Division of Tectonic Units and Their Evolutions within Xinjiang, China to Central Asia
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摘要:
中国新疆–中亚地处特提斯构造域和古亚洲构造域交汇部位，跨全球最重要三大构造（成矿）域中的2个，对认识全球构造演化和资源环境效应具有重要意义，前人对该区域开展了大量研究，提出了不同的大地构造单元和成矿区（带）划分方案，然而不同学派之间存在诸多争议。笔者结合“多岛弧盆系”构造理论，遵循将今论古的比较构造地质学研究原则，以大地构造相的时空结构分析为主线，以对接带、造山系和陆块区3类一级大地构造单元，依据优势大地构造相将研究区划分为12个一级构造单元、32个二级构造单元和74个三级构造单元，并针对二级构造单元的构造环境和岩石建造组合进行描述、总结，以建立研究区总体构造格架和演化历史。在此基础上，依据两大构造域时空演化特征，追溯古亚洲洋和特提斯构造域的构造演化历史。通过对研究区构造单元划分和构造演化的重新厘定，以期为区域基础地质研究和资源能源勘查提供基础依据。
Abstract:The region of Xinjiang (China) to central Asia, located at the intersection of Tethys and ancient Asia tectonic domains, spans two of the three most important tectonic (metallogenic) domains in the world. Therefore, it is of great significance to understand the global tectonic evolution and the effects of resources–environment. Previous researchers have carried out a lot of researches on this region, and proposed different geotectonic units and metallogenic regions (belts) division schemes. However, there are many disputes between different research teams. Based on the structural theory of "multi–island–arc–basin–terrain (MABT)" system by our research team, following the research principle of comparative structural geology, i.e., the present is the key to reveal the past, and taking spatial and temporal structure analysis of tectonic faces and environment as the main approach in which the suture zone, orogenic system and continental block are treated as three first–rank tectonic units. Accordingly, 12 first–rank tectonic units, 32 second–rank tectonic units and 74 third–rank tectonic units are divided following the dominant tectonic faces in the research region of this paper. Moreover, tectonic environment and rock formation combination of the second–rank tectonic units are focused on to establish the overall tectonic framework and evolution history of this region. Based on these, according to their temporal–spatial evolution characteristics, the tectonic evolution histories are reconstructed for Ancient Asian Ocean and Tethys Ocean, respectively. Through the division of tectonic units and the redefinition of tectonic framework, it is expected to provide scientific basis for regional basic geological research and resource–energy exploration practice in this domain.
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Keywords:
- Xinjiang /
- central Asia /
- Tectonic units /
- tectonic facies /
- evolution
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萤石，其主要成分是氟化钙（CaF2），是重要的基础性、战略性非金属矿产资源。高端含氟材料在新能源、新材料、新一代信息技术和航空航天等领域的重要性日益凸显，中国、美国、日本、欧盟等国家都将其列为“战略性矿产”或“关键矿产”（陈军元等，2021）。萤石矿在中国属于优势矿产资源，大中型萤石矿床集中于东部沿海、华中和内蒙古中东部（王吉平等，2015）。通过近年地质工作，在中国西部新疆若羌县阿尔金地区卡尔恰尔一带萤石找矿取得重大新发现，已发现卡尔恰尔、小白河沟、库木塔什、拉依旦北、盖吉克、皮亚孜达坂等多处（超）大–中型萤石矿床，改变了中国萤石矿的分布格局，已初步形成西部最重要的萤石矿产资源基地。近年来，阿尔金高压–超高压变质带、蛇绿构造混杂岩带和岩浆岩等基础地质研究方面取得了重要进展，但与萤石矿有关的研究才刚刚起步，主要对地质特征、控矿因素、花岗岩年龄与元素地球化学特征及流体包裹体等方面做了一定研究（高永宝等，2021；吴益平等，2021，2022），总体研究程度较低。目前，卡尔恰尔超大型萤石矿区花岗岩成岩时代还未见报道，成矿流体与物质来源的研究还很薄弱，制约了矿床成因的研究和下一步找矿勘查。
