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典型造山带由腹陆构造带（Hinterland belt）、前陆逆冲带（Foreland thrust belt）和前陆盆地（Foreland basin）等构造单元组成，因总体呈指向前陆的楔形而被称为造山楔（Orogenic wedge）（Taylor et al.，1980; Willett et al.，1993; DeCelles and Gilest，1996; Yin and Harrison，2000; DeCellesand Coogan，2006; Johnston and Gutierrez-Alonso，2010; Vanderhaeghe，2012; Tremblay and Pinet，2016）。前陆逆冲带是造山带前陆区域在无变质，或者中低级变质作用条件下，由薄皮或者薄皮与厚皮逆冲推覆构造主导形成的变形带（Boyer and Elliott，1982; Shaw et al.，1994，2004; Pfiffner，2006; Fossen，2012; Weil and Yonkee，2012）。前陆逆冲带几何结构上呈复杂的三角楔形，通常被称为逆冲楔（Thrust wedge）（Graveleau et al.，2012）。逆冲楔可以通过不同组合形式构成复杂三角带（Triangle zone）（Hagke and Male，2018）。
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前陆逆冲带和其中的构造网络系统控制了全球许多特大型、大型油气田的生油生气、储集、圈闭、运移，甚至盖层和保存条件，是最重要的油气勘探构造（Tavani et al.，2015）。20世纪60年代以来，在前陆逆冲带构造理论和模式指导下，油气田勘探与开发取得了巨大进步（Engelder and Engelder，1977; Burchfiel，1980; Protzman and Mitra，1990; DeCelles and Giles，1996; Sans et al.，2003; Lacombe et al.，2007; Evans，2010; Tavani et al.，2011，2015; Cummings et al.，2012; Awdal et al.，2013）。此外，许多前陆逆冲带还是地震等新构造活动带（Lacombe et al.，2006; Burchfiel et al.，2008; Xu Zhiqin et al.，2008; Hubbard and Shaw，2009; Jia Dong et al.，2010; DeCelles et al.，2011; Oskin，2012; 崔军文等，2013）。因此，前陆逆冲带不仅是造山带理论研究的核心，而且在油气勘探开发和预防地震等地质灾害方面具有重要应用价值。
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前陆变形从临界状态转入超临界状态，形成新的逆冲楔，从而实现前陆逆冲带生长。同时，早先形成的逆冲楔再变形并卷入前陆逆冲带扩展过程（Tavani et al.，2015）。基于断层-褶皱关系的认识（图1），建立了前陆逆冲带共轴复合扩展的构造运动学模式（Yan Danping et al.，2016及其中文献）。虽然共轴扩展的构造运动学模式被广泛接受和认可，但在前陆逆冲带扩展过程中，特别是侧缘扩展中普遍发育的非共轴变形无法用现有构造模式进行解释。
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四川盆地盆缘发育江南造山带西南部的武陵山-华蓥山前陆逆冲带、北部秦岭-大别造山带南缘的大巴山前陆逆冲带和西部龙门山前陆逆冲带（张岳桥等，2011; 邓宾，2013; Wang Erchie et al.，2014）。这三条造山带前陆逆冲带形成的大地构造背景和时代各不相同，几何结构也各有差异，但均保存有完整的前陆逆冲楔结构和扩展关系，其扩展构造运动学均指向四川盆地内部。三条前陆逆冲带形成演化过程中，不但分别保存了经典造山带前陆共轴递进扩展的复合变形特征，而且在特殊部位形成了构造应力场的联合演化（图2）。尤其重要的是，三条前陆逆冲带在复合和联合演化过程中，造就了四川盆地及盆缘普光、垄岗等数个特大型气田的形成与巨量储集（邓宾，2013; 李英强，2018; 蔚远江等，2019; 郑民等，2019）。同时，在天然气田勘探和开发过程中采集和保存的系统地质-地球物理数据又有助于前陆逆冲带研究的理论总结和提升（图2）。然而，如何区分和理解三条前陆逆冲带的共轴复合与联合演化特征，成为四川盆地盆缘前陆逆冲带研究的关键难题。
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本文在大地构造背景分析基础上，对四川盆地盆缘武陵山-华蓥山前陆逆冲带、大巴山前陆逆冲带和龙门山前陆逆冲带的结构、扩展方式的研究进行总结。在此基础上，对前陆逆冲带研究现状、问题和发展方向进行综述。从研究现状、前沿科学问题和发展方向三个方面进行总结，为未来前陆逆冲带的研究提供方向和参考。
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图1 前陆逆冲带断层相关褶皱典型构造样式与样式组合（据Boyer and Elliott，1982; Jamison，1987; Yan Danping et al.，2016修改）
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Fig.1 Typical structural styles and assemblages of fault-related fold in foreland thrust belt (modified after Boyer and Elliott, 1982; Jamison, 1987; Yan Danping et al., 2016)
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（a）—拆离褶皱;（b）—断展褶皱;（c）—断弯褶皱;（d）—叠瓦状逆冲构造;（e）—被动顶板双重逆冲构造;（f）—主动顶板双重逆冲构造
