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黄土地震滑坡研究综述与展望

钱法桥, 邓亚虹, 刘凡, 门欢

钱法桥，邓亚虹，刘凡，等. 黄土地震滑坡研究综述与展望[J]. 中国地质灾害与防治学报，2024，35(5): 5-20. DOI: 10.16031/j.cnki.issn.1003-8035.202401020
引用本文: 钱法桥，邓亚虹，刘凡，等. 黄土地震滑坡研究综述与展望[J]. 中国地质灾害与防治学报，2024，35(5): 5-20. DOI: 10.16031/j.cnki.issn.1003-8035.202401020
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QIAN Faqiao，DENG Yahong，LIU Fan，et al. A review of earthquake-induced loess landslides research and future prospects[J]. The Chinese Journal of Geological Hazard and Control，2024，35(5): 5-20. DOI: 10.16031/j.cnki.issn.1003-8035.202401020
Citation: QIAN Faqiao，DENG Yahong，LIU Fan，et al. A review of earthquake-induced loess landslides research and future prospects[J]. The Chinese Journal of Geological Hazard and Control，2024，35(5): 5-20. DOI: 10.16031/j.cnki.issn.1003-8035.202401020
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黄土地震滑坡研究综述与展望

  • 1.

    长安大学地质工程与测绘学院，陕西 西安　710054

  • 2.

    矿山地质灾害成灾机理与防控重点实验室，陕西 西安　710054

基金项目: 国家自然科学基金项目(41772275)
详细信息
    作者简介:

    钱法桥（1997—），男，重庆云阳人，博士研究生，主要从事地质灾害及地震工程方面的研究。E-mail：2020226080@chd.edu.cn

    通讯作者:

    邓亚虹（1978—），男，湖南安化人，教授，博士，主要从事土动力学及地震工程方面的研究。E-mail：dgdyh@chd.edu.cn

  • 中图分类号: P642.22

A review of earthquake-induced loess landslides research and future prospects

  • 1.

    College of Geology Engineering and Geomatics, Chang’an University, Xi’an, Shaanxi　710054, China

  • 2.

    Key Laboratory of Mine Geological Hazards Mechanism and Control, Xi’an, Shaanxi　710054, China

Funds: National Natural Science Foundation of China(41772275)

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    摘要
  • 摘要:

    黄土地区地貌形态复杂，地震频发，地震滑坡灾害严重。黄土地震滑坡受多种因素影响，包括黄土边坡地形地貌、地层岩性、动力响应，黄土强度和动力特性，水文地质条件等。目前，黄土地震滑坡研究主要采用室内试验、物理与数值模型试验、野外调研、遥感与监测等手段，研究内容包括黄土地震滑坡成因机理、发育特征与分布、滑坡动力响应和稳定性等方面。文章阐述了黄土地震滑坡国内外研究现状，介绍了一种考虑地震波动特性的拟动力评价方法，并对基于拟动力法开展黄土地震滑坡研究进行了展望。通过分析黄土地震滑坡力学成因机制、研究黄土滑坡地震液化现象、讨论黄土地震滑坡失稳特征，提出能够精确评价黄土地震滑坡稳定性的计算方法，可以为黄土地区防震减灾提供理论依据，也是今后研究的重点。

    Abstract:

    The loess region is characterized by complex geomorphological patterns. This region is prone to frequent earthquakes with serious seismic landslide disasters. Loess seismic landslides are affected by a variety of factors, including the topography and geomorphology of loess slopes, stratigraphic lithology, dynamic responses, strength and dynamic characteristics of loess, and hydrogeological conditions. Current research on loess seismic landslides primarily involves laboratory experiments, physical and numerical simulations, field investigations, and remote sensing and monitoring techniques. The research focuses on the mechanisms, development characteristics, distribution, dynamic responses, and stability of loess seismic landslides. This paper reviews the current state of both domestic and international research on loess seismic landslides, introduces the pseudo-dynamic method that considers seismic wave propagation characteristics, and outlines future research prospects based on this method. By analyzing the mechanics mechanisms of loess seismic landslide, investigating the seismic liquefaction phenomena of loess landslides, and discussing the instability characteristics of these landslides, this study proposes a calculation method to accurately evaluate the stability of loess seismic landslides. This research can provide a theoretical basis for earthquake disaster prevention and mitigation in loess areas, and it represents a key focus for future studies.