稀土元素的地球化学性质具有一定特殊性，如化学性质稳定，高度均一化，不易受变质作用影响等，是示踪成矿流体来源和反演热液成矿作用过程的有效手段之一（Lottermoser，1992）。萤石是富稀土矿物，萤石中的Ca2+与稀土离子半径相似，可容纳大量稀土元素，且继承了成矿热液流体中的稀土元素配分型式（Moller，1983；Bau et al.，1992，1995；Smith et al.，2000；许成等，2001；赵省民等，2002；许东青等，2009；孙海瑞等，2014；Sasmaz et al.，2018），在示踪成矿流体来源与演化及矿床成因机理等方面已得到广泛应用（叶锡芳等，2014；邹灏等，2014，2016；彭强等，2021；许若潮等，2022；游超等，2022；张苏坤等，2022）。笔者选择阿尔金卡尔恰尔超大型萤石矿带中的卡尔恰尔、小白河沟、库木塔什3处典型萤石矿床为研究对象，简要总结其成矿特征，利用LA–ICP–MS锆石U–Pb测年确定卡尔恰尔矿区碱长花岗岩与片麻状钾长花岗岩的形成时代，通过萤石、方解石的稀土元素地球化学及萤石Sr–Nd同位素等研究，探讨成矿流体特征与成矿物质来源，为区域矿床成因研究和指导找矿提供理论依据。
1. 区域地质背景
研究区位于青藏高原北部边缘，地处柴达木地块与塔里木地块接合部位，大地构造位置主要处于阿尔金造山带（图1a、图1b）。区域出露地层以元古界为主，新太古界至新元古界遭受程度不一的变形变质作用改造，以中深变质岩为主（图1c）。新太古界—古元古界阿尔金岩群出露广泛，总体上呈北东向展布，该岩组岩石类型复杂，主要为一套由变质碎屑岩、碳酸盐岩和变质火山碎屑岩组成的变质岩系，主要岩性为黑云斜长片麻岩、斜长或二长变粒岩、石榴矽线黑云片麻岩、二长石英片岩夹石英岩、白云质大理岩、斜长角闪岩透镜体等。中元古界巴什库尔干岩群为一套云母石英片岩、片麻岩、变粒岩、长石石英岩夹变质中基性火山岩、火山碎屑岩的变质岩系。中元古界蓟县纪塔昔达坂岩群可分为下部碎屑岩（木孜萨依组）和上部碳酸盐岩（金雁山组）。新元古界索尔库里群为一套轻变质的碳酸盐岩、碎屑岩夹少量火山碎屑岩地层序列。另外，阿尔金西南缘发育由陆壳深俯冲形成的高压-超高压变质带，岩石的原岩形成时代多为1 000～800 Ma，与区域广泛分布的新元古代花岗片麻岩形成时代基本相同，均与Rodinia超大陆事件引发的全球性岩浆活动相关，而变质时代集中在504～486 Ma之间，代表在～500 Ma发生陆壳深俯冲–碰撞事件（Zhang et al.，2001；刘良等，2007；张建新等，2010；Liu et a1.，2012）。
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图 1 阿尔金造山带卡尔恰尔一带地质矿产图Figure 1. Geological and mineral map of the Kalqiaer area in Altyn Tagh区域构造活动频繁，经历了前寒武纪多期变形变质作用的强烈改造和构造置换，以及显生宙以来多期韧性、脆性构造的相互叠加，构造形迹十分复杂。区内构造主要为断裂，褶皱因受到岩浆侵位及断裂构造的破坏，形态极不完整。区域性大断裂由北至南有卡尔恰尔–阔什断裂、盖吉勒断裂、约马克其–库兰勒格断裂、阿尔金南缘断裂（图1c）。围绕区域深大断裂广泛分布次级断裂，主要以北东–近东西向为主。卡尔恰尔–阔什断裂呈北东东向，东西向延伸大于70 km，呈明显带状，是一个长期活动的断裂，该断裂不仅是早期地质构造单元（阿尔金杂岩和中新元古界隆起带）之间的分界线，还对早古生代中酸性侵入岩体的分布有控制作用，卡尔恰尔超大型萤石矿、小白河沟萤石矿即与该断裂及其派生的众多次级断裂关系密切。盖吉勒断裂呈北东向，为一南倾的逆断层，与库木塔什、拉依旦北等萤石矿床的形成密切相关。约马克其–库兰勒格断裂总体为北东东向，出露长约为10 km，在研究区与布拉克北、皮亚孜达坂等萤石矿床的形成关系密切。阿尔金南缘断裂呈北东东向横贯阿尔金南部，长度大于几千公里，构成阿中地块与阿南缘蛇绿混杂岩带的边界（校培喜等，2014）。
区域经历了多期次岩浆活动，新元古代、早古生代、中生代等均有规模不等的中酸性岩浆侵入，多沿阿尔金山呈北东向带状展布，岩石类型复杂，充分反映了造山带花岗岩类型丰富的特点（图1c）。新元古代侵入岩以花岗质片麻岩、花岗闪长质片麻岩为主，主要出露于研究区东部。早古生代侵入岩分布最为广泛，主要岩性有碱长花岗岩、二长花岗岩、黑云母花岗岩、花岗闪长岩等。区域脉岩极为发育，脉岩类型以碱长花岗岩脉、花岗伟晶岩脉为主，呈北东–北东东走向。其中碱长花岗岩脉主要分布于卡尔恰尔深大断裂南侧，在阿尔金岩群和新元古代花岗质片麻岩中尤为发育，受断裂控制明显，出露宽度普遍较窄，该脉岩与萤石矿关系密切（图1c）。花岗伟晶岩脉主要分布于卡尔恰尔深大断裂北侧，主要就位于阿尔金岩群和新元古代花岗质片麻岩中，脉体中矿物以长石和石英为主，个别含矿伟晶岩脉发育有锂辉石、绿柱石、锂云母、铌钽铁矿等稀有金属矿物。
2. 矿床地质特征
卡尔恰尔超大型萤石矿区出露地层主要为古元古界阿尔金岩群（Pt1A），为一套角闪岩相的中深变质岩系，萤石矿化主要分布于黑云母斜长片麻岩中，矿脉延伸方向与岩层走向基本一致。矿床位于卡尔恰尔–阔什断裂南侧，该区域深大断裂派生的次一级断裂系统对萤石矿产分布有明显的控制作用，断裂呈北东–近东西向展布，沿构造裂隙大量充填萤石–方解石脉，构成区内重要的赋矿构造。矿区岩浆岩类型主要为碱长花岗岩、片麻状钾长花岗岩，岩体与围岩地层接触界限明显（图2a、图2i）。萤石矿化在空间上与碱长花岗岩关系密切，与围岩地层接触关系较明显（图2a～图2c）。矿区圈出31条萤石矿体，由众多萤石-方解石细脉构成，多为复脉型矿脉，北东–近东西向带状展布，长度为1710～4580 m，平均厚度为2.36～4.68 m，最大厚度为23.5 m，矿体延伸稳定，连续性好，钻探验证矿脉有收敛增厚趋势，沿倾向控制最大斜深907 m。矿石中矿物成分较为简单，主要是萤石、方解石，少量石英（图2d～图2h），萤石呈2阶段成矿，早阶段萤石呈白色、淡绿色，晚阶段萤石呈紫色、紫黑色，可见紫色萤石矿脉穿插白色萤石矿脉，或紫色萤石矿脉发育于白色萤石矿脉边部（图2a、图2c）。矿石呈巨晶–粗晶结构、自形–半自形–他形粒状结构、碎裂结构、糜棱结构，矿石自然类型主要有脉状、条带状、角砾状矿石（图2d～图2f）。围岩蚀变主要为碳酸盐化、钾化、硅化、高岭土化、绢云母化、绿帘石化等。矿床成因类型属于热液充填型，矿石工业类型主要是CaF2–CaCO3型，CaF2平均品位为33.9%，探明+控制+推断萤石矿石量为6 631万t，矿物量（CaF2）为2 249万t，达超大型规模。
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图 2 卡尔恰尔超大型萤石矿床矿化特征a～c.萤石矿化与碱长花岗岩关系密切，与围岩界线较清晰，紫色萤石矿脉穿插或发育于白色萤石矿脉边部；d～e.脉状萤石矿化；f.角砾状萤石矿化；g～h.钻孔中萤石矿化；i.片麻状钾长花岗岩侵入于阿尔金岩群黑云斜长片麻岩中；Cal.方解石；Fl.萤石Figure 2. Photos of mineralization features of Kalqiaer super–large fluorite deposit库木塔什萤石矿区出露地层为古元古界阿尔金岩群，岩性主要是黑云斜长片麻岩，其次为大理岩。矿区断裂主要呈北北东向、北东向、近东西向，多为平移断层，并发育韧性–脆性剪切带，北东向及近东西向断裂控制着区内岩脉的发育和展布。矿区内出露的侵入岩主要有碱长花岗岩、片麻状钾长花岗岩，碱长花岗岩脉与萤石矿脉关系十分密切（图3a、图3b），脉岩和矿脉均受断裂控制明显。矿区共圈出14条萤石矿化体，多呈北东向，倾向北北西，倾角为40°～70°，地表出露长为50～980 m，宽为0.3～3.6 m。矿石自然类型主要有脉状、角砾状（图3c～图3i），矿石中矿物成分较为简单，主要是萤石、方解石，另发育较多磷灰石，包括绿色柱状氟磷灰石和草黄色粒状铈磷灰石（图3e）。矿石具粗晶结构、自形–半自形–他形粒状结构、碎裂结构。矿石工业类型主要为CaF2–CaCO3型，CaF2平均品位为25%。围岩蚀变较为发育，主要为碳酸盐化、钾化、绢云母化、高岭土化等。矿床成因属热液充填型。
