越南昆嵩地体三叠纪花岗岩岩石成因及其特提斯构造意义

Petrogenesis of Triassic Granites from Kontum Massif in Vietnam and Its Tethyan Tectonic Implications

摘要

昆嵩地体位于印支陆块的核部，记录了大量的印支期岩浆作用和构造热事件，是了解古特提斯洋演化及印支与华南陆块碰撞拼合过程的关键区域，但目前对该期岩浆事件的成因及其与北部长山带的关系未能得到有效厘定.对昆嵩地体绥安（Huy n Tuy An）和胶寮（Chu Loan）地区的Van Canh花岗岩开展了岩相学、锆石U-Pb年代学、锆石原位Hf同位素和全岩地球化学分析，以限定其形成时代、岩石成因及构造环境.锆石U-Pb定年显示花岗岩样品的结晶年龄为244~239 Ma.该套样品包括了二长花岗岩和钾长花岗岩，均属于高钾钙碱性系列.它们的A/CNK值为1.03~1.21，为S型花岗岩.花岗岩均显示明显的Rb、Th和U富集，以及Nb、Sr、Zr和Ti的亏损，并具有强烈的Eu负异常（Eu/Eu* = 0.24~0.56）.锆石具有富集的原位Hf同位素组成（ε_Hf （t） = -11.2~-0.7）以及古-中元古代的Hf二阶模式年龄（T _DM2 = 1.98~1.31 Ga）.研究表明该套中三叠世花岗岩是古元古代-中元古代变沉积岩部分熔融的产物，并伴有少量变火成岩的加入.研究结合区域地质资料表明昆嵩地体中三叠世Van Canh花岗岩的成因与马江古特提斯分支洋闭合之后的印支与华南陆块的碰撞拼合有关，形成于后碰撞阶段，进而证实了长山带向南可以延伸至昆嵩地体内部.

Abstract

Kontum massif in the central Indochina records abundant Indosinian magmatism and tectonic thermal events, and is a key area for investigating the tectonic evolution of Paleotethyan ocean and subsequent collision between the Indochina and South China blocks. However, the origin of this Indosinian magmatism and its relationship with the Truong Son zone in the north are poorly constrained. In this study, it presents a set of petrographic, zircon U-Pb geochronological, zircon in-situ Hf isotopic, and whole-rock geochemical data for the granites from the Huyen Tuy An and Chu Loan area in the Kontum massif to constrain their crystallization ages, petrogenesis, and tectonic setting. Zircon U-Pb dating shows that the granites formed at 244-239 Ma. These samples contain monzogranites and K-feldspar granites and belong to the high-K calc-alkaline series. They are S-type granites with A/CNK values ranging from 1.03 to 1.21. These samples show enrichment of Rb, Th, and U, and depletion of Nb, Sr, Zr, and Ti, with obvious negative Eu anomalies (Eu/Eu* = 0.24-0.56). Their negative zircon ε_Hf (t) values ((-11.2)-(-0.7)) and Paleo- to Meso-Proterozoic Hf model ages (T _DM2 = 1.98-1.31 Ga) indicate that these granites were derived from the partial melting of the Paleo- to Meso-Proterozoic metasedimentary rocks with a small amount of metaigneous component. Our new data along with the regional geological observations suggest that the Middle Triassic Van Canh granites in the Kontum massif were formed in a post-collisional setting in response to the collision between the Indochina and South China blocks following the closure of Song-Ma Paleotethyan branch. Our studies further suggest that the Truong Son zone can southerly extend to the central Kontum massif.

关键词

印支陆块 / 越南昆嵩地体 / 中三叠世 / S型花岗岩 / 古特提斯洋 / 后碰撞 / 地球化学

Key words

Indochina block / Kontum massif / Middle Triassic / S-type granite / Paleotethyan ocean / post-collision / geochemistry

