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古构造应力场的研究或者恢复一直是构造地质学研究的一个重要领域。断层是地壳中广泛发育的一种构造，不仅可以进行区域古应力的重建与构造解释（Wallace，1951；Bott，1959；Angelier，1984，1994；Ratschbacher et al.，2000，2003），而且还可以用于活动构造和现今地壳应力场的研究（崔效锋等，1999；谢富仁等，2003，2004; Heidbach et al.，2009）。本研究利用目前已有的断层滑动矢量反演数据开展中国尤其是东部中生代不同阶段古构造应力场的统计与分析。由于在我国西部用断层滑动矢量恢复古构造应力场的工作相对很少，本文集中讨论数据较多的中国中东部地区。前人已经在上个世纪后期开展了中国东部地区的古构造应力场恢复工作，出版了第一代中国的中、新生代古构造应力场系列图（万天丰，1989，1993）。这些工作主要基于传统的应力场恢复方法（万天丰，1988，1989，1999），而目前随着断层滑动矢量反演工作的开展，已经积累的一定的数据。因此，一方面需要开展基于前人成果的进一步丰富，另一方面也需要对前人的认识进行必要的补充和修订。本文就基于目前所收集到的断层滑动矢量反演数据，开展中国中、东部古构造应力场的统计与分析。与前人成果（万天丰，1993）比较，本文主要讨论中生代不同阶段的古构造应力场，而不涉及新生代。在此基础上，希望通过对区域性应力场方向的分析，从应力场角度对中国中生代主要变形的机制、环境以及背景进行限定，并对一些存在争论的问题进行讨论。
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1 中生代研究现状与资料来源
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我国中生代的构造变形的研究始于20世纪20年代，通过原中央地质调查所和部分国外地质学家的工作，在全国多个地区，包括北京西山、燕山、阴山、贺兰山、山西北部、四川、大别山东段、宁镇山脉等地，识别出了多处中生代由缩短作用导致的褶皱变形、逆冲推覆构造以及地层之间的不整合接触面（Teihard de Chardin and Licent，1924; Wang Chuchuan，1925，1928; 叶良辅等，1925; Wong Wenhao，1926，1927，1929; 刘季辰等，1927），Wong Wenhao（1926）认为这些缩短变形代表了一期介于海西期和喜马拉雅期之间的造山运动，提出“燕山运动”来指代这一时期的构造事件，并根据中国东部广泛发育的晚侏罗世不整合将该期事件限定于侏罗纪—白垩纪之交（Wong Wenhao，1926，1927，1929）。
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以此为开端，几代学者针对晚中生代构造变形事件开展了长达近百年的研究（Wong Wenhao，1926，1927; Hsieh，1936; 赵宗溥等，1959; 黄汲清，1960; 任纪舜等，1990；赵越等，1990，2002; 万天丰，1993；邓晋福等，2005; 董树文等，2007，2008; 张岳桥等，2007a，2007b，2012; Dong et al.，2015）。随着研究的深入，除上述缩短变形之外，晚中生代大规模伸展（Deng Jinfu et al.，2007; 朱日祥等，2020）以及晚中生代末期的缩短变形（黄汲清，1960; 徐嘉炜等，1985; Zhu Guang et al.，2012; 朱光等，2018）也被越来越多的学者发现，并通过对晚中生代伸展事件的研究，提出了“地台活化”、“克拉通破坏”等认识（朱日祥等，2020），这些研究使得中生代构造变形吸引了更多学者的关注。随着研究的深入，诸多学者对“燕山运动”的启动时间、期次划分和变形特征等提出了多种认识，“燕山运动”的概念也被进一步发展，有学者将中侏罗世至晚白垩世期间的几期重大构造变形事件均囊括于其中（董树文等，2019）。有关晚中生代陆内构造变形事件的研究范围也遍及东亚大部分地区（Davis et al.，1996，1998，2001; 张长厚等，2004b，2011; Faure et al.，2012; Zhang Jin et al.，2014，2020，2021a，2021b，2022; Clinkscales and Kapp，2019; Clinkscales et al.，2020; Zhao Heng et al.，2020; 张北航等，2021）。
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最近几十年，随着现代构造地质学研究手段的应用，构造、岩浆事件的高精度测年数据的积累，我国以及整个东亚地区晚中生代构造变形事件的期次、时代以及构造背景逐渐清晰。根据众多学者的研究成果，东亚地区在晚侏罗世—晚白垩世早期先后经历了晚侏罗世—早白垩世缩短、早白垩世伸展以及早白垩世末—晚白垩世初缩短等多次构造体制的转变（董树文等，2019; 朱日祥等，2020），伴随有一系列特征性的构造变形和岩浆事件，反映了晚中生代欧亚大陆东缘复杂多变的动力学环境。
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自从20世纪后期基于传统方法的全国性古构造应力场的综合统计研究以来，随着根据断层滑动矢量反演古构造应力场方法的提出并逐步成熟，使得古构造应力场的反演成为构造分析中的常规内容（Angelier，1984，1994）。利用断层活动进行区域应力场和构造场定性和定量研究的主要手段就是通过野外露头的断层滑动方向的测量和性质来重建古构造应力场（Angelier，1984，1994）。我国也于20世纪末期引入该类方法，不同的学者在不同地区开展了中、新生代不同阶段的古构造应力场的反演，逐步积累了大量的数据。尤其是随着“华北克拉通破坏”等重大研究计划的执行，中国东部地区针对侏罗纪和白垩纪古构造应力场的详细确定，使得我们对“燕山运动”的实质有了深入的理解（张长厚等，2004a，2004b，2011; Shi Wei et al.，2012，2013a，2013b，2015; Li Jianhua et al.，2014a，2014b）。
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传统的古构造应力场的确定方法主要利用“共轭节理”以及纵弯褶皱进行统计分析（万天丰等，1988，1993），这些方法已经在不同领域进行了有效的运用，如在鄂尔多斯盆地（中国煤田地质总局，1996）。利用这些方法，万天丰（1993）开展了中国东部中、新生代的古构造应力场的统计分析，得到了我国第一代古构造应力场的系列图件，为我们理解我国中、新生代构造演化、地貌变迁以及能源资源的勘探开发起到了重要作用。在中国东部中、新生代古构造应力场的划分中，万天丰等（1993）利用区域性的角度不整合将中国东部中、新生代的演化划分出六个阶段或者构造层，即印支期（250~208 Ma）、燕山期（208~135 Ma）、四川期（135~52 Ma）、华北期（52~23.3 Ma）、喜马拉雅期（23.3~0.7 Ma）、新构造期（0.7 Ma至今）（万天丰，1993）（图1）。本研究也基本遵循此依据，但没有继续使用原术语，而以地质时代划分为主。本文将我国中东部的中生代演化划分为中、晚三叠世、中—晚侏罗世、早白垩世与早白垩世末—晚白垩世初四个阶段。
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图1 万天丰中国东部中、新生代古构造应力场（据万天丰，1993）
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Fig.1 Mesozoic-Cenozoic paleo-stress field in eastern China (after Wan Tianfeng, 1993)