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图 3 库木塔什萤石矿床矿化特征a～b. 萤石矿化与碱长花岗岩关系密切；c～f. 脉状萤石矿化及其矿物组成；g～i. 角砾状萤石矿化及其矿物组成；Cal. 方解石；Fl. 萤石；Ap. 磷灰石Figure 3. Photos of mineralization features of Kumutashi fluorite deposit小白河沟萤石矿区出露地层为古元古界阿尔金岩群，萤石矿化赋存在黑云斜长片麻岩中。矿区出露的侵入岩主要为碱长花岗岩，其与萤石矿脉关系密切（图4a～图4b）。矿区构造以近东西向为主。矿区圈定两条萤石矿化带，南侧矿化带长约为2.5 km，宽约为0.4 km，走向北东东；北侧矿化带宽约0.4为 km，长约为1.7 km，走向近东西。萤石矿体走向近东西，倾向北，倾角为30°～40°，该矿床特点是发育高品位矿石，CaF2品位大于50%，局部可达90%以上。矿石类型主要为块状矿石、纹层状矿石（图4c～图4f），矿石中矿物主要为萤石，局部发育方解石和少量石英；萤石呈白色、绿色、紫色、紫黑色等。矿石具粗晶结构、自形–半自形–他形粒状结构。矿石工业类型主要是CaF2型、CaF2–CaCO3型。围岩蚀变主要为碳酸盐化、钾化、绢云母化、高岭土化等。
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图 4 小白河沟萤石矿床矿化特征a～b.萤石矿化与碱长花岗岩关系密切；c.纹层状萤石矿石；d～f.块状萤石矿石Figure 4. Photos of mineralization features of Xiaobaihegou fluorite deposit3. 采样及测试方法
用于锆石U–Pb年龄测试的样品经人工破碎后分选出锆石单矿物，制靶后进行阴极发光及透反射照相，根据图像选测试点位并进行合理数据解释。锆石U–Pb测年在自然资源部岩浆作用成矿与找矿重点实验室进行。激光剥蚀系统为GeoLas Pro，ICP–MS为Agilent 7700x，每时间分析数据包括大约40 s的样品信号和10 s的空白信号，激光剥蚀采用氦气作载气、氩气为补偿气以调节灵敏度。数据分析采用软件Glitter 4.4（Van Achterbergh et al.，2001）完成，详细测试过程和仪器参数可参考李艳广等（2015）。锆石U–Pb年龄谐和图采用Isoplot/Ex_ver 3（Ludwig，2003）软件绘制。
包含萤石、方解石矿物的矿石样品经过人工破碎后在双目镜下挑纯，挑纯出的小颗粒放入玛瑙研钵中，充分研磨至200目以下呈粉末状用于稀土元素实验测试分析。测试实验在自然资源部岩浆作用成矿与找矿重点实验室完成，萤石、方解石的稀土元素分析测试采用ICP–MS电感耦合等离子体质谱法，检测下限n×10–13～n×10–12，检测误差小于10%。
Rb–Sr、Sm–Nd同位素组成测试在自然资源部中南矿产资源监督检测中心完成。采用热电离质谱仪TRITON分析Rb、Sr、Sm、Nd同位素组成，同位素稀释法计算Rb、Sr、Sm、Nd含量及Sr同位素比值。Nd、Sr同位素比值分析中质量分馏分别采用146Nd/144Nd=0.7219，88Sr/86Sr=8.37521进行幂定律校正。整个分析过程用GBW04411、GBW04419、BCR-2和NBS987、GSW标准物质分别对全流程和仪器进行质量监控。NBS987的87Sr/86Sr测定值为0.71028±1，GBW04411测定值分别为Rb=249.8×10−6、Sr=159.3×10−6和87Sr/86Sr=0.76005±2，与其推荐值在误差范围内一致。全流程Nd、Sm、Sr、Rb空白分别小于9×10−10 g、3×10−10 g、3×10−9 g和4×10−10 g。
4. 测试结果
4.1 锆石U–Pb年龄
卡尔恰尔矿区与成矿相关的碱长花岗岩样品中锆石以自形粒状为主，粒径多为50～150 μm，阴极发光图像揭示大部分锆石具有清晰的岩浆韵律环带（图5a）。锆石U含量为233×10−6～1 095×10−6，Th含量为100×10−6～462×10−6，Th/U值为0.2～0.62，平均为0.45，显示出岩浆锆石的特点（表1）（Hoskin et al.，2000）。22个分析点投影于谐和线上及附近，206Pb/238U加权平均年龄为（455.8±2）Ma，代表了岩浆结晶年龄，表明其形成于中—晚奥陶世（图5b）。
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图 5 卡尔恰尔萤石矿区碱长花岗岩的锆石CL图（a）和U–Pb年龄图（b）Figure 5. (a) Zircon CL images and (b) U–Pb diagram of alkali feldspar granite from the Kalqiaer fluorite deposit表 1 卡尔恰尔萤石矿区碱长花岗岩的锆石LA–ICP–MS U–Pb分析结果表Table 1. LA–ICP–MS zircon U–Pb isotopic data of alkali feldspar granite in Kaerqiaer fluorite deposit测试点 Th U Th/U 207Pb/206Pb 207Pb/235U 206Pb/238U 207Pb/206Pb 207Pb/235U 206Pb/238U （×10-6） 比值 1σ 比值 1σ 比值 1σ Ma 1σ Ma 1σ Ma 1σ KJ01 100 343 0.29 0.0564 0.0021 0.5734 0.0210 0.0737 0.0009 469.0 82.6 460.2 13.5 457.5 5.1 KJ02 137 271 0.51 0.0569 0.0023 0.5760 0.0221 0.0734 0.0009 487.3 86.2 461.9 14.3 456.9 5.3 KJ03 223 457 0.49 0.0553 0.0014 0.5580 0.0136 0.0733 0.0007 422.1 55.8 450.2 8.9 456.0 4.2 KJ04 105 233 0.45 0.0567 0.0020 0.5721 0.0189 0.0732 0.0008 479.0 75.0 459.4 12.2 455.6 4.9 KJ05 364 1095 0.33 0.0588 0.0013 0.5896 0.0122 0.0727 0.0007 561.0 47.4 470.6 7.8 452.5 4.0 KJ06 151 333 0.45 0.0541 0.0019 0.5515 0.0184 0.0739 0.0008 376.3 76.1 446.0 12.1 455.8 4.9 KJ07 137 282 0.49 0.0592 0.0024 0.5975 0.0229 0.0733 0.0009 572.9 84.2 475.6 14.6 456.0 5.3 KJ08 206 369 0.56 0.0547 0.0021 0.5513 0.0205 0.0731 0.0009 400.1 83.6 445.8 13.4 455.0 5.1 KJ09 143 256 0.56 0.0552 0.0025 0.5639 0.0246 0.0741 0.0010 420.0 97.5 454.0 16.0 451.0 5.7 KJ10 152 430 0.35 0.0551 0.0019 0.5646 0.0182 0.0744 