2a)侵入，该闪长岩可能是东冈瓦纳大陆初始裂解的产物，可能与哲拉组和维美组的熔岩流(Bian et al., 2019)、错那基性岩墙群(Zhu et al., 2008; 王亚莹等, 2016; Wang et al., 2018, 2020, 2021)和双峰式岩浆岩(Tian et al., 2019)属于同一期岩浆事件。该花岗闪长岩样品呈浅灰色，半自形中粒结构，块状构造。主要矿物成分为石英、斜长石和角闪石，可见少量黑云母(图 2b)，在镜下还可见透长石和微文象结构(图 2c)，与碱性花岗岩类似。
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图 2 哲古错花岗闪长岩的野外素描图(a)和显微镜下照片(b、c) Qz-石英；Pl-斜长石；Amp-角闪石；Bt-黑云母；Sa-透长石 Fig. 2 Field sketch map (a) and photomicrographs (b, c) of granodiorite (Sample T0919-B) from Zhegu Co area |
为确定样品闪长岩T0919-A和花岗闪长岩T0919-B的年龄，进行了锆石年代学分析。首先，样品锆石通过重液和磁选进行分离，之后在双目镜下挑选晶型较好、无明显裂纹和基本无包裹体的锆石。选定的锆石颗粒被嵌入到25mm的环氧树脂圆盘中，之后将环氧树脂靶进行粗磨和细磨，直到锆石内核部出露，之后进行抛光、清洗并做成样品靶。阴极发光图像是在中国地质科学院北京离子探针中心获得的。阴极发光图像(图 3)和背散射电子成像显示了锆石晶粒的内部生长结构。
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图 3 哲古错地区闪长岩(样品T0919-A) (a)和花岗闪长岩(样品T0919-B) (b)的锆石阴极发光照片及点位和测试年龄 Fig. 3 Cathodoluminescence (CL) images showing the texture, spots, and ages of zircon U-Pb dating for diorite (Sample T0919-A) (a) and granodiorite (Sample T0919-B) (b) from Zhegu Co area |
在中国地质科学院矿产资源研究所采用激光烧蚀多接收电感耦合等离子体质谱仪(LA-MC-ICP-MS)对锆石进行了U、Th和Pb分析，分析离子束直径为25μm，每测定5个未知点插入一次标样，标样为锆石GJ-1(599.8±1.7Ma, Jackson et al., 2004)和锆石Plesovice(337.13±0.37Ma, Sláma et al., 2008)。数据由M257标准锆石校准(U: 840×10-6, Nasdala et al., 2008)，数据处理采用ICPMSDataCal程序(Liu et al., 2010)，锆石年龄协和图使用Isoplot在95%置信水平下计算得出(Ludwig, 2003)。
2.2 全岩地球化学分析为测定样品T0919-B的全岩组分和地球化学组成，进行了全岩地球化学分析。测试在中国地质科学院国家地质实验测试中心完成。全岩的主量元素含量和微量元素含量分别使用X荧光光谱仪3080E(XRF)和电感耦合等离子体质谱仪(ICP-MS)获得。主量元素含量的测试误差小于5%，微量元素含量小于10×10-6的测试误差为10%，微量元素含量大于10×10-6的测试误差为5%。
2.3 全岩Sr-Nd同位素分析样品的Rb-Sr和Sm-Nd同位素分析在中国地质科学院地质研究所同位素分析实验室完成。采用同位素稀释法，利用FinniganMaT-262质谱仪测定全岩Sr同位素组成及元素Rb、Sr、Sm和Nd的含量；利用Nu Plasma HR多接收等离子质谱仪(MC-ICP-MS)获得全岩Nd同位素组成。Sr和Nd同位素分析结果分别按87Sr/86Sr=0.1194和146Nd/144Nd=0.7219进行标准化，之后再进行质量分馏校正。在样品分析过程中，Sr同位素测试标样为NBS987，Nd同位素监测标样为JMC Nd。详细的分析测试方法和流程常参考Chen et al.(2002, 2007)。之后根据锆石U-Pb年龄计算其Sr和Nd同位素初始组成。哲古错花岗闪长岩的结晶年龄约为260.3Ma，分析样品的Sr和Nd同位素的初始值按t=260.3Ma来计算。
