Direct Surface-wave Tomography from Ambient Noise in the Shanxi Rift Zone and Adjacent Areas
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摘要:
山西断陷带是世界上最活跃的新生代大陆裂谷之一，获得该地区地壳精细三维S波速度结构有助于了解大陆裂谷的形成机制。本研究利用2021年1月至2022年12月期间山西、内蒙、河北、河南和陕西等地布设的113个省级固定台站记录的连续波形数据，提取5~40 s周期范围共
4951 条高质量瑞利波相速度频散曲线，采用面波直接反演成像法，获得山西断陷带及其周边地区地壳0~40 km深度的三维S波速度结构。结果表明：5 km深度处的S波速度结构与地表断陷带分布和沉积层厚度存在一定相关性，断陷带整体呈低速异常特征，两侧隆起区为高速异常；随着深度的增加，低速异常区域有所减少，且低速异常从地表一直延伸至15 km深度左右；从25 km深度开始，山西断陷带中南部的太原盆地、临汾盆地和运城盆地由上地壳的低速异常转为下地壳的高速异常，并持续延伸至上地幔顶部，可能为盆地拉张之前第三纪早期的玄武岩岩浆底侵冷却所致；大同火山区的低速异常从上地幔顶部持续延伸至地壳20 km深度左右，并由西向东转移，较清晰地揭示出大同火山下方的岩浆上涌通道；北纬38° 以北大面积的低速异常推测可能为新生代以来大同火山大量的火山活动引起地壳升温导致部分熔融形成。本研究获得的研究区地壳三维高分辨率S波速度结构为进一步理解大陆裂谷的形成机制提供了新的地震学证据。Abstract:The Shanxi rift zone is one of the most active continental rift zones in the world. Obtaining a fine three-dimensionalS-wave velocity structure of the crust in this region helps understand the formation mechanism of continental rifts. In this study, continuous waveform data recorded at 113 fixed provincial stations deployed in Shanxi, Inner Mongolia, Hebei, Henan, and Shaanxi between January 2021 and December 2022 were utilized. A total of
4951 high-quality Rayleigh wave phase velocity dispersion curves in the 5~40 s period range were extracted. Using the direct surface wave imaging method, a three-dimensional S-wave velocity structure of the crust in the Shanxi rift zone and surrounding areas at depths of 0~40 km was obtained. The results show that the S-wave velocity structure at a depth of 5 km correlates with the distribution of surface fault zones and thickness of the sedimentary layers. Rift zones generally exhibit low-velocity anomalies with high-velocity anomalies on both sides of the uplift areas. As depth increases, the low-velocity anomaly gradually decreases, with low-velocity zones extending from the surface to approximately 15 km depth. At a depth of 25 km, the low-velocity anomalies in the central and southern parts of the Shanxi rift zone, including the Taiyuan, Linfen, and Yuncheng basins, transitioned from the upper crust to high-velocity anomalies in the lower crust, extending to the top of the upper mantle. This may have been caused by cooling of the basaltic magma intruding beneath the basins during the early Tertiary period before rifting. In the Datong volcanic region, the low-velocity anomaly extends from the top of the upper mantle to approximately 20 km depth in the crust and shifts from west to east, clearly revealing the magma upwelling pathway beneath Datong. A large low-velocity anomaly north of 38°N was inferred to have been caused by crustal heating and partial melting due to extensive volcanic activity in the Datong volcanic region since the Neogene. The high-resolution three-dimensional S-wave velocity structure of the crust obtained in this study provides valuable insights into the formation mechanisms of continental rifts. -
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图 1 山西断陷带及其周边区域地质构造
注：（a）为山西断陷带周边的主要地质构造单元；（b）为山西断陷带内部的主要地质构造。其中，（a）中的黑色虚线框为本研究的研究区域，黑色线段代表地块边界，红色三角形代表大同火山；（b）中黑色线段代表断层，蓝色圆圈代表该区域历史上发生过的5~8级地震，其余符号与图（a）相同。YSOB，阴山−燕山造山带；HTB，河套盆地；Ordos Block，鄂尔多斯块体；FWB，汾渭盆地；QDOB，秦岭−大别造山带；Shanxi rift zone，山西断陷带；HCB，华北盆地；DTV，大同火山；DTB，大同盆地；XDB，忻定盆地；TYB，太原盆地；LFB，临汾盆地；YCB，运城盆地；Lüliang OB，吕梁山造山带；Taihang OB，太行山造山带；SLG，石岭关隆起；LS，灵石隆起。
