Large Landslides along Active Tectonic Zones of Eastern Tibetan Plateau: Background and Mechanism of Landslide Formation
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摘要: 活动构造带内大型特大型滑坡成灾机理复杂、危害严重，以往关于其发育特征、成灾背景与灾变机理等研究主要侧重于降雨、地层岩性、地震等因素分析，关于其内动力控灾背景和机理研究一直是学术界和工程界的难题.基于遥感解译、资料收集、野外调查和典型案例剖析，建立了青藏高原东部川藏交通廊道地质灾害数据库，提出了一种考虑地形起伏度的区域地壳稳定性评价方法，研究表明约62%的地质灾害发育于地壳不稳定区和较不稳定区内，内动力地质条件对地质灾害的时空分布具有极大影响.大型滑坡的发育分布受活动构造带控制显著，主要表现为复杂地质构造孕育大型滑坡、特殊岩土结构控制大型滑坡、强烈地震活动诱发大型滑坡、断裂持续蠕滑促进大型滑坡灾变等4类特征，具有显著的活动构造带孕灾-控灾-诱灾-促灾等复杂灾变演化过程.研究结果对于促进青藏高原大型特大型滑坡灾害的成因机理，提升特大滑坡灾害风险防范研究具有重要指导意义.Abstract: Large and extremely large landslides along the active tectonic zones are complex and hazardous. Previous researches on these landslides development characteristics, disaster backgrounds, and formation mechanisms have primarily focused on factors such as rainfall, stratigraphic lithology, and seismic activity. However, studies on the endogenic dynamic control of disaster backgrounds and formation mechanisms have remained challenging for both the academic and engineering communities. Based on remote sensing interpretation, data collection, field investigations, and analysis of typical landslide cases, this study established a geological hazard database for the eastern Tibetan Plateau along the Sichuan-Xizang transportation corridor and proposes a regional crustal stability assessment method that considers terrain relief. The study reveals that about 62% of geological hazards occur in the unstable crustal areas and relatively unstable crustal areas, where endogenous geological conditions significantly influence the spatial and temporal distribution of geological hazards. The development and distribution of large landslides are significantly controlled by active tectonic zones, displaying four characteristics: complex geological structures fostering large landslides, specific geotechnical structures controlling large landslides, strong seismic activities inducing large landslides, and continuous fault creep promoting catastrophic landslides. These characteristics contribute to a complex disaster evolution process that includes disaster fostering, control, induction, and promotion within active tectonic zones. The research findings are vitally important for understanding the formation mechanisms of large and extremely large landslides on the Tibetan Plateau and enhancing research on risk prevention for these landslides.
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图 1 青藏高原主要活动断裂与地质灾害分布特征
Fig. 1. Distribution characteristics of major active faults and geological hazards in the Tibetan Plateau
图 2 川藏交通廊道典型大型滑坡发育特征
a. 西藏加查拉岗村滑坡（镜向N）；b. 西藏江达白格滑坡（镜向NW）；c. 四川泸定摩岗岭滑坡（镜向SW）；d. 四川巴塘茶树山滑坡
Fig. 2. Characteristics of typical large landslides on the Sichuan-Xizang traffic corridor
图 3 区域地壳稳定性评价因子
a. 活动断裂影响等级；b. 工程地质岩组；c. 地震活动性；d. 构造应力场；e. 地形变场（据张郢珍等，1992，修改）；f. 大地热流场；g. 地形起伏度；h. 因子叠加计算示意图
Fig. 3. Factors for regional crustal stability assessment
图 4 基于专家打分与层次分析法的区域地壳稳定性评价
Fig. 4. Regional crustal stability assessment based on expert scoring and analytic hierarchy process