3 数据和结果 3.1 花岗闪长岩和闪长岩的年龄为限定侵入花岗闪长岩中的闪长岩脉(T0919-A)的形成时代，对该岩脉也进行了锆石U-Pb定年。闪长岩的锆石颗粒多为自形，呈灰白色短柱状，长100~200μm，长宽比在2∶1和5∶1之间(图 3a)。所有锆石含有较高的U(161×10-6~2087×10-6)和Th(189×10-6~915×10-6)，并且所有锆石颗粒的Th/U比值在0.29~2.01之间(表 1)，表明该闪长岩锆石为岩浆成因(Hoskin and Schaltegger, 2003)。根据样品的U-Pb年龄谐和图和206Pb/238U加权平均年龄图(图 4a, b)，闪长岩年龄为146.5±2.1Ma(N=15，MSWD=0.48)，是闪长岩的结晶年龄。其中有一颗锆石的年龄为161.8Ma，且落在谐和线上，可能代表早期发生的岩浆活动。
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表 1 哲古错地区闪长岩(T0919-A)和花岗闪长岩(T0919-B)的锆石U-Pb同位素测试结果 Table 1 Zircon U-Pb isotopic data of the diorite (T0919-A) and granodiorite (T0919-B) from Zhegu Co area |
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图 4 哲古错地区闪长岩(T0919-A)(a、b)和花岗闪长岩(T0919-B)(c、d)的锆石U-Pb定年谐和图和加权平均年龄图 Fig. 4 U-Pb concordia diagrams and weighted average age diagrams for diorite (T0919-A) (a, b) and granodiorite (T0919-B) (c, d) from Zhegu Co area |
花岗闪长岩的锆石颗粒大多是自形的，呈黑灰色短柱状，长100~250μm，长宽比在1∶1和2∶1之间，并且在CL图像中有环带结构出现(图 3b)。所有的锆石含有相似的U(78×10-6~806×10-6)和Th(165×10-6~593×10-6)，并且所有锆石颗粒的Th/U＞0.1(表 1)，表明该花岗闪长岩的锆石为岩浆成因(Hoskin and Schaltegger, 2003)。结合样品的U-Pb年龄谐和图和206Pb/238U加权平均年龄图(图 4c, d)，该花岗闪长岩样品的年龄为260.3±2.8Ma(N=14，MSWD=1.9)，代表花岗闪长岩的结晶年龄。其中有一颗锆石的年龄为279.4Ma，且落在谐和线上，可能代表早期发生的岩浆活动。
3.2 全岩地球化学结果花岗闪长岩样品在主量元素上表现为含有较高的SiO2(63.00%~66.66%)、MgO(0.83%~1.50%)、CaO(4.39%~5.51%)、Na2O(2.75%~2.95%)、K2O(2.26%~3.52%)和Al2O3(12.62%~13.05%)含量，以及较低的烧失量(LOI=1.62%~1.78%)(表 2、图 5)，表明该花岗闪长岩样品较为新鲜。从图 5可见Al2O3、Na2O、CaO和SiO2有明显的正相关关系，而TiO2、MgO、FeOT(=FeO+Fe2O3×0.8998)、K2O、P2O5和SiO2有明显的负相关关系。在SiO2-K2O图解(图 6a)上，花岗闪长岩样品大多数都落在了高K钙碱性系列区域，结合A/NK比值大于1.0(1.87~2.72)，而A/CNK比值小于1.0(0.74~0.76，图 6b)，表明该花岗闪长岩具有高钾钙碱性、偏铝质花岗岩的特征。
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表 2 哲古错花岗闪长岩的主量元素(wt%)和微量元素(×10-6)分析测试结果 Table 2 Analysis results of major elements (wt%) and trace elements (×10-6) of the granodiorites from Zhegu Co area |