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  • 0.   引言

    强震是人类所面临的最危险的自然灾害之一[1]。在强切割山区，山体在地震作用下往往发生震裂松动，其完整性、强度大幅度降低，诱发一系列的崩、滑灾害[2-3]。崩滑灾害堆积物又会为泥石流的发生提供物源[4-5]。上述“崩滑流”灾害造成的人员伤亡和财产损失往往不亚于地震本身[6]。随着对地震滑坡研究的深入，一些学者认为，山体在地震作用的失稳机理与山体的地震放大效应存在耦合关系。罗永红等[7]对汶川地震次生地质灾害展开调查后，结合灾害区域地貌单元，认为特殊地形尺寸与地震波长的耦合作用导致地震放大效应。范刚[8]基于自贡西山公园台站记录的地震数据，分析了地形对峰值加速度、峰值位移等地震动参数的影响规律，认为地形因素仅对水平向的地震响施加影响，而在垂直向不明显。VALAGUSSA等[9]通过对1993年Papua New Guinea地震、1999年ChiChi地震、1994年Northridge地震、2004年Niigata–Chuetsu地震、2008年Iwate–Miyagi Nairiku地震和2008年汶川地震后造成的地貌改观展开分析，探讨了地震震级和震中距与山体失稳规模的耦合关系。CROISSANT等[10]通过2D数值模拟，发现地震作用下断层作为一种不稳定结构面会对山体的稳定性产生不利影响。GUAN等[11]通过物理模拟，发现隧道深处即山体内部的水平向峰值加速度要小于同一高程山体表面处。HARZTEL等[12]对1989年Loma Prieta地震展开研究后表明，体波在山脊内的多向反射和散射以及瑞利波与勒夫波的相互作用是导致Robinwood山脊受震灾破坏严重的重要原因。CELEBI[13]通过对1976年Guatemala地震和1989年Loma Prieta地震数据展开分析，发现山脊处的地震放大效应与地震波入射角度存在耦合关系。SU等[14]通过对地震波进行小波变换，讨论了地震波不同频率段的地面运动属性。2014年康定地震后，王运生等[15]对冷竹关地震台阵所记录到的数据进行分析，发现山体内部的地震动放大效应要弱于同高程山体表面，且山体表面傅立页谱图较山体内部，成分更为复杂。刘峡等[16]利用小波变换的方法，对地震信号进行了时域特征上的分析。

    地震波是一种复杂的非稳定波型，其携带的能量在时域上和频率域上分布极不均匀[16]，一旦某时刻能量突然集中会对受震物体的结构稳定产生不利影响。目前针对地震动响应的研究多侧重于傅立页谱分析，而傅立页谱仅能表明频率域上能量分布，而忽略掉了相应频率出现的时间。小波分析作为数学放大镜，突破了傅立页变换和短时傅立页变换局限，可以清楚地表明地震波能量、时域、频率域之间的关系，以及地震波成分的演变。因此基于连续小波变换深入探讨地震在特殊山地单元下的地震动响应规律，对揭示地震致灾机理和开展防灾减灾工作意义重大。

