Conglomerate source and source area property of Lower Triassic Hongshuichuan Formation in the East Kunlun Mountains: Evidence from conglomerate characteristics and U-Pb dating
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摘要:
东昆仑东段下三叠统洪水川组主要分布于东昆南断裂带和东昆中断裂带之间的红水川—托索河一带。笔者分别对出露于宝日禾日俄地区和可可沙地区洪水川组底部层位砾岩的砾石成分、磨圆度和粒度进行综合统计对比分析。结果显示：可可沙地区砾石成分主要为灰岩和变质岩，宝日禾日俄地区砾石成分主要为花岗岩和变质岩。从宝日禾日俄地区花岗岩砾石中获得的LA-ICP-Ma锆石U-Pb年龄为（464.9±9.3）Ma（MSWD=2.9）。砾石特征表明可可沙地区物源来自可可沙地区下伏地层哈拉郭勒组，而宝日禾日俄地区物源主要为早古生代岩浆岩，表明洪水川组底部层位物源主要为加里东期弧岩浆岩，而晚滇西—印支期弧岩浆岩并未提供沉积物质。结合前人资料认为，布青山—阿尼玛卿古特提斯洋于晚二叠世开始向北俯冲，洪水川组为一套弧前盆地的沉积产物，早三叠世早期布青山—阿尼玛卿古特提斯洋处于向北俯冲初始阶段。
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关键词:
- 东昆仑东段 /
- 洪水川组 /
- 砾岩 /
- 锆石U-Pb年龄 /
- 布青山-阿尼玛卿古特提斯洋
Abstract:The lower Hongshuichuan Formation is mainly distributed around Tuosuo River between Middle Kunlun orogen and South Kunlun orogen in eastern Kunlun Mountains. In this paper, the authors made a comparative study of the conglomerate of Lower Hongshuichuan Formation distributed in Baoriherie area and Kekesha area in components, psephicity and granularity of gravel. The results show that the main components of the gravel are limestone and metamorphic rock in Kekesha area. The main components of gravel in Baoriherie area are granite and metamorphic rock. LA-ICP-MS zircon U-Pb dating of granite yielded magmatic crystallization age of(464.9 ±9.3) Ma(MSWD=2.9) from Baoriherie area. The characteristics of gravel show that the source of the Kekesha area is Halaguole Formation in Qingshuiquan area, whereas the source of the Baoriherie area is Caledonian magmatic rock. These data indicate that the source of Lower Hongshuichuan Formation is Caledonian magmatic rock rather than arc granite of late Hercynian-Indosinian period. Combined with previous data, the authors hold that the Buqingshan-A'nimaqing Ocean began the northward subduction in late Permian, and the Hongshuichuan Formation was a set of sedimentary products in the fore-arc basin. It is held that Buqingshan-A'nimaqing Ocean began its subduction in early Triassic.
