Three-dimensional crustal velocity structure around Longmenshan and Anninghe fault zones
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摘要:
利用2008—2021年区域地震台网及部分流动地震台阵的近震走时观测资料，采用双差层析成像方法获得了龙门山断裂带和安宁河断裂带周边地区的高分辨率地壳三维P波速度结构。结果显示：四川盆地浅部呈明显的低速异常，在前陆盆地低速异常可一直延伸至约15 km深，推测与该地区接收大量来自青藏高原东缘的沉积物有关；在龙门山断裂带附近，中上地壳存在一些与断裂带平行的高速异常体，它们较好地揭示了该地区穹隆体和逆冲推覆体深浅部的分布特征，例如，位于龙门山断裂带中部的彭灌穹隆体下延深度可达15 km左右，而与之相邻的雪隆山穹隆体下延深度不超过5 km。在安宁河断裂带与大凉山断裂带之间存在震源深度超过20 km的微震活动带，其分布形态与P波高速异常的分布形态基本一致，推测高速异常体的存在可能导致地壳内部脆韧性转换带深度的增加，并且受安宁河与大凉山交会部位强烈变形的影响，该地区出现深度较大的地震活动。上述结果为认识该地区的深部地质构造和地震活动机制提供了新的依据。
Abstract:The Anninghe and Longmenshan fault zones are the eastern boundary of the Tibetan Plateau, and they are also important strong earthquake active zones. The study of the deep structure of the fault zones and surrounding areas is of great significance to understand the dynamic process of the eastward expansion of the Tibetan Plateau and the tectonic mechanism of strong earthquake. In this paper, based on the seismic travel time data from regional seismic network and temporary seismic arrays from 2008 to 2021, the high-resolution 3D crustal P-wave velocity structure around the Longmenshan and Anninghe fault zones is obtained by double difference tomography. There are obvious low-velocity anomalies in the shallow part of the Sichuan Basin, and the low-velocity anomalies can extend to about 15 km near the foreland basin, which is related to the foreland basin receiving sediments from the eastern margin of the Tibetan Plateau. Near the Longmenshan fault zone, there are some high-velocity anomalies in the upper to middle crust parallel to the fault zone, which reveals the spatial distribution of domal complexes and thrust complexes in this area. For example, the Pengguan domal complex located in the middle of the Longmenshan fault zone extends down to a depth of about 15 km, while the adjacent Xuelongshan domal complex extends down to a depth not deeper than 5 km. There is an active microseismic zone with a focal depth deeper than 20 km between the Anninghe and Daliangshan fault zones, which is consistent with the distribution of P-wave high-velocity anomaly, therefore we speculate that the existence of high-velocity anomalies may increase the depth of the crustal brittle-ductile transition zone, and deep seismicity appeared in this region due to the strong deformation at the intersection of the Anninghe and the Daliangshan fault zones. The research results of this paper provide new information for further understanding of the deep geological structure and seismic activity mechanism in this area.
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根据美国地质调查局（United States Geological Survey，缩写为USGS）国家地震信息中心（National Earthquake Information Centre，缩写为NEIC）的测定，2020年6月23日15时29分04秒（UTC），墨西哥南部瓦哈卡州发生了一次矩震级MW7.4的地震，NEIC初步确定的震中（preliminary determination epicenter， 缩写为PDE）位于（15.916 3°N，95.953 3°W），震源深度为20 km。美国地质调查局（USGS，2020）和全球矩心矩张量组（GCMT，2020）随后发布了这次地震的矩心矩张量解（表1）。根据USGS （2020）发布的地震目录，在该主震发生后的48小时内发生了9次较大余震，其中最大余震震级达到MW5.4，5次事件深达35 km。
表 1 不同机构所得墨西哥MW7.4地震矩心矩张量解的比较Table 1. Comparison of the centroid moment tensor solutions for the MW7.4 Mexico earthquake obtained by different institutions机构 矩张量/（1020 N·m） 矩心参数 Mrr Mtt Mpp Mrt Mrp Mtp τc/s 北纬/° 西经/° 矩心深度/km GCMT （2020） 0.729 −0.737 0.008 1.220 −0.712 0.200 7.0 16.04 96.06 20 USGS （2020）（W震相） 0.731 −0.752 0.020 1.104 −0.479 0.168 13.2 15.93 95.90 21.5 USGS （2020）（体波反演） 0.527 −0.544 0.017 0.504 −0.289 0.101 − 16.04 95.90 32 本文 0.700 −0.789 0.089 0.825 −0.491 0.218 8.0 15.96 95.89 22 类似于上述两个组织的工作（Dziewonski et al，1981；Kanamori，Rivera，2008；Duputel et al，2012；Ekström et al，2012），我们收集了震中距处于32.5°—88.9°范围内全球地震台网（Global Seismograph Network，缩写为GSN）和数字地震台网联盟（International Federation of Digital Seismograph Networks，缩写为FDSN）的42个台站的长周期垂直分量数据，基于AK135模型计算格林函数（Wang，1999），利用我们自主研发的反演软件（张喆，许力生，2020），通过反演0.01—0.05 Hz频带内的P波波形得到了这次地震的矩心矩张量解。根据反演结果（图1），矩心时间为8 s，矩心震中位于（15.96°N，95.89°W），矩心深度为22 km，标量地震矩为1.24×1024 N·m，相当于MW7.4。基于矩心矩张量解（表1，图2），我们也求得了相应的最佳双力偶解（图2，表2），最佳双力偶成分占97%。最后，我们利用反演结果计算了合成波形，并与观测波形进行了比较，结果如图3所示，可见二者之间的相关系数平均值达到0.93，大多数台站的相关系数在0.90以上，均方根误差达1.33×10−5 m。