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(a) —Decollement fold; (b) —fault-propagation fold; (c) —fault-bend fold; (d) —imbricated thrust fault; (e) —passive roof duplex; (f) —active roof duplex
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图2 四川盆地、盆缘前陆逆冲带地质图以及区域性地震探测剖面分布图（地质底图据黄崇轲等，2002和相关区域1∶20万区域地质调查图综合编制）
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Fig.2 Geological map of the Sichuan basin and basin marginal foreland thrust belts with distribution of main regional seismic profiles (geology was edited based on Huang Chongke et al., 2002 and relevant 1∶200000 regional geological maps)
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图中地球物理剖面白色实线为地震剖面; 红色虚线为P波和S波速度剖面。注:穿越武陵山-华蓥山前陆逆冲带北、中和南有至少7条地震反射剖面（据王海燕等，2006，2010; Yan Danping et al.，2009; 金宠，2010; 汪昌亮等，2011; Li Sanzhong et al.，2012; Deng Yangfan et al.，2014; Dong Shuwen et al.，2015; Gao Rui et al.，2016; Guo Lianghui and Gao Rui，2018; Li Jianhua et al.，2018; Zhu Xiaoshan et al.，2020）; 穿越大巴山前陆逆冲带西、中和东段至少有6条地震反射剖面（据李智武等，2006; 陈亚平等，2006; 吴小羊等，2008; 李秋生等，2011; Dong Shuwen et al.，2013; Li Jianhua. et al.，2015; Jiang Chengxin et al.，2016; Li Wangpeng et al.，2017; Zhang Yueqiao et al.，2022）; 穿越龙门山前陆逆冲带北中段至少有6条地震反射剖面（据Jia Dong et al.，2006; Yan Danping et al.，2011，2018a; Feng Shaoying et al.，2016; Gao Rui et al.，2016; Li Jianhua et al.，2018）; 三条P波和S波速度结构大剖面和若干大地电磁与重力剖面穿越四川盆地及其盆缘造山带（据Huang Jinli and Zhao Dapeng，2006; Deng Yangfan et al.，2014; Zhang Letian et al.，2015; Guo Lianghui and Gao Rui，2018; Wang Xu et al.，2018）
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White hard lines are seismic profiles, and red dot lines are P-wave and S-wave velocity profiles. Note that at least 7 seismic profiles across the northern, middle and southern segments of the Wulingshan-Huayingshan foreland thrust belt (after Wang Haiyan et al., 2006, 2010; Yan Danping et al., 2009; Jin Chong, 2010; Wang Changliang et al., 2011; Li Sanzhong et al., 2012; Deng Yangfan et al., 2014; Dong Shuwen et al., 2015; Gao Rui et al., 2016; Guo Lianghui and Gao Rui, 2018; Li Jianhua et al., 2018; Zhu Xiaoshan et al., 2020) ; at least 6 seismic profiles across the Longmen Shan foreland thrust belt (after Jia Dong et al., 2006; Yan Danping et al., 2011, 2018a; Feng Shaoying et al., 2016; Gao Rui et al., 2016; Li Jianhua et al., 2018) ; in addition to 3 P-wave and S-wave velocity profiles and several magnetotelluric and gravity profiles across the Sichuan basin and its marginal orogenic belt (after Huang Jinli and Zhao Dapeng, 2006; Deng Yangfan et al., 2014; Zhang Letian et al., 2015; Guo Lianghui and Gao Rui, 2018; Wang Xu et al., 2018)
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1 四川盆地盆缘前陆逆冲带研究概述
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1.1 武陵山-华蓥山前陆逆冲带