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目前在国内开展以断层滑动矢量反演古构造应力场的工作主要集中在中、东部，西部几乎没有数据（图2），中、东部的工作主要集中在燕山—阴山、鄂尔多斯周缘、扬子克拉通东南缘以及一系列大型断裂沿线（图2）。本研究目前共收集数据3800组，其中中生代的古构造应力场数据共2750组（图2）。由于部分文献未提供观测点的具体经纬度，导致数据不好利用，故在本次数据统计中未加以利用。此外，虽然不同的研究都使用了基于断层滑动矢量反演古构造应力场的方法，但使用的具体的方法和软件也有所不同，至于这些不同方法所得到结果之间的对比问题也超出了本文的范围和笔者的能力，本文重点使用已有的研究结果。还需要说明的是，由于中生代的变形多为脆性变形，导致对不同变形的绝对时间的确定非常困难，不同学者或者研究主要基于涉及的地层或者岩石的年龄以及低温热年代学资料确定不同变形活动的时间范围，因此不同研究之间一定存在不同认识或者矛盾。在本文的数据统计中，基本遵循已有研究确定的范围，而对一些不能很好确定时间的变形，一方面将时间范围放大，如在侏罗纪—白垩纪缩短变形中，多数研究将其定为晚侏罗世，但也有学者认为中侏罗世就已经开始，而也有部分学者认为其结束可以延续到早白垩世早期，因此本文将这期变形的时间划定为中侏罗世—早白垩世早期。类似的也包括中、晚三叠世、早白垩世末—晚白垩世初等几个阶段。另一方面，对于一些变形可能存在穿时性，如早白垩世末—晚白垩世初，在中国东部自南向北都存在一期短暂但又明显的缩短事件，但是不同地区该期变形时间上有一定的差异性，因此在本文中考虑到可能相似的变形背景，我们将它们统一划分为一期构造。
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此外，在所划分的不同阶段中，一定有一些区域或者研究地区的古构造应力场与更大范围内的区域古构造应力场存在明显的区别，这有可能代表了局部应力场，也可能是不同的研究对于时代的限定存在不同依据，还可能由于存在不同阶段的构造叠加，造成构造复原存在问题。解决上述问题最好的办法是开展不同地区的构造解析。本研究也尝试这个方法，根据在不同地区的工作经历和变形解释，将一些明显与区域上构造应力场存在差别的结果列为局部应力场或者其他因素而没有进一步的讨论。限于篇幅和笔者工作涵盖的地区并不是很多，本文目前对前人的数据只能根据笔者的经验和认识进行统计分析，讨论中国中、东部不同阶段总的古构造应力场特征。
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图2 中国大陆古构造应力场图数据点（据Ratschbacher et al.，2000，2003; 马寅生等，2002; 施炜等，2007; 常远，2007; 张岳桥等，2007b，2009; 胡召齐等，2010; Shi Wei et al.，2012，2013a，2013b，2015，2022; Li Jianhua et al.，2012，2014b; 苏金宝等，2013; Huang Xingfu et al.，2015; 林逸等，2015; 马之力，2015; 赵伟策，2015; 杨谦，2015，2021; 丁照月，2016; 高健翁，2016; 韩效忠等，2016; Li Yong et al.，2016a; Xu Xianbing et al.，2016，2021; Ju Wei et al.，2017; 李东东，2017; Liu Cheng et al.，2018; 李韶凯等，2019; 梁承华等，2019; 吴玉等，2019; Zhang Shuai et al.，2019; 邓佳良等，2020; Zhang Yu et al.，2020; Zhang Bo et al.，2020，2023; Zhang Jin et al.，2020，2022; Li Chunlin et al.，2021; 张北航等，2021; 周宇章等，2021; Cheng Yongzhi et al.，2022）
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Fig.2 Distribution of the data spots in the paleo-stress field map of China （after Ratschbacher et al., 2000, 2003; Ma Yansheng et al., 2002; Shi Wei et al., 2007, 2012, 2013a, 2013b, 2015, 2022; Chang Yuan, 2007; Zhang Yueqiao et al., 2007b, 2009; Hu Zhaoqi et al., 2010; Li Jianhua et al., 2012, 2014b; Su Jinbao et al., 2013; Huang Xingfu et al., 2015; Lin Yi et al., 2015; Ma Zhili, 2015; Zhao Weice, 2015; Yang Qian, 2015, 2021; Ding Zhaoyue, 2016; Gao Jianwong, 2016; Han Xiaozhong et al., 2016; Li Yong et al., 2016a; Xu Xianbing et al., 2016, 2021; Ju Wei et al., 2017; Li Dongdong, 2017; Liu Cheng et al., 2018; Li Shaokai et al., 2019; Liang Chenghua et al., 2019; Wu Yu et al., 2019; Zhang Shuai et al., 2019; Deng Jialiang et al., 2020; Zhang Yu et al., 2020; Zhang Bo et al., 2020, 2023; Zhang Jin et al., 2020, 2022; Li Chunlin et al., 2021; Zhang Beihang et al., 2021; Zhou Zhangyu et al., 2021; Cheng Yongzhi et al., 2022）
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2 中生代古构造应力场特征
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2.1 中、晚三叠世
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目前有关三叠纪古构造应力场的资料较少，多数研究集中在华南地区（Shi Wei et al.，2012，2015; Li Yong et al.，2016a; 吴玉等，2019; Li Chunlin et al.，2021），在华北，主要的研究集中在华北北缘（赵伟策，2015）以及西部的贺兰山地区（Huang Xingfu et al.，2015; Yang Xiangyang et al.，2020），而东北地区目前尚无数据。总体而言，中国东部秦岭及大巴山等地区以北，中、晚三叠世的古构造应力场主要为近南北向的挤压应力场（图3），这与万天丰（1993）获得的结果基本一致（图1）。但是华南地区同期的古构造应力场显示的方向较多，既有南北向、也有北西-南东向，还有北东-南西向的应力场，但近南北向应力场是主体（图3）。考虑到三叠纪主要的构造事件是华北与扬子克拉通的碰撞，近南北向的古构造应力场应该就是这次事件的反映。前人将华南地区的北东-南西向的应力场解释成扬子与华北克拉通碰撞时发生了60°~90°顺时针的旋转造成的结果（Li Yong et al.，2016a），但同时也不能排除因为华南发生显著的三叠纪陆内造山作用（Wang Yuejun et al.，2005，2013），来自东部古太平洋构造域以及西南部印支板块多个方向的作用可能是重要的因素。需要说明的是，上述不同方向的应力场也不排除多期构造叠加，缺少构造复原的结果。根据上述因素，本研究将中、晚三叠世我国主体的构造古应力场定为近南北向的挤压。
