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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鄂尔多斯盆地奥陶系海相碳酸盐岩层系是一套重要的产气目的层段(黄正良等,2014;徐旺林等,2019;付金华等,2019),盆地中东部米探 1 井在奥陶系马家沟组钻获高产工业气流,实现了奥陶系天然气勘探的重大突破(魏柳斌等,2021;孟强等,2023),指示奥陶系马家沟组天然气勘探潜力巨大(杨华等,2011)。油气在成藏过程中会受到构造热演化的影响(任战利等,2008),下古生界奥陶系碳酸盐岩层系经历了多期构造运动、成藏条件复杂,明确其成藏期次、充注时间及成藏模式是进一步指导天然气勘探的关键(赵兴齐等,2023)。目前研究含油气盆地成藏期次有各种手段(李儒峰等,2010),流体包裹体作为分析含油气盆地成藏期次的重要工具之一,其中蕴含着丰富的地质信息,被广泛应用于成藏年代学的研究。
流体包裹体是矿物结晶生长过程中,因晶体发生缺陷而捕获一部分流体,至今仍保存于矿物中,没有内外介质的交换,它们是油气运移充注过程的遗迹化石记录,记录了当时地层的古环境情况等(陶士振,2006;Chen et al.,2013;邵晓州,2020)。包裹体均一温度是研究地层古地温和油气充注期次的关键(陈刚等,2012,2013;罗枭等,2015;李伟等,2020)。流体包裹体均一温度是通过人工加热,使室温下呈两相或多相的包裹体变成均匀单一相流体时的瞬时温度(Song et al.,2015;昌婷,2019;张钰等,2023)。前人应用流体包裹体法对鄂尔多斯盆地奥陶系碳酸盐岩系储层成藏期次进行研究获得了一些成果,其中赵卫卫等人对鄂尔多斯盆地北部苏里格地区下古生界奥陶系成藏期次进行了研究,确定该区存在两期天然气充注,分别为晚三叠早侏罗世及晚侏罗世早期(赵卫卫等,2011)。钟金银等人对鄂尔多斯盆地南部奥陶系成藏期次进行了研究,提出存在两期充注,时期分别为早侏罗世末期及早白垩世末期(钟金银等,2012)。陈志雄等人对鄂尔多斯盆地西缘下古生界奥陶系成藏期次进行研究,通过包裹体分析、盆地模拟提出奥陶系主要存在两期油气充注,分别为早侏罗世晚期和早白垩世早-中期(陈志雄等,2023)。前人的研究说明鄂尔多斯盆地奥陶系碳酸盐岩层系主要存在两期天然气充注,但北部、南部及西部的成藏时间均不尽相同,说明盆地内不同区域的成藏时期存在差异,同时盆地奥陶系热演化史与油气充注期次之间耦合关系不明确,烃源来源存在争议(杨华等,2011,2014;郭彦如,2014),故开展鄂尔多斯盆地中东部奥陶系成藏期次及成藏模式的研究十分必要,对指导下古生界的天然气勘探具有重要意义。
笔者选取鄂尔多斯盆地中东部地区奥陶系12口井中的14块马家沟组岩石样品,进行包裹体镜下观察并通过实验测量包裹体均一温度。对包裹体的大小、产状、宿主矿物类型等进行详细记录,选取与烃类包裹体同期次的盐水包裹体进行测温,得出包裹体均一温度的分布特征。而后利用petromod软件对盆地中东部奥陶系马家沟组单井埋藏史-热演化史、有机质成熟度演化史进行恢复,综合分析鄂尔多斯盆地中东部奥陶系天然气形成期次及成藏模式。
1. 区域地质概况
鄂尔多斯盆地位于华北地台西部,是一个构造变形边强内弱、多旋回演化、多沉积类型的大型沉积盆地,也是中国第二大含油气盆地(刘池洋等,2006;Zhao et al.,2015)。鄂尔多斯盆地地跨陕、甘、宁、蒙、晋五省区,北起阴山、大青山南抵秦岭西至贺兰山、六盘山,分布面积广,约37×104 km2,为我国重要的能源盆地之一,石油、天然气及煤炭等矿产资源极为丰富(杨俊杰,1988)。整个盆地内部断裂不发育,沉积地层相对平缓,倾角一般小于1°(姚泾利等,2009)。根据构造特征可划分为西缘冲断构造带、天环坳陷、陕北斜坡、渭北隆起、晋西挠褶带、伊盟隆起6个一级构造地质单元(任战利,1996;Darby et al.,2002)(图1a)。