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NNE向雪峰山造山带是华南江南造山带的西南段（Shu Liangshu and Charvet，1996; Yao Jinlong et al.，2019），从南东向北西宽度近600 km，由造山带腹陆带和东西两侧前陆逆冲带组成。腹陆带为雪峰山厚皮逆冲构造带，南东侧前陆逆冲带为湘中复合逆冲带，而北西侧即武陵山-华蓥山前陆逆冲带，包括梵净山-走马穹隆构造带、隔槽式逆冲构造带和隔档式薄皮构造带组成（图3）（Yan Danping et al.，2003a; 汪昌亮等，2011; 颜丹平等，2018），其NW—SE宽度近400 km。作为江南造山带重要组成部分，雪峰山造山带主要经历了新元古代华夏地块与扬子地块的俯冲、碰撞造山作用（Zhao Junlong et al.，2011; Wang Erchie et al.，2012）和中生代以来的总体指向北西的陆内造山作用（Hsü et al.，1990; 陈海泓，1993; 丘元禧等，1999; Yan Danping et al.，2003a; Wang Yuejun et al.，2005; Xiao Wenjiao et al.，2005; Li Zhengxiang and Li Xianhua，2007）。
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前人对武陵山-华蓥山前陆逆冲带变形构造样式组合、构造运动方向及其变形机制进行了广泛深入的研究（Hsü，1981; Hsü et al.，1990; 陈海泓，1993; 丘元禧等，1999; Yan Danping et al.，2003a，2009，2016; Wang Yuejun et al.，2005; Xiao Wenjiao et al.，2005; Li Zhengxiang and Li Xianhua，2007; Lu Guo et al.，2021）。中石化、中石油等在相关区域实施了广泛研究和勘探工作，在区内及相关邻区构造中发现了与上述构造变形过程密切相关的普光、垄岗等特大型天然气田，同时获得了大量地震、钻探和大地电磁探测资料。在中石化支持下，张国伟院士领导的科研团队在2007~2009年对这一区域进行了系统详细的前瞻性地质调查与研究工作（张国伟，2009; 王建等，2010; 李三忠等，2011）。
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Fig.3 Geological map of Xuefengshan orogenic belt and its Wuling-Huaying foreland thrust belt (edit based on Huang Chongke et al., 2002 and relevant 1∶200000 regional geological maps; Yan Danping et al., 2018)
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剖面A—A’（据Dong Shuwen et al.，2015修改）和剖面B—B’（据Li Jianhua et al.，2018修改）均是在地震深反射剖面基础上进行的构造解释
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Profiles A—A’ (modified after Dong Shuwen et al., 2015) and B—B’ (modified after Li Jianhua et al., 2018) are tectonic interpretation based on deep seismic refraction profiles
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1.1.1 武陵山-华蓥山前陆逆冲带构造分带特征
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武陵山-华蓥山前陆逆冲带具有清晰的结构分带，积累的地质和地球物理资料已经能够判断地表和地下构造样式及其组合特征。根据断层-褶皱组合样式特征，从南东至北西武陵山-华蓥山前陆逆冲带可划分为梵净山-走马穹隆带、隔槽式逆冲构造带和隔档式逆冲构造带。
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梵净山-走马穹隆带以梵净山构造穹隆为典型代表。梵净山构造穹隆呈NE向长垣状，穹隆核部出露中元古界梵净山群中深变质岩系，其上角度不整合或者微角度不整合覆盖板溪群浅变质岩系至下古生界。穹隆总体构造样式为西翼陡东翼缓的不对称的箱状背斜，地震剖面揭示穹隆深部发育断坪-断坡式逆冲断层，断坪深切至梵净山群，断坡位于背斜西翼（颜丹平等，2018）。在断坪-断坡逆冲断层作用下，梵净山群和板溪群被小距离逆冲出露地表。因此，梵净山穹隆是厚皮逆冲作用下的断层相关褶皱（图3、图4）。
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隔槽式逆冲构造带位于齐岳山断裂与梵净山-走马穹隆构造带之间，主要发育一系列轴向NE的箱状背斜和尖棱向斜。箱状背斜核部地层主要为寒武系，根据平衡地质剖面原则推断，向深部可能卷入震旦系-板溪群。区域上发育一系列主要倾向NW的高角度逆冲断层，以及倾向SE的反冲断层。综合地面地质调查和地震剖面解释确定为逆冲断层断坪-断坡式相关褶皱（Yan Danping et al.，2003a，2009，2018b）。逆冲断层主要断坪沿变质基底软弱层发育（颜丹平等，2008），基本构造样式与运动学特征与梵净山穹隆体相似，属于厚皮逆冲构造下的断层相关褶皱，但表露层次较浅。
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隔档式逆冲构造带位于华蓥山断裂与齐岳山断裂之间，以发育尖棱背斜和箱状向斜为特征（图5）。尖棱背斜核部主要为三叠系至侏罗系，在南部赤水-宜宾一带翼部卷入下白垩统，而区域上上白垩统没有卷入褶皱变形（四川省地质矿产局，1991）。本构造单元内断坪-断坡式逆冲断层发育，主逆冲断层总体倾向SE，并发育有倾向NW的反向逆冲断层，尖棱背斜为主逆冲断层作用下的断展褶皱。区域性断坪主要沿寒武系底部黑色页岩和三叠系内部泥岩层发育。根据地质剖面和深地震反射剖面解释，在寒武系顶底层下可能形成主动顶板双重逆冲构造（Yan Danping et al.，2009; 颜丹平等，2018）。因此，本构造单元属于薄皮逆冲构造带（图5）。
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1.1.2 武陵山-华蓥山前陆逆冲带变形时序与构造运动学