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关于三叠纪这期应力场发生的时间主要根据卷入变形的岩体时代以及地层时代约束，基本上确定为中、晚三叠世（张义平等，2015; Li Yong et al.，2016a），时间范围较万天丰（1993）的印支期（250~208 Ma）略有不同。需要指出的是，上述基于断层滑动矢量反演的应力场是以脆性变形为基础的，实际上在三叠纪，无论华北（Wang Yu et al.，2013; Zhang Jin et al.，2013，2022）还是华南（Zhao Lei et al.，2018; Li Chunlin et al.，2021），甚至包括东北地区（Liang Chenyue et al.，2020）均发育有很多不同时间的韧性变形，而控制它们的背景和应力场目前是不清楚的。
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图3 中、晚三叠世最大水平古应力方向
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Fig.3 Maximum horizontal paleo-stress direction in the Middle and Late Triassic
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2.2 中侏罗世—早白垩世
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中侏罗世—早白垩世的古构造应力场是目前研究最为详细的阶段，得益于“华北克拉通破坏”以及“燕山运动”等热点问题的研究，我国东部广大地区该阶段的古构造应力场数据较为丰富。总体而言，该期古构造应力场主体以北西-南东向挤压为主（图4），但不同地区也显示存在一定的差异，扬子克拉通东南缘古构造应力场明显表现出西北西-东南东向，鄂尔多斯西缘、燕山-阴山东部以及太行山地区以北西-南东向为特点，阴山西段则表现出近南北向，而大巴山地区则出现与弧形逆冲推覆构造相垂直的多个方向的古构造应力场（图4；Shi Wei et al.，2015），同时，上述的古构造应力场显示出一定的空间变化特征，即越向南和向东，古构造应力场的方向则以西北西-东南东向为主（图4），这一时期古构造应力场方向在空间上的分布和变化特征，暗示中国大陆北方和南方受控的背景可能存在差异。万天丰（1993）恢复的同期（燕山期，208~135 Ma）古构造应力场为北北西-南东东向（图1），与本次统计的大量研究和数据所展示的中侏罗世—早白垩世的古构造应力场方向稍有差别，原因可能与数据的不断积累和研究的不断深入有关，同时也可能与多个方向同期作用的叠加以及所处的不同大地构造位置有关，如在这一时期同时发生了蒙古-鄂霍茨克造山作用、古太平洋板块的低角度俯冲以及羌塘与欧亚板块的碰撞等构造事件（董树文等，2019; Li Chunlin et al.，2023），产生了不同方向的应力场，同时在中国中、东部的影响范围也不尽一致。
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图4 中侏罗世—早白垩世最大水平古应力方向
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Fig.4 Maximum horizontal paleo-stress direction in the Middle Jurassic-Early Cretaceous
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关于该期变形时间范围的确定，不同的学者有不同的划分方案，万天丰（1993）划分的燕山期从晚三叠世开始至早白垩世（208~135 Ma），但三叠纪之后，我国广大地区进入到早、中侏罗世的区域性伸展阶段，明显与前期中、晚三叠世的区域性缩短和走滑变形存在区别，因此该期挤压变形时间从中侏罗世甚至晚侏罗世开始至早白垩世更加合理。
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2.3 早白垩世
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与中、晚侏罗世—早白垩世阶段的研究类似，早白垩世整个东亚区域性的伸展研究已经积累了丰富的成果，一系列断陷盆地、变质核杂岩、玄武岩的喷发都指示了我国中东部强烈的伸展。总体而言，本期的伸展方向主要为北西-南东向，尤其是东部地区最为明显（图5）。这种北西-南东向或近东西向的伸展向西直至阿拉善地区和鄂尔多斯西缘地区均有分布（图5）。但是在中部地区，伸展的方向多变，如在中南部出现了近南北或者近东西向的伸展（图5），目前还不清楚导致上述不同的原因。区域上，白垩纪早期断陷盆地伸展方向以及变质核杂岩的伸展方向几乎都为北西-南东向（Wang Tao et al.，2011; Lin Wei et al.，2020），这种一致性说明该期伸展可能受控于同样的机制。
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前人的通过褶皱和节理恢复的古构造应力场表明这一时期伸展方向为北西-南东向，但强调了北北东-南南西方向的缩短（图1；四川期，135~52 Ma；万天丰，1989，1993）。目前的积累研究表明，我国东部在白垩纪发生了多次性质不同的构造事件，因此需将整个白垩纪划分出不同的阶段，需要根据不同的机制和背景以及年代学工作进行细化。根据前人对该期伸展形成的变质核杂岩和岩浆岩所做的年代学工作，这期区域性的伸展主要发生在白垩纪早期（朱日祥等，2020及所引文献）。而导致这期区域性伸展的机制还存在不同认识，但考虑到区域范围内伸展方向的一致性，它们可能受控于相同的机制，具体见后讨论。
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图5 早白垩世最小水平古应力方向
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Fig.5 Minimum horizontal paleo-stress direction in the Early Cretaceous
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2.4 早白垩世末—晚白垩世初
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早白垩世末—晚白垩世初是一个长期被忽视的阶段，一般认为是处于一个相对比较稳定的阶段，比较明显的特征就是早期发育的断陷盆地在该时期基本都停止断陷，部分盆地甚至发生反转（Suo Yanhui et al.，2020; Feng Zhiqiang et al.，2021）。该阶段被前人划归于四川期（135~52 Ma）的一部分（万天丰，1989，1993），并确定该期的应力场为北北东-南南西向缩短（图1）。根据近年来断层滑动矢量反演得到的应力场数据，表明存在一期主体为北西-南东向的缩短（图6），与前人的结果不同（图1；万天丰，1993）。这期北西-南东向的缩短主要分布在东部地区，从华南南部一直可以到华北北部和大兴安岭南部，而到东北地区除了在长白山地区为北西-南东向缩短外，在其他地区则转为近南北向缩短（图6）。同样北西-南东向的缩短向西在阿拉善地区也存在（图6）。而在华南西部以及太行山北部这一时期古构造应力场却与主体的应力场近于垂直，为北东-南西向（图6），这与前人恢复的古构造应力场却是几乎一致的（万天丰，1993）。
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图6 早白垩世末—晚白垩世初最大水平古应力方向
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Fig.6 Maximum horizontal paleo-stress in the latest Early Cretaceous-Late Cretaceous
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3 讨论
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3.1 三叠纪