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Keywords:
- East Kunlun /
- Hongshuichuan Formation /
- conglomerate /
- Buqingshan-A'nimaqing Ocean /
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1. 引言
祁连山位于华北板块西南缘，与秦岭、昆仑一起构成中国大陆内部巨型的中央造山带，是中国大陆主要造山带之一。北祁连造山带雄踞于河西走廊之南，成为青藏高原的东北界，东南与西秦岭相连，西北被阿尔金山截断（葛肖虹等，1999；杨永春等，2019；图 1a）。前人通过大量岩石学、沉积等研究对北祁连洋盆的俯冲极向做过研究，主要形成了双向俯冲（肖序常等，1978；王荃等，1981；左国朝等，1987；吴才来等，2010）、向北俯冲（许志琴等，1994；夏林圻等, 1996, 1998；张建新等, 1997, 1998；夏林圻等，2016）、向南俯冲（宋述光，1997；刘传周等，2005），目前尚无统一的认识。已有研究表明，通过花岗岩类地球化学特征及同位素年代学的研究可以提供有关其形成的大地构造背景信息，可以作为地质构造示踪剂（徐卫东等，2007；秦海鹏，2012）。目前，在北祁连山造山带毛藏寺、银硐梁、大野口等多处发现有埃达克岩或埃达克质岩石，这类岩石为区域构造背景研究提供了依据，本文试图利用车路沟岩体对北祁连构造演化进行研究。
研究区位于北祁连造山带西段，区内广泛发育寒武系黑茨沟组裂谷火山岩（王晓伟等，2018）、奥陶系阴沟群和扣门子组岛弧-弧后扩张脊型火山岩以及志留系复理石沉积，分布有俯冲混杂岩带，具有典型的沟弧盆体系（夏林圻等，2001），车路沟岩体位于前人所划分的奥陶系岛弧火山岩-沉积岩系中。前人对岩体特征和时代做了一些研究（杨建国等，2003；宋忠宝等，2004；贾群子等，2005），但多围绕其与金成矿作用方面的研究，宋忠宝等（2005）通过对车路沟中英安斑岩进行年代学、地球化学研究，认为车路沟岩体属于碰撞型花岗岩类，形成于碰撞作用晚期。本文通过对车路沟岩体中英云闪长玢岩的岩石学、地球化学、锆石U-Pb年代学等方面的研究，分析其岩石成因，揭示其形成时的构造背景，为北祁连造山带构造演化提供约束。
2. 区域地质概况
研究区大地构造位置属北祁连早古生代造山带西段之西端（杨建国等，2003），距离北祁连造山带与阿尔金断裂交汇部位4 km。区域上地层北部有古元古界敦煌岩群零星分布外，以古生界为主，主要有寒武系、奥陶系、志留系，其次为石炭系。区域上侵入岩较为发育，以明芨芨沟岩体、青石峡岩体、青山岩体和车路沟岩体为主，分布范围较大，多呈岩株状分布，展布方向和区域构造线方向基本一致，多呈北西、北西西向。
车路沟岩体位于北祁连造山带西段，紧邻阿尔金走滑断裂南侧，出露面积较大（图 1b），自阴凹大泉至照壁山一带广泛分布，多侵入于奥陶系扣门子组中，岩体被断裂构造破坏严重，形态呈不规则块状，呈岩基状东西向条带状分布，边界明显的受控于断裂构造（夏林圻等，2001），多与地层呈断层接触，接触部位具明显的片理化，反映岩体的形成与板块俯冲、碰撞和造山带上不同的块体之间的构造作用密切相关（吴才来等，2010）。
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图 1 车路沟一带地质简图1—第四系冲、洪积物；2—二叠系砂岩；3—石炭系砂岩；4—志留系复理石建造；5—奥陶系扣门子组火山岩系；6—奥陶系中堡群火山-碎屑岩系；7—奥陶系阴沟群火山岩系；8—石英二长闪长岩；9—英云闪长玢岩；10—闪长玢岩；11—实测断裂构造；12—同位素测年样品采样位置；13—岩石全分析样品采样位置Figure 1. Regional geological map of the Chelugou pluton1- Quaternary; 2- Permian sandstone; 3- Carboniferous sandstone; 4- Silurian flysch formation; 5- Volcanic rocks of Ordovician Koumenzi Formation; 6- Volcanic clastic rocks of Ordovician Zhongbu Group; 7- Volcanic rocks of Ordovician Yingou Group; 8- Quartz monzodiorite; 9- Quartz mica dioritic porphyry; 10-Diorite porphyry; 11-Fault; 12-Sampling position for isotope dating; 13- Sampling position for rock analysis3. 岩石学特征