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武陵山-华蓥山前陆逆冲带变形时序约束是在构造关系分析的基础上结合了年代学的证据。综合韧性剪切带白云母和黑云母40Ar/39Ar年龄、磷灰石和锆石裂变径迹和（U-Th）/He年龄，雪峰山造山带腹陆带变形时间可能为244~195 Ma（Wang Yuejun et al.，2005），梵净山-走马穹隆构造带变形起始时间可能为晚侏罗世（~165 Ma），在150~140 Ma递进扩展至隔槽式逆冲构造带，而华蓥山褶皱逆冲带变形时间可能至晚白垩世早期（95 Ma）（Yan Danping et al.，2003a; 梅廉夫等，2010; Tang Shuangli et al.，2013）。因此，武陵山-华蓥山前陆逆冲带从SE向NW自晚侏罗世开始，逐渐演化至晚白垩世早期。
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图4 梵净山背斜穹隆构造西翼、转折端和东翼地层及产状特征
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Fig.4 Strata and occurrence in the west limb, hinges and east limb of the Fanjingshan anticlinal dome
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图5 隔档式逆冲构造带地质廊带图（a）和地质剖面B—B’及其构造解释（b）（据颜丹平等，2018; Li Jianhua et al.，2018修改; 剖面位置见图3）
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Fig.5 Geological map (a) and B—B’ profile with structural interpretation (b) of the cuspate anticline belt (modified after Yan Danping et al., 2018; Li Jianhua et al., 2018; profile location is shown in Fig.3)
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武陵山-华蓥山前陆逆冲带是典型的厚皮-薄皮构造样式组合（丘元禧，1994; 丘元禧等，1999; 颜丹平等，2000，2018; 朱光和刘国生，2000; Yan Danping et al.，2003a，2016; 丁道桂等，2005，2007）。从深向浅部构造层次逐渐发育从后展式逆冲断层-褶皱构造组合向前展式逆冲断层-褶皱组合，在平面上表现为从腹陆向前陆的厚皮向薄皮逆冲构造组合转化的构造分带（Yan Danping et al.，2009，2016）（图3）。其中薄皮逆冲构造组合以寒武系底部（黑色页岩组合）拆离断层为主导，沿寒武系—奥陶系、志留系和三叠系等的页岩层和盐层形成多层区域性拆离滑脱断层（孙岩等，1992; Yan Danping et al.，2003，2009; 颜丹平等，2008; 张必龙等，2009）。
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综上所述，武陵山-华蓥山前陆逆冲带为晚侏罗世—晚白垩世早期，在中生代NW—SE向陆内挤压作用下，通过从SE向NW的递进逆冲构造作用下，以断坪-断坡式逆冲断层主导相关褶皱的形成和扩展。三个构造单元的分带性特征不但是从SE向NW递进变形作用下共轴复合逆冲构造作用的体现，而且还体现了构造层次及其剥露关系（Yan Danping et al.，2003a，2009; 颜丹平等，2008，2018）。
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1.2 大巴山前陆逆冲带
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大巴山前陆逆冲带位于秦岭-大别造山带南缘，其东西两端分别受到黄陵穹隆和汉南-米仓构造结的制约，表现为一系列北北西—北西—东西走向紧密排列的褶皱-逆冲带，并呈弧形向南突出（图6a、b）（董树文等，2006，2010），经城口-房县断裂带分为南大巴山和北大巴山逆冲带（李智武，2006; 李智武等，2006; 张岳桥等，2010; Dong Shuwen et al.，2013）。大巴山前陆逆冲带是秦岭-大别造山作用进入陆内变形阶段变形的产物。
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北大巴山逆冲带位于安康断裂与城口-房县断裂（向NW分支出镇巴断裂）之间。北大巴山逆冲带由一系列总体倾向NE和构造运动学指向SW的复杂逆冲断层和太古界—中元古界基底变质岩卷入的逆冲岩片组合形成叠瓦状逆冲推覆构造（图6a、c），因此属于厚皮逆冲构造。南大巴山逆冲带位于城口-房县断裂以SW，与四川盆地北部渐变过渡。据深地震反射剖面解释结果，可能沿震旦系底部（可能为陡山沱组煤层或炭质页岩）与上三叠统底部形成区域性滑脱拆离断层，从而形成主动顶板式双重逆冲构造，浅部则形成构造运动学指向SW的叠瓦状逆冲构造，并卷入下白垩统（图6c）（董云鹏等，2008; 张岳桥等，2011; Dong Shuwen et al.，2013）。
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图6 大巴山前陆逆冲带地质图（a）（据四川区域地质志，1991; 黄崇轲等，2002 综合编制）和深地震反射剖面C-C'及其构造解释（b）（据Dong Shuwen et al.，2013; Li Jianhua et al.，2015; Zhang Yueqiao et al.，2022修改）
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Fig.6 Geological map of the Dabashan foreland thrust belt with seismic profile and structural interpretation (a) (edited based on SBGMR, 1991; Huang Chongke et al., 2002) , seismic refraction profile C-C' and tectonic interpretation (b) (modified after Dong Shuwen et al., 2013; Li Jianhua et al., 2015; Zhang Yueqiao et al., 2022)