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三叠纪随着北方古亚洲洋的关闭以及南侧古特提斯洋的关闭，东亚中国的轮廓初步形成（Huang Tekan，1945; 任纪舜，1990; Xiao Wenjiao et al.，2015），中国绝大部分进入陆相演化环境。三叠纪因此在我国地质演化中是一个承前启后的阶段。从目前得到的古构造应力场可以看出，华南与华北中、晚三叠世古构造应力场存在明显的差异，而东北地区该时期的应力场还缺少有效的控制。其主要原因是华南地区作为“印支运动”最为发育的地区，构造行迹也最为明显与丰富，构造叠加也最普遍，相关的研究较多。
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由于三叠纪是我国构造演化中关键的阶段，其变形也是非常典型。在华南形成了广阔的褶皱与逆冲推覆构造，奠定了华南中生代变形的轮廓与样式（图7），虽然其形成机制还存在不同认识（Hsü Jinghwa et al.，1990; Wang Yuejun et al.，2005; Lin Shoufa et al.，2018; Zhang Jin et al.，2018）。由于华南地区三叠纪东、西以及北侧均发生了与不同板块或块体的碰撞拼贴，期间华南也伴随着顺时针旋转，致使其发生了典型的变形叠加的过程（Shi Wei et al.，2012，2013，2015; 苏金宝等，2013; 张义平等，2015; Zhang Jin et al.，2018; Chu Yang et al.，2018; Lin Shoufa et al.，2018），这可能也是华南地区中、晚三叠世古构造应力场方向多变的重要原因。相对于华南，我国北方三叠纪的变形则表现的不是很明显，而且遭受了侏罗纪和白垩纪的连续叠加与破坏，致使识别相对困难，这也是华北东部与东北地区目前还缺少中、晚三叠世古构造应力场数据的重要原因。
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需要指出的是，上述中国中东部中、晚三叠世的古构造应力场数据测量与反演全部是通过脆性变形反演而成，事实上，我国中东部三叠纪还经历了多期的韧性变形，而导致这些韧性变形的原因和背景也是存在很多认识。在华南，主要的韧性变形多沿着北东向断裂分布，主要分布在雪峰山（Wang Yuejun et al.，2005）、八都（Li Jianhua et al.，2017a）、合浦（Zhang Kaijun et al.，2009）、吴川-四会断裂（Wang Yuejun et al.，2007）以及闽西北（Lin Shoufa et al.，2023）等断裂上（图7）。在东北，三叠纪的韧性变形主要分布于几条大的边界断裂上（图8），如西拉木伦-延吉缝合带东段（Liang Chenyue et al.，2020）、黑河-嫩江断裂带（赵衡等，2017）以及德尔布干断裂带等（Zhao Pan et al.，2015），但是目前这些韧性变形时代多数还缺少很好的限定。在华北目前有关三叠纪韧性变形可以划分为2期，早期为三叠纪早中期（约250~230 Ma），为分布与华北北缘以及中亚造山带东段的一系列近东西向的右行韧性剪切带（Wang Zhihong et al.，2014; Zhang Jin et al.，2022）；晚期（约230~210 Ma）为切割这些近东西剪切带的大型韧性走滑断裂，如西部的狼山-巴彦乌拉山断裂（Zhang Jin et al.，2013）、东部的德尔布干断裂（Zhao Pan et al.，2015）（图8）。其中早期的变形被解释成中亚造山带的整体变形（Zhang Jin et al.，2022）或者与古亚洲洋的关闭有关（Wang Zhihong et al.，2014）；而晚期的韧性变形多被认为与华北与扬子的碰撞有关（Zhang Jin et al.，2013）。在华北与晚期韧性变形配套的脆性变形在贺兰山（Huang Xingfu et al.，2015; Yang Xiangyang et al.，2020）以及卫宁北山（Zhang Jin et al.，2021a）等地区有报道，均为近南北向的古构造应力场（图3）。可以看出，不论华南还是华北（含东北），三叠纪的韧性变形虽然复杂，方向多变，但均分布在克拉通的边缘或者相邻的造山带范围内（图7、8）。而脆性变形，尤其是明显逆冲推覆构造在两个地区却存在明显的差别，华北地区缺少成规模的区域性的逆冲推覆构造，而华南地区，大量扬子克拉通东南缘带状分布的逆冲推覆构造则是重要的特征，这些变形的异同可能显示了不同的变形条件。
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3.2 中侏罗世—早白垩世
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中侏罗世—早白垩世的缩短变形是我国最为鲜明的构造，在20世纪20年代即已被多数学者发现（Teihard de Chardin and Licent，1924; Wang Chuchuan，1925，1928; Wong Wenhao，1926，1927，1929）。该期变形形成了上侏罗统髫髻山组与下伏和上覆地层之间发育的两个角度不整合，是“燕山运动”的重要组成部分（Wong Wenhao，1929; 赵越等，2002，2004; 刘健等，2006; Li Chengming et al.，2016b）。多数学者据此认为这一时期呈幕式发生过先后两次区域挤压构造事件（董树文等，2019），而两个不整合面之间的火山岩则代表了两期缩短变形事件之间的一期弱伸展变形（Wong Wenhao，1929; 董树文等，2019; 朱日祥等，2020）。在华北多个地区可见该期缩短导致的逆冲推覆构造（Davis et al.，1998; 张岳桥等，2007a，2007b; Zhang Jin et al.，2014，2020，2021b; Zhao Heng et al.，2020; 张北航等，2021），以及伴生的地层褶皱和生长地层的发育（张岳桥等，2007a，2007b; 王永超等，2017; 陈宣华等，2019; Zhang Jin et al.，2020，2021a，2022; Zhao Heng et al.，2020）。在华北北缘的阴山-燕山构造带和内蒙阿拉善北缘雅干地区，该期挤压主要表现为一系列近东西走向展布的、由北往南的逆冲推覆构造（郑亚东等，1990，1998; Zheng Yadong et al.，1996; Davis et al.，1996，1998，2001; 刘正宏等，2003; 张长厚等，2011; Li Chengming et al.，2016b）。
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图7 华南地区三叠纪韧性变形分布
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Fig.7 Distribution of the Triassic ductile deformation in South China
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FCSZ—防城-灵山剪切带（253~204 Ma；丁汝鑫等，2015; Li Jianhua et al.，2017a）；HPSZ—合浦剪切带（213~195 Ma; Zhang Kaijun et al.，2009）; WCSZ—吴川-四会剪切带（248~200 Ma; Wang Yuejun et al.，2007）；CTSZ—长汀剪切带（239~230 Ma; Xu Xianbing et al.，2011）；MXBSZ—闽西北剪切带（245~228 Ma; Li Jianhua et al.，2017b; Lin Shoufa et al.，2018，2023）；JSSZ—江绍剪切带（232 Ma; Shu Liangshu et al.，2015）; XFSZ—雪峰山剪切带（244~195 Ma; Wang Yuejun et al.，2005）