车路沟岩体主要由英云闪长玢岩、闪长玢岩组成，局部为石英闪长玢岩、英云闪长岩等，岩体与地层接触部位产出车路沟金矿、昌马金矿等多个金矿床。主要岩石特征如下：
英云闪长玢岩，灰白色，斑状结构，基质微粒花岗结构，块状构造。斑晶主要是斜长石和角闪石（10%~15%），粒径0.25~1.90 mm。斜长石为自形—半自形晶板条状，角闪石多为长柱状，斜长石具高岭土化、绿帘石化。基质成分由长石、角闪石、石英和不透明矿物组成，粒径小于0.10 mm（图 2a，b）。
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图 2 车路沟岩体野外露头及显微照片（a，b英云闪长玢岩；c，d闪长玢岩）Figure 2. Field photos and representative microphotographs of quartz diorite porphyry (a, b) and diorite porphyry (c, b) from the Chelugou pluton闪长玢岩，浅灰黑色，斑状结构，显微粒状半自形柱状粒状结构，块状构造。斑晶为角闪石及少量斜长石，大小一般1~5 mm，星散状分布，含量15%~20%。基质为斜长石、石英、角闪石，大小一般0.1~0.2 mm，少0.02~0.1 mm（细），部分0.2~0.3 mm（细），杂乱分布。具绢云母化、绿帘石化、碳酸盐化（图 2c，d）。
4. 样品采集及分析方法
本次工作分别在岩体的不同地方采集了4件新鲜的岩石样品，做了岩石地球化学全分析，所采岩石类型均为英云闪长玢岩，样品重量均大于2 kg，利用玛瑙球磨机研磨至200目进行分析，样品加工由河北省区域地质调查研究所实验室承担，样品的加工过程均是在无污染设备中进行。在岩体西部二家台一带采集了新鲜英云闪长玢岩岩石样品1件，样品重量为11.3 kg，以挑选锆石进行U-Pb同位素测年。
锆石分选、制靶、透反射光拍照和阴极发光拍照均在廊坊诚信地质服务有限公司完成。锆石的激光剥蚀电感耦合等离子体质谱(LA-ICP-MS)原位U-Pb定年在中国地质调查局西安地质调查中心自然资源部岩浆作用成矿与找矿重点实验室完成。激光剥蚀系统为GeoLas Pro，ICP-MS为Agilent 7700x。激光剥蚀过程中采用氦气作载气、氩气为补偿气以调节灵敏度。对分析数据的离线处理（包括对样品和空白信号的选择、仪器灵敏度漂移校正、元素含量及U-Th-Pb同位素比值和年龄计算）采用软件Glitter 4.4完成，详细仪器参数和测试过程参见李艳广等（2015）。采用锆石标准91500作为标样进行同位素分馏校正。对于与分析时间有关的U-Th-Pb同位素比值漂移，利用91500的变化采用线性内插的方式进行了校正。锆石样品的U-Pb年龄谐和图绘制和年龄权重平均计算均采用Isoplot Exver 3完成。
5. 分析结果
5.1 地球化学特征
从表 1可知，岩石中SiO2含量60.37% ~66.73%，平均63.75%，Al2O3含量15.65%~16.45%，平均16.01%，Na2O/K2O值7.47~9.96，平均8.38，Na2O高于K2O数倍，P2O5含量SiO2呈反比，与表明其源于贫钾的玄武质岩石（张旗等，2002），为I型花岗岩，里特曼指数（σ43）1.28~2.22，为低钾富钠钙碱性花岗岩，A/CNK为0.90~1.00，平均0.93，为准铝质，且经CIPW标准矿物计算出现刚玉，说明具有活动大陆边缘环境I-S过渡型花岗岩的特征（秦海鹏，2012）。MgO含量1.78~3.95，平均2.63；分异指数DI大于59.55，分异程度中等略高。
表 1 车路沟岩体主量元素（%）、微量元素（10-6）分析结果Table 1. Analytical results of major elements (%) and trace elements (10-6) of the Chelugou rock mass
从微量元素原始地幔标准化蛛网图中可以看出（图 3、表 1），大离子亲石元素（LILE）富集Ba、Sr、Hf，高场强元素（HFSE）明显贫Nb、Ti、Yb，相对富集Zr。稀土总量33.40×10-6~39.27×10-6，平均35.99×10-6，远低于中性岩稀土总量196×10-6和花岗岩稀土总量290×10-6。LREE/HREE值3.95~6.51，轻稀土元素较富集，HREE含量较低，平均6.01×10-6，Y含量7.46×10-6~13.44×10-6，Yb含量0.58×10-6~1.36×10-6，（La/Yb）N值2.87~6.29（表 1），稀土元素球粒陨石标准化分配曲线为右倾型（图 3），轻、重稀土元素分异明显，δEu值1.23~1.49，Eu呈正异常，说明岩浆源区无残留斜长石。稀土元素特征与埃达克岩亏损重稀土、低Y、Yb及正铕异常的特征相符（Defant et al., 1990）。