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一般认为，大巴山由印支期秦岭碰撞造山和中晚侏罗世板内造山等多期构造事件复合形成（董云鹏等，2008; 张岳桥等，2010，2011）。大巴山前陆逆冲带具有清晰的垂直走向方向构造分带和平行走向的西、中和东构造分段（张国伟等，2001; 李智武等，2006; 董云鹏等，2008; 张岳桥等，2010），在垂向上存在多个滑脱层并主导和控制了变形样式和组合（李智武等，2006）。北大巴山逆冲带主要是叠瓦状逆冲楔，而南大巴山广泛出露共轴叠加褶皱，主要变形包括:① 245~189 Ma华南-华北碰撞过程中形成的前陆逆冲构造和指向南的北西走向脆-韧性剪切带; ② 178~143 Ma的逆冲叠加构造和北北西走向右行走滑韧性剪切带和双重构造（Hu Jianmin et al.，2012; Li Pengyuan et al.，2012; Li Jianhua et al.，2013，2015; Li Wangpeng et al.，2017）（图6c）。总之，大巴山前陆逆冲带逆冲楔的基本样式是共轴递进前展复合褶皱逆冲构造，其形成受华南-华北碰撞作用及其后续陆内持续向南的挤压作用控制。
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大巴山前陆逆冲带中NW向剪切带逆冲起始时间约为245~189 Ma，NNW向韧性剪切带活动时间为178~143 Ma（Li Jianhua et al.，2013，2015），城口断裂同变形绢云母40Ar/39Ar年龄为145~143 Ma（Li Pengyuan et al.，2012），北大巴山逆冲楔约于100~90 Ma终止扩展（Yang Zhao et al.，2017）。南大巴山逆冲楔开始于晚白垩世之前，扩展终止于约85~70 Ma（Hu Jianmin et al.，2012; Tian Yuntao et al.，2012; Zhang Zengbao et al.，2013）。因此，大巴山前陆逆冲带穿时活动于印支期至燕山末期（董树文等，2006; Wang Ruirui et al.，2019）。
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大巴山前陆逆冲带NW和SE两侧断层-褶皱走向发生强烈变化。北西侧形成近SN向的镇巴构造带，其基本样式为指向西的断层相关褶皱（图7c）。南东侧为近EW向的断层-褶皱带，以秭归褶皱带为例，J3-K1至少经历近EW向断层-褶皱构造作用、近SN向褶皱和NE—SW向逆冲作用三期变形（施炜等，2007; 董树文等，2010; 宋庆伟等，2014）。
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通过构造应力场重建，复杂的秭归褶皱带被认为是大巴山前陆逆冲带与武陵山-华蓥山前陆逆冲带在J3-K1时期联合作用的结果（宋庆伟等，2014）。这种联合作用不仅对大巴山前陆逆冲带扩展作用认识具有理论意义，而且现实指导了油气田的勘探开发工作（李承三和郭令智，1943; 许志琴等，1986; 董树文等，2010; 黄光明等，2016）。
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1.3 龙门山前陆逆冲带
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龙门山前陆逆冲带位于青藏高原东缘、四川盆地西缘，目前呈NE走向，向北东与秦岭-大别造山带相接，向南西被NW向鲜水河断裂切割后，归入盐源-木里弧形构造带（图2）（Yan Danping et al.，2003b，2018b）。NE向的北川-映秀断层将龙门山前陆逆冲带与西侧的腹陆构造带隔离开来，但SE侧狭窄的前陆逆冲带仅有几千米至数十千米宽，其前缘以断续出露的NE向灌县-安县断层与川西前陆盆地分隔（Chen Shefa and Wilson，1996; Worley and Wilson，1996; Arne et al.，1997; Meng Qingren et al.，2005; Jin Wenzheng et al.，2010; Yan Danping et al.，2011，2018a，2018b; Sun Ming et al.，2018）。
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研究证明，龙门山前陆逆冲带西界北川-映秀断层与东界灌县-安县断层均表现为早期糜棱岩叠加后期碎裂岩与断层泥，并具有倾向NW的断坪-断坡式结构，从而形成构造运动学指向SE的逆冲楔（Burchfiel et al.，2008; Parsons et al.，2008; Jin Wenzheng et al.，2010; Zheng Yong et al.，2016）。其中北川-映秀断层是2008年汶川地震的发震断层，自晚三叠世以来活动（Burchfiel et al.，1995; Arne et al.，1997; Kirby et al.，2002; Xu Zhiqin et al.，2008; Yan Danping et al.，2008a，2011，2018a; Zheng Yong et al.，2016）。灌县-安县断层倾向NW，呈断坪-断坡样式，断坡倾角30°~50°，切过三叠系至第四系，表明具有新构造活动（四川省地质矿产局，1991; Li Yong et al.，2003; Xu Zhiqin et al.，2008; Yan Danping et al.，2008a，2008b）。