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图 5 哲古错花岗闪长岩及同时代辉绿岩和英安岩的主量元素TiO2 (a)、Al2O3 (b)、MgO (c)、FeOT (d)、Na2O (e)、CaO (f)、K2O (g)、P2O5 (h)与SiO2之间的协变图 Fig. 5 Co-variation diagram of major elements TiO2 (a), Al2O3 (b), MgO (c), FeOT (d), Na2O (e), CaO (f), K2O (g) and P2O5 (h) against SiO2 in granodiorite from Zhegu Co and contemporaneous diabase and dacite |
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图 6 哲古错花岗闪长岩的K2O-SiO2 (a, 据Le Maitre et al., 1989; Rickwood, 1989)和A/NK-A/CNK (b, 据Maniar and Piccoli, 1989)关系图解 Fig. 6 Plots of K2O vs. SiO2 (a, after Le Maitre et al., 1989; Rickwood, 1989) and A/NK vs. A/CNK (b, after Maniar and Piccoli, 1989) for granodiorite from Zhegu Co |
花岗闪长岩样品在稀土元素上富集LREE而亏损HREE(图 7a)，轻重稀土分馏明显((La/Yb)N=9.27~10.58，表 2)，但没有明显的Eu异常(Eu/Eu*=0.94~1.10)，表明斜长石分离结晶作用不明显。在原始地幔标准化微量元素蛛网图解中(图 7b)，所有花岗闪长岩样品显示出富集大离子亲石元素(LILE)，特别是K、Rb、Ba、Th；亏损Nb、Ta、Ti等高场强元素(HFSE)，具有明显的Zr、Hf正异常和Sr负异常。同时具有较高的Rb/Sr比值(0.21~0.29)和Zr/Hf比值(41.66~50.07)，较低的Sr/Y比值(4.15~6.45)，Nb/Ta比值(11.76~12.69)。
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图 7 哲古错花岗闪长岩的球粒陨石标准化稀土元素配分图解(a)和原始地幔标准化蜘蛛网图(b)(标准化值据Sun and McDonough, 1989) Fig. 7 Chondrite-normalized rare earth elements distribution pattern (a) and primitive mantle (PM)-normalized trace elements spider diagrams (b) for granodiorite from Zhegu Co (normalization values after Sun and McDonough, 1989) |
为确定花岗闪长岩的Sr-Nd同位素组成特征，对其进行了Sr-Nd同位素分析测试。测试结果见表 3。
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表 3 哲古错花岗闪长岩的全岩Sr-Nd同位素分析测试结果 Table 3 Analysis results of whole-rock Sr-Nd isotopic compositions of the granodiorites from Zhegu Co area |
花岗闪长岩具有较低的Rb(54.1×10-6~88.7×10-6)和Sr(237×10-6~308×10-6)，较高的Sm(12.6×10-6~14.7×10-6)和Nd(63.5×10-6~80.7×10-6)，较高的Rb/Sr比值(0.63~0.85)和较低的Sm/Nd比值(0.116~0.122)。现今87Sr/86Sr比值较高为0.706588~0.707126，而初始(t=260.3Ma)87Sr/86Sr(t)比值较低，为0.703456~0.704804，Nd同位素组成较亏损(εNd(t)=+1.1~+2.3，图 8)。
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图 8 特提斯喜马拉雅带内晚二叠世岩浆岩εNd(t)-87Sr/86Sr(t)关系图解 Fig. 8 Plot of εNd(t) vs. 87Sr/86Sr(t) of Late Permian magmatic rocks from the Tethyan Himalayan |