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图 3 车路沟岩体稀土元素配分模式（a）和微量元素原始地幔标准化蛛网图（b）Figure 3. Chondrite-normalized REE patterns (a) and primitive mantle-normalized trace element patterns (b) of the Chelugou pluton5.2 U-Pb年代学特征
锆石多呈长柱状或菱形柱体，为典型的锆石晶体形状，多呈自形、半截状，锆石具有明显的震荡环带，部分锆石内部有继承核存在，生长纹路清晰，为典型的岩浆锆石（图 4），本次利用LA ICP-MS对锆石进行了测试，锆石Th/U比值0.07~1.73，平均0.57，具岩浆锆石的特征（表 2）。测试结果中，共有12个测试点具有谐和年龄，表面年龄分为2组（图 5），第一组有5个点，表面年龄406.2~422.9 Ma，获得加权平均年龄（416.6±9.5）M a，MSWD =1.7；第二组有7个点，表面年龄457.7~465 Ma，获得加权平均年龄（462.1±3.8）Ma，MSWD=0.15。第二组年龄应是岩浆侵位结晶年龄，第一组年龄可能反映了后期的岩浆热事件。
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图 4 车路沟英云闪长玢岩中锆石CL图像及LA ICP-MS测点位置Figure 4. Cathodoluminescence images of zircons from quartz mica dioritic porphyry表 2 车路沟岩体中LA ICP-MS锆石U-Pb同位素测年结果Table 2. Zircon LA ICP-MS U-Pb isotopic data of the Chelugou pluton
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图 5 车路沟岩体中LA ICP-MS锆石U-Pb年龄谐和图及加权平均年龄图Figure 5. Zircon LA-ICP-MS U-Pb concordia diagrams and weighted average age of the Chelugou pluton5.3 年代学讨论
宋忠宝等（2005）在车路沟岩体中采集英安斑岩同位素样品进行了U-Pb同位素年龄为（427.7±4.5）Ma，本次工作在开展区内地质调查过程中，结合薄片鉴定认为，前人所认为的英安斑岩即为车路沟岩体中的闪长玢岩，贾群子等（2007）在岩体西部二家台沟采集英云闪长玢岩进行了单颗粒锆石U-Pb年龄测定，获得加权平均年龄为（445.6±3.2）Ma，认为该年龄是锆石的结晶年龄，接近岩体的形成年龄。
结合前人测试结果，笔者认为车路沟岩体可能为复式岩体或者岩浆演化经历了较长的时间，岩体中两种岩性整体为同源岩浆演化，岩体演化早期阶段为英云闪长玢岩为主，伴随有中酸性—中性岩浆的分异，后期演化为闪长玢岩。因此，该岩体就位时间为（462.1±3.8）Ma，为中奥陶世。
6. 讨论
埃达克岩是一套具有特定地球化学特征的钙碱性中酸性喷出/侵入岩（Defant et al., 1990），具有高SiO2（≥56%）、高铝（Al2O3≥15%）、富钠（Na2O＞K2O）、高Sr（＞400×10-6）、低Y（＜18×10-6）和Yb（＜1.9×10-6）以及不明显的Eu异常等地球化学特征。车路沟岩体SiO2含量为60.37% ~66.31%，Al2O3含量15.72%~16.45%，Na2O含量4.86%~6.19%，K2O含量0.62%~0.72%，Na2O/K2O为7.47~9.96，Sr含量299.52×10-6~525.85×10-6，Y含量7.46×10-6~13.44×10-6，Yb含量0.58×10-6~1.36×10-6，Sr/Y值为30.90~70.48。该岩体轻稀土富集，轻重稀土分馏明显，亏损高场强元素，同时在Y-Sr/Y图解中（图 6a）全部落入埃达克岩区域。上述特征表明，车路沟岩体与典型埃达克岩的特征一致（Defant et al., 1990, 2002；毛启贵等, 2010；Zheng et al., 2018）。