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通过区域构造大数据的总结和解剖，龙门山前陆逆冲带经历至少三期变形，D1期指向SSW的递进逆冲推覆构造，从北向南包括碧口、唐王寨、龙王庙，以及可能的丹巴等3~4个逆冲推覆体，其形成北部碧口逆冲推覆体从237 Ma开始，结束于201 Ma（Yan Danping et al.，2011，2018a; Liu Shaofeng et al.，2015），唐王寨逆冲推覆体活动于220~207 Ma（Airaghi et al.，2018），龙王庙逆冲推覆体起始于209 Ma前，结束于174 Ma，向南可能还存在更年轻的逆冲构造，延续至156 Ma结束（Zhou Meifu et al.，2008; Zheng Yong et al.，2016; Airaghi et al.，2017，2018; Yan Danping et al.，2018a）。D2期为早侏罗世开始的指向SE的区域伸展构造，并形成变质核杂岩构造和局部伸展盆地（Yan Danping et al.，2011）。D1期和D2期构造属于秦岭造山带陆内变形阶段持续向南挤压和造山后伸展构造（Yan Danping et al.，2018a）。
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图7 龙门山复合生长逆冲带结构模式图（据颜丹平等，2020修改）
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Fig.7 Tectonic model sketch of the Longmen Shan tectonic complex (modified after Yan Danping et al., 2020)
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D3期为新生代指向SE的前陆逆冲作用（Burchfiel et al.，1995，2012; Worley and Wilson，1996; Arne et al.，1997; Harrowfield and Wilson，2005; Jia Dong et al.，2006，2010; Yan Danping et al.，2011，2018a，2018b; Oskin et al.，2012; Billerot et al.，2017），其可能起始于40~35 Ma，于渐新世末结束，并于20~16 Ma和~5 Ma分期形成指向SE的前陆扩展（Yan Danping et al.，2011; Wang Erchie et al.，2012，2014）。可见，龙门山实际包含了D1期指向SSW和D3期指向SE两期前陆逆冲构造，因此是一条非共轴的复合前陆逆冲构造（Yan Danping et al.，2018a，2018b）（图7）。D3期为新生代青藏高原向SE挤压和生长的结果。
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2 前陆逆冲带扩展方式
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总结四川盆地盆缘武陵山-华蓥山、大巴山和龙门山前陆逆冲带的构造特征，虽然形成的大地构造背景、时间和扩展方向各有差异，但通过构造运动学总结，其形成的大地构造背景均为造山作用进入陆内的持续变形阶段，并存在三种扩展方式，即共轴递进逆冲扩展、非共轴叠加扩展和联合扩展。
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2.1 共轴递进逆冲扩展
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作为前陆逆冲带普遍存在的扩展方式，在武陵山-华蓥山、大巴山和龙门山前陆逆冲带中均典型发育。共轴递进逆冲扩展作用具有以下构造特征:
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（1）主要构造样式和组合样式是断层相关褶皱主导下的叠瓦状逆冲构造组合和双重逆冲构造组合形式。其中双重逆冲构造组合还没有在野外调查中实地观测到，均是在平衡地质剖面基础上，通过地震剖面解释推测构建的。
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（2）平面上具有明显的构造分带，表现为从靠近腹陆的厚皮构造带向前陆方向转变为薄皮构造带。目前识别出来的厚皮逆冲构造组合均为主动顶板双重逆冲构造。推测厚皮逆冲推覆构造组合是在薄皮逆冲构造组合基础上，在共轴叠加和复合作用下，逐步卷入深层次变质基底岩石而形成的。
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（3）基本一致的构造运动学方向。在各前陆逆冲带主体构造部位，武陵山-华蓥山前陆逆冲带始终指向NW，大巴山前陆逆冲带则始终指向SW，龙门山前陆逆冲带D1期一致指向SSW，D3期指向SE。这些方向均为当时的前陆盆地所在方向。
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（4）从腹陆向前陆方向逐渐年轻但具有穿时的时间序列。四川盆地盆缘的三条前陆逆冲带各构造单元时间约束还不够精细，但从构造关系分析，结合已经获得的时间约束结果，可能表现出穿时变形的时间序列。
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2.2 非共轴叠加扩展
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龙门山复合前陆逆冲带是典型的非共轴叠加扩展实例（颜丹平等，2020）。龙门山复合前陆逆冲带中D1和D3两期前陆逆冲带构造轴向近于直交，其运动学方向也大角度相交（Burchfiel et al.，1995，2012; Worley and Wilson，1996; Arne et al.，1997; Harrowfield and Wilson，2005; Yan Danping et al.，2011，2018a，2018b; Oskin et al.，2012; Billerot et al.，2017; 颜丹平等，2020）。新生代的前陆逆冲构造（D3）可能并不是原来认为的窄条带，而很可能已经向东发展至成都以东的龙泉山逆冲构造（Jia Dong et al.，2006; Oskin et al.，2012; Feng Shaoying et al.，2016; Yan Danping et al.，2018a）（图7）。因此，龙门山复合前陆逆冲带有可能是一个近似非共轴横跨叠加的褶皱-逆冲推覆构造。
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2.3 联合扩展
