Reviews on seismic anisotropy based on shear-wave splitting in the Tibetan Plateau
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摘要: 有关青藏高原横波分裂的各向异性研究已经开展了近30年，在理论方法和实际应用方面取得了重要进展，并获取了大量的横波分裂测量结果，为认识青藏高原壳幔各向异性变形特征和动力学机制提供了重要的依据. 本文首先介绍了地震各向异性的来源与应用，随后回顾了横波分裂分析方法的发展，简述了各种横波分裂方法的原理，最后通过总结近30年来青藏高原上地壳、整个地壳和上地幔横波分裂各向异性研究成果，系统分析了青藏高原壳幔各向异性变形特征. 基于各横波分裂结果的对比分析来看，XKS波分裂测量结果最为稳定，近震直达S波分裂测量结果次之，而Pms波分裂测量结果相对离散，往往相同区域内不同的研究结果差异较大，主要原因可能是相比XKS波和近震直达S波，Pms波的信噪比较低，次要原因可能是各研究在方法和处理分析等方面的差异.Abstract: The research on the anisotropy of shear wave splitting in the Tibetan Plateau has been carried out for nearly 30 years, and important progress has been made in theoretical methods and practical applications. A large number of shear wave splitting results obtained from teleseismic records, which provides an important basis for understanding the deformation characteristics and dynamic mechanism of the crust and mantle anisotropy in the Tibetan Plateau. In this paper, we first introduce the source and application of seismic anisotropy in the Earth's interior; then review the development of shear wave splitting analysis methods, briefly expounds the principle of various shear wave splitting methods; finally, systematically analyze the crust-mantle anisotropic characteristics in the Tibetan Plateau by summarizing the shear wave splitting results of the anisotropy in the upper crust, crust and upper mantle in the Tibetan Plateau over the past 30 years. Based on the comparison of the shear wave splitting results, we find the XKS wave splitting results are the most stable, the direct S wave splitting results from local earthquakes are better, but the Pms wave splitting results are more discrete. The Pms wave splitting results of different studies in the same research area are often different. The main reason may be the signal-to-noise ratio of the Pms wave is lower than that of the XKS wave and the direct S wave of the local earthquake. The secondary reason may be the differences in methods and processing analysis of various studies.
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Key words:
- Tibetan Plateau /
- shear wave splitting /
- anisotropy /
- lithospheric deformation /
- deep structure
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图 1 青藏高原及邻区地质构造图（修改自滕吉文等，2019）. MBT：主边界逆冲断裂；IYS：雅鲁藏布江缝合带；BNS：班公—怒江缝合带；JS：金沙江缝合带；AKMS：阿尼玛卿—昆仑—慕孜塔格缝合带；SQS：南祁连缝合带；NQS：北祁连缝合带；HB：喜马拉雅块体；LB：拉萨块体；QB：羌塘块体；SB：松潘—甘孜块体；KB：昆仑—柴达木块体
Figure 1. Geological structure map of the Tibetan Plateau and surrounding areas (modified from Teng et al., 2019). MBT: Main Boundary Thrust; IYS: Indus-Yarlung Suture; BNS: Bangong-Nujiang Suture; JS: Jinshajiang Suture; AKMS: Anyimaqen-Kunlun-Mutztagh Suture; SQS: South Qilian Suture; NQS: North Qilian Suture; HB: Himalayan Block; LB: Lhasa Block; QB: Qiangtang Block; SB: Songpan-Ganzi Block; KB: Kunlun-Qaidam Block
图 2 横波穿过各向异性介质分裂现象示意图（修改自Crampin and Chastin, 2003）
Figure 2. Schematic of shear wave splitting (modified from Crampin and Chastin, 2003)
图 3 互相关函数分析法横波分裂测量示例（修改自Bowman and Ando, 1987）. （a）水平面内的质点原始运动轨迹；（b）按照（a）中确定的快波方向旋转的地震波形图；（c）慢波波形前移0.54 s后的波形图，这时两水平分量的互相关系数达到最大；（d）各向异性校正后的质点运动轨迹
Figure 3. An example of the cross-correlation analysis technique (modified from Bowman and Ando, 1987). (a) Original horizontal particle motion; (b) Seismograms rotated by angle determined in (a); (c) Rotated seismograms with upper trace advanced by 0.54 s, the time shift which gives maximum absolute value of cross-correlation coefficient between traces; (d) Particle motion corrected for anisotropy
图 4 可视化测量方法横波分裂测量示例（修改自常利军，2014）.（a）原始波形的三分量记录图; （b）两个水平分量的地震记录图; （c）水平面内的横波质点运动轨迹; （d）将水平向地震记录旋转至快、慢波方向的地震图
Figure 4. An example of the visual measurement technique (modified from Chang, 2014). (a) Three-component records of original seismic waveform; (b) Two horizontal components of seismograms; (c) Shear wave particle motion in horizontal; (d) Seismograms rotated to the fast and slow shear wave directions
图 5 最小切向能量方法横波分裂测量示例（修改自Teanby et al., 2004）.（a）原始波形旋转至径向、切向和垂向上的三分量波形图，A和F限定了横波分裂窗口；（b）稳定解的收敛置信区间，最优解用十字标记；（c）快、慢波坐标系下，时间校正前后的快、慢波波形和质点运动轨迹，快、慢波波形相似，质点运动图由时间校正前的椭圆变为校正后的线性；（d）径向和切向坐标系下，分裂校正前后的波形图，校正前的切向分量明显，校正后的切向分量变得很小.
Figure 5. An example of shear-wave splitting measurement results with minimum tangential energy method (modified from Teanby et al., 2004). (a) Raw data rotated to the radial and tangential directions; A and F are the beginning and end of the shear-wave analysis window; (b) A grid search over the shear wave splitting parameters is performed to find the parameters that best linearize the particle motion; (c) Fast and slow shear waveforms and particle motion before and after the shear- wave splitting correction. The fast and slow waves have similar waveforms, and the particle motion has been linearized after the correction; (d) Radial and transverse components before and after the splitting correction. The energy should be minimized on the corrected transverse component in the shear-wave analysis window
图 6 横波穿过双层各向异性介质分裂现象示意图（修改自Silver and Savage, 1994）
Figure 6. Schematic of shear wave splitting in the case of two anisotropic layers (modified from Silver and Savage, 1994)
图 7 青藏高原近震直达S波和Pms波分裂测量结果分布图. 红色线段为近震直达S波分裂结果，蓝色线段为Pms波分裂结果，线段方向代表快波偏振方向，长度代表延迟时间（近震直达S波分裂延迟时间按上地壳厚度为25 km计算）
Figure 7. Distribution of local seismic S wave and Pms wave splitting measurement results in the Tibetan Plateau.The red lines are the results of local seismic S wave splitting, and the blue lines are the results of Pms wave splitting. The direction of the line represents the polarization direction of the fast wave and the length represents the delay time (The local seismic S wave delay time is calculated based on the upper crust thickness of 25 km)
图 8 青藏高原Pms波和XKS波分裂测量结果分布图. 红色线段为XKS波分裂结果，蓝色线段为Pms波分裂结果. 线段方向代表快波偏振方向，长度代表延迟时间
Figure 8. Distribution of Pms wave and XKS wave splitting measurement results in the Tibetan Plateau.The red lines are the results of XKS wave splitting, and the blue lines are the results of Pms wave splitting. The direction of the line represents the polarization direction of the fast wave and the length represents the delay time
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