京西北地区地壳速度结构与地震重新定位联合反演

doi:10.3969/j.issn.0253-4967.2025.04.20240014

地震地质 ›› 2025, Vol. 47 ›› Issue (4): 1132-1151.DOI: 10.3969/j.issn.0253-4967.2025.04.20240014

京西北地区地壳速度结构与地震重新定位联合反演

宫猛¹^,²⁾(), 邹献昆²⁾, 王晓山³⁾^,^*(), 李广²⁾, 盛书中²⁾, 李红星²⁾, 徐荣华⁴⁾, 路昌胜²⁾

1)东华理工大学, 铀资源探采与核遥感全国重点实验室, 南昌 330013
2)南昌市地质灾害智能感知技术与仪器重点实验室, 南昌 330013
3)河北省地震局, 石家庄 050021
4)江西省地质调查勘查院, 南昌 330000

收稿日期:2024-01-29 修回日期:2024-06-13 出版日期:2025-08-20 发布日期:2025-10-09
通讯作者: *王晓山, 男, 1980年生, 博士, 高级工程师, 主要从事地震定位和地震构造探查工作, E-mail: wangxsh2022@163.com。
作者简介:
宫猛, 男, 1983年生, 博士, 副研究员, 主要从事壳-幔速度结构与地震活动性分析研究, E-mail: mrgongm@163.com。
基金资助:
国家自然科学基金(42474197); 河北省地震科技星火计划项目(DZ20200827054); 河北省地震科技星火计划项目(DZ2024083000001); 江西省自然基金(20242BAB26049); 东华理工大学研究生创新基金(YC2023-S577)

SIMULTANEOUS INVERSION OF CRUSTAL VELOCITY STRUCTURE AND EARTHQUAKE RELOCATION IN THE NORTHWEST OF THE BEIJING AREA

GONG Meng¹^,²⁾(), ZOU Xian-kun²⁾, WANG Xiao-shan³⁾^,^*(), LI Guang²⁾, SHENG Shu-zhong²⁾, LI Hong-xing²⁾, XU Rong-hua⁴⁾, LU Chang-sheng²⁾

1)National Key Laboratory of Uranium Resource Exploration and Nuclear Remote Sensing, East China ; University of Technology, Nanchang 330013, China
2)Nanchang Key Laboratory of Intelligent Sensing Technology and Instrumentation for Geological Hazards, Nanchang 330013, China
3)Hebei Earthquake Agency, Shijiazhuang 050021, China
4)Geological Survey and Exploration Institute of Jiangxi Province, Nanchang 330000, China

Received:2024-01-29 Revised:2024-06-13 Online:2025-08-20 Published:2025-10-09

摘要/Abstract

摘要：

文中利用河北、山西和内蒙古区域地震台网中145个国家地震台站记录到的2009年1月—2020年12月发生在京西北地区(37°~41°N, 111°~118°E)的20 442个地震的震相走时数据, 采用双差层析成像方法反演该区地壳三维P波速度结构, 同时获得17 613个地震震源参数。结果显示, 京西北地区的地壳结构变化与地形、地貌及构造环境具有较好的相关性, 震源深度主要分布在5~25km范围, 且地震空间分布能较好地刻画出深部断层的几何形态。小地震重定位结果显示, 张-渤地震带内部发育一系列倾角较陡的深断层, 存在NW和NE向共轭状断层。其中, 夏垫断裂和新河断裂均为近直立的高倾角深大断裂。P波速度结构显示, 晋冀蒙交界区地壳内部的速度相对较低, 河北平原带地壳内部结构存在较强的横向不均匀性; 张-渤地震带中下地壳存在显著的低速异常, 山西断陷带地壳内部低速异常的深度分布由南至北逐渐加深。整体来看, 京西北地区的地震活动与深、浅断裂的发育及地壳速度结构分布特征密切相关, 绝大部分地震发生在脆性上地壳内及上地壳与下地壳相交的脆-韧性转换带。

关键词: 双差成像, P波速度结构, 地震重定位, 断层形态

Abstract:

The northwest Beijing area is located in the northwest of the ancient North China Craton block. Due to the long-term and frequent geological structure evolution and tectonic movement of the North China block, the complex geological structure pattern has been created in this area, with the Yanshan tectonic belt in the north, the North China rift basin in the south, the Shanxi depression belt in the west, and the Bohai Sea in the east. Due to its unique geographical location and frequent seismic activity, this area has long been a key concern for geologists and seismologists.