0 引言

古特提斯洋是晚古生代至早中生代存在于东南亚陆块群和东基梅里大陆之间的古大洋，该洋西起欧洲阿尔卑斯山脉，经中亚、西藏及我国西南部，进而延伸至东南亚等地（Bullard et al.， 1965； Acharyya， 1998； Metcalfe， 1998， 2006， 2011，， 2013， 2017， 2021； Wakita and Metcalfe， 2005； Wang et al.， 2018； 栾锡武等，2021； 钱鑫等，2022）.随着古特提斯洋的俯冲闭合，一系列由冈瓦纳北缘分离的陆块（华南、印支、滇缅马和思茅等）与欧亚大陆东南缘发生碰撞拼合进而形成了中南半岛.目前在中南半岛已识别出多个古特提斯缝合带/构造带，包括了清迈-清莱古特提斯主缝合带、哀牢山-马江古特提斯分支洋缝合带、黎府-碧差汶、长山带、琅勃拉邦和景洪-难河-程逸-沙缴带等（图1a，Metcalfe， 1996， 2021； Sone and Metcalfe， 2008； Yang et al.， 2016； Zhao et al.， 2016； Qian et al.， 2016a， 2016b， 2016c，， 2019； Wang et al.， 2016b， 2018， 2020； 赵国锋等，2018； Zhang et al.， 2020；吴松洋等，2022）.其中，马江带被认为是印支与华南的缝合边界，其系统记录了三叠纪时期的俯冲-闭合演化历史（Chung et al.，1997； Sone and Metcalfe，2008； Jian et al.，2009； Zi et al.，2012a， 2012b； Zhang et al.，2014， 2020； Wang et al.，2018）.此外，长山带主体沿中南半岛东北部延伸，其北界为越南北部的马江带，南界为昆嵩地体北部的三岐-福山带，绵延约1 000 km，构成了印支陆块北部最大的构造岩浆岩带（图1a）.已有的研究证实了长山带内保存了晚古生代-早中生代与马江古特提斯分支洋的俯冲-闭合及随后的印支与华南陆块碰撞拼合有关的岩浆-沉积记录（Lepvrier et al.，2008， 2011； Liu et al.，2012； Hieu et al.，2012， 2020； Wang et al.，2016a； van Thanh et al.，2019； Qian et al.，2019； 钱鑫等，2022）.

越南中部的昆嵩地体被认为是印支陆块的古老基底，已报道的年代学数据也显示该地体存在前寒武纪角闪岩相-麻粒岩相变质基底（Le Van De， 1997； 李兴振等， 2004； Tri and Khuc， 2011； 施美凤等， 2011； Zhang et al.， 2019）.此外，该地体还保存了加里东期（奥陶纪-志留纪）和印支期（二叠纪-三叠纪）的岩浆与变质作用，其中加里东期岩浆-变质事件被认为与原特提斯洋的演化有关（如Usuki et al.， 2009； Shi et al.， 2015； Hieu et al.， 2016； Owada et al.， 2016； Nguyen et al.， 2019； Minh et al.， 2020； Jiang et al.， 2020； Wang et al.， 2020， 2021； Trong et al.， 2021； Nakano et al.， 2021）.但是对印支期的岩浆作用及变质事件则存在不同的认识，包括了地幔柱成因（Owada et al.， 2007， 2016， 2020；Osanai et al.， 2008； Faure et al.， 2018）和古特提斯洋俯冲-闭合及之后的碰撞造山成因（Carter et al.， 2001； Lepvrier et al.， 2004， 2008； Hoa et al.， 2008， 2016；Usuki et al.， 2009； Sang， 2011； Nakano et al.， 2013， 2021； Hieu et al.， 2013， 2015， 2017，， 2020； van Thanh et al.， 2019；Hung et al.， 2022）.此外，已有的研究也主要集中在有限的年代学资料和沉积研究上（Nagy et al.， 2001； Hoa et al.， 2008；Nakano et al.， 2013； Hieu et al.， 2015； Kawaguchi et al.， 2021）.因此，昆嵩地体二叠纪-三叠纪长英质火成岩的形成时代、岩石成因及与长山带的关系等均未能得到有效限定.

针对上述问题，作者在越南中部的昆嵩地区开展了系统的野外调查，并在绥安和胶寮地区识别出了一套保存完好的花岗岩岩体（图1b）.针对这些花岗岩岩体，本文开展了系统的岩相学、锆石U-Pb年代学、锆石Lu-Hf同位素以及全岩地球化学分析，并结合区域同期长英质火成岩数据及相关地质资料，为昆嵩地体内古特提斯岩浆作用及构造演化提供新的约束.

