Determination of the double-layer structure in orogenic belts and its geological significance
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摘要: 当前，增生型造山带和碰撞型造山带的研究均取得了丰富的成果和创新性认识。二者过渡期间常常发生陆壳俯冲。然而，该俯冲具有什么样的构造变形特点，并如何影响造山带演化过程，长期未受到足够的关注。基于此，文中选择曾发生了陆壳俯冲的两个新生代时期的造山带（中国台湾造山带和雅鲁藏布江造山带）和一个中生代时期的造山带（羌塘造山带）开展研究，以期阐明陆壳俯冲的独特构造变形特征以及和造山过程的交互作用。研究发现，陆壳俯冲常常在造山带形成双层结构，上部为一套由史密斯地层组成的逆冲叠瓦扇构造体系，下部为一套具“岩块–基质”结构特征的俯冲杂岩。双层结构的上下部分物质组成相似，均以斜坡相–海底扇相沉积为主，也有陆棚相沉积。因此，由于构造变形时间相近，双层结构应是由同一套被动陆缘物质俯冲形成的深浅不同的构造体系。研究认为，在陆壳俯冲过程中，早期的斜坡–海底扇俯冲是形成双层结构的主要因素。后续的陆棚俯冲则对碰撞作用的发生起到了主导作用，从而使应变逐渐向克拉通内部扩展，形成前陆褶皱–冲断带。随着碰撞作用的持续，双层结构常常遭到构造破坏，深部的俯冲杂岩因此得以剥露至浅表。因此，文章的研究强调了陆壳俯冲和深俯冲物质的折返在造山带演化中的重要意义。Abstract: At present, the study of accretionary orogenic belts and collisional orogenic belts has achieved numerous insights and improvements. However, continental subduction, which often occurs during the oceanic and continental transition, has not received enough attention for a long time, such as what kind of structural deformation characteristics it has and how it affects the evolution of the orogenic belt. This paper studied two Cenozoic orogenic belts (the Taiwan orogenic belt and the Yarlung Zangbo River orogenic belt) and one Mesozoic orogenic belt (the Qiangtang orogenic belt) in order to clarify the unique structural deformation characteristics of continental subduction and its interaction with orogenic processes. It is found that the subduction of continental crust often forms a double-layer structure in the orogenic belt. The upper part is a set of thrust imbricate composed of Smith strata, and the lower part is a set of subduction complexes with a “blocks in the matrix” structure. The upper and lower parts of the double-layer structure are similar, mainly slope facies–submarine fan facies rocks and little shelf facies rocks. Due to the similar deformation time, the double-layer structure should be a structural system formed in different depths by the subduction of the same passive continental margin. We suppose that the subduction of the slope–submarine fan is the main factor for the formation of the double-layer structure. The subsequent continental shelf subduction could induce the collision and thus lead to strain’s gradual propagation to the craton’s interior, resulting in the foreland fold-thrust. Also, the double-layer structure is often destroyed during the collision, so the deeply underplated continental subduction complex can be exhumed to the shallow level. Therefore, this study also emphasizes the importance of continental subduction and the exhumation of subducted crustal rocks in the evolution of orogenic belts.