图 5 区域地壳稳定性评价与地质灾害分布图
a. 基于传统方法的区域地壳稳定性评价图；b. 考虑地形起伏度的区域地壳稳定性评价图；c. 基于传统方法评价的四川宝兴县地区局部放大图；d. 考虑地形起伏度评价的四川宝兴县地区局部放大图；e. 基于传统方法评价的朗县-加查县地区局部放大图；f. 考虑地形起伏度评价的朗县-加查县地区局部放大图
Fig. 5. Regional crustal stability assessment and geological hazard distribution maps
图 6 汶川地震诱发大型滑坡分布(据张永双等, 2016)
Fig. 6. Distribution of large landslides induced by the Wenchuan earthquake(after Zhang et al., 2016)
图 7 三峡库区谢家包背斜区滑坡发育特征(据王孔伟等, 2015)
Fig. 7. Landslide development characteristics in the Xiejiabao anticline area of the Three Gorges reservoir region (after Wang et al., 2015)
图 8 正断层孕育大型滑坡的主要特征(据Chang et al., 2018)
Fig. 8. Main characteristics of large landslides associated with normal faults (after Chang et al., 2018)
图 9 逆断层孕育大型滑坡的主要特征
a. 谢家店子滑坡发育特征（据张永双等，2016）；b. 逆断层促进谢家店子滑坡形成（据Dai et al.，2011a修编）
Fig. 9. Main characteristics of large landslides associated with reverse faults
图 10 走滑断层孕育大型滑坡的主要特征
a. 断层蠕滑导致滑坡产生裂缝；b. 降雨沿裂缝入渗导致滑坡蠕滑；c. 蠕滑加剧导致水渠损坏渗漏，加速了滑坡变形；d. 滑坡持续变形导致滑坡后缘不断拉裂；据Zhang et al.（2023）
Fig. 10. Main characteristics of large landslides associated with strike-slip faults
图 11 背斜构造控制下的唐家山高位远程滑坡形成模式
a. 唐家山滑坡受褶皱挤压影响；b. 唐家山滑坡形成滑坡-堵江灾害链
Fig. 11. Formation process of the Tangjiashan high-altitude and long run-out landslide controlled by anticline structures
图 12 鲜水河断裂带岩土体与典型大型滑坡发育特征
a. 鲜水河断裂带道孚亚拖村滑坡群；b. 鲜水河断裂带炉霍55道班滑坡；c. 鲜水河断裂带八美土石林；d. 鲜水河断裂带两侧近直立陡倾破碎岩体
Fig. 12. Characteristics of rock-soil masses and typical large landslides in the Xianshuihe fault zone
图 13 怒江构造混杂岩带黏土化蚀变岩特征与剪切强度特征
a. 怒江八宿多拉寺滑坡黏土化蚀变岩样品；b. 黏土化蚀变岩遇水崩解；c. 不同含水率条件下黏土化蚀变岩剪切强度；据张永双等（2023）
Fig. 13. Characteristics of clayey altered rocks and shear strength in the Nujiang tectonic mélange belt
图 14 汶川地震滑坡动力演化过程
a. 初始斜坡；b. 地震抛掷；c. 撞击崩裂；d. 高速滑坡；据殷跃平（2008）
Fig. 14. Dynamic evolution process of landslides during the Wenchuan earthquake
图 15 大光包滑坡启动过程模型
a. 地震动放大-振动冲击-滑带扩容阶段；b. 滑带水击-滑坡启程剧动阶段；c. 滑带扩容-水击效应滑体失稳阶段；d. 滑坡高速滑动-滑体扰动堆积阶段；据裴向军等（2018）
Fig. 15. Model of Daguangbao landslide initiation
图 16 断裂活动对斜坡变形的影响
a~d. 正断层活动状态下斜坡体折减系数F分别为1.0、1.2、1.4、1.6条件下断错0.5 m时的斜坡塑性区分布特征；e~f. 正断层活动状态下斜坡体折减系数F分别为1.0、1.2、1.4、1.6条件下断错1.0 m时的斜坡塑性区分布特征；i~l. 逆断层活动状态下斜坡体折减系数F分别为1.0、1.2、1.4、1.6条件下断错0.5 m时的斜坡塑性区分布特征；m~p. 逆断层活动状态下斜坡体折减系数F分别为1.0、1.2、1.4、1.6条件下断错1.0 m时的斜坡塑性区分布特征；据郭长宝等（2012）
Fig. 16. The influence of active fault slipping on slope deformation
表 1 地壳稳定性评价结果统计
Table 1. Statisticsl table of crustal stability assessment results
分区 基于传统方法的区域地壳稳定性评价
(Crust_B)考虑地形起伏度的区域地壳稳定性评价
(Relief_ Crust_B)面积（km2） 面积占比（%） 面积（km2） 面积占比（%） 稳定区 227 370.15 27.12 179 799.60 21.45 较稳定区 253 240.11 30.20 237 616.68 28.34 较不稳定区 250 407.04 29.87 290 037.55 34.59 不稳定区 107 363.10 12.81 130 926.57 15.62 
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表 2 地质灾害分布统计
Table 2. Statisticsl table of geological hazard distribution
分区 基于传统方法的区域地壳稳定性评价
(Crust_B)考虑地形起伏度的区域地壳稳定性评价
(Relief_Crust_B)地质灾害数量(个) 数量占比(%) 地质灾害数量(个) 数量占比(%) 稳定区 4 161 19.01 3 229 14.75 较稳定区 5 760 26.32 5 039 23.02 较不稳定区 7 604 34.74 7 769 35.50 不稳定区 4 363 19.93 5 851 26.73
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