| Citation: | JIA Ting,
WANG Yong,
PU Qing-yu,
et al.,
2016. REVIEW ON THE LOWER BOUNDARY OF QUATERNARY IN CHINA. Journal of Geomechanics, 22 (1): 162-177.
|
2008年5月12日四川汶川发生的特大地震, 特点是持续时间长, 破坏性强, 滑坡、泥石流、堰塞湖等次生灾害严重[1]。地震发生在龙门山断裂带上。地震破裂开始于汶川映秀, 然后以每秒2.8km的速度沿断裂带向NE向扩展, 直到青川, 破裂长度约300km。破裂持续时间约100s。震源机制比较复杂, 在地震过程中震源机制随着时间和空间发生变化。在地震的开始阶段表现为逆冲为主, 但后来向NE方向逐渐转变为以走滑为主。这次大地震对周围地区断层应力和地震活动有何影响, 是人们关心的一个问题。为此, 我们计算了这次大震后周边地区一些主要断层的库仑应力的变化, 据此分析了该区地震的活动性。
近年来, 大地震产生的库仑破裂应力变化对后续地震活动影响的研究受到广泛关注[2]。很小的静态库仑应力变化就可能对地震活动性、地震的时空分布产生较大的影响[3~4]。许多震例表明, 大地震后库仑应力的变化与后续地震活动有促进作用。大多数库仑破裂应力增加的地区地震活动速率增高; 而库仑破裂应力减小的地区, 地震活动减小[5~8]。一些地区库仑破裂应力增加量大于0.01~0.03 MPa就有可能触发地震活动[9~10], 库仑破裂应力变化起触发作用的典型值是0.1~1MPa[11]。库仑应力对地震的触发作用有一个延迟时间。一般来说, 延迟时间可为几秒到几十年[2, 9]。库仑应力的研究对地震危险性分析具有重要意义。
库仑破裂应力是作用在断层面上, 克服摩擦阻力使断层滑动的力。库仑破裂应力的变化是指库仑破裂应力的改变量。
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(1) |
式中, Δτ为断层面滑动方向上的剪切应力的变化, 剪切应力Δτ与断面滑动方向一致时定义库仑应力的变化为正值, 否则为负值。Δσ为断面上正应力的变化(拉伸应力为正值), μ为内摩擦系数, 参照文献[14], 我们取μ=0.4。
根据大震后产生的断层的静态位移, 计算出库仑应力的变化, 增强或减弱, 来分析地震活动性。
Δτcf >0和Δτcf < 0分别表示断面上被加载(库仑应力加大)或被卸载(库仑应力减小)的情况。Δτcf时, 对地震活动有加强作用, Δτcf < 0时对地震活动有减弱作用。
采用大型有限元ANSYS软件[16]进行断层静态位移引起的库仑应力的计算。模型的范围为东经98.5°到东经107.5°, 北纬27.5°到北纬34°, 深度为40km。地质构造参考中国活动构造图[17]经简化而成(图 1)。将龙门山断裂带看成不连续面, 采用接触单元处理。其他断层看成连续介质, 具有一定的宽度。断层带内的弹性模量低于周围介质的弹性模量, 断层带以外为均匀介质。采用六面体八节点单元, 共有单元13010个, 结点15046个(图 2)。模型的四边分别为东西向和南北向约束, 底部为沿深度方向约束。
由震源机制解得知汶川地震破裂面走向为230°, 倾向320°, 倾角39°, 滑动角120°。由地震波反演得到了地震断层面的同震静态位移分布如图 3 ①。可以看出沿断层面的静态位移约为6.7m。最大静态位移在震中和震中的NE方向约100km范围内, 其他地区位移量较小。根据该地震位错模型计算了区域上的位移分布和库仑应力的变化。