1 地质概况与岩相学特征

印支陆块东部与华南陆块的交界为哀牢山-马江带，其西部则以景洪-难河-程逸-沙缴缝合带为界与临沧-素可泰-庄他武里地体分开（图1a）.越南中部的昆嵩地体位于印支陆块东部，其北以原特提斯三岐-福山带为界与长山带所分离，南与大叻带相连.该地体主要由前寒武纪结晶基底及盖层组成（Hutchison，1989； Le Van De， 1997； 李兴振等， 2004），包括了太古宙和元古宙岩石单元，其中太古宙岩石可分为下、中、上三部分，下部为变基性火成岩和镁铁质麻粒岩，中部为具镁铁质至硅铝质过渡特征的斜长片麻岩，上部为硅铝质花岗质岩石.元古宙岩石由斜长片麻岩、辉长岩、角闪岩、矽线石片岩和混合岩组成（Le Van De， 1997； 李兴振等， 2004； 施美凤等， 2011）.昆嵩地体的盖层主要由中三叠统、中侏罗统和白垩系沉积岩组成，其中中三叠统主要由碎屑岩、碳酸盐岩、砂砾岩和页岩组成，中侏罗统为磨拉石相砂砾岩层，白垩系为红层、泥灰岩、粉砂页岩和含膏岩层等（如Le Van De， 1997； 李兴振等， 2004； 王宏等， 2015； Xu et al.， 2022）.此外，昆嵩地体内还存在3个主要的变质杂岩体（图1b），根据变质等级的不同分为麻粒岩相Kannak岩体、角闪岩相Ngoc Linh岩体和绿片岩相Kham Duc岩体.变质岩和花岗岩的独居石U-Th-Pb定年结果显示该地体的变质杂岩主要受到460~430 Ma和245~230 Ma两期构造热事件的影响，而花岗岩的侵位年龄则主要集中于240~220 Ma，为中-晚三叠世（Nakano et al.， 2013）.

昆嵩地体发育了奥陶纪-志留纪（Thanh et al.， 2014； Hieu et al.， 2016； Minh et al.， 2020）、二叠纪-三叠纪（Nagy et al.， 2001； Hoa et al.， 2008； Nakano et al.， 2013；Hieu et al.， 2015）和白垩纪（Nguyen et al.， 2004； Shellnutt et al.， 2013）三期长英质岩浆作用.其中奥陶纪-志留纪主要有Chu Lai花岗岩（454~445 Ma， 如Thanh et al.， 2014）、Dai Loc花岗岩（426~423 Ma， 如Hieu et al.， 2016）、Kan Nack片麻岩和Ngoc Linh片麻岩（450~422 Ma和462~429 Ma， Nakano et al.， 2013）.这些花岗质岩石主要以I型和S型为特征，表现出与俯冲或碰撞相关的地球化学特征.二叠纪-三叠纪主要以Kan Nack紫苏花岗岩和片麻岩（249 Ma和248~230 Ma， Nagy et al.， 2001； Nakano et al.， 2013）、Van Canh花岗岩（251~229 Ma， 如Hung et al.， 2022）、Kham Duc片麻岩（236 Ma， 如Nakano et al.， 2013）和Ngoc Linh片麻岩（251~230 Ma， Nakano et al.， 2013）为代表，并被认为与地幔柱或印支与华南陆块的碰撞有关（Nagy et al.， 2001； Owada et al.， 2007， 2016， 2020； Osanai et al.， 2008； Hieu et al.， 2015； Hung et al.， 2022）.白垩纪花岗岩主要零星分布在昆嵩地体的南部地区，并被认为与古太平洋的演化有关（Nguyen et al.， 2004； Shellnutt et al.， 2013）.

昆嵩地体北部的Hai Van花岗岩体主要由含堇青石的花岗岩、黑云母花岗岩、花岗闪长岩、二云母花岗岩和细晶花岗岩组成，年龄为242~224 Ma，被认为是长山带最南部的岩体（图1b；如Thuc and Trung， 1995； Nakano et al.， 2013； Hieu et al.， 2015； van Thanh et al.， 2019）.三叠纪Van Canh花岗岩体是昆嵩地体最大的花岗岩体，主要呈北西-南东向分布在地体的南部，总面积超过2 000 km²，由Van Canh、Hoa Lac、Tra Buon、Chu Loan、Kong Choro等多个次级岩体组成（图1b； Hung et al.， 2022）.Van Canh花岗岩主要侵入前寒武纪变质岩系，并被侏罗纪沉积物不整合覆盖（Thuc and Trung， 1995； Tri and Khuc， 2011）.最近的研究表明Van Canh花岗岩锆石年龄为251~229 Ma（图1b； Cuong et al.， 2021；Hung et al.， 2022）.