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0. 引言
新生代以来，印−欧大陆板块的持续碰撞与挤压造成了青藏高原的隆升和地壳缩短，在青藏高原东南缘形成了高黎贡断裂、哀牢山−红河断裂、鲜水河−小江断裂等大型走滑断裂（Wang et al.，1998）。其中，川滇地块受鲜水河−小江左行走滑断裂和哀牢山−红河右行走滑断裂的影响，向东南方向发生了大规模挤出逃逸和顺时针旋转（Wang et al.，1998；Tapponnier et al.，2001；Tong et al.，2015；王恒和杨振宇，2019），因此，川滇地块是研究青藏高原东南缘新生代构造旋转的理想地区。
相关学者利用古地磁方法针对西昌、会东、白路、楚雄、元谋、剑川、大姚以及大理等地区对川滇地块旋转运动进行了研究，认为从新生代以来川滇地块北部西昌的逆时针旋转（13.9°± 6.2°），向南逐渐变化为楚雄的顺时针旋转（36.4° ± 18°）（Huang et al.，1992；Yoshioka et al.，2003；Tamai et al.，2004；Zhu et al.，2008；Li et al.，2013，2015；Tong et al.，2015；王恒和杨振宇，2019）。由于滇中地块东部主要出露古生界，新生界出露较少，目前对滇中地块东部开展的古地磁研究相对较少。构造地貌学方法对揭示构造变形具有很好的作用（曹鹏举等，2021；关雪等，2021），河流地貌分析是还原地块构造演化历史的一个有效方法。河流作为陆地地形地貌演化过程中最活跃的影响因子之一，通常能对地块抬升、沉降（Fox et al.，2014；王乃瑞等，2015；段佳鑫等，2021）或旋转（Castelltort et al.，2012；Goren et al.，2015；Yıldırım and Tüysüz，2017）做出很好地响应。因此，该研究主要利用构造地貌学方法来揭示川滇地块东部老鹰山的旋转特征，进一步认识整个川滇地块新生代晚期的隆升与旋转构造变形过程。
1. 地质背景
鲜水河−小江断裂是一个长约2000 km的左行走滑断裂，其与哀牢山−红河右行断裂共同构成了川滇菱形地块的边界。南部的小江断裂呈南北走向，全长约为400 km。小江断裂在东川以南30 km处，分为东、西2支，2支断裂大致平行，间距约为15 km（Shen et al.，2003）。其中，西支断裂走滑速率为6.4 mm/a，东支断裂走滑速率为4.8 mm/a（宋方敏等，1998；李西，2015）。在东、西支断裂之间，发育了大量北东走向的新生代断裂及褶皱。在小江断裂西侧还发育有近乎平行的南北走向的元谋−绿汁江断裂和易门断裂和普渡河断裂等（余华玉等，2023；图1）。
图 1 研究区构造简图（Huang et al.，1992；Yoshioka et al.，2003；Tamai et al.，2004；Zhu et al.，2008；Li et al.，2013，2015；Tong et al.，2015；王恒和杨振宇，2019；余华玉等，2023）Figure 1. Structural diagram of the study area (Huang et al., 1992; Yoshioka et al., 2003; Tamai et al., 2004; Zhu et al., 2008; Gao, 2013; Li et al., 2013; Tong et al., 2015; Wang and Yang, 2019; Yu et al., 2023)老鹰山地区位于小江断裂东、西2支断裂之间（图2），其山脉水系呈南北向延伸，边界被四甲河、大白河、功山大河以及摆宰河围限，主要出露二叠系玄武岩以及茅口组灰岩、白云岩，局部出露寒武系页岩及灰岩。元古代地层少量出露，部分河流中发育有新生代地层（图2）。研究区自古近纪—早更新世时期构造运动以整体间歇抬升为主，在这一时期发育有多个盆地，如晚更新世发育的甸沙盆地、中更新世发育的沧溪盆地、阿旺盆地、功山盆地以及金所盆地（图2；宋方敏等，1998；Shen et al.，2003；郑立龙等，2019）。
图 2 老鹰山地区地质图（据覃胜荣，1978修改）Figure 2. Geological map of Laoyingshan (modified from Qin, 1978)2. 研究方法
基于30 m分辨率的数字高程模型（DEM），研究利用ArcGIS 10.7和Matlab 2015b提取了老鹰山地区的22条流域，获得了相关的构造地貌参数。
2.1 区域地形起伏度和地表隆起量