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图 6 车路沟岩体Y/Sr-Y和A/MF-C/MF图解Figure 6. Sr/Y-Y(a)and A/MF-C/MF(b)diagrams of the Chelugou pluton埃达克岩最早被认为是由于年轻的俯冲大洋板片在榴辉岩相下熔融形成火山岩和侵入岩（Defant et al., 1990），随着研究的深入，越来越多与埃达克岩相似地球化学属性的岩石被发现。目前对埃达克岩的成因模式主要有以下4种：（1）俯冲洋壳的部分熔融，随后与上覆楔形地幔橄榄岩发生反应形成埃达克岩（Defant et al., 1990, 2002；Kay，1993；Martin et al., 2005；Wang et al., 2007, 2008a；Tang et al., 2010；毛启贵等, 2010；Zheng et al., 2018）；（2）含水玄武质岩浆高/低压条件下发生结晶分异作用（Castillo et al., 1999, 2012；Macpherson et al., 2006）；（3）受玄武质岩浆底侵作用或俯冲大陆地壳发生部分熔融产物（Wang et al., 2008b；Lai et al., 2013）；（4）增厚下地壳拆沉作用导致部分熔融产生的流体和地幔橄榄岩相互作用形成的高Mg#埃达克岩（Rudnick et al., 1995；Wareham et al., 1997；Chung et al., 2003；Gao et al., 2004；Wang et al., 2006；朱涛等，2014；王楠等，2016）。
车路沟岩体岩石地球化学研究表明，K2O含量0.62%~0.72%，Na2O/K2O值7.47~9.96，与洋壳特征相似，其岩石类型为富Na2O的钙碱性岩浆，这与俯冲洋壳熔融形成的埃达克岩一致（Defant et al., 2002）。岩体具较高的Cr（27.30 × 10-6~70.79 × 10-6）、Ni（27.01×10-6~46.65×10-6）及Mg#值（52.24~59.79），应该是板片俯冲熔融产生的埃达克岩浆与地幔楔相互作用导致MgO加入的结果。车路沟岩体以较低的Nb（1.92×10-6~2.15×10-6）含量与洋岛玄武岩（＞20×10-6）Nb值存在明显的差异，反映其并非含水玄武质岩浆结晶分异而成。俯冲大陆地壳发生部分熔融产生的埃达克岩，具有明显的富钾特征（K2O＞Na2O），较高的Th含量、Th/U、Th/Ba和Rb/Ba比值，以及Sr的弱异常。车路沟岩体具富钠特征（Na2O＞K2O），具有较低的Th含量（0.68 × 10-6~1.57×10-6），以及较低的Th/Ba（0.001~0.004）和Rb/Ba（0.02~0.04）比值和较高的Sr含量（299.52 ×10-6~525.85×10-6），可与俯冲大陆地壳发生部分熔融产生的埃达克岩相区别。拆沉下地壳熔融产生的埃达克岩浆在上升过程中与地幔橄榄岩发生反应从而获得较高的Mg#，拆沉下地壳来源的埃达克岩通常含有壳源继承锆石，而本次研究中锆石结构均一，没有继承性锆石。因此，车路沟岩体应为俯冲洋壳熔融形成的埃达克岩，而非其他成因的埃达克岩。
地球化学特征表明车路沟岩体源于贫钾的玄武质岩石，通过A/MF-C/MF图解对岩浆成因进行了判别，所有数据均落入基性岩的部分熔融（图 6b），推测岩浆来源与新生基性火山岩的部分熔融有关（Zhang et al., 2017），这一点，在野外地质分布特征中也可以分辨，岩体大部分侵入于奥陶系扣门子组弧后扩张型火山岩中，但未见到志留纪复理石建造中有侵入特征，说明其形成与俯冲作用有关。车路沟岩体δEu变化范围为1.10~1.49，平均1.285，表明在岩浆分离结晶过程中斜长石不占据元素总分配系数的主导地位，岩浆中应残留石榴子石或者角闪石。前人研究认为，岩浆源区中以角闪石为残留相时，形成的熔体具轻微上凹的HREE配分模式，且Y/Yb比值一般接近10；当源区中以石榴子石为残留相时，形成的熔体具有倾斜的HREE配分模式同时其Y/Yb比值明显大于10（Rollinson, 1993; 高永丰等，2003）。车路沟岩体Y/Yb比值为9.91~12.90，平均为11.34，稀土配分模式显示（图 3），其为基本向右倾斜的HREE配分模式，表明岩浆岩区残留相以石榴子石为主，由此推测车路沟埃达克岩体来源于基性玄武质岩浆的部分熔融。
在（Y+Nb）-Rb和Y-Nb构造判别图上（图 7），车路沟岩体分别落入火山弧花岗岩（VAG）和火山弧+同碰撞花岗岩（VAG+Sny+COLG）区域内，反映出与火山弧花岗岩的亲缘性。同时，岩体Nb、Ti的负异常其形成于俯冲背景下，Cr、Ni正异常代表有地幔物质的参与。由此推测，车路沟岩体可能是俯冲板片流体交代地幔楔诱发地壳富含石榴石相的基性玄武岩质岩石部分熔融，并在上升过程中混染了火山弧物质所形成的埃达克岩。