花岗闪长岩具有高SiO2、Na2O+K2O、Nb、Y和Ce，低CaO和Sr，Zr和Hf正异常等特征，这和A型花岗岩的特征类似(Whalen et al., 1987)。在主量元素对图解中(图 5)，花岗闪长岩的Al2O3、Na2O、CaO和SiO2有明显的正相关关系，而TiO2、MgO、FeOT、K2O、P2O5和SiO2有明显的负相关关系，与同时代基性岩对比(曾令森等, 2012)，除Al2O3和P2O5之外，其余主量元素都显现出一定的相关关系，表明二者可能具有成因上的联系。与此同时，在与Panjal Traps的英安岩(Shellnutt et al., 2012)对比中，发现二者SiO2含量几乎一致，且在TiO2、MgO、FeOT和P2O5上极为相似，但在Al2O3、Na2O、CaO和K2O上有较大区别，表明二者可能经过不同的分离结晶过程。在SiO2-K2O关系图解中(图 6a)，绝大多数花岗闪长岩样品都落在高K钙碱性区域，这和显微文象结构(图 2c)相一致，表明其具有碱性花岗岩属性，与A型花岗岩相似。与错那~137Ma的花岗岩(Tian et al., 2019)及同时代英安岩(Shellnutt et al., 2012)对比，可见三者都基本属于高K钙碱性系列(图 6a)。在A/CNK-A/NK关系图解中(图 6b)，花岗闪长岩样品和英安岩落在了偏铝质区域，而错那花岗岩则落在了过铝质区域，表明三者源区物质存在一定区别。在(K2O+Na2O)-10000Ga/Al判别图解(图 9a)中，该花岗闪长岩样品、英安岩和错那花岗岩都落在了A型花岗岩区域，揭示了其三者A型花岗岩的属性。但在Ce-Nb-Y三角判别图解中(图 9b)，所有的花岗闪长岩样品和英安岩都落在了A2型花岗岩区域，表明这些花岗闪长岩和英安岩具有A2型花岗岩属性；而所有的错那花岗岩都落在了A1型花岗岩区域。
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图 9 哲古错花岗闪长岩(K2O+Na2O)-10000 Ga/Al判别图解(a, 据Whalen et al., 1987)和Nb-Y-Ce判别图解(b, 据Eby, 1992) Fig. 9 Plots of (K2O+Na2O) vs. 10000 Ga/Al (a, after Whalen et al., 1987) and Nb-Y-Ce discrimination diagram (b, after Eby, 1992) of granodiorite from Zhegu Co |
A型花岗岩是花岗岩类(ISAM)的典型类别之一，具有碱性、贫水的特征，是非造山作用背景下的产物(Eby, 1990)。根据源区和构造环境的不同，A型花岗岩又被细分为A1型和A2型花岗岩，一般来说，A1型花岗岩与热点、地幔柱或非造山环境的大陆裂谷带相关。A2型花岗岩则表明其岩浆源区为经历过陆-陆碰撞或弧岩浆作用旋回的陆壳或下地壳(Eby, 1992)。一般认为酸性岩有三种成因机制：(1)长英质熔体来自于镁铁质下地壳部分熔融(Draper, 1991; Borg and Clynne, 1998; He et al., 2011)；(2)酸性岩是由单一地幔岩浆源区经历不同程度的分离结晶而形成(Barker and Arth, 1976; Mccurry et al., 2008)；(3)长英质熔体和镁铁质熔体混合形成(Vernon, 1990; Bateman, 1995)。哲古错花岗闪长岩都显示出高的A/NK比值，在A/CNK-A/NK图解中(图 6b)，所有的花岗闪长岩样品都表现出偏铝质组成。结合微量元素对比值La/Sm-Ba/Th(图 10a)关系图解和Zr/Nb-U/Th(图 10b)关系图解，表明岩浆来自沉积来源熔体，但有一定的亏损地幔物质加入。所有样品的εNd(t)=+1.1~+2.3，同样表明可能有地幔物质的加入。而同时代的英安岩(Shellnutt et al., 2012)则没有地幔物质的加入(图 10b)。所有样品富集LREE而亏损HREE(图 7a)，但没有明显的Eu异常(Eu/Eu*=0.94~1.10)，表明斜长石分离结晶作用不明显，样品与初始岩浆接近。在原始地幔标准化微量元素图解中(图 7b)，所有样品显示出富集LILE，特别是K、Rb、Ba、Th等元素，高场强元素Nb、Ta、Ti负异常，但Zr和Hf为正异常，与典型的弧岩浆岩不同，但与伸展构造背景下形成的岩浆岩类似。