We collected P waves’ absolute and relative travel time of 20 442 earthquakes in the northwest of the Beijing area record by 145 seismic stations deployed in Hebei, Shanxi and Neimeng Provinces, during January 2009 to December 2020 and used double-difference seismic tomography joint inverted the Seismic source location parameters and the 3D P-wave velocity structure of the study area. To improve the uniformity of ray coverage and the accuracy of data in inversion, seismic phases were selected based on the following conditions. 1)The P-wave phases of each earthquake are required to be recorded by at least four stations; 2)Seismic phases with error greater than ±0.5s were eliminated by using the epicentral distance-travel time fitting curve of the selected earthquake; 3)The distance between each earthquake pair is required to be less than 10km, and the number of double difference data formed by each earthquake pair is required to be larger than 8.

In the inversion process, the research area is divided into three dimensional grids according to the station location and earthquake distribution. The horizontal direction is divided into 0.3°×0.3° grids, In vertical depth, nodes are set at 0km, 5km, 10km, 15km, 20km, 25km, 30km, 35km, 42km, 50km, and 60km respectively. The value of the damping coefficient is set to 600, the value of the smoothness factor is set to 40, and the number of iterations is set to 10. Thus, after 10 iterations of inversion, the distribution range of residual travel time of seismic data decreases from ±3s to±1s, and the horizontal and vertical errors of the source location after relocation are 0.1~0.9km and 0.1~1.5km, respectively. In order to ensure the accuracy of velocity structure inversion, the reliability of the results is evaluated by using Differential Weighted Sum of Nodes(DWS) and a detection board. Finally, the P-wave velocity structure at depths less than 50km underground in the study area, along with the relocation source parameters of 17613 earthquakes, are obtained.

The results show that: 1)The focal depth of earthquakes is mainly distributed in the 5~25km depth range. The relocated earthquakes are more closely clustered near the fault zone and the seismic spatial distribution can better describe the geometric morphology of deep faults. There are several NE-trending and NW-trending faults with deep development and steep dip Angle in the Zhang-Bo earthquake zone. Both the Xiadian fault and the Xinhe fault are nearly vertical deep faults with a high dip Angle. 2)The variation of the P-wave velocity had a good correlation with the topography, geomorphology and tectonic environment. Influenced by the surface sediments, the P-wave velocity in shallow crust of the Shanxi fault depression belt, Hebei plain and inter-mountain basin shows low-velocity anomalies. The P-wave velocity in the crust of the junction area of Shanxi, Hebei, and Mongolia is relatively low. The significant low-velocity anomaly of the Zhang-Bo earthquake belt at depth of 42km underground is related to the Destruction of the North China Craton and the upwelling of deep thermal materials. 3)Based on the P-wave velocity structure and seismic relocation results, the fault is developed in the earthquake-prone areas in the northwest of Beijing and its adjacent areas. Most earthquakes occur in the brittle-ductile transition zone between the brittle upper crust and the ductile middle and lower crust. In summary, the seismicity in the northwest Beijing area is closely related to the development of deep and shallow faults and the velocity structure.

Key words: double-difference seismic tomography, P-wave velocity structure, earthquake relocation, fault geometry

宫猛, 邹献昆, 王晓山, 李广, 盛书中, 李红星, 徐荣华, 路昌胜. 京西北地区地壳速度结构与地震重新定位联合反演[J]. 地震地质, 2025, 47(4): 1132-1151.