    1.   监测数据来源与地震动响应分析

    1.1   强震监测点概况

    据中国地震台网，2019年6月17日22时55分，四川省宜宾市长宁县发生Ms6.0级地震，震中位于长宁县双河镇附近，震源深度16 km。云南，四川和重庆等多地均有明显震感。成都理工大学地质灾害防治与地质环境保护国家重点实验室依托中国地震局“川西深切河谷斜坡地震动评价技术研究”项目，在雅安市石棉县南桠河两岸设立的3个地震监测点记录到了此次Ms6.0级地震。其中南桠河右岸鸡公山上放置有两台强震监测仪，左岸陈家包山上放置有一台强震监测仪器，其监测点分布位置如图1所示。鸡公山上两台站置于前震旦纪晋宁期具碎裂结构的弱风化花岗岩平硐内，陈家包台站置于坡残积厚覆盖层之上，下伏前震旦纪晋宁期花岗岩，在南桠河左岸坡脚有部分出露。红色剖面线所代表的地质剖面图见图2。三台站仪器放置场地稳定，无外界因素干扰。其场地属性如表1所示。用于地震监测的仪器则由中国地震局工程力学研究所研制的G01NET-3结构与斜坡震动监测仪，采样时间间隔为0.00512 s。同时，四川省地震局也提供了石棉县先锋台阵记录到Ms6.0级地震监测数据作为参照基准。

    图  1  南桠河两岸监测仪器分布图（方位角118°）
    Figure  1.  Distribution of monitoring sites on both banks of Nanya River
    下载: 全尺寸图片 幻灯片
    图  2  南桠河两岸红线地质剖面图
    Figure  2.  Geological profile of both banks at Nanya River
    下载: 全尺寸图片 幻灯片
    表  1  各监测点所在位置场地属性
    Table  1.  Properties of monitoring sites
    监测点编号绝对高程/m震中距/km监测点所在部位场地类型
    1#1150265山体平坡处基岩（花岗岩）
    2#1060265山脊处基岩（花岗岩）
    3#1102267山脊处厚覆盖层
    参照点（石棉先锋）×××薄覆盖层
    下载: 导出CSV 
    | 显示表格

    1.2   石棉县南桠河两岸山体地震动响应综述

    山体的地震动响应主要表现在峰值加速度（Peak Ground Acceleration, PGA）和阿里亚斯强度（Arias Intensity, AI）的放大[17]。对3个监测点以及1个参照点所记录到Ms6.0级地震的数据进行低通30 Hz滤波处理后，通过软件SeismoSignal处理后可以读出其地震动响应的基本参数属性。其4个点的峰值加速度、阿里亚斯强度以及峰值加速度放大倍数如表2所示。

    表  2  各监测点地震动响应参数
    Table  2.  Ground motion response parameters at each monitoring site
    监测点编号峰值加速度/gal阿里亚斯强度/(cm·s−1)
    EWSNUDEWSNUD
    1#1.222.942.230.361.220.89
    2#2.133.642.350.551.800.81
    3#7.4210.182.9415.0913.262.75
    *参照点1.743.361.880.882.700.87
    　　注：1 gal=1 cm/s2
    下载: 导出CSV 
    | 显示表格

    罗永红[17]、贺建先等[18]、祁生文等[19]结合大量实测地震数据分析发现，山体的山脊处，山体转折部位以及第四纪覆盖层会对山体的地震动响应起控制作用，具体表现为上述部位的峰值加速度放大，在地震来临时候更加强烈的震动响应会导致山体发生失稳。由表2可见，同位于鸡公山上的1#及2#监测点，位于山脊处的2#监测点其峰值加速度要大于1#监测点。而3#监测点场地类型为厚覆盖层，其水平向峰值加速度远远大于1#和2#监测点，而垂直向峰值加速度放大效应则弱于水平向，但也有一定程度的放大。可以明显看出，峰值加速度的放大效应在水平和垂直方向上具有显著的差异。

    2.   地震信号的时频分析

    傅立页变换作为一种良好的信号分析手段，在世界范围内被广泛应用[16]。但对于非稳定信号，傅立页变换只能体现出信号的频域特性，而隐略了随机信号中的时域特性。小波变换自1986年被发明以来，因其具有良好的时频分析能力，在信号处理领域内发展迅速[20]。小波变换分析不仅可以描述非稳定信号的局部变化特征，而且可以通过尺度变换，从不同频域上观察信号的演变特征。因此，相较于使用传统手段傅立页变换对地震信号频率域上展开解析，利用小波变换分析地震信号，可以反映地震信号的时频特性，明确地震时频演变规律。