盆地内不同地区奥陶系发育特征不同,地层划分方案有所差异,对应的岩石地层名称也不尽统一。由于早古生代怀远运动和加里东运动的影响,奥陶系经历了剥蚀,奥陶系顶部与上古生界本溪组之间存在不整合面,致使不同地区地层厚度具有差异性。目前,根据鄂尔多斯盆地沉积环境及构造演化背景方面的差异,一般将盆地奥陶系分为南部、西部及中东部三个区域。其中,南部奥陶系上统、中统、下统均发育;西部奥陶系上统被剥蚀,中统和下统均发育;中东部奥陶系上统和中统被剥蚀,下统主要发育马家沟组,从上至下可划分为马一马六共六段,其中马五段又细分为马五10至马五1亚段(任军峰等,2021;党文龙等,2022)。
盆地石炭系本溪组发育煤层及暗色泥岩,有机质类型主要为腐殖型(Ⅲ型)干酪根,泥页岩有机碳含量平均2.49%,煤层有机碳含量平均72.53,Ro平均值为1.78%(牛小兵等,2023),在盆地内分布稳定,盆地中部及陕北斜坡东部的烃源岩生烃强度最高(张雯等,2023),奥陶系马家沟组碳酸盐岩-膏盐岩交替发育(王禹诺等,2015;苏中堂等,2017;吴东旭等,2023)(图1b),马一段主要以发育灰黄色白云岩为主,马二段岩性主要为石灰岩与白云岩,部分地区发育少量的膏岩,马三段主要发育一套白云岩、膏岩和盐岩组合地层,马四段沉积了一套白云岩与石灰岩地层,其中广泛发育有斑状白云岩,马五段主要为白云岩、灰岩与硬石膏互层,马六段地层以灰岩沉积为主。马家沟组烃源岩主要为马一及马三段,为泥质碳酸盐岩,盆地中东部烃源岩厚度可达10 m,有机质类型为腐泥型(I型)干酪根,有机碳含量最高可达3.5%,Ro介于1.8%~3%(郭彦如等,2016)。
2. 储层特征
鄂尔多斯盆地中东部奥陶系马家沟组发育碳酸盐岩-膏盐岩层系,岩石类型主要为白云岩、部分灰岩,云质灰岩(图2)。岩石主要由白云石、方解石、泥质、硅质、黄铁矿等矿物组成,其中白云石含量最高,平均为71.58%,其次为方解石,平均含量为24.42%,泥质平均含量为3.08%,硅质、黄铁矿等其他矿物含量极少普遍低于1%(图3)。白云石以细粉晶为主,见少量泥晶、粗粉晶,呈半自形菱形粒状胶结颗粒分布(图4a);偶见方解石呈它形胶结颗粒;见膏岩假晶,呈板状分布,被方解石全交代(图4b)。颗粒见砾屑、砂屑,呈细粉晶或泥晶结构(图4c),磨圆为次圆状,分选好,岩石结构致密、均一。储层孔隙类型主要为晶间孔(图4d)、溶蚀孔隙(图4e~图4g)和裂缝(图4h~图4i),溶孔多被方解石、泥质等充填,储层中孔隙及裂缝的发育为马家沟组天然气的充注提供了基础,是有效的储集体。马家沟组储层的孔隙度呈近似对数正态分布,主要介于1%~8%,峰值位于2%,平均3.5%(图5a),渗透率同样具对数分布特征,主要介于0.01×10−3~10×10−3 μm2,峰值位于0.25×10−3 μm2,平均为1.5×10−3 μm2(图5b)。
图 4 鄂尔多斯盆地中东部奥陶系马家沟组储层镜下照片a. 自形菱形粒状白云石,Y1141,3 922.29 m,单偏光;b. 板状膏岩假晶发育,被方解石全交代,Y1207,3 931.72 m,单偏光;c. 细粉晶结构,Y1232,4 007 m,单偏光;d. 储层发育大量晶间孔,Y1366,3 977.5 m,单偏光;e. 圆形溶孔被亮晶方解石全充填,Y1207,3 932.8 m,单偏光;f. 晶间溶孔被亮晶方解石全充填,单偏光;g. 溶孔被方解石、黄铁矿、泥质全充填,Y1362,4 023.3 m,单偏光;h. 构造裂缝发育,部分被有机质浸染,Y1353,4 001.1 m,单偏光;i. 压溶缝合线发育,Y1142,3 865.5 m,单偏光Figure 4. Microscopic photos of the reservoirs in the Ordovician Majiagou Formation in the Central and Eastern parts of the Ordos Basin3. 包裹体特征
3.1 岩相学特征