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图 1 矩心矩张量反演过程（a） 矩心时间搜索；（b） 矩心搜索；（c） 矩心深度搜索；（d） PDE位置（灰色）和矩心位置（红色）反演得到的矩张量解Figure 1. Inversion process of the centroid moment tensor（a） Search for the centroid time；（b） Search for the centroid；（c） Search for the centroid depth； （d） The moment tensor solutions at the PDE （gray） and centroid （red） locations![]()
图 2 矩心矩张量反演参数以及台站分布与反演结果Figure 2. The parameters of the centroid moment tensor inversion，the station distribution and the inversion results表 2 不同机构所得墨西哥MW7.4地震的最佳双偶解Table 2. The best double-couple solutions for the MW7.4 Mexico earthquake obtained by different institutes机构 标量地震矩
/（1020 N·m）双力偶成分
占比节面Ⅰ 节面Ⅱ 走向/° 倾角/° 滑动角/° 走向/° 倾角/° 滑动角/° GCMT （2020） 1.600 100% 270 16 62 118 76 97 USGS （2020）（W震相） 1.423 96% 271 17 70 112 74 96 USGS （2020）（体波） 0.797 99% 266 24 63 114 69 101 本文 1.236 97% 266 22 60 118 71 101 ![]()
图 3 观测波形与合成波形的比较Figure 3. Comparison between the observed （blue） and synthetic （red） waveforms与USGS和GCMT的结果相比（图4），我们反演所得矩心位置（15.96°N，95.89°W，深度22 km）、矩心时间、最佳双力偶解均与其非常相近。根据最佳双力解的节面参数、矩心位置、余震分布以及地震所处的构造环境，我们判断走向266°、倾角22°、滑动角60°的节面为真实的发震断层面（图4）。这是一次以逆冲为主、具有相当走滑分量的断层错动，或者说这是一次发生在俯冲带的斜滑事件。
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图 4 主震震源机制解与余震分布不同颜色的沙滩球和正方形代表不同机构确定的震源机制解及其矩心位置，小圆圈表示余震（来自USGS地震目录），大圆圈表示主震的PDE位置，圆圈和正方形的填充色显示了震源深度Figure 4. The focal mechanism solutions of the mainshock and the aftershock distributionColored beach-balls and squares represent the focal mechanism solutions and centroid locations determined by the various institutions，the small circles refer to the aftershocks （from the USGS catalog），and the large circle indicates the PED locations of the mainshock. The colors filled in the circles and squares indicate the focal depths本研究使用的数字波形数据均通过地震学联合研究会（Incorporated Research Institutions for Seismology，缩写为IRIS）数据中心获取，震源机制数据分别来自全球矩心矩张量（GCMT）和美国地质调查局（USGS），余震数据来自于美国地质调查局（USGS），作者在此表示感谢！
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图 9 剖面AA′ （a），BB′ （b），CC′ （c），DD′ （d），EE′ （e）的P波速度及地震分布图
左侧为P波绝对速度剖面，右侧为P波速度扰动剖面；黑色实线为地形，黑色圆点为距离剖面两侧10 km范围内的地震
Figure 9. P wave velocity along vertical profiles AA′ （a），BB′ （b），CC ′ （c），DD ′ （d），EE ′ （e） and earthquake distribution
Left column is the profile of absolute P wave velocity，right column is the perturbation velocity of P wave；black line represents topography，black dots denote seismic events within 10 km from both sides of the profile
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图 1 研究区构造背景及历史强震分布图（引自邓起东等，2002）
F1：鲜水河断裂带；F2：安宁河断裂带；F3：汶川—茂县断裂；F4：映秀—北川断裂；F5：灌县—江油断裂，下同
Figure 1. Tectonic settings and historical strong earthquake distribution of the studied area （after Deng et al，2002）
F1：Xianshuihe fault zone；F2：Anninghe fault zone；F3：Wenchuan-Maoxian fault；F4：Yingxiu-Beichuan fault；F5：Guanxian-Jiangyou fault，the same below
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图 3 三维P波初始模型图
图（a−f）分别为研究区不同深度的P波速度初始模型图；图（g，h）分别为沿102°E和30°N剖面的P波速度初始模型图
Figure 3. Three-dimensional P-wave initial model
Figs. （a−f） are the three-dimensional P-wave initial models at different depths in the studied area；Figs. （g，h） are the P-wave initial models of the profiles along 102°E and 30°N
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图 4 利用L-curve选取的最优平滑因子（a）和阻尼因子（b）曲线图
Figure 4. The optimal smoothing factor （a） and damping factor （b） curves selected by L-curve
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图 6 研究区不同深度的P波速度分布图
灰色实线为断层，白色线条为垂直剖面位置，黑色实线为板块边界线
Figure 6. P wave velocity distribution at different depths in the studied area
The gray lines represent faults，the white lines show the vertical sections position，and the black lines represent the plate boundary lines
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图 7 重定位前（左）、后（右）的震中（a，b）和震源深度（c，d）分布图
Figure 7. Distribution of epicenters （a，b） and focal depths （c，d） before （left） and after （right） relocation
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