区域地形起伏度指单位面积内最大相对高程差，可反映地面相对高差，能够反映区域地表的切割剥蚀程度，是描述地貌形态的定量指标（张会平等，2006；刘静等，2006）。其计算公式如下：
R=Hmax−Hmin (1) 式中：R—地形起伏度；Hmax—单位面积内最大高程值；Hmin—单位面积内最小高程值。通过ArcGIS工具箱中的焦点统计工具，在给定的采样空间窗口（如1 km × 1 km）中分别获取该窗口内的最大高程和最小高程值，最后利用DEM栅格数据的插值运算，实现局部地形起伏的定量化（张会平等，2006；Yıldırım and Tüysüz，2017）。研究中，区域地形起伏度采用2 km × 2 km的采样窗口（包含研究流域的一个山脊和山谷组合，可以反映山谷到山脊的起伏特征），利用焦点邻域工具，采用公式（1）对该窗口进行计算，获得研究区的局部地形起伏度。
2.2 河流陡峭指数和河流纵剖面
在稳定的气候及构造条件下，河流纵剖面为平滑下凹形态（Whipple，2001；Yıldırım and Tüysüz，2017），但是当岩性、气候、沉积物通量以及活动构造发生变化时都会导致河流处于瞬态的不平衡状态（Kirby et al.，2003），在河流纵剖面上出现上凸的异常部位，即裂点（戴岩等，2016）。当河流流域面积未发生变化时，现存河流出水口的高程与在裂点处稳态时河流投影出水处的高程差揭示了自隆起开始以来的地表隆升量（Kirby and Whipple，2012；Yıldırım and Tüysüz，2017）。河流纵剖面的特征作为侵蚀作用和构造隆升相互竞争的结果，在不同的构造、气候和岩性条件下会呈现出不同的形态，因此通过对河流纵剖面的形态特征进行定量研究可以很好地指示区域隆升过程及相关的构造变形特征（Kirby and Whipple，2001；张东越等，2023）。其中，河流陡峭指数可以反映基岩隆升速率的空间分布特征（Goren et al.，2014；余华玉等，2023）。在构造隆升地区，由于河流纵剖面高程变化通常是河道隆升与下切之间竞争的结果，河道某点在一定时间（dt）内的高程变化（dz）是由岩石隆升速率（U）和侵蚀速率（E）共同决定的（Goren et al.，2014；Fox et al.，2015）：
dz/dt=U−E (2) 另外，河道侵蚀速率（E）可以表示为流域面积（A）与河流局部坡度（S）的函数：
E=KAmSn (3) 式中，K—侵蚀系数，由气候和岩石性质决定（Willett，1999）；m和n是描述河道侵蚀速率对流域面积和河道坡度相关性的正指数（Whipple and Tucker，1999）。当岩石隆升速率等于侵蚀速率时，河道的高程不随时间变化，因此，河道坡度为：
S=(U/K)1/nA−m/n (4) 在均一的岩性、隆升速率和气候条件下，河流坡度（S）与流域面积（A）呈幂律关系：
S=KsA−θ (5) 式中，Ks—河道陡峭指数，θ—河道凹曲度指数。利用DEM计算出河道坡度和流域面积，将数据投在双对数图上，稳定态的河段数据呈直线分布，线性拟合获得的斜率与截距就是河道凹曲度指数（θ）和陡峭指数（Ks），为了对不同大小的流域之间进行比较，Ks通常被归一化，归一化河流陡峭指数为Ksn（Whipple and Tucker，1999）。
研究表明可以利用参考凹曲度指数（θref）对公式（5）计算得到归一化陡峭指数（Ksn），Ksn可以用来反映构造抬升速率的相对大小（Trauerstein et al.，2013；王乃瑞等，2015）。Ksn可靠性在于其不受坡度−面积线性拟合的截距以及下游面积变化的影响（王乃瑞等，2015），并且已经在不同研究区域得到验证（Snyder et al.，2000；Wobus et al.，2003，2006；Yıldırım and Tüysüz，2017；张东越等，2023）。因为凹曲度在不同地貌中往往变化不大，陡度指数通常使用参考凹曲度指数（θref）计算（Snyder et al.，2000；Wobus et al.，2003，2006；Yıldırım and Tüysüz，2017）。将θref设定为0.45（Wobus et al.，2003，2006；Yıldırım and Tüysüz，2017），其程序代码来自
http://www.geomorphtools.org ，根据其相关数据提取了研究区归一化河道陡峭指数（Ksn）。因归一化河道陡峭指数（Ksn）受岩性和气候影响，故采用型号HT-225回弹仪测量了研究区岩性的硬度，来判断岩性对Ksn的影响（Cruslock et al.，2010；王乃瑞等，2015；Bernard et al.，2019）。2.3 流域方位角