GONG Meng, ZOU Xian-kun, WANG Xiao-shan, LI Guang, SHENG Shu-zhong, LI Hong-xing, XU Rong-hua, LU Chang-sheng. SIMULTANEOUS INVERSION OF CRUSTAL VELOCITY STRUCTURE AND EARTHQUAKE RELOCATION IN THE NORTHWEST OF THE BEIJING AREA[J]. SEISMOLOGY AND GEOLOGY, 2025, 47(4): 1132-1151.

图/表 11

图1 研究区域地貌、断层展布及有记录以来MS≥6地震的分布带颜色的圆圈表示历史上6级以上的地震震中, 黑色线段表示断层展布, 红色直线为图10中4条剖面的位置

Fig. 1 Simplified topographical map and the strong earthquakes(MS≥6) distribution in the northwest of the Beijing area.

图2 研究中所用的台站及地震分布图红色三角形为台站位置, 黑色空心圆表示地震分布

Fig. 2 Distribution of earthquakes and stations used in this study.

图3 研究中使用的P波震相走时-震中距关系图

Fig. 3 Travel time-epicentral distance curve of the P wave.

表1 研究区一维P波速度模型

Table1 1-D P-wave velocity model for the study region

深度/km	0	5	10	15	20	25	30	35	42	50	62
V_P/km·s^-1	4.8	5.5	6.1	6.2	6.3	6.4	6.5	6.7	7.5	8.1	9.0

图4 阻尼系数和光滑因子的均衡曲线 a 使用不同阻尼系数值得到的模型和残差的归一化均衡曲线, 阻尼参数最优解为600; b 设置阻尼参数为600时, 使用不同光滑因子值所得到的模型和残差的归一化均衡曲线, 光滑因子最优取值为40

Fig. 4 L-curve of damping and smoothing factor.

图5 研究区不同深度的DWS分布图右下角为对应的深度, 颜色表示射线的密度值

Fig. 5 DWS distribution maps at different depths in the study area.

图6 不同深度层的检测板分辨率检测结果

Fig. 6 P wave velocity checkerboard test results at different depths.

图7 反演前后地震数据走时残差图和定位后误差分布图

Fig. 7 Histograms of the residual before and after the inversion and the errors after relocation.

图8 地震定位前、后的参数对比图 a、 c、 e 定位前的结果图; b、 d、 f 定位后的结果图。其中, 图a、 b为地震在平面位置上的分布图; 图c、 d为地震沿经度剖面的深度分布; 图e、 f为地震在不同深度的频次图

Fig. 8 Comparison epicenter parameters of earthquake before and after relocation.

图9 不同深度的P波速度扰动分布图像

Fig. 9 Estimated P-wave velocity perturbation maps at different depths.

图10 图1中4条轴线方向剖面的P波速度结构及对应深度的地震分布图圆圈为地震, 黑色线段为断层在地表的位置, 红色线段为勾画的断层形态。F1蛮汉山山前断裂; F2天镇-阳高盆地北缘断裂; F3阳原盆地北缘断裂; F4怀涿盆地北缘断裂; F5延庆-矾山盆地北缘断裂; F6东北旺-小汤山断裂; F7黄庄-高丽营断裂; F8顺义-良乡断裂; F9夏垫断裂; F10香河断裂; F11口泉断裂; F12六棱山北麓断裂; F13蔚县盆地南缘断裂; F14孙庄子-乌龙沟断裂; F15太行山山前断裂; F16容城东断裂; F17牛东断裂; F18大城东断裂; F19沧东断裂; F20恒山北麓断裂; F21五台山断裂; F22系舟山山前断裂; F23晋县断裂; F24新河断裂; F25离石断裂; F26交城断裂; F27太谷断裂

Fig. 10 Vertical slices of the estimated P-wave velocity perturbation and the earthquake distribution are plotted along the four profiles identified in Fig. 1.

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京西北地区地壳速度结构与地震重新定位联合反演

SIMULTANEOUS INVERSION OF CRUSTAL VELOCITY STRUCTURE AND EARTHQUAKE RELOCATION IN THE NORTHWEST OF THE BEIJING AREA

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