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FCSZ—Fangcheng-Lingshan shear zone (253~204 Ma; Ding Ruxin et al., 2015; Li Jianhua et al., 2017a）; HPSZ—Hepu shear zone (213~195 Ma; Zhang Kaijun et al., 2009）; WCSZ—Wuchuan-Sihui shear zone （248~200 Ma; Wang Yuejun et al., 2007）; CTSZ—Changting shear zone （239~230 Ma; Xu Xianbing et al., 2011）; MXBSZ—Minxibei shear zone （245~228 Ma; Li Jianhua et al., 2017b; Lin Shoufa et al., 2018, 2023）; JSSZ—Jiangshao shear zone （232 Ma; Shu Liangshu et al., 2015）; XFSZ—Xuefengshan shear zone （244~195 Ma; Wang Yuejun et al., 2005）
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图8 华北—东北地区三叠纪韧性变形分布
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Fig.8 Distribution of the Triassic ductile deformation in North and Northeastern China
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SASZ—南阿拉善剪切带（Zhang Jin et al.，2022）；LBSZ—狼山剪切带（Zhang Jin et al.，2013）；DEBGSZ—德尔布干剪切带（Zhao Pan et al.，2015）；XMSZ—西拉木伦剪切带（Liang Chenyue et al.，2020; Zhang Jin et al.，2022）；HNHSZ—贺根山-嫩江-黑河剪切带（赵衡等，2017）
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SASZ—Southern Alxa shear zone （Zhang Jin et al., 2022）; LBSZ—Langshan shear zone （Zhang Jin et al., 2013）; DEBGSZ—Derbugan shear zone （Zhao Pan et al., 2015）; XMSZ—Xar Moron shear zone （Liang Chenyue et al., 2020; Zhang Jin et al., 2022）; HNHSZ—Hegenshan-Nenjiang-Heihe shear zone (Zhao Heng et al., 2017）
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在阿拉善东缘、鄂尔多斯西缘，以及华北中部吕梁山、太行山地区则表现为一系列近南北走向或NNE-SSW走向的逆冲构造（Darby and Ritts，2002; 张岳桥等，2007b; 张长厚等，2011; Faure et al.，2012; Zhang Jin et al.，2014，2020，2021a，2021b，2022; Clinkscales and Kapp，2019; Zhao Heng et al.，2020; 张北航等，2021），根据与逆冲相关的生长地层、逆冲构造带中相关矿物的同位素测年以及不整合面上下的地层时代，限定该期逆冲主要发育于175~143 Ma（Davis et al.，1996，1998，2001; 赵越等，2002，2004; 刘健等，2006; 张长厚等，2011; Li Chengming et al.，2016b; 王永超等，2017; 陈宣华等，2019）。通过不同构造带内逆冲构造变形的运动学和几何学特征，以及对逆冲断层开展的构造解析和数值模拟研究，阴山-燕山构造带内的挤压变形形成于近南北向的挤压，而华北中部和阿拉善东缘该期挤压事件的主压应力优势方位为NWW-SEE向（张岳桥等，2007b; Zhang Jin et al.，2020; Zhao Heng et al.，2020; 张北航等，2021）（图4）。这可能就体现了来自不同方向作用的结果，其中近南北向的与北方的蒙古-鄂霍茨克洋关闭造山有关，而在扬子克拉通北缘的大巴山地区，这一时期的褶皱逆冲构造主要为NNW-NW-EW走向，形成向南西方向凸出的弧形构造带，该弧形构造的主体变形样式为叠瓦状逆冲构造和隔挡式褶皱，是一个具有多层滑脱特征的薄皮褶皱冲断构造带（张岳桥等，2010; Li Jianhua et al.，2015，2017c）。深反射地震剖面显示大巴山是一个形成于上地壳滑脱带之上的陆内薄皮造山带（Dong Shuwen et al.，2013）。这一褶皱冲断构造带中卷入的最新地层为中侏罗统，而下白垩统则未发生明显褶皱变形，表明褶皱冲断构造形成于中侏罗世之后，早白垩世之前（Shi Wei et al.，2012）。大巴山地区的这一时期的挤压变形形成于近南北向缩短作用下，与华北北缘同时期变形的主压应力方向一致。而西北西-东南东向则与古太平洋板块的低角度俯冲有关（Faure et al.，2012; Zhang Jin et al.，2021b），因此区域性的古应力方向统计能够有效约束可能的成因机制，同时也可以进一步划分出不同构造域可能的影响区域，对于古太平洋构造域，其西侧影响范围至少可以到阿拉善的东缘地区，而蒙古-鄂霍茨克构造域的影响范围可能到大巴山一线。
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华南地区中侏罗世—早白垩世构造变形同样发育广泛，主体是一系列北东走向的褶皱逆冲带，宽约1300 km（张岳桥等，2012）。深反射地震剖面揭示了华南地区中—上地壳以褶皱和冲断为主，对应显生宙盖层和前寒武纪基底分别卷入变形的薄皮和厚皮叠瓦式褶皱冲断构造；褶皱冲断带之下发育一条地壳尺度的主逆冲拆离断层，具明显的断坪-断坡-断坪结构，谐调了薄皮和厚皮冲断褶皱构造的变形差异（Li Jianhua et al.，2018; 张岳桥等，2019）。综合地球物理资料显示华南东南部的拆离断层数量多于西北部，东南侧拆离断层相对北西较深（颜丹平等，2000; 金宠等，2009）。构造变形呈现南东向北西逆冲扩展的规律，卷入变形的地壳层次逐渐变浅（张岳桥等，2019）。在东南沿海地区，这一时期的挤压事件形成了一系列NE走向的断裂带，如长乐-南澳断裂带带和莲花山断裂带，发生了指向NW的韧性逆冲剪切运动、变形变质作用以及地壳深熔作用（Liu Qian et al.，2012; Cui Jianjun et al.，2013; Li Jianhua et al.，2020）。岩浆岩锆石U-Pb年龄限定这一韧性逆冲构造发生于153~136 Ma（Cui Jianjun et al.，2013; Li Jianhua et al.，2020）。往西至扬子克拉通东部的雪峰山和武陵山地区，则发育一系列走向NE的厚皮和薄皮褶皱逆冲带（Yan Danping et al.，2003; Li Jianhua et al.，2012，2018; 李建华等，2024），卷入这一褶皱变形的最年轻地层为中侏罗统，同时被下白垩统不整合覆盖（Li Jianhua et al.，2012）。
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同时，在华南多个地区，如湘中涟源地区、鄂西南湘北地区、赣中地区、广西柳州地区以及南岭中段等地区，均可见NE走向的褶皱叠加于早期近东西走向褶皱之上（张岳桥等，2009），这期东西走向褶皱是扬子与华北克拉通碰撞的产物（张义平等，2015；Shi Wei et al.，2015），而晚期NE走向的褶皱则是晚侏罗世—早白垩世华南地区挤压变形的体现。造成华南地区这一时期挤压变形的主压应力场为近东西向（张岳桥等，2012; Li Jianhua et al.，2014，2018），这与华北中部同期变形是一致的（图4；Zhang Jin et al.，2021b）。