0.0008 416.5 72.8 454.5 11.8 452.3 4.9 KJ11 127 277 0.46 0.0574 0.0019 0.5796 0.0184 0.0732 0.0008 508.1 71.3 464.2 11.8 455.6 4.8 KJ12 149 325 0.46 0.0569 0.0020 0.5774 0.0192 0.0736 0.0008 488.1 75.2 462.8 12.4 457.9 4.9 KJ13 164 398 0.41 0.0569 0.0016 0.5771 0.0158 0.0736 0.0008 487.1 62.6 462.6 10.2 457.8 4.5 KJ14 199 370 0.54 0.0559 0.0016 0.5674 0.0158 0.0736 0.0008 449.1 63.3 456.3 10.2 458.0 4.5 KJ15 258 678 0.38 0.0550 0.0015 0.5550 0.0144 0.0732 0.0007 412.1 58.9 448.3 9.4 455.6 4.4 KJ16 101 509 0.20 0.0577 0.0016 0.5878 0.0151 0.0739 0.0007 519.0 58.1 469.4 9.6 456.6 4.4 KJ17 168 488 0.34 0.0570 0.0016 0.5799 0.0151 0.0739 0.0007 489.0 59.9 464.4 9.7 453.6 4.5 KJ18 233 432 0.54 0.0561 0.0016 0.5697 0.0156 0.0737 0.0008 455.6 62.3 457.8 10.1 455.5 4.5 KJ19 462 797 0.58 0.0565 0.0014 0.5729 0.0136 0.0736 0.0007 470.2 54.9 459.9 8.8 458.0 4.3 KJ20 293 472 0.62 0.0570 0.0017 0.5767 0.0160 0.0735 0.0008 488.8 63.4 462.3 10.3 457.2 4.6 KJ21 170 495 0.34 0.0553 0.0016 0.5630 0.0155 0.0738 0.0008 425.9 62.3 453.4 10.0 454.2 4.5 KJ22 188 415 0.45 0.0575 0.0017 0.5846 0.0164 0.0738 0.0008 510.8 63.5 467.4 10.5 457.9 4.6 卡尔恰尔矿区片麻状钾长花岗岩样品中锆石以自形粒状为主，颗粒较大，粒径多为60～200 μm，阴极发光图像揭示大部分锆石具有清晰的岩浆韵律环带（图6a）。片麻状钾长花岗岩中锆石的U含量为90×10−6～765×10−6，Th含量为24×10−6～270×10−6，Th/U值为0.33～1.76，平均为0.27，显示出岩浆锆石的特点（表2）。16个分析点投影于谐和线上及附近，206Pb/238U加权平均年龄为（914.5±4.1）Ma，代表了岩浆结晶年龄，表明其形成于新元古代早期（图6b）。
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图 6 卡尔恰尔萤石矿区片麻状钾长花岗岩的锆石CL图（a）和U−Pb年龄图（b）Figure 6. (a) Zircon CL images and (b) U–Pb diagram of gneissic feldspar granite from the Kalqiaer fluorite deposit表 2 卡尔恰尔萤石矿区片麻状钾长花岗岩的锆石LA–ICP–MS U–Pb分析结果表Table 2. LA–ICP–MS zircon U–Pb isotopic data of gneissic feldspar granite in Kaerqiaer fluorite deposit测试点 Th U Th/U 207Pb/206Pb 207Pb/235U 206Pb/238U 207Pb/206Pb 207Pb/235U 206Pb/238U （×10-6） 比值 1σ 比值 1σ 比值 1σ Ma 1σ Ma 1σ Ma 1σ KC01 158 440 0.36 0.0685 0.0017 1.3024 0.0298 0.1380 0.0014 883.4 49.1 846.8 13.1 853.5 7.8 KC02 24 305 0.08 0.0705 0.0017 1.5206 0.0348 0.1566 0.0016 941.9 48.7 938.7 14.0 938.0 8.8 KC03 100 407 0.25 0.0689 0.0015 1.4817 0.0305 0.1561 0.0015 895.4 44.4 922.9 12.5 935.2 8.4 KC04 229 443 0.52 0.0698 0.0014 1.4771 0.0269 0.1538 0.0015 920.9 39.3 921.0 11.0 922.0 8.1 KC05 140 401 0.35 0.0685 0.0014 1.4364 0.0280 0.1523 0.0015 882.9 42.1 904.2 11.7 913.8 8.2 KC06 64 260 0.25 0.0686 0.0016 1.4725 0.0335 0.1559 0.0016 886.6 48.6 919.2 13.8 933.7 8.8 KC07 97 291 0.33 0.0737 0.0016 1.6255 0.0340 0.1601 0.0016 1033.7 44.1 980.1 13.1 957.1 8.8 KC08 28 90 0.32 0.0760 0.0030 2.0298 0.0760 0.1939 0.0026 1094.5 75.8 1125.6 25.5 1142.6 14.1 KC09 137 435 0.31 0.0705 0.0014 1.4788 0.0279 0.1522 0.0014 943.4 40.7 921.7 11.4 913.5 8.1 KC10 27 485 0.05 0.0698 0.0014 1.4277 0.0269 0.1485 0.0014 922.4 40.7 900.6 11.3 892.5 7.9 KC11 79 360 0.22 0.0700 0.0016 1.4820 0.0313 0.1536 0.0015 929.0 45.2 923.0 12.8 921.3 8.5 KC12 175 765 0.23 0.0686 0.0013 1.3880 0.0248 0.1469 0.0014 886.9 39.0 883.8 10.5 883.3 7.7 KC13 270 677 0.40 0.0703 0.0013 1.4973 0.0250 0.1546 0.0014 938.1 36.4 929.3 10.2 926.4 8.0 KC14 84 297 0.28 0.0694 0.0016 1.4965 0.0336 0.1566 0.0016 909.9 47.9 928.9 13.7 937.8 8.8 KC15 103 489 0.21 0.0710 0.0014 1.4375 0.0259 0.1469 0.0014 958.6 38.9 904.7 10.8 883.5 7.8 KC16 135 212 0.64 0.1106 0.0019 4.7430 0.0752 0.3114 0.0030 1808.6 31.0 1774.9 13.3 1747.6 14.7 KC17 103 747 0.14 0.0710 0.0012 1.5322 0.0247 0.1566 0.0014 958.0 35.1 943.4 9.9 938.0 8.0 KC18 51 367 0.14 0.0877 0.0016 2.4895 0.0415 0.2061 0.0020 1375.5 34.0 1269.0 12.1 1208.2 10.5 KC19 80 468 0.17 0.0688 0.0014 1.4277 0.0265 0.1506 0.0014 893.2 40.2 900.6 11.1 904.5 8.0 KC20 102 533 0.19 0.0701 0.0013 1.4933 0.0258 0.1546 0.0014 932.5 37.4 927.7 10.5 926.5 8.1 4.2 稀土元素特征