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图 7 车路沟岩体（Y+Nb）-Rb（a）和Y-Nb图解（b）Figure 7. (Y+Nb)-Rb(a)and Y-Nb(b)diagrams of the Chelugou pluton区域构造研究表明，北祁连从古元古代中期开始，大陆岩石圈拉伸、减薄，并发生裂谷化(左国朝等，1987；夏林圻等, 1996, 2000；葛肖虹等，1999); 至新元古代，裂谷作用进一步加强，发育以双峰式火山岩为特征的大陆裂谷火山作用；到晚寒武世，最终发生大陆裂解和分离，形成北祁连早古生代洋盆，于奥陶纪北祁连洋盆进入俯冲消减和弧后盆地协同演化阶段，发育大量岛弧和弧后盆地火山岩（左国朝等，1987；夏林圻等, 1991, 1996；葛肖虹等，1999；张旗等，2000；Xia et al., 2003；曾建元等，2007；夏小洪等，2010；Song et al., 2013)，至445~424 Ma，洋盆闭合进入陆内碰撞和深俯冲过程(Xia et al., 2003；吴才来等，2006；Zhang et al., 2007)。夏林圻等认为，北祁连加里东造山带是在前寒武纪基底之上发生拉张（679~574 Ma）, 至寒武纪末期到早奥陶世（522~495 Ma）形成洋盆，奥陶纪（469~445 Ma）自南西向北东往华北大陆板块之下俯冲，大洋板块持续俯冲致使洋盆闭合（445~428 Ma）。
前人在北祁连造山带中段毛藏寺、北祁连东段银硐梁、北祁连走廊南山北坡大野口均发现了埃达克岩，上述埃达克岩体同位素年龄集中在446~455.8 Ma，均为北祁连早古生代沟弧盆构造环境的产物(王金荣等，2006；赵辛敏等，2018；唐卓等，2018)。本文获得的车路沟岩体的结晶年龄为（462.1±3.8）Ma，与前人研究认为祁连洋向北俯冲的时间吻合，说明车路沟岩体是在奥陶纪祁连洋自南西往北东持续向华北板块之下俯冲过程中形成的。
如前文所述，车路沟岩体具埃达克岩特征，是奥陶纪时期与祁连洋持续向华北板块俯冲作用有关的俯冲洋壳部分熔融和壳幔岩浆混合成因的花岗岩。
7. 结论
（1）车路沟岩体为准铝质低钾钙碱性系列，具有富硅、富铝、富钠、高Mg#、高Sr、高Sr/Y和低HREE、低Y、低Yb的特征，具典型埃达克岩的地球化学特征。
（2）车路沟岩体中英云闪长玢岩的锆石LA -ICP-MS U-Pb测年结果表明，其结晶年龄为（462.1±3.8）Ma，属中奥陶世。
（3）根据岩石学、岩石地球化学研究，结合前人区域构造研究成果，推测车路沟岩体为奥陶纪祁连洋持续向华北板块俯冲，诱使俯冲洋壳部分熔融形成的埃达克岩。
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图 1 东昆仑造山带东段洪水川—可可沙地区区域地质简图
1—第四系；2—古近系；3—中三叠统闹仓坚沟组；4—下三叠统洪水川组第六段；5—下三叠统洪水川组第五段；6—下三叠统洪水川组第四段；7—下三叠统洪水川组第三段；8—下三叠统洪水川组第二段；9—下三叠统洪水川组第一段；10—下三叠统洪水川组c段；11—下三叠统洪水川组b段；12—下三叠统洪水川组a段；13—上二叠统格曲组；14—中下二叠统马尔争组；15—上石炭—下二叠统树维门科组；16—上石炭统浩特洛哇组；17—下石炭统哈拉郭勒组；18—下古生界纳赤台岩群；19—新元古界万宝沟岩群；20—中元古界长城系小庙岩组；21—中元古界苦海岩群；22—古元古界白沙河岩组；23—早三叠世钾长花岗岩；24—早三叠世二长花岗岩；25—早三叠世花岗闪长岩；26—奥陶纪花岗闪长岩；27—寒武纪石英闪长岩；28—超镁铁质岩；29—地质界线；30—角度不整合；31—一般断裂；32—边界断裂；33—韧性剪切带；34—东昆南断裂带；35—砾石采集点；36—同位素年龄样品采集点
Figure 1. Simplified geological map of the Hongshuichuan Formation in the East Kulun ogrogenic belt
1-Quaternary; 2-Palaeogene; 3-Middle Triassic Naocangjiangou Formation; 4-Sixth section of Lower Triassic Hongshuichuan Formation; 5- Fifth section of Lower Triassic Hongshuichuan Formation; 6- Fourth section of Lower Triassic Hongshuichuan Formation; 7-Third section of Lower Triassic Hongshuichuan Formation; 8- Second section of Lower Triassic Hongshuichuan Formation; 9- First section of Lower Triassic Hongshuichuan Formation; 10-The c section of Lower Triassic Hongshuichuan Formation; 11-The b section of Lower