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华北和华南地区中侏罗世—早白垩世的缩短构造变形在构造样式和空间分布上存在一定的差异，但是均表明了该期事件在东亚地区广泛发育，在远离板块边缘的陆内形成了大规模的逆冲-褶皱构造。同时不同地区的构造变形所反映的构造应力场方向并不一致，这说明这一广泛发育的缩短变形并不是由单一的构造应力场所控制的。董树文等（2019）认为这一时期的变形具有多向性、同时性、弥散性等特点。在晚侏罗世，东亚周缘多板块汇聚形成了三个大型的陆缘汇聚造山系统：北部的蒙古-鄂霍茨克碰撞造山带、东部陆缘的Cordillera型俯冲增生造山系统，以及西南部的班公湖-怒江俯冲碰撞造山系统（董树文等，2019），正是东亚陆缘存在的多向汇聚体系，导致了陆内多向性的挤压变形构造的形成。而中侏罗世—早白垩世阶段的古构造应力场也反映出了类似特点，存在不同方向的古构造应力场（图4），但是总体而言，在中国的中东部，西北西-东南东的古构造应力场是主要的（图4），一些地区虽然显示了北西-南东向（燕山、太行山），这可能与多方向的作用叠加有关，而主体的近东西向（尤其是东部）显示了来自古太平洋构造域的影响。近些年来有关古太平洋板块该阶段低角度向西俯冲（Li Zhengxiang et al.，2007），不仅造成了吕梁山、贺兰山的崛起（Darby and Ritts，2002; Zhang Jin et al.，2020，2021a，2021b; Zhao Heng et al.，2020），而且也造成华南超宽陆缘弧背前陆逆冲带的形成（Li Jianhua et al.，2014）。
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需要强调的是，中侏罗世—早白垩世，虽然华北与华南的东部都经历了近东西向的缩短，但是两者的变形方式和样式是不一样，华南发育了几乎面状分布的逆冲与褶皱构造，一直可以深入扬子克拉通内部，而且以典型的薄皮构造为特点，并主要分布在扬子克拉通的东南缘。华北则以典型的厚皮构造为特点，而且主要分布在在早期的前寒武纪造山带为基底的地区（华北中部造山带—吕梁山以及华北西部孔兹岩带—贺兰山），这个差别一方面说明克拉通具有长距离传递应力的作用，另一方面也说明早期的造山带是应变最容易集中的地区。
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3.3 早白垩世
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早白垩世大规模的地壳伸展是整个中国东部，乃至整个东亚地区，是最为显著的一期构造事件，其分布范围北至俄罗斯外贝加尔湖地区，西至甘肃北山地区，最东可达西太平洋边界（Wang Tao et al.，2011; 郭磊等，2015; Lin Wei et al.，2020）。该期伸展导致了东北亚显著的岩石圈减薄、大规模岩浆活动以及相关的浅地表构造变形（如变质核杂岩、伸展穹隆、大量正断层、断陷盆地等）。这期变形也是“燕山运动”的重要组成部分（Wong Wenhao，1926，1927，1929），近年来也是“华北克拉通破坏”的重要研究内容（Meng Qingren，2003; Meng Qingren et al.，2003; Wang Tao et al.，2011 and references herein; 朱日祥等，2011，2012，2020; 林伟等，2013; 郭磊等，2015; Zhu Rixiang et al.，2015，2017; Zhang Fengqi et al.，2017; Lin Wei et al.，2020; Hui Jie et al.，2021; 王丹阳等，2024）。
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该期伸展在华北克拉通及其邻近地区形成大量的断陷盆地，影响的地区最西部可以到阿拉善以及更西侧的北山地区，这些盆地大多受控于盆地边缘NE-SW走向的高角度正断层或低角度拆离断层（Meng Qingren et al.，2003; Darby and Ritts，2007; Zhou Yinzhang et al.，2012; Zhang Jin et al.，2014，2021a）。同时，该期伸展还形成了另一种特征构造-变质核杂岩，如阿拉善北缘的亚干变质核杂岩、阴山-燕山构造带内的呼和浩特变质核杂岩、云蒙山变质核杂岩、辽南变质核杂岩、瓦子峪变质核杂岩，以及华北南缘的小秦岭变质核杂岩等（Davis et al.，1996，2002; Darby et al.，2004; Liu Junlai et al.，2005，2013; Lin Wei et al.，2008; Davis and Darby，2010; Guo Lei et al.，2012; Zhu Guang et al.，2015）。这些正断层和变质核杂岩的运动学特征指示了NW-SE的伸展。根据与变质核杂岩相关的韧性剪切带中云母40Ar/39Ar年龄，该期伸展发生在140~120 Ma，并且有从西往东逐渐变年轻的趋势。此外，阿拉善和华北北部地区在这一时期发育大量的基性岩浆侵位（Zhang Hongfu et al.，2002; Zhu Rixiang et al.，2004; 卫平生等，2005; 钟福平等，2011; Wang Jun et al.，2015; Wu Kai et al.，2017; 陈志鹏等，2019; Hui Jie et al.，2021），并且这些基性岩浆岩年龄有从东往西变年轻的特征（Hui Jie et al.，2021）。
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华南地区这一时期也发育同样的伸展构造，主要表现为大量发育的岩浆穹隆、伸展盆地以及少量的变质核杂岩或穹隆（舒良树等，2004，2006; Li Zhengxiang et al.，2007; 张岳桥等，2012及所引参考文献）。与华北地区广泛分布的伸展构造相比，华南该时期的伸展构造具有不均一性。伸展形成的穹隆和变质核杂岩主要分布在广东北部、江西、湖南、湖北和安徽南部一带，如洪镇穹隆、庐山穹隆、武功山核部浒坑岩浆穹隆、大云山变质核杂岩、衡山变质核杂岩和越城岭变质核杂岩等（Faure et al.，1996; Lin Wei et al.，2000; Zhu Guang et al.，2010; Ji Wenbin et al.，2017; Chu Yang，2017），这些穹隆和变质核杂岩整体呈向北东方向开口的Y字形分布（Lin Wei et al.，2020），而远离这一穹隆带，伸展构造则相对较弱且分布零散，主要表现为一些相对独立的不同岩性的侵入岩以及地堑、半地堑盆地（Zhou Xinmin et al.，2000; Li Zhengxiang et al.，2007; Shu Liangshu et al.，2009），这些盆地大多受近南北向或NE-SW走向正断层的控制（Li Jianhua et al.，2012，2014b）。除伸展形式的构造变形外，华南地区还发育有大量形成于136~118 Ma的侵入岩和火山岩（Li Xianhua，2000; Zhou Xinmin et al.，2000; Wang Qiang et al.，2006; Yang Shuiyuan et al.，2010，2011，2012; Jiang Yaohui et al.，2011; Wu Fuyuan et al.，2012; Yang Wei et al.，2012; Li Jianhua et al.，2014a，2014b; Li Wuxian et al.，2017d），虽然这些岩浆岩的岩石成因过程有所差别，但是均反映了早白垩世时期的软流圈上涌，以及由此引发的岩石圈伸展（Wong Jean et al.，2009; Zheng Wei et al.，2017）。