卡尔恰尔矿床萤石的ΣREE值为39.4×10−6～57.19×10−6，LREE/HREE值为3.20～3.91，（La/Yb）N值为2.97～4.41，δEu值为0.39～0.42。小白河沟矿床萤石ΣREE值为44.73×10−6～65.79×10−6，LREE/HREE值为2.99～3.61，（La/Yb）N值为2.57～3.59，δEu值为0.38～0.44。库木塔什矿床萤石ΣREE值为41.5×10−6～81.01×10−6，LREE/HREE值为6.5～8.53，（La/Yb）N值为11.6～13.55，δEu值为0.46～0.55（表3）。
表 3 卡尔恰尔（KE）、小白河沟（XB）、库木塔什（KM）矿床的萤石、方解石稀土元素组成表（ 10−6）Table 3. Rare earth element data of fluorites and calcites from the Kaerqiaer, Xiaobaihegou and Kumutashi deposit矿物 样号 La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Y ΣREE LREE HREE LREE/HREE （La/Yb）N δEu δCe 萤
石KE-1 6.04 12.9 1.85 8.61 2.28 0.32 2.40 0.39 2.32 0.46 1.21 0.19 1.11 0.16 31.5 40.24 32.00 8.24 3.88 3.90 0.42 0.94 KE-2 6.40 12.2 1.86 8.31 2.29 0.32 2.34 0.38 2.28 0.46 1.18 0.18 1.04 0.16 32.0 39.40 31.38 8.02 3.91 4.41 0.42 0.86 KE-3 8.64 18.0 2.72 11.9 3.18 0.46 3.63 0.58 3.38 0.70 1.85 0.27 1.65 0.23 47.6 57.19 44.90 12.29 3.65 3.76 0.41 0.90 KE-4 5.76 12.9 1.92 9.40 2.78 0.37 2.96 0.51 2.89 0.58 1.58 0.23 1.39 0.21 47.3 43.48 33.13 10.35 3.20 2.97 0.39 0.95 XB-1 6.40 14.1 2.12 9.38 2.62 0.40 2.88 0.47 2.71 0.55 1.44 0.20 1.28 0.18 38.3 44.73 35.02 9.71 3.61 3.59 0.44 0.93 XB-2 7.81 18.8 2.98 15.0 4.26 0.57 4.80 0.78 4.56 0.93 2.42 0.36 2.20 0.32 68.6 65.79 49.42 16.37 3.02 2.55 0.38 0.96 XB-3 6.63 14.7 2.39 11.5 3.57 0.45 3.66 0.61 3.63 0.78 2.02 0.30 1.85 0.26 59.5 52.35 39.24 13.11 2.99 2.57 0.38 0.90 KM-1 16.5 32.7 4.21 11.7 2.89 0.51 2.71 0.44 2.37 0.46 1.19 0.16 1.02 0.15 31.1 81.01 72.51 8.50 8.53 11.6 0.55 0.94 KM-2 10.2 15.4 1.80 6.67 1.64 0.26 1.80 0.30 1.64 0.30 0.78 0.10 0.54 0.07 31.5 41.50 35.97 5.53 6.50 13.55 0.46 0.81 方
解
石KE-1 69.9 165 18.4 66.6 11.8 1.41 8.89 1.48 8.02 1.61 4.75 0.85 5.44 0.87 40.5 365.02 333.11 31.91 10.44 9.22 0.40 1.10 KE-2 77.7 180 20.7 74.6 13.7 1.62 10.3 1.77 8.53 1.78 5.13 0.85 5.76 0.98 46.6 403.42 368.32 35.10 10.49 9.68 0.40 1.08 KE-3 83.5 213 25.1 96.8 18.1 2.15 13.9 2.52 13.5 2.67 7.74 1.34 8.64 1.44 73.7 490.40 438.65 51.75 8.48 6.93 0.40 1.13 XB-1 103 245 28.5 98.8 18.5 2.26 15.8 2.60 13.2 2.80 8.31 1.48 9.74 1.58 70.5 551.57 496.06 55.51 8.94 7.59 0.39 1.09 XB-2 158 378 43.3 144 26.5 2.94 20.0 3.41 17.2 3.47 9.91 1.72 11.5 1.95 91.7 821.90 752.74 69.16 10.88 9.86 0.37 1.10 XB-3 80.1 202 22.8 83.3 15.4 1.82 12.3 2.21 10.8 2.26 6.97 1.26 8.42 1.39 64.4 451.03 405.42 45.61 8.89 6.82 0.39 1.14 KM-1 68.5 162 18.3 66.8 13.0 1.46 9.77 1.62 9.12 1.73 5.07 0.85 5.70 0.92 45.8 364.84 330.06 34.78 9.49 8.62 0.38 1.10 KM-2 74.7 160 18.9 64.3 12.6 1.28 8.87 1.59 7.70 1.51 4.21 0.72 4.72 0.72 37.2 361.82 331.78 30.04 11.04 11.35 0.35 1.02 KM-3 69.5 158 17.8 62.2 12.0 1.33 9.01 1.65 8.76 1.70 4.83 0.83 5.66 0.94 43.0 354.21 320.83 33.38 9.61 8.81 0.38 1.07 KM-4 75.1 163 19.9 65.2 12.4 1.31 9.17 1.56 7.65 1.54 4.29 0.74 4.88 0.76 40.8 367.50 336.91 30.59 11.01 11.04 0.36 1.01 卡尔恰尔矿床方解石ΣREE值为365×10−6～490×10−6，LREE/HREE值为8.48～10.49，（La/Yb）N值为6.93～9.68，δEu值为0.4。小白河沟矿床方解石ΣREE值为451×10−6～822×10−6，LREE/HREE值为8.89～10.88，（La/Yb）N值为7.59～9.86，δEu值为0.37～0.39。库木塔什矿床方解石ΣREE值为354×10−6～368×10−6，LREE/HREE值为9.49～11.04，（La/Yb）N值为8.62～11.35，δEu值为0.35～0.38（表3）。