本文样品采自昆嵩地体南部的Van Canh花岗岩体（图1b），其中20VN-23采样点（109°17′46″E，13°15′43″N）距绥和北部约18 km，位于Chua Long Hai Tuy An Phu Yen寺庙南1 km公路旁；20VN-24采样点（109°17′35″E，13°16′31″N）距绥和北部约20 km，位于Chua Long Hai Tuy An Phu Yen寺庙北0.5 km公路旁；样品20VN-29 （108°32′52″E，13°20′22″N）采自胶寮东约15 km的QL25公路旁.这3个点位的样品均为块状构造的二长花岗岩，表面风化较为严重，风化面破碎呈土褐色，选取灰白色新鲜面采集样品.此外，样品20VN-25 （109°17′37″E，13°21′14″N）采自距绥和北部约35 km的Ganh Da Dia海湾内，为肉红色块状构造的钾长花岗岩，可见新生代玄武岩覆盖于花岗岩之上（图2e）.镜下薄片观察表明二长花岗岩样品为细粒花岗结构，矿物粒径为0.2~2.0 mm，主要矿物为石英（35%~40%）、碱性长石（~30%）、斜长石（20%~30%），含有少量黑云母（~5%）、白云母（~3%）与绿帘石（~3%）等.其中，黑云母至斜长石、碱性长石、石英的矿物颗粒自形程度依次降低，黑云母为半自形-自形，斜长石自形程度高于钾长石和石英，石英为他形.两种长石含量相近，碱性长石主要为条纹长石和正长石，具条纹结构及卡斯巴双晶，表面土化呈土黄褐色，斜长石发育聚片双晶，部分斜长石可见绢云母化（图2b， 2d， 2f， 2h）.样品中还可见少量锂云母（<1%），其呈片状分布于钾长石边缘（图2b）.钾长花岗岩样品（20VN-29）为肉红色，具细粒花岗结构，矿物粒径在0.1~0.3 mm之间，矿物组成为石英（~40%）、钾长石（~38%）、斜长石（~17%）以及少量黑云母（2%~5%）和绿帘石（<1%） （图2h）.

2 分析方法

2.1　锆石U-Pb定年及原位Lu-Hf同位素测定

本文研究样品在河北省廊坊市地质测绘院实验室通过磁选法和重液法进行锆石颗粒分选后制靶.锆石的阴极发光图像（CL图）在广州拓岩检测技术有限公司利用TESCAN MIRA3 场发射扫描电子显微镜完成，使用扫描电压为10 kV、束流为15 nA、放大倍率为300~500倍.锆石U-Pb同位素定年在中山大学广东省地球动力作用与地质灾害重点实验室使用激光剥蚀系统与电感耦合等离子体质谱仪联用（LA-ICP-MS）完成.实验中使用的激光束斑直径为32 μm，激光脉冲频率为5 Hz，详细的分析测试过程见Wang et al. （2020）.采用标准锆石91500 （1 062.4±0.6 Ma； Wiedenbeck et al.， 1995）用于U-Pb同位素分馏校正，玻璃标准物质NIST 610用于微量元素校正.利用Glitter4.4.5 （Griffin et al.， 2008）对原始数据进行处理，使用ISOPLOT软件进行锆石U-Pb年龄谐和图的绘制以及加权平均年龄的计算（Ludwig，2003）.标样91500的分析结果介于1 060~1 066 Ma，与国际标准值（1 062.4 Ma， Wiedenbeck et al.， 1995） 的方差和标准差分别为1.85和1.36，其离散程度小，表明仪器状态稳定.

锆石原位Lu-Hf同位素分析在中山大学广东省地球动力作用与地质灾害重点实验室完成.通过Geolas HD准分子ArF激光剥蚀系统和Neptune Plus多接收电感耦合等离子体质谱仪（MC-ICP-MS）联用完成测试，详细分析流程类似于Hu et al. （2012）.标样为91500和Plešovice，激光斑束直径和激光频率分别为44 μm和8 Hz.计算Hf初始同位素值选用1.867×10^-11a^-1的¹⁷⁶Lu衰变常数（如Söderlund et al.， 2004），计算相对于亏损地幔的Hf模式年龄（T _DM）使用¹⁷⁶Hf/¹⁷⁷Hf = 0.282 772和¹⁷⁶Lu/¹⁷⁷Hf = 0.033 2 （如Blichert-Toft and Albarède， 1997），用大陆地壳平均值¹⁷⁶Lu/¹⁷⁷Hf=0.015和ƒ _cc=-0.55（Griffin et al.， 2002）计算Hf的二阶模式年龄（T _DM2）.

2.2　全岩主、微量元素分析

选用新鲜样品无污染粉碎至200目，在中山大学广东省地球动力作用与地质灾害重点实验室完成全岩主量和微量元素测定.全岩主量元素分析使用ARL Perform’X 4200型X射线荧光光谱仪（XRF），采用熔片法制备样品，称量烘干的样品与硼酸锂混合溶剂于坩埚中，加入饱和的碘化铵（NH₄I）溶液，移入铂金坩埚中加热至1 050 ℃共熔制成熔片，分析精度优于5%.详细实验方法见Wang et al. （2020）.全岩微量元素溶液分析使用Thermo Scientific iCAP RQ ICP-MS进行测试，分析精度一般优于5%，详细测试流程参考Wang et al. （2020）.