鄂尔多斯盆地中东部奥陶系烃类流体包裹体广泛发育,利用徕卡4500P多功能显微镜对包裹体特征进行观察可知,包裹体产出类型和特征比较复杂,在方解石、白云石中均发育不同大小和形态的流体包裹体,形态呈规则形、不规则形、浑圆或三角形,长度一般<10 μm,宽度一般<5 μm。早期烃类流体包裹体主要发育在溶蚀孔中,以充填亮晶方解石、缝洞白云石的形式存在,少数发育在早期裂隙的重结晶方解石中(刘二虎等,2022;吴小力等,2022)。晚期烃类流体包裹体多发育在白云石脉体或充填膏模孔的晚期方解石之中,少数发育在晚期裂隙的亮晶方解石中。
奥陶系马家沟组碳酸盐岩储层粒间孔隙油气侵染,粒间孔隙荧光,部分粒间孔隙弱黄绿色、弱黄褐色荧光(图6a~图6c)。其中发育油气包裹体、气包裹体及盐水包裹体,油气包裹体呈灰黑色,弱黄绿色荧光或弱红褐色荧光(图6d~图6i),平均占比58%;气包裹体呈黑色或灰黑色,无荧光(图6j~图6l),平均占比41.7%;与油气伴生的盐水包裹体呈无色,无荧光,油气包裹体丰度低GOI≤1%。
图 6 鄂尔多斯盆地中东部奥陶系马家沟组流体包裹体显微照片a. 粒间孔隙油气侵染,Y1355,4 093.68 m;b. 部分粒间孔隙弱的的黄绿色荧光,与a同一视域;c. 部分粒间孔隙弱黄绿色、黄褐色荧光,Y1362,4 023.3 m;d. 缝洞白云石中发育油气包裹体,Y1147,4 057.85 m;e. 与d同一视域,油气包裹体发弱黄绿色荧光;f. 白云石脉中发育灰黑色油气包裹体,Y1355,4 093.68 m;g.与f同一视域,油气包裹体发弱红褐色荧光;h.方解石脉中发育灰黑色油气包裹体,Y1366,3 976 m;i. 缝洞方解石中灰黑色油气包裹体,盐水包裹体,Y1366,3 976 m;j. 缝洞方解石中灰黑色气包裹体和盐水包裹体,Y1366,3 976 m;k. 缝洞白云石中灰黑色气包裹体,Y1147,4 057.85 m;l. 与k同一视域下,气包裹体和盐水包裹体无荧光Figure 6. Microscopic photos of fluid inclusions in the Ordovician Majiagou Formation in the Central and Eastern parts of the Ordos Basin3.2 均一温度特征
对鄂尔多斯盆地中东部地区12口井14块样品的158个测点进行了流体包裹体测温研究,均一温度的测定采用Likam THMSG600 型显微冷热台进行。测试方法如下:将包裹体薄片放入热台,调节显微镜使之聚焦找到同一期次形成的、宿主矿物相同的一群体积较大、形状和边界清晰明显的包裹体,进行显微测温分析。测量均一温度时,控制升温速度在3 ℃/min –10 ℃/min,时刻注意观察流体包裹体中相态的细微变化,温度每上升10 ℃暂停观察一次。在包裹体接近均一时,升温速度降低为小于2 ℃/min,观察流体包裹体的气相或液相消失时的温度,即为均一温度,考虑到在流体包裹体内壁可能有细微的气泡附着,在达到均一相时应继续加热5~10 ℃,为避免此过程中发生爆裂,温度要缓慢上升,以确定真正达到均一相后降温到室温。
油气包裹体内含有大量有机质,在加热加压的情况下组分不够稳定,测定结果会受到影响而产生误差,而与烃类伴生的盐水包裹体的组分更加稳定,测定其均一温度能够更好地反映捕获温度,以此来代表油气充注时的地层温度(Chi et al.,2003;时保宏等,2012;唐胜利等,2021;陶华等,2022)。具体测试数据如表1所示。应用统计学原理对包裹体均一温度结果整理并制作分布直方图,研究区奥陶系碳酸盐岩包裹体均一温度从76 ℃~182 ℃连续分布,在110~130 ℃和160~170 ℃两个区间内出现峰值,说明研究区奥陶系主要有两期天然气充注(图7)。