4.3 Sr−Nd同位素
卡尔恰尔矿区6件萤石的Rb含量为0.03×10−6～0.06×10−6，Sr含量为340×10−6～343×10−6，Sm含量为1.77×10−6～1.83×10−6， Nd含量为6.40×10−6～6.82×10−6， 87Rb/86Sr值为0.00029～0.00046，87Sr/86Sr值为0.71005～0.71009，147Sm/144Nd值为0.1626～0.1682，143Nd/144Nd值为0.511917～0.512040（表4）。
表 4 卡尔恰尔（KE）、小白河沟（XB）、库木塔什（KM）矿床的萤石Sr−Nd同位素组成表Table 4. Sr−Nd isotopic composition of fluorites from Kaerqiaer, Xiaobaihegou and Kumutashi deposit样号 Rb/10-6 Sr/10-6 87Rb/86Sr 87Sr/86Sr Sm/10-6 Nd/10-6 147Sm/144Nd 143Nd/144Nd KE-1 0.05 343 0.00039 0.71005 1.77 6.55 0.1633 0.511987 KE-2 0.03 340 0.00029 0.71005 1.83 6.82 0.1626 0.511917 KE-3 0.04 342 0.00036 0.71007 1.79 6.48 0.1672 0.511932 KE-4 0.05 342 0.00041 0.71008 1.83 6.71 0.1655 0.511975 KE-5 0.06 342 0.00046 0.71009 1.78 6.40 0.1682 0.512040 KE-6 0.05 343 0.00046 0.71004 1.80 6.49 0.1678 0.512036 XB-1 0.26 264 0.00287 0.71025 2.62 9.36 0.1696 0.511930 XB-2 0.13 293 0.00131 0.71015 2.60 9.45 0.1664 0.511919 XB-3 0.18 368 0.00145 0.71025 3.26 11.88 0.1659 0.512039 XB-4 0.16 399 0.00118 0.71023 2.98 10.68 0.1688 0.512062 XB-5 0.21 375 0.00161 0.71036 3.94 14.15 0.1684 0.512061 KM-1 1.30 199 0.01878 0.70950 1.32 3.90 0.2044 0.512071 KM-2 0.02 261 0.00025 0.70952 1.29 3.88 0.2002 0.512061 KM-3 0.02 208 0.00029 0.70955 1.32 3.94 0.2024 0.512044 小白河沟矿区5件萤石的Rb含量为0.13×10−6～0.26×10−6，Sr含量为264×10−6～399×10−6，Sm含量为2.60×10−6～3.94×10−6，Nd含量为9.36×10−6～14.15×10−6，87Rb/86Sr值为0.00118～0.00287，87Sr/86Sr值为0.71015～0.71036，147Sm/144Nd值为0.1659～0.1696 ，143Nd/144Nd值为0.511919～0.512062（表4）。
库木塔什矿区3件萤石的Rb含量为0.02×10−6～1.3×10−6，Sr含量为199×10−6～261×10−6，Sm含量为1.29×10−6～1.32×10−6，Nd含量为3.88×10−6～3.94×10−6， 87Rb/86Sr值为0.00025～0.01878，87Sr/86Sr值为0.70950～0.70955，147Sm/144Nd值为0.2002～0.2044，143Nd/144Nd值为0.512044～0.512071（表4）。
5. 讨论
5.1 成岩时代与构造背景
本次研究工作对卡尔恰尔超大型萤石矿区碱长花岗岩进行LA−ICP−MS锆石U−Pb定年，获得成岩年龄为（455.8±2）Ma，表明其形成于中—晚奥陶世。一般岩浆热液型萤石矿的成矿时代稍晚于成矿岩体形成时代，卡尔恰尔一带各萤石矿区均见发育有肉红色碱长花岗岩脉体，萤石矿化主要赋存于岩体内外接触带附近，常见萤石−方解石细脉穿插于碱长花岗岩脉体中，碱长花岗岩因强烈热液活动而发育碳酸盐化、萤石化、硅化、绢云母化等矿化蚀变。同时库木塔什萤石矿的研究显示，该矿区碱长花岗岩体属高氟岩体[w（F）＞0.1%]，成岩年龄为（450±2.7）Ma（高永宝等，2021），与萤石共生的磷灰石LA−ICP−MS U−Pb年龄为（448±27）Ma（待见刊），均表明该区碱长花岗岩与萤石成矿具有密切的时空、成因关系。
区域上，阿尔金西南缘发育大规模早古生代岩浆岩，均为阿中地块与柴达木地块之间洋-陆转换过程中岩浆活动的产物（曹玉亭等，2010；孙吉明等，2012；杨文强等，2012；郭金城等，2014；徐旭明等，2014；董洪凯等，2014；康磊等，2016；过磊等，2019）。区域超高压变质岩研究表明，峰期变质时代集中于504～486 Ma，退变质作用时代为～450 Ma（Zhang et al.，2001；刘良等，2007；Liu et al.，2012）。卡尔恰尔周边邻近的花岗岩研究显示，帕夏拉依档沟一带二长花岗岩锆石U–Pb年龄为（460±4 ）Ma、正长花岗岩锆石U−Pb年龄为（455±3.6）Ma，形成于挤压体制向拉张体制转换的构造环境（张若愚等，2016，2018），清水泉一带花岗质岩石锆石U−Pb年龄为（451±4）Ma，形成于伸展构造背景（王立社等，2016），而镁铁−超镁铁质侵入体（465 Ma）暗示此时碰撞造山已转入伸展阶段（马中平等，2011）。上述研究均表明，中—晚奥陶世阿中地块和柴达木地块由挤压造山转变成伸展构造背景，卡尔恰尔超大型萤石矿带正是该时期岩浆活动的产物。另外，区域上发育大规模形成于早—中奥陶世碰撞造山阶段的伟晶岩脉群，如吐格曼锂铍稀有金属矿床的成矿黑云母二长花岗岩锆石U−Pb年龄为475～482 Ma，含矿伟晶岩脉中铌钽铁矿U−Pb年龄为（472±8）Ma、锡石U−Pb年龄为（468±8.7）Ma（徐兴旺等，2019；李杭等，2020；Gao et al.，2021）。综上，早古生代加里东期是区域萤石矿、锂铍稀有金属矿的重要成矿期，萤石成矿稍晚于锂铍稀有金属矿。
卡尔恰尔超大型萤石矿区片麻状钾长花岗岩获得LA−ICP−MS锆石U−Pb年龄为（914.5±4.1）Ma，表明其形成于新元古代早期。区域上，阿尔金西南缘已发现多处新元古代花岗（片麻）岩，可能与～900 Ma Rodinia超大陆事件引发的全球性岩浆活动相关，在空间分布上自西向东有江尕勒萨依、库如克萨依、清水泉、肖鲁布拉克、亚干布阳等地区花岗（片麻）岩呈带状分布，构成了一条与Rodinia超大陆汇聚相关的花岗岩带，正是这次构造事件使阿中地块和柴达木地块固结，该类同碰撞型花岗质片麻岩年龄大多为870～945 Ma（王超等，2006；校培喜等，2014；朱小辉等，2014；王立社等，2015；李琦等，2018；马拓等，2018；PAK Sang Wan，2019；曾忠诚，2020），卡尔恰尔萤石矿区的片麻状钾长花岗岩即为Rodinia 超大陆汇聚引发的岩浆活动的产物。