Figure 1. Geological structures of the Shanxi rift zone and surrounding areas
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图 2 山西断陷带及其周边区域台站分布
注：黑色线段代表断层，红色三角形代表大同火山，蓝色和白色三角形代表本研究所使用的113个固定台站。其中，白色三角为图3所用的台站ANZ。
Figure 2. Distribution of seismic stations in the Shanxi rift zone and surrounding areas
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图 3 在5~40 s周期范围内台站ANZ（如图2中的白色三角所示）与所有台站的噪声互相关函数。在正负延迟中均能清楚地看到一致的瑞利波信号
Figure 3. The noise cross-correlation functions between station ANZ (as indicated by the white triangle in Fig.2) and all other stations in the 5~40 s period range. Consistent Rayleigh wave signals can be clearly observed in both positive and negative delays
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图 4 质量控制后用于最终反演的5~40 s周期相速度频散曲线。黄色实线是每个周期的平均相速度
Figure 4. Phase velocity dispersion curves for the 5~40 s period range used in the final inversion after quality control. The yellow solid line represents the average phase velocity in each period
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图 5 5~40 s不同周期的射线路径数量
Figure 5. Number of ray paths for different periods in the 5~40 s range
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图 6 不同周期的台站射线路径覆盖
注：蓝色三角形代表台站，黑线代表射线路径，各周期射线路径的数量见图件上部。
Figure 6. Ray-path coverage for different periods
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图 7 （a）反演后速度模型，（b）敏感核测试结果
Figure 7. (a) Velocity model after inversion， (b) Sensitivity kernel test
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图 8 （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 8. (a) Comparison of the initial S-wave model (red line) and final model (blue line). (b) Comparison of the average observed Rayleigh wave phase velocity dispersion curves (black solid line), dispersion curve fitted by the initial model (red dashed line), and dispersion curve fitted by the final model (blue dashed line) for different periods
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图 9 水平方向异常尺度为 2°×2° 检测板实验结果
注：红色三角形为研究区域内的大同火山，黑色实线表示为活动断层和构造边界。
Figure 9. Results of a checkerboard resolution test for velocity anomalies on a 2° × 2° horizontal scale
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图 10 水平方向异常尺度为 1.5°×1.5° 检测板实验结果
注：红色三角形为研究区域内的大同火山，黑色实线表示为活动断层和构造边界。
Figure 10. Results of a checkerboard resolution test for velocity anomalies on a 1.5°× 1.5° horizontal scale
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图 11 水平方向异常尺度为 1°×1° 模型检测板实验结果
注：红色三角形为研究区域内的大同火山，黑色实线表示为活动断层和构造边界。
Figure 11. Results of a checkerboard resolution test for velocity anomalies on a 1 °× 1 °horizontal scale
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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
Figure 12. (a) Variation in surface wave root-mean-square (RMS) travel time residuals with number of inversion iterations. (b) Dispersion curves before (dashed line) and after (solid line) inversion
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图 13 不同深度的S波速度成像结果图
注：DTV，大同火山；XZ，忻州；SLG，石岭关隆起；TY，太原；LS，灵石隆起；LF，临汾；YC，运城。不同深度的平均速度见在图件上部。色标位于图底。其余符号标注与图1相同。
Figure 13. Images of S-wave velocities at different depths
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图 14 不同垂向剖面的S波速度成像结果图
注：DTV，大同火山；XZ，忻州；SLG，石岭关隆起；TY，太原；LS，灵石隆起；LF，临汾；YC，运城。色标位于图底。速度扰动相对于一维平均速度模型。每条剖面的地形在顶部绘制。
Figure 14. Vertical S-wave velocity profiles
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