表 1 包裹体均一温度测试结果Table 1. Test results of the homogenization temperature of inclusions井号 深度(m) 层位 宿主矿物 形态 包体产状 气液比(%) 均一相态 成因 均一温度(℃) 测点数 Y1147 4057.85 O1m 白云石 规则 脉体、孔洞充填 ≤5 液相 原生 128~150 4 Y1355 4093.68 O1m 白云石 规则 脉体、孔洞充填 ≤5 液相 原生 125~155 6 Y1366 3976 O1m 方解石 规则 脉体、孔洞充填 ≤5 液相 原生 122~182 14 L3 4183.7 O1m 方解石 不规则 脉体充填 3~8 液相 原生 90~155 13 S101 4065 O1m 方解石 不规则、三角形 孔洞充填 3~8 液相 原生 85~140 11 S96 3298 O1m 方解石 不规则 孔洞充填 3~8 液相 原生 112~168 15 S110 3575.5 O1m 方解石 不规则 孔洞充填 3~8 液相 原生 105~138 12 S110 3579.8 O1m 方解石 不规则 孔洞充填 3~8 液相 原生 102~163 10 S111 3522.9 O1m 方解石 浑圆、三角形 孔洞充填 3~8 液相 原生 78~116 9 S123 3850.5 O1m 方解石 不规则 孔洞充填 3~8 液相 原生 96~170 14 S138 3787.4 O1m 方解石 不规则 孔洞充填 3~8 液相 原生 78~146 12 L6 4351 O1m 方解石 不规则、三角形 孔洞充填 3~8 液相 原生 98~148 13 L6 4508.9 O1m 方解石 不规则、三角形 孔洞充填 3~8 液相 原生 106~116 10 S44 4089 O1m 方解石 浑圆、三角形 孔洞充填 3~8 液相 原生 103~178 15 4. 天然气成藏特征
4.1 成藏期次
鄂尔多斯盆地构造热演化对油气生成、运移、聚集与成藏有重要控制作用,是分析油气资源潜力和勘探前景的关键问题(崔军平等,2011;周勇水等,2021)。应用Petromod软件结合EasyRo%法对鄂尔多斯盆地中东部奥陶系及上古生界有机质成熟度演化史进行恢复,首先在Petromod软件中输入相关模拟数据,包括地层、年代、剥蚀厚度、地温梯度及古水深等,再设定初始热流值(任战利等,2007;宗奕等,2010;田刚,2017;邹德,2020),在软件内计算古地温与Ro;然后比较计算的Ro与实测Ro,当二者拟合度差时,则调整热流模型,重新开始模拟;当计算的Ro趋势与实测Ro数据拟合程度最好时,则可输出该井的热演化史、成熟史等相关模拟图件。单井热史模拟结果表明研究区晚二叠世前,地层缓慢沉降,温度较低,相应有机质成熟度低。二叠世至至早白垩世末,地层温度快速升高,深部地层如奥陶系及上古生界地层中有机质成熟,液态烃生成,在晚白垩世达到高-过成熟阶段,以生天然气为主(图8a)。
上古生界烃源岩在中三叠世进入生烃门限,Ro达到0.5%,中三叠世-早白垩世末(260~100 Ma)属于快速升温阶段,烃源岩进一步成熟,地层埋深达到最大,Ro达到2%。晚白垩世(100 Ma),盆地遭受大规模抬升剥蚀,地温快速降低,Ro不再升高(图8b)。奥陶系烃源岩在中三叠世进入生烃门限,Ro达到0.5%,中三叠世—早白垩世末(290~100 Ma)属于快速升温阶段,烃源岩进一步成熟,地层埋深达到最大,Ro达到2%。晚白垩世(100 Ma),盆地遭受大规模抬升剥蚀,地温快速降低,Ro不再升高(图8c)。
流体包裹体均一温度法是解决油气成藏期次问题的一种可靠有效的方法,将实验测得的流体包裹体均一温度峰值在埋藏-热演化史图上进行投点,确定达到相应温度的地质历史时间,进而判断油气充注时期(Hu et al.,2010;Guo et al.,2015;赵桂萍,2017)。通过对比得到:马家沟组第一期包裹体形成时间较早,包裹体均一温度峰值为110~130 ℃,充注时间距今210~165 Ma,为晚三叠世末到中侏罗世末;第二期包裹体均一温度峰值为160~170 ℃,充注时间距今123~97 Ma,为早白垩世末期(图8a)。两次大规模天然气充注时期恰好对应于中三叠世-早白垩世末的地层快速升温阶段,并与前人的研究具有较好的一致性(胡国艺,2003;李贤庆等,2004)。