    2.1   连续小波变换

    将四台强震监测仪记录到的地震数据做小波变换处理。所选用的变换方式为连续小波变换（Continuous Wavelet Transform），小波基函数为Mexh，其中心频率（Centre Frequency）为0.25。选择矢量尺度为1至140，由140至1作公差为−0.5的递减。由尺度-频率换算公式计算可得，其覆盖频率范围0.35～50 Hz。

    地震数据进行连续小波变换后，可以三维的方式呈现，其中x轴表示时间，单位为s；y轴表示频率，单位为Hz；z轴表示地震加速度幅值，单位为20 gal。3个监测点的地震时频图如表3所示。地震信号经过连续小波变换之后，透过传统时程图增加了频率信息，做到了时域和频率域上的结合。

    表  3  监测点3分量连续小波分解图
    Table  3.  Three-component continuous wavelet decomposition
    东西方向南北方向垂直方向
    下载: 导出CSV 
    | 显示表格

    2.2   地震信号时频成分统计

    地震信号经过连续小波变换后，其时域频域的结合有助与对地震信号成分的分析。4处监测点的3分量地震信号时频图中，随着时间增加，有两个波峰，其中峰值较低先到达的为P波，而后到达的峰值较大的则为S波。在S波后面则为一段由体波激发的面波。S波在到达受震地表后，分异为高频和低频两种成分：形状尖锐、变化剧烈的低频成分与光滑平顺、平稳降低的高频成分。地震发生时，受震物体的破坏主要依靠S波和体波交会激发的面波[21]。P波主要为垂直方向上的振动，且幅值小于S波，对受震物体结构破坏较小[6]，因此本文分析重点为S波成分变化。现对各监测点三分量上P波和S波波峰空间坐标进行测量，其结果如表4所示，其中第一行表示波峰出现的时间位置，第二行表示波峰出现的频率位置，第三行表示波峰幅值绝对值。

    表  4  监测点波峰成分统计表
    Table  4.  Statistical table of signal peak at each site
    方向S波高频波峰S波低频波峰
    1#2#3#参照点1#2#3#参照点
    东西27.23 s37.67 s×32.02 s27.00 s37.76 s36.03 s31.70 s
    2.8 Hz3.9 Hz×3.2 Hz1.4 Hz1.4 Hz1.3 Hz1.1 Hz
    0.0450.078×0.0760.0630.0720.6300.068
    南北26.50 s36.52 s×32.00 s27.09 s36.41 s35.09 s32.27 s
    2.8 Hz3.5 Hz×2.5 Hz1.1 Hz1.1 Hz1.1 Hz1.1 Hz
    0.1200.183×0.1880.1100.1150.6560.138
    垂直26.77 s37.73 s34.85 s32.88 s27.19 s38.13 s35.28 s32.36 s
    3.5 Hz3.5 Hz2.8 Hz3.2 Hz1.1 Hz1.1 Hz1.1 Hz1.1 Hz
    0.0860.1070.1500.0760.0900.0680.0890.068
    下载: 导出CSV 
    | 显示表格

