Advances in passive seismic analysis of sediment structure and applications in some typical basins
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摘要: 准确的沉积层结构，对盆地地区油气资源调查与勘探、地震动场地效应评估和壳幔深部结构成像等研究均具有重要意义. 近二十年来，随着地震观测技术的进步和大量流动台阵数据的积累，利用被动源资料探测沉积层结构的地震学方法研究取得了长足的发展. 本文对这些主要方法进行了归纳总结，阐述了基本原理及相关进展. 其中，基于远震体波数据的研究方法主要有：接收函数和转换函数、波场反延拓的H-β方法、以及P波质点运动分析等. 基于近场体波资料约束沉积层结构通常采用的是高频波形拟合方法. 此外，还简要介绍了谱比法、背景噪声面波成像和Rayleigh波Z/H幅度比，以及多种方法的联合反演. 最后，对我国东部典型盆地地区，如松辽盆地和华北盆地下方沉积层结构已取得的研究进展进行了总结.Abstract: Accurate constraints on sediment structure are of great importance for investigation and exploration of oil and gas resources, evaluation of site response, and imaging of deep crust and mantle structure. With the advance of seismic observation and the accumulation of large data from portable arrays, seismological methods using passive source to resolve sediment structures with high resolution have developed. In this paper, we review the advances in the seismological analyses and their basic principles, including receiver functions, transfer functions, H-β technique based on wavefield downward continuation, and P-wave particle motion using teleseismic data. Waveform fitting with high frequency is usually used for sediment structure constraints from local earthquakes. In addition, we also briefly review the analyses of spectral ratio, ambient noise tomography, Rayleigh wave Z/H amplitude ratio, and their joint inversion. Finally, we summarize the progress of research work on the structure of the shallow crust beneath the Songliao and North China basins based on these methods.
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图 1 均匀介质中，不同地震台站（基岩和位于盆地内）下方远震和近震P波响应的射线路径示意图. 实线表示P波，虚线表示S波
Figure 1. Schematic ray paths of the P (black solid lines) and S (red dashed lines) waves beneath stations (located on bedrock and sediment) in response to an incoming P wave both at teleseismic and local distances
图 2 （a）利用相邻算法获得的A001台站的接收函数波形拟合结果. 黑色为实际波形，红色为理论地震图.（b）最优的S波速度模型与波速比（修改自武岩等，2014）
Figure 2. (a) Comparison of receiver functions at A001 station between the observations (black lines) and synthetics (red lines) derived from neighborhood algorithm inversion. (b) The best fitting S wave velocity model together with VP/VS ratio (modified from Wu et al., 2014)
图 3 沉积盆地台站下方射线路径示意图，其中实线表示上行和下行 P 波，虚线表示上行和下行 S 波（修改自Tao et al., 2014）
Figure 3. Schematic ray paths of the upgoing and downgoing P (solid lines) and S (dashed lines) waves inside the sediment, crust and mantle in response to an incoming P wave at teleseismic distance (modified from Tao et al., 2014)
图 4 （a）NE96台站记录到的2010年2月15日发生的远震事件的垂向和径向分量，经过1～10 s的带通滤波后的波形示意图.（b）P波质点运动轨迹图，时窗范围见图（a）所示.（c）位于盆地内NE96台站（红色正方形）和基岩上方NEA3台站（蓝色圆圈，位于）测得的不同周期下的平均AP分裂时间（修改自Bao and Niu, 2017）
Figure 4. (a) Normalized vertical-(BHZ) and radial-component (BHR) recordings of NE96 from a teleseismic earthquake occurring on 15 February 2010, which is filtered in the period band of 1～10 s. (b) The particle motion of the P wave, which is denoted by the shaded time window in Fig. 4a. (c) Comparison of the average AP splitting times as a function of period measured at NE96 (red solid squares) and NEA3 stations (open blue circles), which are deployed on sediment and bedrock, respectively (modified from Bao and Niu, 2017)