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当两条毗邻的前陆逆冲带扩展活动方向大角度相交，且时间上具有交集时，就形成了不同程度的构造应力场联合，从而产生联合扩展。区内武陵山-华蓥山和大巴山前陆逆冲带叠合区内的秭归复式褶皱带即是联合扩展的结果（宋庆伟等，2014）。详细的构造解析和构造应力场恢复表明，晚侏罗世为大巴山前陆逆冲带主导形成了近EW向褶皱带，经过过渡变形阶段后，早白垩世—晚白垩世早期则以武陵山-华蓥山逆冲带主导形成NE向叠加褶皱。在这个过程中，二条前陆逆冲带构造应力场的联合作用在不同阶段具有穿时交错主导特点（宋庆伟等，2014; Lu Guo et al.，2021）。
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3 前陆逆冲带扩展研究中的主要问题与发展方向
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通过上述四川盆地盆缘有关前陆逆冲带扩展研究的概述，结合阿巴拉契亚、科迪勒拉、阿尔卑斯、喜马拉雅、比利牛斯山等经典造山带前陆逆冲带的比较和研究实践，就其研究上存在的主要问题和发展方向总结如下:
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（1）古构造应力场σ2悖论与递进变形。根据Anderson（1951）断层形成机制模式，正断层和逆断层形成时σ2保持水平，而走滑断层的σ2则为垂直状态。然而，受X轴方向应变εx、前陆盆地沉积负载和岩石弹性参数（杨式模量和柏松比）等影响，在递进变形过程中和顺层缩短作用下，σ2由前陆盆地水平状态（图8的T3）却转变为前陆逆冲带垂直状态（图8的T4）（Tavani et al.，2015）。野外调查中发现这种现象是普遍存在的（图9）。那么，这种逆冲断层的走滑构造应力场悖论在前陆逆冲带普遍存在的原因是什么，其构造意义又是什么?目前尚没有合理的机制能够解释。
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（2）应力-应变（σ-ε）关系问题。造山带前陆逆冲带扩展的核心，在于构造驱动力作用（构造应力场）下发生变形（应变），而且随变形的扩展，构造应力场发生调整和转变。因此，只有利用保存的变形形迹解析和反演古构造应力场，才能在此基础上进行精细的前陆逆冲带扩展构造分析，并讨论其构造机制。然而，① 由于前陆逆冲带很难完整保存有限应变的信息，有限应变标志也很少，因此应变分析非常薄弱; ② 除有严格条件约束的平衡地质剖面外，无法对前陆逆冲带扩展过程的应力场调整与增量应变关系进行相关计算; ③ 虽然逆冲楔是前陆逆冲带的基本结构和前展单元（Storti et al.，1997; Sun Chuang et al.，2016），但针对性的构造解剖和σ-ε关系研究却非常薄弱。因此，目前尚未建立起前陆逆冲带σ-ε本构关系（Constitutive equation），也就无法就扩展机制建立定量约束关系。
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（3）系统平衡的问题。作为前陆逆冲带最重要的定量研究方法，平衡地质剖面在实践应用中遇到三个方面的挑战（Yan Danping et al.，2003a; 颜丹平等，2003; Shaw et al.，2004; Espurt et al.，2019）:① 平衡地质剖面分析提出的体积或者层长守衡和无沉积间断的假定条件，在野外实际中大多难以满足，在前陆逆冲带实际计算中更是遭遇难题; ② 平衡地质剖面分析完全忽略节理和小断层网络系统引起的变形，而这部分变形有时可以达到10%~30%; ③ 顺层缩短（LPS）和拆离断层、劈理等韧性、脆韧性变形无法进行平衡计算。
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图8 造山带前陆逆冲带结构与应力-应变特征（据Tavani et al.，2015; Yan Danping et al.，2016修改）
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Fig.8 Structure and stress-strain (σ-ε) distribution of the foreland thrust belt of orogenic belt (modified after Tavani et al., 2015; Yan Danping et al., 2016)
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（a）—前陆逆冲带基本组成结构，其中的T0~T5代表前陆逆冲带扩展的构造位置及其对应演化阶段;（b）—T0~T5构造演化阶段的应力状态及变化;（c）—T0~T5各阶段Flinn图解中可能的三维应变类型和分布
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(a) —Structure of the foreland thrust belt with corresponded tectonic locations and stages of T0~T5; (b) —stress state and evolution of T0~T5; (c) —three-dimentional strain types and strain distribution of T0~T5 in Flinn diagram
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图9 龙门山前陆逆冲带（宝轮-红岩）侏罗系中的D3期共轭剪切节理（a）以及重建的古构造应力场（b）
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Fig.9 D3 conjugate joints cross-cutting the Jurassic in the Longmen Shan foreland thrust belt (a) and reconstructed paleotectonic stress (b)
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面对上述挑战，我们该如何将平衡剖面分析（Sb）、节理+小断层网络分析（SJ）和有限应变测量（SS）结果综合起来进行系统平衡分析呢?