Triassic Hongshuichuan Formation; 12- The a section of Lower Triassic Hongshuichuan Formation; 13-Upper Permian Gequ Formation; 14-Middle—Lower Permian Maerzheng Formation; 15-Upper Carboniferous—Middle—Lower Permian Shuweimenke Formation; 16-Upper Carboniferous Haoteluowa Formation; 17-Lower Carboniferous Halaguole Formation; 18-Lower Palaeozoic Naijtai Group; 19-Neoproterozoic Wanbaogou Group; 20-Mesoproterozoic Xiaomiao Formation; 21-Neoproterozoic Kuhai Group; 22-Paleoproterozolc Baishahe Formation; 23-Early Triassic moyite; 24- Early Triassic Monzonitei granite; 25- Early Triassic granodiorite; 26—Ordovician granodiorite; 27-Cambrian Quartz diorite; 28-Ultramafic rock; 29-Geological boundary; 30-Angular unconformity; 31-Fault; 32-Boundary fault; 33—Ductile shear zone; 34-South Kunlun orogen; 35-Gravel collection site; 36-Isotope age sampling site
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图 2 洪水川组砾岩层野外宏观照片
γ—花岗岩；m—变质岩；ss—砂岩；p—泥质岩
Figure 2. Macroscopic characteristics of Hongshuichuan Formation conglomerate layer
γ-Granite; m-Metamorphic rock; ss-Sandstone; p-Pelite
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图 3 南带宝日禾日俄地区洪水川组第二段地层柱状图及砾石特征
1—泥晶灰岩；2—粉砂质页岩；3—粉砂质泥岩；4—钙质长石石英砂岩；5—长石石英砂岩；6—长石砂岩；7—含砾长石石英砂岩；8—含砾长石砂岩；9—砾岩
Figure 3. The histogram and the gravel characteristics of second section in southern Hongshuichuan Formation
1-Micrite; 2-Silty shale; 3-Sily mudstone; 4-Calcareous feldspathic quartz arenite; 5-Feldspathic quartz arenite; 6-Arkose; 7-Shingly feldspathic quartz arenite; 8-Shingly arkose; 9-Conglomerate
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图 4 北带可可沙地区洪水川组a段地层柱状图及砾石特征
1—灰岩；2—白云质灰岩；3—钙质粉砂岩；4—含砾长石砂岩；5—砾岩
Figure 4. The histogram and the gravel characteristics of a section in northern Hongshuichuan Formation
1-Limestone; 2-Dolomite limestone; 3-Calcareous siltstone; 4-Shingly arkose; 5-Conglomerate
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图 5 洪水川组砾岩综合累计频率曲线图及频率直方图
Figure 5. The curvilinear diagram and the histogram of size-frequency distribution from conglomerate layer in Hongshuichuan Formation