流域盆地的方位角用于定义流域方向，可以用来确定块体的旋转量。流域方位角（BA）是流域主河道的源头和出口之间的投影中线的方位。未受构造作用时，BA垂直于分水岭的方向发育，其随着持续的构造作用而发生旋转（Ramsey et al.，2007；Castelltort et al.，2012；Goren et al.，2015；Guerit et al.，2016；Yıldırım and Tüysüz，2017）。以流域中线作为对象，如果流域旋转，中线的方向必须偏离初始变形区和流域分水岭之间的垂线，流域中线和垂直于分水岭方位之间的夹角即为该区域的旋转量。依据Goren et al.（2015）对黎巴嫩流域和Yıldırım and Tüysüz（2017）对Almacık地块提取流域方位角方法对大白河及功山大河周围的流域进行提取（Goren et al.，2015；Yıldırım and Tüysüz，2017）。
3. 研究结果
3.1 区域地形起伏
老鹰山地区低起伏区域主要位于老鹰山西侧四甲河以及摆宰河附近，高起伏区域主要位于老鹰山东侧大白河及功山大河附近（图3），即大白河及功山大河周围地形的起伏度大于老鹰山西侧四甲河周围的地形起伏度。根据区域地形起伏度的方法得出老鹰山地区的平均高程差为324 m（图3）。
3.2 河道陡峭指数和河流纵剖面
老鹰山地区流域归一化河流陡峭指数（Ksn）的范围为0 m0.9~ 1282 m0.9，Ksn值整体分布趋势由北向南逐渐降低，高值区（> 260 m0.9）主要分布在阿旺镇和金源乡附近，与小江断裂东、西2支断裂相重合，低值区（< 65 m0.9）主要分布在研究区老鹰山顶部以及摆宰河南部（图4）。
研究中共选择了22条河流（图5），通过用稳定状态和瞬时状态的河流纵剖面的高差来估计地表隆升（具体河流纵剖面图可扫描文后OSID码查看）。老鹰山分水岭东部河流（h1—h12，河流h9未发现裂点）的地表隆升量分别为200 m、220 m、500 m、290 m、300 m、140 m、250 m、200 m、350 m、400 m和180 m，东部地表隆升量为140 ~ 500 m；老鹰山分水岭西部河流（h13—h22）的地表隆升量分别为260 m、260 m、360 m、810 m、650 m、640 m、400 m、360 m、300 m和440 m，西部地表隆升量在260 ~ 440 m之间，局部流域的地表隆升较高，如h16流域的地表隆升量高达810 m，老鹰山北部的地表隆升量平均低于南部的隆升量。由此可知该地区整体的平均表面隆升为358 ± 200 m，这与表明局部区域地形起伏分析相吻合。
图 5 老鹰山地区22条河流纵剖面分布情况Figure 5. Longitudinal profile distribution of 22 rivers in the Laoyingshan3.3 流域方位角和地块的旋转
为确定老鹰山地区的旋转量，测定了研究区大白河及功山大河西侧和东侧的流域方位角（图6a），并根据其方位角制作了玫瑰图（图6b、6c）。大白河、功山大河西侧流域方位角揭示出其逆时针旋转量约为15°（表1）；大白河、功山大河东侧流域方位角揭示出其逆时针旋转量约为12°（表2）。
图 6 大白河、功山大河两侧流域方位角及生成的玫瑰图a—大白河、功山大河两侧生成的流域方位角；b—大白河、功山大河西侧流域方位角生成的玫瑰图；c—大白河、功山大河东侧流域方位角生成的玫瑰图Figure 6. The azimuth of the basins on both sides of Dabai River and Gongshan River and the generated rose diagram(a) Basin azimuth generated on both sides of Dabai River and Gongshan River；(b) Rose diagram of the basin azimuth analysis on the western side of Dabai River and Gongshan River；(c) Rose diagram of the basin azimuth analysis on the east side of Dabai River and Gongshan River表 1 大白河、功山大河西侧流域方位角Table 1. Basin azimuth on the western side of Dabai River and Gongshan River河流 流域中线方位角/