3 分析结果

3.1　锆石U-Pb年代学及原位Hf同位素特征

越南中部昆嵩地体Van Canh花岗岩体的4个样品（20VN-23， 20VN-24， 20VN-25和20VN-29）的锆石颗粒大多为无色透明的长柱状或短柱状的自形至半自形晶体，长为100~300 μm，长宽比为1∶1.5~1∶3.锆石阴极发光图像显示其内部发育有明显的振荡环带（图3），其对应的Th/U比值较高，分别为0.60~1.94、0.50~1.67、0.32~1.61和0.81~1.42，反映了岩浆成因锆石的特点（吴元保和郑永飞，2004）.锆石U-Pb年代学测试结果见附表1.二长花岗岩样品（20VN-23、20VN-24、20VN-25）的锆石加权平均年龄分别为239±2 Ma （MSWD=0.49， N=22； 图4a）、240±2 Ma （MSWD=0.16， N=17； 图4b）和244±2 Ma （MSWD=0.27， N=21； 图4c），钾长花岗岩的加权平均年龄为239±2 Ma （MSWD=0.70， N=24； 图4d）.

作者对4件花岗岩的锆石颗粒分别选取了15个锆石U-Pb测试点进行原位的Hf同位素分析，分析数据结果见附表2.其中3个二长花岗岩样品具有类似的Hf同位素组成，其锆石ε_Hf （t）值和二阶段模式年龄（T _DM2）分别为-8.5~-0.7和1.31~1.81 Ga、-8.5~-1.6和1.37~1.80 Ga以及-11.2~-3.5和1.49~1.98 Ga，钾长花岗岩（20VN-29）的锆石ε_Hf （t）值和二阶段模式年龄（T _DM2）分别为-7.5~-0.8和1.32~1.74 Ga.这些样品的ε_Hf （t）值与昆嵩地体北部长山带三叠纪Hai Van花岗岩（ε_Hf （t） = -11.1~-7.7， Hieu et al.， 2015）和昆嵩地体三叠纪花岗岩（ε_Hf （t） =-10.6~-6.7；Hung et al.， 2022）相类似（图5）.

3.2　岩石地球化学特征

本文三叠纪Van Canh花岗岩样品的全岩主量和微量元素分析结果见附表3.样品的烧失量（LOI）较低（0.32%~0.97%），表明样品未遭受明显的后期蚀变作用.样品具有较高的SiO₂含量（72.98%~79.37%）和Al₂O₃含量（11.41%~13.36%），较低的CaO含量（0.08%~0.87%）、Fe₂O₃含量（0.25%~4.00%）、MgO含量（0.03%~0.54%）、TiO₂含量（0.08%~0.24%）和P₂O₅含量（0.01%~0.06%）.CIPW标准化矿物计算显示其体积含量为：石英（33.6%~44.0%）、正长石（27.6%~34.4%）、钠长石（17.8%~28.2%）、钙长石（0.36%~4.17%）和刚玉分子（0.49%~2.30%）.所有样品在An-Ab-Or三角图解主要落在了花岗岩区域（图6a）.样品具有较高的全碱（K₂O+Na₂O = 6.97%~8.80%）含量和较高的K₂O/Na₂O （1.40~2.32）比值，在K₂O-SiO₂图解中（图6b），样品落于高钾钙碱性系列.样品的铝饱和指数A/CNK值介于1.03~1.21，其A/NK值介于1.13~1.40，具有过铝质花岗岩的特征（图6c）.在哈克图解中，除K₂O和Na₂O趋势不明显外，Al₂O₃、Fe₂O₃t、MgO、CaO、TiO₂和P₂O₅与SiO₂均呈负相关关系.样品主量元素特征总体也与昆嵩地体北部的长山带三叠纪Hai Van花岗岩以及昆嵩地体中部三叠纪花岗质岩石相类似（Hieu et al.， 2015； Hung et al.， 2022） （图7）.

本文三叠纪Van Canh花岗岩样品的稀土元素总量（∑REE）较高，为38.2×10^-6~254.2×10^-6 g/g，球粒陨石标准化稀土元素配分图解具有显著的右倾特征，轻重稀土分异明显（图8a），其（La/Yb）_N为1.85~16.27，（Gd/Yb）_N为0.73~2.19，并具明显的Eu负异常（Eu/Eu* = 0.24~0.56）.在原始地幔标准化微量元素蛛网图中（图8b），样品显示出大离子亲石元素的富集（Rb、Th、U）和高场强元素的亏损（Nb、Ta、Ti），并具有明显的Sr和Ba的负异常.此外，本文样品显示出与长山带三叠纪Hai Van花岗岩相类似的稀土和微量元素配分模式特征（图8； Hieu et al.， 2015）.