① 陈运泰, 许力生, 张勇, 等.2008年5月12日汶川特大地震震源特性分析报告.2008, www.cea-igp.ac.cn汶川地震专题地震情况
根据图 3给出的地震位错模型, 通过有限元计算得到的地表位移分布如图 4到图 6。图中给出了沿龙门山断裂带走向、垂直走向和铅直方向的位移分布。由沿断裂带走向的位移(图 4)可以看出, 断层两侧有一个右旋走滑扭动, 相对错动量最大为3.5m。位移影响的范围达数百公里。由垂直走向的位移(图 5)可以看出, 断层上盘(西侧)向SE方向位移, 位移量最大为4.5m, 下盘向NW方向位移位移量最大为1.5m, 反映了断层的挤压特点。铅直方向位移(图 6)表现为上盘向上位移, 下盘向下位移, 反映了逆冲断层的特性。
由地震断层静态位移引起的应力, 通过式(1)计算出断层的库仑应力变化。龙门山断层的产状, 与断层位移模型使用的产状相同, 为逆冲右旋走滑断层。其他断层没有产状资料, 皆按近似直立的走滑断层处理。鲜水河断裂以及大部分NW向断裂按左旋走滑处理。NE向断裂按右旋走滑处理。共计算了28个断层段, 结果如图 7和图 8。图 7给出了库仑应力增加和降低的地区, 图 8给出了相应断层的应力增加或降低数值大小。图 7中, 黄色区域为库仑应力增加区, 蓝色区域为库仑应力降低区, 绿色区域为库仑应力变化不明显区域(变化量小于0.01MPa)。库仑应力变化的情况如下:
沿龙门山断层的库仑应力分布是不均匀的, 大部分为库仑应力增加区(图 7), 增加的幅度较大, 为0.25~1.7 MPa (图 8), 少部分为降低区, 但降低幅度不大, 最大降低幅度为-0.3MPa。余震, 特别是5级以上较大余震的分布, 与龙门山断层及附近断层的库仑应力增加区有较好的对应关系。北川、青川、宁强、平武等地皆为库仑应力增加区, 这些地区都有较强余震。甘肃陇南地区和阿尼玛卿断裂为应力增加区, 应注意这些地区的强余震。
鲜水河断裂北段和南段为库仑应力下降区或应力变化不明显区。只有中部一小段约60km为升高区, 升高幅度为0.04~0.17MPa。故鲜水河断裂带上大部分地区为卸载区, 不利于地震活动, 但局部应力增加地段, 应注意地震活动的可能性。
成都至德阳地段, 为库仑应力增加区。成都西南地区断层为库仑应力降低区。从余震看, 成都西北有余震, 而东南没有。
总体上来看, 由震中区向NE方向延伸直到青川、宁强、陇南一带为应力增强区, 5级以上强余震分布较多, 应加强监视。震中区西南方向主要为应力下降区, 小部分为增强区, 但幅度与东北部相比相对较小。
(1) 沿龙门山断裂带大部分为库仑应力增加区。较大余震的分布与库仑应力增加区有较好的对应关系。北川、青川、宁强一带为应力增加区(大于0.25~1.5MPa), 5级以上余震多分布于此。余震主要向NE方向发展。
(2) 鲜水河断裂带北段为库仑应力下降区, 南段应力变化不明显区。只有中部一小段(约60km)为升高区, 升高幅度较小, 为0.04~0.17MPa。库仑应力变化对鲜水河断裂带上大部分地区地震活动不利, 只在局部应力增加地段, 对地震有触发作用。
(3) 甘肃陇南地区和阿尼玛卿断裂为库仑应力增加区。成都至德阳段断裂为库仑应力增加区, 成都东南为库仑应力降低区。
(4) 库仑应力的变化情况与断层产状、断层的力学性质、摩擦强度以及地震的位错模式有关。要提高库仑应力变化计算精度, 必须正确考虑这些因素。库仑应力的变化只是地震的一个触发因素, 能否发生地震还取决于区域应力状态及其变化情况。虽然如此, 库仑应力的变化对大震后地震的趋势和余震的分析仍有重要意义。
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