5.2 成矿流体特征
卡尔恰尔、小白河沟、库木塔什矿床萤石、方解石稀土元素特征表明，萤石、方解石的稀土元素配分曲线特征与碱长花岗岩、地层变质杂岩（黑云斜长片麻岩）较相似，均表现为右倾的LREE富集型，具有明显的负Eu异常特征（图7），表明萤石、方解石的稀土可能继承了岩体、地层的稀土配分模式。相比较，库木塔什矿区的萤石矿物具有更高的轻重稀土分馏程度。研究表明，萤石形成过程中REE含量的分布与结晶作用所处阶段有关，一般结晶早阶段的萤石富集 LREE，而结晶晚阶段萤石富集HREE（Moller et al.，1983；Schonenberger et al.，2008），卡尔恰尔、小白河沟、库木塔什矿床中萤石均表现为明显的LREE富集型，可知其均形成于结晶作用的早阶段。
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图 7 卡尔恰尔一带萤石矿床的稀土元素配分模式图碱长花岗岩与黑云母斜长片麻岩数据引自高永宝等（2021）与吴益平等（2021）Figure 7. Normalized REE patterns of fluorite deposits from the Kaerqiaer areaMoller等（1976） 在全球 150 多个萤石矿床研究基础上提出Tb/La−Tb/Ca双变量关系图解，用以判别萤石的成因类型，Tb/La原子数比值可反映成矿流体中稀土元素的分馏程度， Tb/Ca原子数比值可代表萤石结晶时的化学环境，具成因指示意义；卡尔恰尔、小白河沟、库木塔什矿床的萤石样品点均落在热液成因区域（图8a），表明该区萤石矿均为岩浆热液作用的产物。Y、Ho元素由于半径、电价相近，具有相似的地球化学性质，故Y/Ho值常作为一种重要参数来示踪成矿流体作用过程（Deng et al.，2014；Graupner et al.，2015；Mondillo et al.，2016），在富含 F 的成矿流体体系中，Y相对于 Ho 元素含量会较富集，两者比值一般大于28（Veksler et al.，2005）。Bau等（1995）在研究欧洲数个萤石矿床后提出La/Ho−Y/Ho关系图，可有效判别成矿流体来源，同源同期结晶的萤石Y/Ho 值不变而在图上表现为直线，而不同来源的萤石Y/Ho 值变化较大。卡尔恰尔、小白河沟、库木塔什矿床萤石样品在La/Ho−Y/Ho图中呈水平直线展布（图8b），且萤石样品Y/Ho 值（68～105）均远大于28，表明该区萤石矿为同源同期流体成矿，成矿流体是具有相同物化性质的富含F 的成矿流体。前已述及，不同矿区萤石、方解石的稀土元素配分模式具有一致性，同样是同源同期流体的反映。同时，图8中可看出卡尔恰尔、小白河沟矿床的萤石矿物Tb/La、La/Ho值相近，且与库木塔什矿床有明显区别，表明同处于卡尔恰尔断裂的卡尔恰尔、小白河沟矿床萤石的稀土分馏程度相近，而处于盖吉勒断裂的库木塔什萤石矿具有相对更高的轻重稀土分馏程度，可能反映同一成矿流体体系下不同断裂处分布的萤石矿床成矿环境略有差异。
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计算Tb/Ca原子数比采用CaF2中Ca的理论值（51.332 8%）Figure 8. Tb/Ca−Tb/La and La/Ho−Y/Ho diagram of fluorite from the Kaerqiaer areaδEu特征能记录成矿流体的氧化还原条件及温度，还原条件下形成的萤石因Eu2+具较大离子半径而不利于取代Ca2+进入到晶格中，导致Eu2+与稀土体系分离而形成Eu负异常，氧化条件下形成的萤石通常呈Eu正异常（Bau et al.，1992）。同时强烈的Eu负异常指示沉淀时成矿流体处于中低温环境（＜250 ℃），而当温度超过250 ℃时则表现出正Eu异常（Bau et al.，1992）。卡尔恰尔、小白河沟、库木塔什矿床中萤石、方解石的δEu＜0，表示沉淀时成矿流体处于还原条件下中低温环境。
5.3 成矿物质来源
在反映成矿物质来源的 La/Yb−ΣREE关系图中（图9a），不同矿区的萤石样品均落在沉积岩、钙质泥岩区及其附近，说明成矿物质可能一部分来自围岩。在（Y+La）−Y/La 关系图（图9b）中，样品均落在钙碱性花岗岩区域内，说明萤石矿在成因上确实与花岗岩的侵入有密切关系。显然，元素图解不仅展示了围岩地层对成矿物质的影响，还显示了岩浆热液对成矿作用的影响，且该区成矿碱长花岗岩体属高氟岩体[w（F）＞0.1%]，可为萤石成矿提供氟物质，萤石赋矿地层具有一定选择性，主要为阿尔金岩群中的黑云斜长片麻岩、碳酸盐岩等富钙质岩系。因此，初步认为成矿主要物质之一的 Ca 元素可能主要是由岩浆热液对地层的淋滤萃取而来，而F元素则可能主要来源于成矿岩体碱长花岗岩。
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图 9 卡尔恰尔一带萤石的La/Yb−ΣREE与（Y+La）−Y/La图解（底图据Allegre et al.，1978）Figure 9. La/Yb−ΣREE and (Y+La)−Y/La diagram of fluorite from the Kaerqiaer area萤石一般具有较低的Rb含量和较高的Sr含量，此次Sr、Nd同位素测试结果显示，卡尔恰尔一带萤石具有较低的Rb/Sr值，使得萤石的87Sr/86Sr组成可以直接代表成矿流体的87Sr/86Sr初始比值。卡尔恰尔矿区萤石的87Sr/86Sr值为0.71005～0.71009，小白河沟矿区萤石的87Sr/86Sr值为0.71015～0.71036，库木塔什矿区萤石的87Sr/86Sr值为0.70950～0.70955，可看出各矿区成矿流体的87Sr/86Sr值基本一致，反映了成矿流体中Sr可能同源。卡尔恰尔矿区萤石的143Nd/144Nd值为0.511917～0.512040，小白河沟矿区萤石的143Nd/144Nd值为0.511919～0.512062，库木塔什矿区萤石的143Nd/144Nd值为0.512044～0.512071，均介于上、下地壳143Nd/144Nd值（0.50071～0.51212）之间。在87Sr/86Sr −143Nd/144Nd图解中（图10），萤石样品点均落于上、下地壳之间区域，说明萤石成矿物质来源于地壳。
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图 10 卡尔恰尔一带萤石的87Sr/86Sr −143Nd/144Nd图解Figure 10. 87Sr/86Sr −143Nd/144Nd diagram of fluorite from the Kaerqiaer area6. 结论
（1）阿尔金卡尔恰尔超大型萤石矿带成矿与碱长花岗岩关系密切，萤石矿化主要赋存于岩体内外接触带附近，赋矿围岩主要为阿尔金岩群中的黑云斜长片麻岩、碳酸盐岩等富钙质岩系，矿体明显受北东向断裂构造控制，矿石类型主要有脉状、角砾状、块状、条带状矿石，矿物组成主要是萤石、方解石。
（2）卡尔恰尔超大型萤石矿区与成矿有关的碱长花岗岩成岩年龄为（455.8±2） Ma，结合前人研究，认为该萤石矿带形成于加里东期中—晚奥陶世，为挤压造山转变成伸展构造背景下岩浆活动的的产物。矿区片麻状钾长花岗岩成岩年龄为（914.5±4.1）Ma，形成于新元古代早期，与 Rodinia 超大陆汇聚事件有关。