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图 6 洪水川组下部层位砾石岩性统计柱状图
Figure 6. The histogram of gravel lithology in Hongshuichuan Formation
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图 7 洪水川组第二段花岗岩砾石手标本及显微照片（左—单偏光；右—正交偏光）
Pl—斜长石；Bt—黑云母；Mic—微斜长石；Pth—条纹长石；Qz—石英
Figure 7. Hand specimen photographs and microphotographs (Left—plainlight; right—crossed nicols) for the gravel of granite
Pl-Plagioclase; Bt-Biotite; Mic-Microcline; Pth-Perthite; Qz-Quartz
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图 8 洪水川组第二段花岗岩砾石（样品XRD368-1）的锆石阴极发光（CL）图像及其年龄值
Figure 8. The zircon cathodoluminescence(CL)images of sample XRD368-1
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图 9 洪水川组第二段花岗岩砾石（样品XRD368-1）的锆石微量元素特征（球粒陨石标准化数据引自Sun, 1989）
Figure 9. The trace element characteristics of zircon from Sample XRD368-1
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图 10 洪水川组第二段花岗岩砾石LA-ICP-MS锆石U-Pb年龄谐和图
Figure 10. Zircon LA-ICP-MS age diagram of granite gravel in the second member of Hongshuichuan Formation
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图 11 洪水川组弧前盆地构造原型示意图（据李瑞保等（2015）改）
Figure 11. Schematic diagram of Hongshuichuan for-arc basin
表 1 南带宝日禾日俄地区洪水川组第二段砾石统计结果
Table 1 The statistical results of the gravel in the second section of southern Hongshuichuan Formation
下载: 导出CSV
表 2 北带可可沙地区洪水川组a段砾石统计结果
Table 2 The statistical results of the gravel in the a section of northern Hongshuichuan Formation
下载: 导出CSV
表 3 洪水川组砾岩综合粒径累计频率分布统计量（Krumbein, 1934）
Table 3 Cumulative frequency curve of phi—transformed grain—size data of Hongshuichuan Formation gavel (after Krumbein, 1934)
下载: 导出CSV
表 4 宝日禾日俄地区洪水川组第二段花岗岩砾石（XRD368-1）LA-ICP-MS锆石U-Pb同位素测试结果
Table 4 LA-ICP-MS zircon U-Pb isotope data of granite from Hongshuichuan Formation(XRD368-1)
下载: 导出CSV
表 5 宝日禾日俄地区洪水川组第二段花岗岩砾石（XRD368-1）锆石稀土元素含量测试结果
Table 5 Rare earth element composition of granite zircon from Hongchuichuan Formation(XRD368
下载: 导出CSV
表 6 东昆仑地区已发表的早古生代侵入岩年龄统计
Table 6 The statistics of published data about early Paleozoic ages in East Kunlun
下载: 导出CSV
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