(°)垂线方位角/
(°)旋转量/
(°)平均旋转量/
(°)1 47.4035 35.5030 11.9005 14.9956 2 56.8472 39.2746 17.5726 3 61.7182 43.5887 18.1295 4 36.7287 24.0545 12.6742 5 34.9060 23.0075 11.8985 6 18.4842 8.4548 10.0294 7 30.4826 13.6866 16.7960 8 31.1446 14.6053 16.5393 9 29.4522 21.8166 7.6356 10 30.9373 14.6053 16.3320 11 26.3950 0.9501 25.4449 表 2 大白河、功山大河东侧流域方位角Table 2. Basin azimuth on the eastern side of Dabai River and Gongshan River河流 流域中线方位角/
(°)垂线方位角/
(°)旋转量/
(°)平均旋转量/
(°)1 222.3619 206.4810 15.8809 12.2181 2 213.5884 208.1903 5.3981 3 219.7653 208.5652 11.2002 4 229.0780 211.4550 17.6230 5 230.8436 220.5600 10.2836 6 216.6224 203.6995 12.9229 3.4 岩性硬度
大白河、功山大河地区岩性大多为二叠系玄武岩，回弹值约为46.97，四甲河流域岩性相对复杂，除二叠系玄武岩，局部有寒武系灰岩、砂岩、白云岩以及页岩，结果显示其不同岩性硬度的差别较小（图7），回弹值主要集中在46.97 ~ 64.38之间。
图 7 老鹰山地区Schmidt hammer回弹值柱状图Figure 7. Bar chart of Schmidt hammer rebound values in the Laoyingshan region4. 分析与讨论
4.1 地表差异隆升
河流陡峭指数受岩性和气候影响（Snyder et al.，2000；Wobus et al.，2003，2006；张东越等，2023），根据硬度测试结果，不同岩性的硬度差异较小，表明岩性对老鹰山地区河流陡峭指数的影响较低；同时研究区范围较小，可忽略气候对其产生的影响。因此，在排除岩性、气候影响后河流陡峭指数可视为抬升速率，老鹰山地区顶部河流陡峭指数较高，表明其抬升速率较小，可能是高海拔低起伏的古残留面（宋方敏等，1998；冯金良等，2004）。大白河、功山大河附近以及四甲河附近河流的陡峭指数较高，且分布在小江东、西支断裂附近，表示该地区的抬升速率较大，其河流陡峭指数主要受构造活动影响。研究表明老鹰山地区产生了324 m的局部起伏作为地表隆起的响应（图3），且高起伏度区域主要分布在断裂附近（图3），说明研究区地表隆起主要受断裂构造的影响，这与其河流陡峭指数数据相吻合。河流纵剖面显示老鹰山东侧的垂直位移量由北向南逐渐增大，平均隆起量为358 m。同时河流的纵剖面结果表明河流h16、h17、h18的隆起量较高（图5），分别为810 m、650 m和640 m，因为其地理位置位于金源乡附近的沧溪拉分盆地周围，并且根据野外地质观察及图5河流和断裂分布，发现河流h16附近有部分断裂以及褶皱，说明该地区构造运动较活跃，故河流h16、h17、h18地表隆起量较高的原因可能是盆地局部伸展构造的结果。
研究区地处青藏高原东南缘，位于川滇菱形地块的边界处，因此该地区的新构造运动与青藏高原隆升、挤压密切相关。始新世、上新世、早更新世区内发育有多个盆地，反映地壳运动在间歇性抬升的背景下，局部还存在垂直差异运动特征（林向东，2009），因此，研究区内盆地、河流及湖泊等是地壳升降运动形成的地貌（宋方敏等，1998）。研究区内河流与小江断裂重合，暗示两者的形成时间应大致相当。以往研究表明小江断裂开始活动的时间在中新世晚期（Roger et al.，1995；Li et al.，2015；Zhang et al.，2017），因此老鹰山地区的隆升时间开始于晚中新世，暗示老鹰山地区晚中新世以来的隆升量为358 m。研究基于河流地貌得到的隆升结果与滇中地区先锋盆地利用古植物恢复古高程的研究结果（Jacques et al.，2014；Li et al.，2015）相吻合。
4.2 地块旋转