（3）稀土元素特征显示，卡尔恰尔、小白河沟、库木塔什3个矿床的萤石、方解石稀土元素配分模式均为右倾的LREE富集型，具有明显负Eu异常，与成矿岩体、围岩地层十分相似，表明萤石、方解石的稀土可能继承了岩体、地层的稀土配分模式。各矿床萤石均为热液成因，表现出同源同期成矿流体的特征，成矿环境为还原条件下的中低温环境。
（4）各矿区萤石Sr−Nd同位素组成显示成矿物质来源于地壳，结合成矿特征，初步认为Ca可能主要来自于岩浆热液对地层的淋滤萃取，而F可能主要来源于成矿岩体碱长花岗岩。
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图 1 全球奥陶纪洋–陆格局示意图（据Scotese，2006；王立全等，2021）
Figure 1. Diagram of global ocean–continent pattern in Ordovician
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图 2 中国新疆–中亚地区大地构造单元划分图
a. 全球三大构造域分布简图；b. 中国新疆–中亚构造单元图
Figure 2. Division diagram of geotectonic units within Xinjiang (China)–Central Asia
表 1 中国新疆–中亚地区大地构造单元划分表
Table 1 Division framework of tectonic units within Xinjiang (China)– Central Asia
一级构造单元 二级构造单元 三级构造单元 代号 名称 代号 名称 代号 名称 Ⅰ 阿尔泰（–兴蒙）造山系 Ⅰ1 阿尔泰弧盆系 Ⅰ1-1 南阿尔泰陆缘弧（Pz1–C） Ⅰ1-2 南阿尔泰南缘增生弧（Pz2） Ⅱ 斋桑–额尔齐斯对接带 Ⅱ1 额尔齐斯断陷盆地（N–Q） Ⅱ2 额尔齐斯–斋桑结合带 Ⅱ2-1 卡尔巴–额尔齐斯增生楔（O–C） Ⅱ2-2 斋桑-布尔根蛇绿混杂岩带（Pz1–C） Ⅱ2-3 吉木乃–北准噶尔洋内弧（Pz2） Ⅲ 乌拉尔–哈萨克斯坦–天山造山系 Ⅲ1 东准噶尔弧盆系 Ⅲ1-1 三塘湖岛弧（O–C） Ⅲ1-2 卡拉麦里蛇绿混杂岩带（Pz1–C） Ⅲ2 东天山弧盆系 Ⅲ2-1 哈尔里克-大南湖岛弧（O–C） Ⅲ2-2 康古尔塔格蛇绿混杂岩带（Pz1–C） Ⅲ2-3 觉罗塔格岛弧（D–C） Ⅲ3 准噶尔–吐哈地块 Ⅲ3-1 准噶尔地块（AnNh） Ⅲ3-2 博格达裂谷盆地（C–P） Ⅲ3-3 吐哈地块（Pz1-C） Ⅲ4 塔尔巴哈台-西准噶尔弧盆系 Ⅲ4-1 萨雷扎尔–扎尔马岛弧（Pz1） Ⅲ4-2 塔尔巴哈台–赛米斯台岛弧（Pz2） Ⅲ4-3 唐巴勒–达拉布特蛇绿混杂岩带（O–C） Ⅲ4-4 阿克塔斯特-萨亚克蛇绿混杂岩带（Pz1-C） Ⅲ5 巴音沟–米什沟结合带 Ⅲ5-1 依连哈比尔尕蛇绿混杂岩带（Pz2） Ⅲ5-2 米什沟–冰达坂蛇绿混杂岩带（Pz1–C） Ⅲ6 莫因特–巴尔喀什–中天山地块 Ⅲ6-1 卡拉索尔–巴尔喀什–博罗科努陆缘弧（O-C） Ⅲ6-2 阿加德尔–莫因特–伊犁裂谷盆地（C–P） Ⅲ6-3 巴彦乌拉尔–扎拉依尔奈曼–中天山陆缘弧（O–C） Ⅲ7 希迭尔特–热尔套山–卡拉科尔结合带 Ⅲ7-1 希迭尔特-萨雷苏蛇绿混杂岩带（Pz1-C） Ⅲ7-2 热尔套山-卡拉科尔蛇绿混杂岩带（Pz1–C） Ⅲ8 图尔盖–塔拉斯地块 Ⅲ8-1 田吉兹湖–热兹卡兹甘陆缘弧（O–P） Ⅲ8-2 伊希姆–斯捷普尼亚克逆冲带（Ar？陆核） Ⅲ8-3 图尔盖-克孜勒库姆前陆盆地（Mz） Ⅲ8-4 卡拉套基底断隆带（K–Q右行走滑） Ⅲ8-5 塔拉斯–吉尔吉斯山增生弧（O–P） Ⅲ8-6 布坎套–费尔干纳陆缘弧（O–P） Ⅲ9 乌拉尔弧盆系 Ⅲ9-1 主乌拉尔蛇绿混杂岩带（Pz1–C） Ⅲ9-2 东乌拉尔岛弧（O–P） Ⅳ 东欧陆块区 Ⅳ1 前乌拉尔地块（An€） Ⅳ2 北里海残余盆地（Mz–E） Ⅴ 突厥斯坦–阿特巴什–南天山对接带 Ⅴ1 阿特巴什–南天山结合带 Ⅴ1-1 碱泉蛇绿混杂岩带（D–C） Ⅴ1-2 额尔宾山–库米什蛇绿混杂岩带（D–C） Ⅴ1-3 哈尔克山高压–超高压变质带（Pz1–C） Ⅴ1-4 阿特巴什–西南天山蛇绿混杂岩带（Pz1–C） Ⅴ2 乌兹别克–突厥斯坦结合带 Ⅴ2-1 乌兹别克–阿赖蛇绿混杂岩带（Pz1–C） Ⅴ2-2 曼格什拉克–萨雷卡梅什湖蛇绿混杂岩带（Pz1–C） 
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续表1 一级构造单元 二级构造单元 三级构造单元 代号 名称 代号 名称 代号 名称 Ⅵ 卡拉库姆–塔里木陆块区 Ⅵ1 敦煌陆块 Ⅵ1-1 柳园（阿克塔格）逆冲带（Pz2陆缘裂谷） Ⅵ1-2 敦煌断陷盆地（Cz） Ⅵ1-3 阿尔金北逆冲带（Ar2-3陆核） Ⅵ2 塔里木陆块 Ⅵ2-1 库鲁克塔格逆冲带（Pz1陆缘盆地） Ⅵ2-2 西南天山–霍拉山逆冲带（Pz1陆缘裂谷） Ⅵ2-3 塔里木前陆盆地（Mz） Ⅵ2-4 铁克里克逆冲带（Pt裂谷盆地） Ⅵ3 卡拉库姆陆块 Ⅵ3-1 撒马尔罕–克孜勒苏河逆冲带（Pz1陆缘盆地） Ⅵ3-2 卡拉库姆–马扎里沙里夫前陆盆地（Mz） Ⅵ3-3 法扎巴德–桑格沃尔德逆冲带（C–P陆缘裂谷） Ⅵ3-4 兴都库什岩浆弧（Mz） Ⅶ 北帕米尔–阿尔金–昆仑造山系 Ⅶ1 阿尔金弧盆系 Ⅶ1-1 红柳沟-拉配泉蛇绿混杂岩带（Pz1） Ⅶ1-2 阿中地块（AnNh） Ⅶ1-3 阿帕–茫崖蛇绿混杂岩带（Pz1） Ⅶ1-4 江尕孜萨依–巴什瓦克高压变质岩带（Pt3–Pz1） Ⅶ2 柴达木地块（Cz断陷盆地） Ⅶ3 东昆仑弧盆系 Ⅶ3-1 祁漫塔格北坡–夏日哈岩浆弧（O–S） Ⅶ3-2 祁漫塔格蛇绿混杂岩带（Pz1） Ⅶ3-3 北昆仑岩浆弧（O–T2） Ⅶ3-4 乌鲁赛赤河弧间裂谷盆地（C–P） Ⅶ4 北帕米尔–西昆仑弧盆系 Ⅶ4-1 恰尔隆–库尔良弧后裂谷盆地（C–P） Ⅶ4-2 北帕米尔–柳什塔格岛弧（Pz–T2） Ⅶ4-3 库地–其曼于特蛇绿混杂岩带（Pz1） Ⅶ4-4 奥依且克–塔木其岛弧（O–S） Ⅷ 塔尼马斯–康西瓦–南昆仑对接带 Ⅷ1 南昆仑结合带 Ⅷ1-1 东昆仑南坡增生杂岩带（Pt3–Pz1） Ⅷ1-2 木孜塔格–布喀达坂蛇绿混杂岩带（Pz2–T2） Ⅷ2 塔尼马斯-康西瓦结合带 Ⅷ2-1 康西瓦–苏巴什蛇绿混杂岩带（Pz） Ⅷ2-2 塔尼马斯（Tanymas）蛇绿混杂岩带（Pz2） Ⅸ 中帕米尔（–羌塘–三江）造山系 Ⅸ1 喀拉塔格–巴颜喀拉地块 Ⅸ1-1 巴颜喀拉前陆盆地（T3） Ⅸ1-2 喀拉塔格前陆盆地（T3） Ⅸ2 中帕米尔–甜水海地块（AnNh） Ⅹ 巴扎拉克–鲁山普哈特（–班公湖–双湖–怒江）对接带 Ⅹ1 巴扎拉克–鲁山普哈特结合带 Ⅹ1-1 鲁山普哈特（Rushan–Pshart）蛇绿混杂岩带（Pz2–K？） Ⅹ1-2 潘焦–巴扎拉克蛇绿混杂岩带（Pz2-K？） Ⅺ 南帕米尔–拉达克
（–冈底斯–喜马拉雅）造山系Ⅺ1 南帕米尔（–冈底斯）弧盆系 Ⅺ1-1 南帕米尔（–昂龙岗日–班戈–腾冲）岩浆弧 Ⅺ1-2 什约克（Shyok）（–狮泉河–申扎–嘉黎）蛇绿混杂岩带 Ⅺ1-3 科西斯坦–拉达克（–冈底斯–察隅）岩浆弧 Ⅺ2 喀布尔–印度河（–雅鲁藏布江）结合带 Ⅺ2-1 印度河蛇绿混杂岩带（T–K） Ⅺ2-2 喀布尔蛇绿混杂岩带（T–K） Ⅺ3 白沙瓦–斯里那加（–喜马拉雅）地块（An€） Ⅻ 印度陆块区 Ⅻ1 杰赫勒姆前陆盆地（Cz）
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