4 讨论

4.1　岩石成因

本文花岗岩样品在微量元素上具有明显的Ba和Sr负异常，结合Rb-Sr和Ba-Sr图解（图9b~9c）的特征，表明该套花岗岩样品在演化过程中发生了明显的斜长石和钾长石的分离结晶.此外，样品显示强烈的P亏损（图8），表明其可能经历了磷灰石的分离结晶.部分样品具有高的硅含量（>75%），且镜下可见少量锂云母矿物（图2e），暗示其高演化的特征（吴福元等，2017）.花岗岩的分异指数DI （DI=Q+Or+Ab+Ne+Lc+Kp）较高，为89~98，结合其强烈的Eu负异常及“海鸥状”的稀土元素配分模式，均显示出与高分异花岗岩相似的地球化学特征（图8a； Wu et al.， 2017）.在图6f中，样品也主要落在了分异型的钙碱性花岗岩区域内，同时样品的锆石Zr/Hf比值为0.16~16.68（<25），进一步证实了其高分异的特征（Breiter et al.， 2014）.此外，花岗岩的稀土元素四分组强度TE_1，3为0.85~1.02（<1.1），表明岩浆演化中不存在明显的流体-熔体相互作用.因此，本文花岗岩样品应为无流体相的高分异花岗岩（如陶继华等， 2013； Ballouard et al.， 2016； 余小清等，2021）.样品的10 000×Ga/Al值为1.30~2.83，Zr+Nb+Ce+Y平均含量为234×10^-6，均低于Whalen et al. （1987）提出的A型花岗岩元素含量，而落入结晶分异的I、M、S型花岗岩区域.此外，样品镜下无明显的碱性暗色矿物，并可见S型花岗岩常见的白云母等特征矿物，其铝饱和指数较高（1.03~1.21），CIPW标准矿物中的刚玉体积含量均大于1%.上述这些特征结合图解6d，均表明本文的样品属于高分异S型花岗岩.

本文花岗岩具有较低的CaO值（0.08%~0.87%）和变化较大的Al₂O₃/（FeOt+MgO）值（2.92~74.7），表明该花岗岩样品可能主要源自变沉积岩源区，混有少量变火成岩（图10a，Laurent et al.，2014）.在图10b中，本文样品主要落在泥质岩部分熔融区域，个别落在角闪岩部分熔融区域内.一般的单一岩浆源区的火成岩具有比较均一的La/Ce和Rb/Ti比值（Marjorie， 1993），而本文花岗岩具有变化的La/Ce比值（0.48~0.94）和Rb/Ti比值（0.15~0.43），暗示它们存在混合源区的特征.本文样品在野外于岩体中部采样，且岩体内未发现有围岩同化混染相关的捕虏体（李名则等，2020），也未见围岩同化混染导致的结构构造不均一的现象.此外，Yang et al. （2007）认为围岩同化混染过程会导致侵入体中含有从围岩中捕获的继承锆石，而本文样品锆石均为岩浆成因锆石，年龄均一，未见继承锆石.因此，本文样品应该未受明显的围岩同化混染作用.样品的锆石具有富集且变化范围较大的ε_Hf （t）值（-11.2~-0.7），这个特征结合La/Sm-La图解均表明本文样品具有源区不均一性的特征（图9a）.此外，样品富集的Hf同位素及较老的Hf二阶模式年龄（T _DM2=1.31~1.98 Ga），均与区域上马江带Muong Lat花岗岩（251~235 Ma，ε_Hf（t）=-13.1~-9.4，T _DM2=1.87~2.07 Ga，如van Thanh et al.， 2019）和Phia Bioc花岗岩（244 Ma，ε_Hf（t）=-10.0~-6.6，T _DM2=1.17~1.35 Ga，Hieu et al.， 2017）、长山带Hai Van花岗岩（242~224 Ma，ε_Hf （t）=-11.1~-7.7，T _DM2=1.69~1.98 Ga， Hieu et al.， 2015）以及昆嵩地体中部花岗岩（251~229 Ma，ε_Hf （t）=-11.1~-6.7，T _DM2=1.70~1.97 Ga， Hung et al.， 2022）等主要来源于“古老”地壳部分熔融的花岗岩相一致.综合昆嵩地体古生代-中生代沉积岩碎屑锆石的主要峰值特征（1.44 Ga和1.78~1.80 Ga）（Kawaguchi et al.， 2021），作者认为本文花岗岩源自古-中元古代变泥质岩部分熔融，并有少量变火成岩的加入.