自印−欧大陆碰撞以来，导致川滇地块的侧向逃逸与旋转（Wang et al.，1998；Zhu et al.，2008；高亮，2013；Li et al.，2013；吴中海等，2015；Tong et al.，2015；王恒和杨振宇，2019）。但是由于地壳物质组成和结构构造的复杂性，这种旋转并不表现为简单均一的运动。川滇地块中部和西部（丽江−小金河断裂以南、元谋断裂以西）的研究表明剑川地区始新世以来的顺时针旋转量约为20°（Tong et al.，2015）；楚雄盆地核部、剑川盆地以及渔泡江断裂东侧三岔河镇以南白垩纪以来的顺时针旋转量约为20°（王恒和杨振宇，2019）；对宁蒗地区古新统宁蒗组进行古地磁研究发现该地区顺时针旋转量为16.7° ± 6°（高亮，2013）；大理地区新近纪晚期以来的顺时针旋转量为4.4° ± 2.5°（Li et al.，2013）。
流域方位角研究表明，老鹰山地区河流经历了大约15°的顺时针旋转（图6）。由于大白河、功山大河和四甲河主要沿小江断裂发育（图2），推断老鹰山地区的河流发生的逆时针旋转是由断裂走滑造成的。川滇地块东部（元谋断裂以东）以逆时针旋转为主，例如，元谋盆地4.9 ~ 1.4 Ma发生了约12°的逆时针旋转运动（Li et al.，2015）；Huang et al.（1992）对会东地区古新世地层的古地磁研究表明该地区逆时针旋转了6.1° ± 7.2°（Huang et al.，1992）；Li et al.（2015）发现小龙潭盆地晚中新世地层逆时针旋转了8° ± 3°（Li et al.，2015），上述研究结果与文中基于河流地貌得到的地块旋转方向和旋转量相一致。因此，研究推测川滇地块内元谋断裂以西受走滑断裂影响较小，主要发生顺时针旋转；元谋断裂以东地层受走滑断裂等强烈的左行走滑影响，发生了逆时针旋转并伴随着差异隆升。
4.3 区域构造演化
始新世以来，在印−欧板块的碰撞作用下，青藏高原向东挤出，受华南块体的阻挡，使高原东部发生了显著的构造变形，主要表现为一系列北北西向的大型走滑断裂和褶皱带以及北北东向的褶皱逆冲带（Chen and Wilson，1996；Wang et al.，1998；Roger et al.，2004；陶亚玲等，2020），如鲜水河−小江断裂、哀牢山−红河断裂等，这些大型断裂控制着青藏高原东缘的构造及地貌特征（陶亚玲等，2020）。鲜水河–小江断裂是青藏高原东缘的大型走滑断裂之一，对高原的差异性变形及东构造节东侧地块顺时针旋转具有重要的调节作用（图8；Wang et al.，1998；Schoenbohm et al.，2006）。以往研究发现鲜水河−小江断裂不同段开始活动的时间不同，Roger et al.（1995）和 Zhang et al.（2004）根据花岗岩锆石U-Pb测年和云母39Ar/40Ar测年表明，鲜水河断裂活动开始于12.8 Ma，随后逐渐演变为边界断裂，之后青藏高原持续隆升造成其川滇地块向东南方向侧向逃逸，鲜水河断裂通过安宁河−则木河断裂逐渐向南发展；Liu et al.（2015）根据元谋断裂南、北两侧正长石锆石U-Pb测年数据，认为元谋断裂的活动时间在11 ~ 12 Ma，据此可以推测在上新世以前川滇地块的边界为鲜水河−安宁河−则木河−元谋断裂（图8a）；Tong et al.（2015）根据白垩系和古近系古地磁资料表明元谋−绿汁江断裂西侧经历了15°~20°的顺时针旋转，之后随着地块继续向东南方向挤出，旋转变形也继续向东南扩展；在上新世以后，小江断裂逐渐取代元谋−绿汁江断裂，成为川滇地块的东边界（图8b；Tong et al.，2015）。
a—b—17 Ma以来川滇地块的构造演化过程；c—老鹰山地区受力旋转过程Figure 8. Evolution of tectonic activity in the Sichuan-Yunnan block (modified according to Tong et al., 2015; Wu et al., 2015)(a)—(b) Tectonic evolution of the Sichuan-Yunnan block since 17 Ma；(c) Rotational stress process in Laoyingshan region因老鹰山地区正处于小江断裂中段东、西2支断裂中间，在高原隆升活动早期，小江断裂的活动性质以挤压为主，小江断裂中段区间表现为垂直差异运动，导致小江断裂区间形成南北向的地块隆起（宋方敏等，1998；冯金良等，2004）；之后受小江断裂东、西2支断裂左行走滑的影响，老鹰山地区受到挤压应力作用，发生了15°逆时针旋转以及358 m左右的差异隆升，以此来调节该应力作用（图8c）。
5. 结论