    3.   放大效应分析

    3.1   山脊部位放大效应分析

    历史地震监测表明，地震作用下山脊部位往往放大效应更为显著[17-18]。根据表2的时程数据分析结果来看，2#监测点所处的山脊部位，其水平向上PGA和AI数值要高于同在山腰部位的1#监测点。其中PGA放大系数（2#/1#）在东西南北和垂直向上分别为1.74、1.23和1.05；AI放大系数（2#/1#）在三个方向上则分别为1.52、1.47和0.91。这说明2#监测点所在山体部位地震动力响应更为强烈。由表4可以看到地震成分的演变，1#与2#监测点的S波低频部分，其波峰在频域上的发生位置完全相同，这可能与两处监测点位于一座山体有关。相较于1#监测点，2#监测点的东西向、南北向和垂直向S波高频成分，波峰幅值放大倍数分别为1.73、1.53和1.16，而S波低频部分的放大倍数则分别为1.14、1.04和0.76。2#监测点三分量S波高频波峰幅值全部高于低频部分，而1#监测点则相反。即在基岩场地下，山脊相较于山腰，地震放大效应主要体现为高频成分能量的增加，低频部分有小幅增大，但远不如高频部分。此外，放大效应还存在显著的方向性，无论是在PGA、AI放大系数上还是地震波峰成分演变上，水平方向的放大效应要更为显著。受地震作用，在2#点所在的山脊处，落石与斜坡变形较其他地方更为发育（图3）。

    图  3  2#监测点附近山脊部位的落石以及斜坡变形
    Figure  3.  Rock falls and slope deformation around monitoring site 2# in Shimian County
    下载: 全尺寸图片 幻灯片

    3.2   覆盖层场地放大效应分析

    3#监测点的场地条件为厚覆盖层，下伏同晋宁期花岗岩，仅在南桠河左岸边坡支护剖面上有所出露。通过表3可以看到，3#监测点水平向时频三维图上高频成分衰减剧烈，其低频波峰幅值在东西向和南北向更是分别高达0.630和0.656，相较于同在山脊部位的2#监测点S波最大幅值，其放大倍数达8.08和3.53。但在垂直向，依然可以清楚地看到S波的高频和低频成分，低频成分在时间序列上出现的次数更多。此外，参照点场地条件为薄覆盖层，下伏同套岩组。同样可以看到，薄覆盖层场地的低频部分相较于基岩场地，其低频部分已经有所发育。而PGA放大系数（3#/2#）在东西、南北和垂直向上的放大系数为3.48、2.79和1.25；AI放大系数（3#/2#）则分别为27.4、7.36和3.39。地震时，震感更加强烈。

    现有研究表明，当成层厚覆盖层接收来自基岩传来的剪切波时，在地震波向地表传播的过程中，会发生多次反射与折射，波能量发生叠加而进一步增强，尤其为长周期波更为显著，这与表征能量的AI显著放大相吻合[21-22]。此外，覆盖层土体对入射剪切波具有吸收和放大作用。当剪切波由基岩入射到覆盖层后，其中短周期成分被吸收，而长周期成分由于与土体自身振动周期相近，极易发生共振作用[22]。为了探究3#厚覆盖层场地的S波低频部分剧烈变化是否为共振效应引起，现在对3#监测数据进行加速度反应谱分析。加速度反应谱即在某一阻尼比的作用下，反应一系列单质点在振动时，其最大响应绝对值与场地结构周期的关系的频谱图。现采用0.05，0.1，0.2的阻尼比[20]，对3#监测点三分量加速度反应谱展开计算，用于评价场地的特征周期。其三分量反应谱图如表5所示。加速度反应谱中有多个波峰，表明覆盖层成分不均匀。其最高点所代表的时间即为场地的特征周期[20]，分析后其特征周期如表6。同时，由同样方法求得基岩场地特征周期如表7。

    表  5  3#监测点场地3分量反应图谱
    Table  5.  Three-component response spectrum of monitoring site No.3
    东西向南北向垂直向
    下载: 导出CSV 
    | 显示表格
    表  6  3#监测点三分量特征周期/频率表
    Table  6.  Dominant period / frequency of site 3#
    东西向南北向垂直向
    特征周期/s0.740.880.36
    特征频率/Hz1.351.132.77
    下载: 导出CSV 
    | 显示表格
    表  7  1#与2#监测点三分量特征周期
    Table  7.  Dominant period of site 1# and 2#
    监测点编号特征周期/s
    东西向南北向垂直向
    1#0.260.260.25
    2#0.260.260.28
    下载: 导出CSV 
    | 显示表格