4.2　区域对比与构造意义

印支运动传统被认为是与古特提斯洋的俯冲-闭合有关，并导致了印支陆块广泛发育二叠纪-三叠纪的构造热事件及相关岩浆-变质作用（Carter et al.， 2001； Lepvrier et al.， 2004， 2008； Metcalfe， 2013； Faure et al.， 2014）.随着马江古特提斯分支洋的俯冲闭合及随后的印支与华南陆块碰撞拼贴，在印支陆块东北部形成了长山构造岩浆岩带，而该带也是东南亚最重要的多金属成矿带（Kamvong et al.， 2014； Tran et al.， 2014； Manaka et al.， 2014）.也有学者认为，该区大规模侵位的三叠纪花岗岩为区域成矿提供了大量的热量和成矿物质，如深部的岩浆热液通过断层运移与较浅地壳中的大气水混合形成了越南北部的Binh Do铅锌矿床（Huang et al.， 2019）.已有的研究在长山带老挝境内及越南北部识别出了大量晚古生代306~260 Ma与马江支洋盆俯冲有关的岛弧岩浆作用（图1a； Liu et al.， 2012； Tran et al.， 2014； Shi et al.， 2015； Hieu et al.， 2016， 2017，2020； Pham et al.， 2018；Qian et al.， 2019）.此外，在该带及其周缘地区还识别出了大量的晚二叠世晚期-三叠纪的岩浆及变质事件的记录，如越南北部马江带的Muong Lat花岗岩（251~235 Ma， van Thanh et al.， 2019）；老挝北部的Lat Boua花岗岩（255~245 Ma）、Kham花岗岩（253~234 Ma）、Phon Thong花岗岩（250~245 Ma）、Lua花岗岩（239~234 Ma）和Na The花岗岩（256~240 Ma）（Wang et al.， 2016c）；越南西北部奠边地区花岗岩（242~225 Ma， Roger et al.， 2014； Shi et al.， 2015； Hieu et al.， 2020）以及越南中部的Hai Van花岗岩（242~224 Ma， Hieu et al.， 2015）等.变质作用的研究也表明长山带及周缘的变质作用主要发生在早三叠世之后，如越北Nam Co组和马江组糜棱岩的变形年龄为~250~240 Ma （Maluskia et al.， 2005； Liu et al.， 2012； 钱鑫等，2022）.此外，马江带榴辉岩的锆石和独居石U-Pb年龄分别为230±8 Ma和243±4 Ma，类似同期泥质麻粒岩的进变质时代和同造山期的构造热时代，分别为233±5 Ma和~251~229 Ma （Lepvrier et al.， 1997， 2004； Nakano et al.， 2008， 2010； Zhang et al.， 2013， 2014）.在越南中部昆嵩地体同样也记录了显著的三叠纪时期的变质热事件，其年龄多集中在251~222 Ma （图12， 如Tran， 1998； Carter et al.，2001； Lan et al.， 2003； Maluskia et al.， 2005； Owada et al.， 2006， 2007， 2016； Nakano et al.，2013）.近年来，也有部分学者在昆嵩地体中部的中生代岩体中识别出了三叠纪（251~229 Ma）时期的花岗质岩石（Tinh et al.， 2021； Cuong et al.， 2021；Hung et al.， 2022）.而本文研究的花岗岩样品位于昆嵩地体南部的Van Canh花岗岩，其形成时代为中三叠世（244~239 Ma），与昆嵩地体和长山带同期岩浆和变质事件相一致（图12），表明该区这一系列三叠纪火成岩可从老越交界的马江地区经长山带向南延伸至越南中部昆嵩地区，证实了整个越南中部地区均经历了强烈的晚二叠世-三叠纪的印支造山运动.

Wang et al. （2018）系统综述了长山带和金沙江-哀牢山-马江古特提斯带内的火成岩，并综合提出3阶段的构造演化过程：初始闭合（~247 Ma）、同碰撞（~247~237 Ma）和碰撞后（~237~200 Ma）的演化模型.已有的研究也表明越南西北部马江带中的I型和S型花岗岩均与晚二叠世-早三叠世期间印支与华南地块的碰撞拼合有关（Hieu et al.， 2017， 2020；van Thanh et al.， 2019）.随后，在中-晚三叠世（~237~220 Ma），由于碰撞后重力崩塌和区域热梯度的变化，引起了软流圈上涌造成了中-下地壳物质发生大规模的部分熔融，从而形成了长山带晚三叠世花岗质岩浆（Qian et al.， 2019； 钱鑫等，2022）.但是，对于昆嵩地体二叠纪-三叠纪长英质火成岩的成因则存在不同观点，包括了峨眉山地幔柱成因和碰撞造山成因.部分学者认为地幔柱可引发大规模岩浆侵入到昆嵩地体深部，并作为热源诱发了下地壳的部分熔融和超高温变质作用，从而形成区域变质岩及相对应的花岗质岩石（Owada et al.， 2007， 2016， 2020；Osanai et al.， 2008）.而大部分学者则认为该期岩浆活动与印支和华南陆块的碰撞造山有关（Hoa et al.， 2008； Nakano et al.， 2013， 2021； Hieu et al.， 2015， 2017， 2020； van Thanh et al.， 2019）.目前，已有研究显示峨眉山大火成岩省仅局限于中国西南部和越南东北部松大裂谷地区，尚无明显证据显示其分布在马江缝合带西南部（Liu et al.， 2012； Hieu et al.， 2016； Qian et al.， 2019）.因此，结合上述区域大规模的岩浆及变质作用，作者认为越南中部昆嵩地体这套Van Canh花岗岩的形成与马江古特提斯分支洋闭合后的印支和华南陆块的碰撞拼贴有关.