图 5 （a）从震源（8 km深度）出发的P波和S波系列震相的射线参数随震中距变化图. 其中，两个圆圈表示PEBM台站记录到的地震事件6的P波和S波的射线参数，水平线表示S波在基底处发生相移的临界射线参数（修改自Langston, 2003）. （b）f–k方法计算的爆炸源（黑线）和平面波（虚线）的理论地震图的比较，其中震源深度和震中距在径向分量中已标识（修改自Ni et al., 2014）
Figure 5. (a) Ray parameter versus distance curve for incident P and S phases from a source at 8-km depth. The two open circles show P and S ray parameters for event 6 at PEBM. The horizontal line shows the critical ray parameter where S phases undergo a phase shift due to a complex transmission coefficient at the basement boundary (modified from Langston, 2003). (b) Comparisons of the waveforms computed by f–k with explosion source (black lines) and plane-wave synthetics (dashed lines). The focal depth and epicentral distance used in the f–k computations are labeled above each radial waveform (modified from Ni et al., 2014)
图 6 V45A台站（沉积层厚度为869 m）得到的H/V谱比曲线（a）和V/H谱比曲线（b），括号表示最大峰值频率区域. W44A台站记录到的8个地震事件得到的的H/V谱比曲线（c）和V/H谱比曲线（d）. 其中，H/V谱的最大峰值共振频率为0.2～0.4，但V/H谱的最大峰值共振频率较为复杂（修改自Mostafanejad and Langston, 2017）
Figure 6. (a) H/V and (b) V/H power spectral ratios for observed teleseismic P waves at station V45A with sediment thickness of 869 m. Brackets point out the areas of maximum peak frequency. (c) H/V and (d) V/H power spectral ratio for station W44A with overlying spectra of eight different teleseismic P waves. Brackets show the frequency band that the peak resonance may be in. Although maximum peak resonance frequency for H/V spectra is definitely arriving on 0.2～0.4, it is more complicated to recognize where maximum peak occurs for V/H spectra (modified from Mostafanejad and Langston, 2017)
图 7 松辽盆地沉积层厚度分布图.（a）和（b）分别是利用H-β方法（修改自况春利等，2022）和高频近震P波转换波震相估算的沉积层厚度图（修改自马海超，2020）.（c）背景噪声成像中2.9 km/s的速度等值线对应的沉积层厚度分布图（修改自王仁涛等，2019）.（d）基于频率相关的P波质点运动方法获得的沉积层厚度分布图（修改自Bao and Niu, 2017）
Figure 7. Sediment thickness in the Songliao basin obtained by H-β method. (a) (modified from Kuang et al., 2022), and by high-frequency Ps converted from local deep earthquakes (b) (modified from Ma et al., 2020). (c) The sediment thickness at 2.9 km/s velocity isosurface obtained from short-period ambient noise tomography (modified from Wang et al., 2019). (d) The sediment thickness obtained by P-wave frequency-dependent P Wave particle motion (modified from Bao and Niu, 2017)
图 8 华北克拉通中部和东部地区沉积层厚度分布图. 其中（a）和（b）分别是利用背景噪声面波和接收函数联合反演方法（修改自姜磊等，2021）和采用人工地震测深（修改自段永红，2016）得到的沉积层厚度分布图. （c）和（d）分别是采用接收函数波形反演方法（修改自武岩等，2014）和序贯接收函数H-κ扫描方法（修改自Zhang and Huang, 2019）获得的渤海地区沉积层厚度分布图
Figure 8. Sediment thickness beneath the central and eastern North China Craton, obtained by joint inversion of receiver function and Rayleigh wave dispersions (a) (modified from Jiang et al., 2021) and deep seismic sounding (b) (modified from Duan et al 2016). The sediment thickness of Bohai Bay basin derived by receiver function waveform fitting (c) (modified from Wu et al., 2014) and sequential H-κ stacking method (d) (modified from Zhang and Huang, 2019)
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