综上天然气充注期次与烃源岩成熟史演化阶段具有良好的对应性,两期天然气充注均处于地层快速升温、有机质成熟度快速增长的阶段,该阶段生烃强度大,地层温压条件好,为天然气的大规模充注奠定了基础。
4.2 成藏模式
鄂尔多斯盆地中东部地区奥陶系主要发育以马家沟组为代表的碳酸盐岩层系,顶部与底部地层分别与石炭系本溪组和奥陶系冶里组呈不整合接触。马家沟组在纵向上构成良好的生储盖配置,马一及马三段沉积期海水收缩,以云坪、含膏云坪、膏、盐湖沉积为主(张涛等,2023),发育以泥质白云岩、生物白云岩为主的烃源岩层系,赋存于白云岩与膏盐岩层组合(周进高,2023);马四段沉积期区域海平面上升,主要发育了一套白云岩和石灰岩地层(于洲等,2023),储集性能好;马五段沉积期海平面下降,岩性主要为白云岩、灰岩与硬石膏互层,构成了盐下马四段气藏的区域性盖层。
晚奥陶世,奥陶系整体遭受抬升经历了长期的风化剥蚀,马四段大面积暴露(姚泾利等,2015;谢康等,2020;魏柳斌等,2021)。晚石炭世盆地再次沉降,使上古生界煤系烃源岩与马四段直接接触,形成源-储对接的供烃窗口,加里东风化壳区域地层剥蚀使得供烃窗口大范围稳定分布,存在于整个生烃过程(杨华等,2014)。随着煤系烃源岩的逐步成熟,天然气也逐渐生成,并在早白垩世达到生排烃高峰期,产生巨大的生烃增压作用(包洪平,2020),大量天然气在压力作用下,通过中央古隆起剥蚀区侧向运移进入盐下储层,中央古隆起剥蚀区是盐下侧向供烃的高效窗口。
天然气组分及碳同位素资料进行气源对比分析表明,奥陶系马家沟组天然气为以上古生界煤系烃源岩生成的煤型气为主,下古生界碳酸盐岩烃源岩生成的油型气为辅的混源天然气(李军等,2016)。盆地中东部位于奥陶系尖灭线附近(党文龙等,2022),上古生界生成的天然气通过剥蚀区窗口向下伏马家沟组直接输入并向东发生侧向运聚,马家沟组海相烃源岩生成的天然气通过断裂缝隙发生向上运移在马五段及马四段上倾方向白云岩岩性圈闭中聚集成藏。盆地中东部奥陶系位于陕北斜坡构造单元具有东高西低的构造背景,更有利于天然气的运移聚集(图9)。
5. 结论
(1) 鄂尔多斯盆地中东部奥陶系为碳酸盐岩-膏盐岩层系,储层发育油气包裹体、气包裹体及伴生盐水包裹体,主要分布于碳酸盐岩储层缝洞白云石、白云石脉、缝洞方解石及方解石脉中。包裹体均一温度介于76~182 ℃,呈两段峰值。第一期峰值 110~130 ℃,对应天然气充注时期为 210~165 Ma(晚三叠世末到中侏罗世末);第二期峰值 160~170 ℃,对应天然气充注时期为123~97 Ma(早白垩世末期)。
(2) 鄂尔多斯盆地中东部奥陶系主要经历三个热演化阶段:1.晚二叠世前缓慢升温阶段,有机质未成熟;2.晚二叠世末至早白垩世末快速升温阶段,有机质成熟-过成熟,平均升温速率 0.86 ℃/Ma,两期天然气充注均处于此阶段;3.早白垩世末快速降温,盆地抬升剥蚀,地温骤降,平均降温速率 0.63 ℃/Ma,生烃停止。天然气成藏烃源来自上覆石炭系煤系烃源岩和下部海相烃源岩自生自储式运移,天然气经储层孔隙及断缝运移,最终在地层上倾方向岩性相变带附近的白云岩岩性圈闭中聚集成藏。
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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
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) 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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