Crustal velocity structure and seismogenic environments in the source areas of the 2013 Tongliao, Inner Mongolia, MS5.3 earthquake
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摘要:
为了解2013年内蒙古通辽MS5.3地震震源区地壳速度结构与孕震环境, 本研究基于"中国地震科学台阵——华北地区东部"29个流动地震台站自2017年1月至2019年4月期间记录的连续波形数据, 应用面波直接反演背景噪声成像方法, 获得通辽地震震源区与周边地区地壳三维S波速度结构.结果显示, 通辽MS5.3地震震源区与周边地区地壳S波速度结构呈现明显横向不均匀性.浅层S波速度结构分布特征与地表地质构造密切相关: 盆地内侧呈明显低速异常, 可能反映了沉积层结构, 而大兴安岭下方则呈现明显高速异常, 可能反映了造山带较为致密的古生代结晶基底岩.在中下地壳, 震源区低速异常向西南方向延展至南北重力梯度带.通辽MS5.3地震与该区域速度结构存在密切关系, 地震震中位于低速异常边缘, 表明该低速异常可能代表深部流体作用降低断层面有效正应力从而触发地震.结合前人全球的和区域尺度的地震层析成像结果展示上地幔存在明显低波速异常与地幔转换带存在明显高波速异常, 推测通辽MS5.3地震的发生可能与太平洋板块深俯冲至我国东北地区下方地幔转换带内形成"大地幔楔"中结构与动力学密切相关.在"大地幔楔"结构中, 由于地幔转换带中滞留板块脱水作用和地幔角流作用, 容易形成湿热物质上涌, 进而引起松辽盆地西南部岩石圈物质拆沉和携带流体的地幔热湿物质上涌至地壳后作用于断裂带、降低了断层面有效正应力, 从而导致了中强度地震的发生.
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关键词:
- 背景噪声面波直接成像方法 /
- 通辽地震 /
- 地壳速度结构 /
- 孕震环境
Abstract:To understand the crustal velocity structure and seismogenic environment of the 2013 Tongliao, Inner Mongolia, MS5.3 earthquake, we obtain a 3-D S-wave velocity structure of the crust around the Tongliao earthquake source areas by applying the direct ambient-noise surface-wave tomography technique to the continuous waveform data recorded at the 29 portable seismic stations of eastern North China ChinArray during January 2017 to April 2019. Our results show that there are obvious lateral heterogeneities in the S-wave velocity structure around the Tongliao MS5.3 earthquake source areas at the shallow crust. There is a close relationship between the shallower structural features and surface geological tectonics. Obvious low-velocity anomalies are imaged under the inner side of the Songliao basin, likely reflecting the sedimentary structure, whereas obvious high-velocity anomalies appear under the Great Xing'an range, possibly denoting dense Palaeozoic crystalline basement. In the mid-lower crust, the low-velocity anomalies extend southwestward to the North-South Gravity Lineament. The Tongliao MS5.3 earthquake is closely related to the regional crustal velocity structure. The epicenter of the Tongliao MS5.3 earthquake is located at the boundary of low-velocity anomalies, suggesting that the low-velocity anomalies may denote the deep fluids that could decrease the effective normal stress of the fault planes to trigger the earthquakes. Integrating with previous global and regional upper-mantle tomographic results showing low-velocity anomalies in the upper mantle and high-velocity anomalies in the mantle transition zone, we propose that the Tongliao MS5.3 earthquake could be related to the structure and dynamics of the big mantle wedge caused by the deep subduction of the Pacific slab down to the mantle transition zone. In the big mantle wedge structure, due to the stagnancy and dehydration of the Pacific slab in the mantle transition zone or the corner flow, it is easy to generate hot and wet mantle upwelling, leading to the lithospheric delamination under the southwestern Songliao basin and the hot and wet mantle upwelling intruding to the crust and then affecting the fault zone to decrease the effective normal stress of the fault planes. These processes could result in the generation of moderate-size earthquakes in the source areas.
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图 1
本研究区域地质构造
Figure 1.
Sketch map of regional geological tectonics in the study region
图 2
全部台站的噪声互相关波形
Figure 2.
Ambient noise cross-correlation waveforms of all seismic stations
图 3
质量控制后最终用于反演的5~25 s周期相速度频散曲线(黑线)
Figure 3.
The selected phase velocity dispersions (black lines) of 5~25 s periods used in the final inversion after quality controls
图 4
5、15、20和25 s周期相速度射线路径分布图
Figure 4.
Ray paths of phase velocity at 5, 15, 20 and 25 s periods
图 6
(a) S波初始模型(红线)和最终模型(蓝线)对比图.(b) 不同周期Rayleigh波相速度平均观测频散曲线(黑色实线)、初始模型拟合的频散曲线(红色虚线)和最终模型拟合的频散曲线(蓝色虚线)对比图
Figure 6.
(a) Comparison between the initial S-wave velocity model (red line) and final velocity model (blue line). (b) Comparison between observed and averaged dispersion curves (solid black line), synthetic dispersion curves from initial model (dashed red line) and final model (dashed blue line) for Rayleigh wave phase velocities at different periods
图 7
不同深度反演网格点对应的平均DWS
Figure 7.
The average DWS values for inverting nodes at different depths
图 8
波速异常水平向尺度为0.375°×0.375°模型不同深度的检测板实验结果
Figure 8.
Results of the checkerboard resolution tests at different depths with a velocity anomaly size of 0.375°×0.375° in the horizontal directions
图 9
波速异常水平向尺度为0.75°×0.375°模型不同深度的检测板实验结果
Figure 9.
Results of the checkerboard resolution tests at different depths with a velocity anomaly size of 0.75°×0.375° in the horizontal directions
图 10
波速异常尺度为0.75°×0.375°模型检测板实验结果纵剖面
Figure 10.
Vertical cross-section of the results of a checkerboard resolution test with a velocity anomaly size of 0.75°×0.375°
图 11
波速异常水平向尺度为0.75°×0.75°模型不同深度检测板实验结果
Figure 11.
Results of a checkerboard resolution test at different depths with a velocity anomaly size of 0.75°×0.75° in the horizontal directions
图 12
(a) 面波均方根走时残差随反演迭代次数的变化. (b)反演前(虚线)和反演后(实线)的频散曲线走时残差分布图
Figure 12.
(a) Variations of the surface-wave travel-time RMS residuals with iterations. (b) Comparison between travel-time residual histograms before (dashed line) and after (solid line) inversion
图 14
穿过2013年通辽MS5.3地震震中的三条纵剖面速度结构图
Figure 14.
Three vertical cross-sections of velocity structures passing through the earthquake hypocenter of the 2013 Tongliao MS5.3 earthquake
图 15
本研究结果(a)与前人(Song and Lei, 2022)研究结果(b)的对比其中的符号与图 1相同.
Figure 15.
Comparison between the present (a) and previous (Song and Lei, 2022) (b) tomographic results The symbol is the same as that in Fig. 1.
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