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目前，针对该期伸展的构造成因还存在多种观点，如蒙古-鄂霍茨克洋中脊的向南俯冲（Zhang Kaijun，2014）、古太平洋俯冲板块的后撤（Zhu Rixiang et al.，2017 and references therein; Hui Jie et al.，2021）、地幔上涌（Okada，1999; Zhang Kaijun et al.，2019）、蒙古-鄂霍次克洋闭合造成的加厚地壳的垮塌（Meng Qingren，2003; Wang Tao et al.，2011; Zhang Kaijun，2012）等。不管是华北还是华南，该期伸展的方向主体为NW-SE向，与古太平洋板块的俯冲方向一致，并且，华南这一时期的岩浆岩年龄呈现出往SE方向逐渐变年轻，εNd（t）往南东方向变大，而TDMC年龄往南东方向逐渐减小的趋势（Jahn et al.，1976; Gilder et al.，1996; Chen Jiangfeng et al.，1998）。而古构造应力场的统计也表明，虽然存在一些局部地区的差别，中国中东部（甚至包括西部）早白垩世的伸展基本上均为北西-南东向（图5），这种区域性的一致性，说明受控于统一的机制，而早白垩世古太平洋板块快速的后撤可以很好的解释这个特征。综合上述各种特征，东亚地区在早白垩世广泛发育的伸展，可能更多地受控于古太平洋板块后撤所导致的弧后伸展（Zhu Rixiang et al.，2017; Li Jianhua et al.，2020; Hui Jie et al.，2021），而蒙古-鄂霍茨克造山带的伸展垮塌以及深部的地幔物质上涌也是重要原因。此外还可以看出，古太平洋板块后撤影响的范围甚至可以达到华北西部的阿拉善地区。
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3.4 早白垩世末—晚白垩世初
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早白垩世末—晚白垩世初整个东亚地区再次进入一个长期被忽视的挤压构造环境。挤压导致了华南、华北以及东北地区早白垩世形成的伸展盆地发生了构造反转（Li Jianhua et al.，2014a; Suo Yanhui et al.，2020），形成了盆地内上、下白垩统之间的角度不整合（黄汲清，1960; 马寅生等，2002; 邴志波等，2003; 吴根耀等，2003; 吴跃东等，2003; 邓晋福等，2004; 刘伟等，2004; Guo Zhixin et al.，2018）。该期挤压造成的最显著的变形是一系列NE-SW或NNE-SSW走向的左行走滑断层，20世纪80年代即已被学者发现（徐嘉炜等，1985）。华北克拉通中部吕梁山—太行山地区，NNE-SSW走向的太行山断裂、霍山断裂和离石断裂在这一时期发生明显左行走滑剪切，与之伴生的还有一系列近东西走向的逆冲构造和褶皱（Zhao Heng et al.，2020; Zhang Jin et al.，2020）。华北克拉通西部，阿拉善地块与鄂尔多斯地块之间的贺兰山、桌子山和狼山地区，在晚白垩世发育一系列近南北走向的左行走滑断层以及北东向的逆冲断层（图9）（Darby and Ritts，2002; Zhang Jin et al.，2014，2021a; 张北航等，2021）。这期变形卷入了古元古代至早白垩世岩石，走滑距离约60 km，并形成了一系列的小的飞来峰构造（图9）（Darby and Ritts，2002; Zhang Jin et al.，2021a）；同时这一左行走滑断裂还导致了断裂西侧阿拉善地区早白垩世盆地内一系列近东西走向的褶皱和逆冲断层（Zhang Jin et al.，2021a）。通过对华北中部太行山、吕梁山地区，以及阿拉善东北缘狼山地区该期左行走滑断层的断层面解得出这些左行走滑的最大主应力方向为NNW-SSE向（Zhang Jin et al.，2020; 张北航等，2021）。
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华南地区在这一时期同样发育一系列左行剪切事件（徐嘉炜等，1985; 刘欢等，2021）。包括郯庐断裂带的左行韧性剪切（Zhu Guang et al.，2005，2010; 王微等，2015; 韩雨等，2015; 朱光等，2018）、皖南地区一系列北东走向的左行走滑断层（梁承华等，2019; 王朝等，2021）以及东南沿海长乐-南澳剪切带的左行走滑剪切（Tong Weixing et al.，1996; Wang Zhihong et al.，2000; 舒良树等，2000; 徐先兵等，2014）和局部的高级变质作用（Cui Jianjun et al.，2013）等。同时，在东南沿海长乐-南澳断裂带和莲花山断裂带，还分别发育有与左行走滑剪切同期的上盘指向南东和北西方向的逆冲构造（Wei Wei et al.，2015; Li Jianhua et al.，2020）。根据被切割的地层，以及被剪切带错断的岩浆岩脉体的锆石U-Pb年龄和剪切带中白云母的40Ar/39Ar测年结果，限定该期左行走滑发生于124~110 Ma。
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大量的低温热年代学数据同样也记录了这一时期构造事件的发生。在华南地区，磷灰石裂变径迹数据表明早、晚白垩世之间的构造事件发生于130~110 Ma（张沛等，2009; 刘文浩等，2012; 李天义等，2012; 王丹萍等，2014; 李朋等，2018; 邹耀遥等，2018）；华北中部的磷灰石裂变径迹数据则揭示了该期构造发生于125~80 Ma（刘武生等，2008; Zhao Junfeng et al.，2016; 黄志刚等，2018; Chang Jian et al.，2019; Zhang Jin et al.，2021b），并且，华北中部这一时期的磷灰石裂变径迹年代表现出由南往北逐渐变年轻的趋势（Zhang Jin et al.，2021b）。在东北地区，与该期挤压构造相关的磷灰石裂变径迹年代集中于95~65 Ma（杨峰平等，1995; 向才富等，2007; 温泉波等，2008; Cheng Yinhang et al.，2018; 杨雪叶等，2021）。整体来看，不仅在华北中部，在整个东亚，这一时期的磷灰石裂变径迹年龄也表现出了由南往北逐渐变年轻的趋势。需要指出的是，目前该期事件在华北和华南地区表现比较明显，而且年龄相对比较确定，而东北地区相关的年龄限定还较少，解释也还存在一定的争议，本项研究主要根据华北和华南地区的变形限定这次阶段。
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图9 狼山北部晚白垩世飞来峰构造
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Fig.9 Late Cretaceous klippe in northern Langshan
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关于这一时期在东亚广泛发育的构造事件的形成原因目前有多种看法，但普遍认为与欧亚板块东缘的构造有关。有学者认为此时古太平洋板块仍保持着相对低的角度向西俯冲于欧亚板块之下，并且俯冲速度也较高（Northrup et al.，1995; Liu Shaofeng et al.，2017; 朱光等，2018）。Li Jianhua et al.（2020）根据华南地区在晚中生代连续多次的挤压-伸展构造事件的交替出现，认为晚白垩世早期的挤压事件仍与古太平洋板块的俯冲角度有关，早白垩世回撤的古太平洋板块端部发生榴辉岩化，从板块上断离，引起俯冲板块的回弹，使得古太平洋板块再次向西发生低角度俯冲，从而导致了这一时期挤压构造事件的发育。更多的学者则认为，此时一个陆块或洋底高原与欧亚板块东南缘发生了碰撞（Faure，1989; Yang Yongtai，2013; Niu Yaoling et al.，2015）。Faure（1989）认为该陆块是西菲律宾板块，而Yang Yongtai（2013）则称之为Okhotomorsk地块，并且认为这一陆块在与欧亚板块东南缘碰撞之后，沿欧亚板块边缘继续向北运移，从而导致了东亚地区这一时期大量左行走滑剪切的发生。这一构造模型也与低温热年代学数据以及早白垩世盆地反转时间从南往北逐渐变年轻相一致。同样，区域性稳定的古构造应力场也反映了这期变形受控于东侧统一的作用，而且其影响范围最西部可以达到阿拉善东缘（图6）。
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4 结论