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综合上述分析，造山带前陆逆冲带扩展研究面临三个方面的挑战，这也是未来重要的研究方向。三个问题的核心在于如何将前陆逆冲带扩展进行定量化和精细化的约束。上述研究的最终目的，是要与造山带腹陆带的俯冲、碰撞和缝合信息相结合，进行造山带构造动力学研究（Willett and Fullsack，1993; Yin An and Harrison，2000; Xiao Wenjiao et al.，2003; Zhang Guowei et al.，2004; Wang Xiaoxia et al.，2013; Zhao Guochun et al.，2014）。
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4 主要结论
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综合四川盆地东部武陵山-华蓥山、大巴山和龙门山三条前陆逆冲带扩展问题的研究，本文得出以下结论:
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（1）具有不同大地构造背景的四川盆地盆缘前陆逆冲带均表现为从厚皮逆冲构造至薄皮逆冲构造组合的结构分带，这种结构分带均是在陆内造山作用阶段断层-褶皱关系主导下稳定的指向前陆盆地方向共轴递进扩展作用的结果。
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（2）以武陵山-华蓥山、大巴山和龙门山三条前陆逆冲带扩展实例分析为基础，总结了共轴扩展、非共轴叠加复合和联合构造作用三种前陆逆冲带扩展方式。
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（3）结合阿巴拉契亚、科迪勒拉、阿尔卑斯、喜马拉雅、比利牛斯山等经典造山带前陆逆冲带扩展的研究，提出前陆逆冲带扩展面临古构造应力场σ2悖论与递进变形、应力-应变（σ-ε）关系和系统平衡等问题的挑战，这些问题的核心在于如何定量化和精准化约束前陆逆冲带的扩展，从而成为造山带生长构造动力学研究的关键。
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致谢:感谢刘俊来教授邀请撰写此文，特别感谢审稿人细致和建设性的建议。自2000年以来部分博士和硕士生在论文工作阶段提供了开放的思想和研究思路，在此一并致谢!
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摘要
前陆逆冲带扩展方式是理解造山带生长的关键。四川盆地东缘、北缘和西缘分别发育不同时代和不同构造背景下形成的武陵山-华蓥山、大巴山和龙门山前陆逆冲带,前人对他们的结构和构造运动学进行了详尽的研究。本文在总结这些研究的基础上,揭示武陵山-华蓥山、大巴山和龙门山三条前陆逆冲带的结构分带均表现为从厚皮逆冲构造至薄皮逆冲构造组合的变化,构造解析表明结构分带是断层-褶皱关系主导的指向前陆盆地方向共轴递进扩展作用的结果。同时,在前陆逆冲带扩展分析基础上,总结了四川盆地盆缘共轴扩展、非共轴叠加复合扩展和联合构造扩展三种前陆逆冲带扩展方式。结合阿巴拉契亚、科迪勒拉、阿尔卑斯、喜马拉雅、比利牛斯山等经典造山带前陆逆冲带扩展的研究现状,提出前陆逆冲带扩展研究中存在古构造应力场的σ2悖论、应力-应变 (σ-ε)关系难以建立和系统不平衡等问题,并认为这些问题是未来定量化约束前陆逆冲带扩展,进而解决造山带生长构造动力学研究的主要挑战。
Abstract
Propagation of the foreland thrust belt is the key to understand the growth of orogenic belt. Xuefeng-Huaying, Daba and Longmen Shan foreland thrust belts formed in different times and different tectonic settings are developed in the eastern, northern and western margins of Sichuan basin, respectively. Previous researches have been focusing on their tectonic composition and kinematics. Summarizing these of the studies, this paper reveals a transformation of structural assemblage from thick-skinned thrust to thin-skinned thrust for all three foreland thrust belts. Further structural analysis shows that the structure assemblages and their transformation are dominated by fault-related fold with foreland basin-pointing coaxial progressive propagation. Three types of propagation of foreland thrust belt, i.e., coaxial, non-coaxial superimposed composite and composite propogations, are proposed by summarized kinematics propagation of the foreland thrust belts. Meanwhile, integrated with the studies of propagation of the classical orogenic belts, such as Appalachian, Cordillera, Alpine, Himalayan and Pyrenees, three scientific issues for the propagation of foreland thrust belt, i.e., σ2 paradox of paleotectonic stress field, difficulty in establishing the stress-strain (σ-ε) relationship and system structural imbalance, are suggested. These of the scientific issues are the main challenges to quantitatively constrain foreland thrust belt propagation and to understand the growth dynamics of orogenic belts in the future.