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图 10 哲古错花岗闪长岩不相容元素对La/Sm-Ba/Th(a, 据Elliott, 2003)和Zr/Nb-U/Th(b, 据Stern et al., 2006)关系图解 Fig. 10 Plots of incompatible trace elements La/Sm vs. Ba/Th (a, after Elliott, 2003) and Zr/Nb vs. U/Th (b, after Stern et al., 2006) of granodiorite from Zhegu Co |
终上所述，哲古错花岗闪长岩与英安岩和错那花岗岩的构造背景相似，都形成于伸展构造背景，但三者物质源区不同，英安岩来源于中地壳部分熔融(Shellnutt et al., 2012)，错那花岗岩来源于上地壳含石榴子石变泥质岩的部分熔融(Tian et al., 2019)，哲古错花岗闪长岩的源区为被亏损地幔物质改造过的沉积岩或变沉积岩。
4.2 地球动力学意义在中-晚二叠世，特提斯喜马拉雅带内广泛发育着以Panjal溢流玄武岩为代表的基性岩浆作用(Spencer et al., 1995; Chauvet et al., 2008)，藏南打拉地区也发现了相同时代的辉绿岩(曾令森等, 2012)，吉隆Bhote Kosi玄武岩以及东喜马拉雅的Abor火山岩(Garzanti et al., 1999; 朱同兴等, 2002; 朱弟成等, 2009)也是同一时期的岩浆活动产物。这些岩浆活动被认为代表冈瓦纳大陆北缘裂解和新特提斯洋开启相关的岩浆活动。在拉萨地块江达地区发现的267Ma的A1型花岗岩(王海涛, 2021)也被认为和上述岩浆作用的动力学背景相同。在羌塘地块的羌塘大火成岩省被认为和Panjal大火成岩省是同一个大火成岩省，同时期的岩浆作用也被认为与冈瓦纳大陆北缘裂解和新特提斯洋开启相关(Dan et al., 2021)。
哲古错花岗闪长岩属于高K钙碱性岩石，这类岩石形成过程中通常需要异常高的地温梯度使源区物质发生部分熔融，经过上述讨论，可知中-晚二叠世存在一大火成岩省，哲古错花岗闪长岩形成所需的热源可能就来自于此时的地幔柱。花岗闪长岩岩浆源区中混入的基性幔源物质可能也与二叠纪基性大火成岩省有成因上的联系，地幔柱(Hill et al., 1992; Hill, 1993)既可以为地壳物质的熔融直接提供热源，又可以提供基性岩浆的混入以改造源区沉积岩或变沉积岩的部分熔融(Huppert and Sparks, 1988; Annen and Sparks, 2002)。哲古错花岗闪长岩与英安岩和错那花岗岩同属高K钙碱性岩石，其最大的区别在于源区物质不同(图 6b)，哲古错花岗闪长岩的源区为经亏损地幔物质改造过的沉积岩或变沉积岩，而英安岩来源于中地壳部分熔融(Shellnutt et al., 2012)，错那花岗岩的源区则为上地壳含石榴子石变泥质岩(Tian et al., 2019)，不过三者都是产于伸展构造背景中，哲古错花岗闪长岩和英安岩与冈瓦纳大陆北缘裂解和新特提斯洋的开启有关，而错那花岗岩与东冈瓦纳大陆的初始裂解有关(Tian et al., 2019)。
本次研究中的酸性岩浆活动与二叠纪基性岩浆活动发生时期相近，也有着一样的构造背景。所以本研究中的花岗闪长岩是伸展构造背景下的产物，同时地幔柱为地壳物质的熔融提供了热源和混入的基性岩浆，这一次酸性岩浆事件活动代表了与冈瓦纳大陆北缘裂解和新特提斯洋开启有关的岩浆活动。这一期裂解事件在不同地区导致的岩浆活动时期不完全一致，可能说明冈瓦纳大陆北缘裂解不是同时进行的，西部裂解时间可能早于东部。
5 结论哲古错花岗闪长岩形成于260.3±2.8Ma，为晚二叠世。样品富集LREE，亏损HREE；富集Th、K、Rb、Ba等大离子亲石元素；亏损Nb、Ta、Ti等高场强元素，具有明显的Zr、Hf正异常和Sr负异常。花岗闪长岩有较低的87Sr/86Sr(t)=0.703456~0.704804，较亏损的Nd同位素组成，εNd(t)=+1.1~+2.3。
该花岗闪长岩具有A型花岗岩特征，代表了伸展构造背景下的岩浆作用，其源区为经亏损地幔物质改造过的沉积岩或变沉积岩，地幔柱为地壳物质的熔融提供了热源和亏损地幔物质。此次酸性岩浆事件代表了与冈瓦纳大陆北缘裂解和新特提斯洋的开启有关的岩浆活动。
致谢 感谢中国地质科学院地质研究所董昕研究员和中国科学院地质与地球物理研究所纪伟强副研究员的细致审稿，提出诸多建设性修改意见。
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