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古构造应力场是构造演化研究中重要的参数。我国西部还缺少通过断层滑动矢量反演的古构造应力场资料，但目前的中国中、东部的工作已经为我们提供了这方面的可能，为我们提供了从构造应力场讨论一级构造环境的可能。现有的统计表明，中国中、东部中生代可以划分出4个不同阶段的古构造应力场，即中、晚三叠世、中侏罗世—早白垩世、早白垩世和早白垩世末—晚白垩世初。而应力场区域性特征可以用来约束主要构造阶段的环境与背景。中国中、东部中生代的陆内演化或者变形与不同时代来自不同方向的板缘作用有重要关系，当然也不排除其他因素的可能性。
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致谢：谨以此文祝贺任纪舜院士90华诞。在参加任院士的项目过程中，先生一直长期关注我们的工作，本文的撰写也一直得到任先生的启发。感谢贵州大学曹鹏硕士帮助本文编辑图件。在撰写本文的过程中，一些想法或者认识尚属浅薄，也不可避免存在错误，希望能够抛砖引玉，得到更多的讨论。
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摘要
中生代是中国中东部重要的演化阶段，发育有不同阶段鲜明和丰富的陆内变形。通过统计分析基于断层滑动矢量反演得到的古构造应力场数据，进一步细化了前人关于中国东部古构造应力场的划分方案，将我国中东部的中生代演化划分为4个阶段，即中、晚三叠世、中侏罗世—早白垩世、早白垩世、早白垩世末—晚白垩世初。古构造应力场区域性特征可以用来约束主要构造阶段的环境与背景。统计表明，中、晚三叠世北方以近南北向缩短为主而南方由于旋转以及多板块的作用，显示不同方向的古构造应力场，三叠纪早期还发育有不同性质的韧性变形，古亚洲洋关闭后的陆内变形、华北与扬子板块的碰撞、扬子与印支地块的碰撞以及东、西华夏地块之间的作用是导致不同地区不同变形以及不同古构造应力场的背景；中侏罗世—早白垩世在总体一致的西北西-东南东向区域应力场条件下，叠加了蒙古-鄂霍茨克造山带的作用，同期的古太平洋板块低角度的俯冲是主控因素；早白垩世的区域性北西-南东向伸展指示具有一致的背景，古太平洋板块的回撤可能是主控因素；早白垩世末—晚白垩世初在中国中东部存在一期短暂的北西-南东向缩短，从南向北，变形的时代依次变年轻，指示欧亚大陆东缘存在一期从南至北的构造作用，可能与外来地块的碰撞作用有关。中国中东部中生代的陆内演化或者变形与不同时代来自不同方向的板缘作用有重要关系，当然也不排除其他因素的可能性。
Abstract
The Mesozoic period is an important phase for central-eastern China, characterized by multistage, distinct, and abundant intracontinental deformation. According to statistical analysis of paleo-stress data retrieved from fault slip vectors, the Mesozoic tectonic evolution in central-eastern China can be divided into four stages: Middle-Late Triassic, Middle Jurassic-Early Cretaceous, Early Cretaceous, and latest Early Cretaceous-early Late Cretaceous, which further refined the previous division. Regional paleo-stress patterns are crucial for outlining the tectonic settings of major tectonic stages. Statistical analysis reveals that during the Middle-Late Triassic, northern China experienced north-south compression, while southern China exhibited various paleo-stress directions due to the rotation and tectonics of multiple plates. Additionally, ductile deformation with varying kinematics also developed during the Early Triassic. These distinct deformation and paleo-stress patterns across different regions were driven by intracontinental deformation processes, initiated by the closure of the Paleo-Asian Ocean, the collision between the North China Craton and the Yangtze Craton, the collision between the Yangtze Craton and Indochina Block, and tectonic interactions between the eastern and western Cathaysia blocks. During the Middle Jurassic to Early Cretaceous, the regional paleo-stress field was characterized by west-northwest to east-southeast compression, which dominantly resulted from the low-angle subduction of the Paleo-Pacific Plate, superimposed by the Mongol-Okhotsk Orogeny. The Early Cretaceous regional northwest-southeast extension indicates a consistent tectonic setting, which may be mainly controlled by the retreating subduction of the Paleo-Pacific Plate. In the latest Early Cretaceous to early Late Cretaceous, central-eastern China experienced a short-term northwest-southeast compression, with deformation times gradually shifting from south to north. This indicates a tectonism migration from south to north along the eastern margin of Eurasia, possibly triggered by a collision with an unknown block against East Asia. The Mesozoic intracontinental deformation, or tectonic evolution, in central-eastern China was dominantly controlled by far-field effects of plate margins with different orientations across periods. However, other potential factors may contribute to the observed tectonic evolution, which remain to be fully explored.
Keywords
central-eastern China ； paleo-stress field ； tectonic evolution ； fault slip vector ； Mesozoic