    由表6和表7可知，基岩场地特征周期远小于厚覆盖层场地。3#监测点东西向和南北向特征频率分别为1.35 Hz和1.13 Hz，即场地的特征频率十分接近于S波低频成分波峰峰值处频率，频率差值分别为0.05 Hz和0.03 Hz。而垂直向特征频率则与水平向有较大差异。在水平方向上，由于频率接近，地震发生时，S波中低频成分振动与场地自振交汇，产生强烈的共振效应，导致频率域上其特征周期附近区间内振动峰值显著增加。加之厚覆盖层土体对短周期波成分的吸收效应和长周期波成分的折射叠加效应，3#监测点的S波高频部分衰减显著[21-22]。厚覆盖层对地震波显著放大，地震时其震感更加强烈，加重震害损失，这一现象在震中长宁灾害调查中得以体现。3#点所在村落多为刚度大，结合性差的低矮砖混结构房屋和土坯房，此次地震由于震中距较大，震级较小，未对3#点所在村落建筑物造成严重损害。但如果震级加大，受到山脊放大效应和覆盖层放大效应的双重影响，震感强烈，相较于基岩场地这里会遭受更加严重地表震害。

    4.   结论

    基于连续小波变换的信号处理手段，对石棉县城南桠河两岸强震监测点所记录到的长宁Ms6.0级地震数据，作三维时频图谱，并结合时域和频域对地震信号成分进行分析。现有结论如下：

    （1）通过连续小波变换所呈的三维时频图，可以清楚看到S波到达地表时分为高频和低频两种成分。其中高频成分主频在3.5 Hz附近，而低频成分主频在1.1 Hz附近，两种成分在时域上近乎同时出现。

    （2）地震时山脊部分的地震动响应更加强烈。山脊部位场地类型为基岩，通过时频分析结果可知，放大效应主要体现为S波高频成分能量的增加，而低频部分则无明显变化。

    （3）覆盖层场地对S波具有显著的低频放大和高频衰减效应。S波在厚覆盖层的折射和反射作用，以及3#覆盖层场地水平方向的自振与S波低频成分交汇产生共振效应，是导致覆盖层场地低频放大效应显著的原因。地震发生时，3#场地震感强烈，地表震害将更加严重。

    （4）地震动响应规律具有极强的方向差异性，从时程分析结果和时频分析结果可以看出，其差异性主要体现在水平向和垂直向上，其水平向的放大效应相较于垂直向要更为显著。

  • 图  1   黄土高原梁、峁、丘陵地貌[20]

    Figure  1.   The loess ridges, hillocks, and hill landscapes of the loess plateau[20]

    下载: 全尺寸图片 幻灯片

    图  2   黄土高原地区崩塌、滑坡、泥石流、、地面塌陷易发程度图

    Figure  2.   Susceptibility to avalanches, landslides, debris flows, and surface collapses in the loess plateau

    下载: 全尺寸图片 幻灯片

    图  3   黄土高原及周边地区地震分布[36]

    Figure  3.   Earthquake distribution in the loess plateau and surrounding areas[36]

    下载: 全尺寸图片 幻灯片

    图  4   拟动力法的地震波传播过程与条块地震力计算

    Figure  4.   Seismic wave propagation process and strip seismic force calculation using the pseudo-dynamic method

    下载: 全尺寸图片 幻灯片
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  • 收稿日期:  2024-01-12
  • 修回日期:  2024-04-25
  • 录用日期:  2024-07-15
  • 网络出版日期:  2024-07-28
  • 刊出日期:  2024-10-24

目录

摘要
HTML全文

  • 0.   引言

  • 1.   监测数据来源与地震动响应分析

  • 1.1   强震监测点概况

  • 1.2   石棉县南桠河两岸山体地震动响应综述

  • 2.   地震信号的时频分析

  • 2.1   连续小波变换

  • 2.2   地震信号时频成分统计

  • 3.   放大效应分析

  • 3.1   山脊部位放大效应分析

  • 3.2   覆盖层场地放大效应分析

  • 4.   结论

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