（1）老鹰山地区的区域地形起伏、河流陡峭指数以及河流纵剖面结果显示，受构造活动影响其自晚中新世以来发生了358 m左右的隆升，总体呈西北高、东南低的趋势。
（2）根据老鹰山地区流域方位角表明，大白河和功山大河附近流域对研究区的旋转很敏感，并且该地区受小江断裂影响较大，产生了15°左右的逆时针旋转。
（3）川滇地块内元谋断裂以西地区受走滑断裂影响较小，以印度向欧亚大陆强烈的北东向挤压为主，主要发生顺时针旋转；元谋断裂以东地区受强烈的左行走滑断裂影响，通过调节地块内部的应力差异，发生逆时针旋转并伴随着差异隆升。
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图 2 羌塘造山带物质组成示意图
Figure 2. Schematic diagram of the composition of the Qiangtang accretionary orogenic belt
图 3 羌塘造山带双层构造体系示意图
Figure 3. Schematic diagram of the double-layer structure in the Qiangtang accretionary complex
图 4 雅鲁藏布江造山带地质简图
Figure 4. Simplified geological map of the Yarlung Zangbo River orogenic belt
图 5 加查增生杂岩物质组成示意图
Figure 5. Schematic diagram of the composition of the Jiacha accretionary complex
图 6 雅鲁藏布江造山带双层构造体系示意图及中央直立带
Figure 6. Schematic diagram of the double-layer structure in the Yarlung Zangbo River orogenic belt and the central steep belt
图 7 中国台湾造山带地质简图（据Huang et al.，2000修改）
Figure 7. Simplified geological map of the Taiwan orogenic belt in China (modified from Huang et al., 2000)
图 8 中国台湾造山带地质剖面简图（剖面AB位置见图7；据Huang et al.，2000修改）
Figure 8. Simplified geological profile of the Taiwan orogenic belt in China (modified from Huang et al., 2000)
图 9 中央山脉变质岩系片岩变形特征
a—褶劈理S2；b—石英透镜体，具有右行剪切变形；c—构造片理被置换；d—长英质脉体揉流褶皱
Figure 9. Deformation characteristics of the schists in the Central Range complex
(a) Crenulation S2; (b) Quartz vein lens with dextral shear sense; (c) Schistose foliation was imposed; (d) Flow folds of felsic veins
图 10 中国台湾中央山脉变质岩系中大理岩变形特征
a—XY面不对称褶皱；b、c—YZ面鞘褶皱；d—大理岩转折端流变加厚
Figure 10. Sheath folds of the marbles in the Central Range complex of Taiwan, China
(a) Asymmetric fold on the XY profile; (b) and (c) Sheath fold on the YZ profile; (d) The hinge zone of the sheath fold was thickened
图 11 中国台湾造山带深部结构示意图（据Huang et al. ，2015；Chen et al. ，2019修改）
Figure 11. Schematic diagram of the deep structure of the orogenic belt in Taiwan, China (modified from Huang et al., 2015; Chen, 2019)
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