如前所述，昆嵩地体广泛发育三叠纪高温或伸展相关的岩浆及变质记录以及相对应的构造变形.越南中部Song Ba河地区的Kannack紫苏花岗岩的岩浆形成与侵位时间一致，具有相似的锆石U-Pb年龄（249 Ma）和黑云母Ar-Ar年龄（243 Ma），表明早三叠世期间的新生地壳快速剥露，暗示该区可能已经进入大陆碰撞期间（Nagy et al.， 2001）.昆嵩地体中部~247 Ma的Ngoc Linh榴辉岩和~248 Ma的Kannak超高压麻粒岩相变质岩具有减压的P-T轨迹，表明其具有伸展的构造背景（Osanai et al.， 2004； Nakano et al.， 2007， 2013； Zheng et al.， 2021）.此外，保存在昆嵩地体的同变质构造事件主要发育于早三叠世的伸展构造环境中，并造成地壳发生广泛的部分熔融，形成了普遍发育北西-南东向拉伸线理的Ngoc Linh变质核杂岩，随后在240~224 Ma Ngoc Linh变质核杂岩叠加了右旋走滑断层（Faure et al.， 2018）.因此，这些岩浆、变质和变形的地质记录均显示昆嵩地体在~240 Ma已进入后碰撞阶段.一般来说，高钾钙碱性火成岩主要形成于造山期由挤压向伸展转换的环境中（邓晋福等，2004）.而已有的研究表明长山带和马江带广泛发育三叠纪高钾钙碱性花岗岩，包括形成于后碰撞构造背景的奠边府花岗岩、Muong Luan I型花岗岩、老挝北部花岗岩和昆嵩地体北部的Hai Van花岗岩（Liu et al.， 2012；Hieu et al.， 2015， 2020； Qian et al.， 2019；van Thanh et al.， 2019）.昆嵩地体中部Van Canh花岗岩也显示高钾钙碱性的特征（Hieu et al.， 2015； Hung et al.， 2022）.因此，本文研究的中三叠世Van Canh高钾钙碱性花岗岩及区域同期花岗岩均具有类似的后碰撞地球化学特征，且在构造判别图上也都落在后碰撞的构造背景（图11），表明越南中部昆嵩地区广泛发育中-晚三叠世后碰撞相关的岩浆作用.前人研究表明，在后碰撞伸展背景下，由于加厚的岩石圈拆沉和软流圈底侵，岩石圈上部部分熔融可以形成花岗质岩石（Huang et al.， 2019； 徐畅等，2020）.综合上述分析，认为本文昆嵩地区的中三叠世花岗质岩石均形成于后碰撞的伸展背景.由于马江古特提斯分支洋的俯冲闭合导致了印支和华南陆块在晚二叠世-早三叠世发生碰撞拼合，并在随后的中三叠世进入到后碰撞阶段，加厚地壳发生拆沉，软流圈物质上涌导致了区域的伸展作用，并造成了“古老的”变沉积岩和变火山岩发生大规模部分熔融，从而形成了昆嵩地体内部广泛分布的中-晚三叠世高钾钙碱性花岗质岩石.

5 结论

（1） 昆嵩地体南部Van Canh花岗岩的锆石U-Pb年龄为244~239 Ma，为中三叠世，其锆石原位ε_Hf （t）值为-11.2~-0.7.

（2） 昆嵩地体南部Van Canh花岗岩为高钾钙碱性的高分异S型花岗岩，源自古-中元古代变泥质岩部分熔融，并有少量变火成岩的加入.

（3） Van Canh中三叠世花岗岩形成于后碰撞背景，与印支和华南陆块的碰撞拼合后的地壳拆沉有关.

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基金资助

国家自然科学基金项目(41830211;42072256)

广东省基础与应用基础研究基金项目(2018B030312007;2019B1515120019)

中山大学高校基本业务费(22lgqb14)