Joint inversion of receiver function, ambient noise dispersion, and Rayleigh wave ZH ratio for the crustal structure beneath the northeastern margin of the Tibetan plateau and its surrounding regions
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摘要:
本文对在青藏高原东北缘及邻近地区架设的571套宽频带流动地震台站记录到的连续波形数据进行处理，通过联合反演P波接收函数、背景噪声频散和Rayleigh波ZH振幅比，获得了研究区高分辨率三维地壳S波速度（VS）结构.研究结果显示，松潘—甘孜块体和西秦岭造山带以及北祁连造山带下方15~40 km的深度范围内存在很显著的S波低速异常体.其中，松潘—甘孜块体和西秦岭造山带下方的低速异常体很可能与部分熔融有关，且造成部分熔融的原因除了剪切加热外，还有可能是软流圈物质上涌和地壳内部的放射生热.而北祁连造山带的低速异常体则可能由地表隆升和地壳增厚所造成.阿拉善块体内部分布有很多不太显著的低速异常体，这可能与阿拉善块体经历了复杂的构造变形有关.在银川—河套地堑下方20~35 km的深度范围内同样观测到了相对不太显著的低速异常体，这更可能与基性岩浆的底侵作用有关.
Abstract:We process the continuous waveform data recorded by 571 broadband temporary seismic stations in the northeastern (NE) margin of the Tibetan plateau and its surrounding regions, and jointly invert the ambient noise dispersion, Rayleigh wave ZH ratio, and P-wave receiver function to obtain high-resolution 3D S-wave velocity structure (VS) of the crust. The results demonstrate that significant low-velocity anomalies of S-wave appear in the depth interval of 15~40 km beneath the Songpan-Garzê block and the western Qinling orogen as well as the northern Qilian orogen. The low-velocity zone below the Songpan-Garzê block and the western Qinling orogen may be related to the crustal partial melting, and the causes of partial melting are not only shear heating but also asthenosphere material upwelling and crustal radioactivity. While that of the northern Qilian orogen may be related to surface uplift and crustal thickening. Many insignificant low-velocity anomalies are observed beneath the Alxa block, which may be related to the complex tectonic deformation of the Alxa block. Relatively insignificant low-velocity anomalies are also observed at the depth interval of 20~35 km beneath the Yinchuan-Hetao graben, which is more likely to be related to the underplating of mafic magmas.
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图 1
(a) 青藏高原东北缘及周边地区的地形与地质单元分布图；(b) 研究所使用的宽频带流动地震台站位置图
Figure 1.
(a) The topography and tectonic sketch map of the NE margin of the Tibetan plateau and surrounding regions; (b) Locations of broad-band temporary seismic stations used in this study
图 2
(a) 周期范围为5~50 s的Rayleigh波相速度频散曲线；(b) 每个周期点Rayleigh波相速度频散曲线条数
Figure 2.
(a) Phase velocity dispersion curves of Rayleigh wave within the period band 5~50 s; (b) Numbers of phase velocity dispersion measurements of Rayleigh wave at each period
图 3
运用L曲线法估计最佳平滑参数和阻尼参数
Figure 3.
L-curve method is used to determine the optimal smoothing parameter and damping parameter
图 4
(a)、(d)和(g)分别表示在10 s、24 s和32 s周期的射线覆盖情况；(b)、(e)和(h)分别表示10 s、24 s和32 s周期的检测板测试恢复结果，其中红色虚线表示最终确定的层析成像范围；(a)、(d)和(g)中的红色圆点和(b)、(e)和(h)中的黑色圆点为研究区内的流动地震台站；(c)、(f)和(i)分别表示10 s、24 s和32 s周期的Vsv分布；(a)—(i)中的蓝色实线和黑色虚线所表示的含义与图 1的相同
Figure 4.
(a), (d) and (g) represent the ray path coverage at 10 s, 24 s and 32 s, respectively. (b), (e) and (h) represent the recovered checkerboard tests at 10 s, 24 s and 32 s, respectively, where red dashed lines enclose the well-resolved range of the final tomography; The red solid dots in (a), (d) and (g) and black solid dots in (b), (e) and (h) denote temporary seismic stations in the study region; (c), (f) and (i) represent the Vsv maps at 10 s, 24 s and 32 s, respectively; The meanings of the blue solid lines and black dashed lines in (a)—(i) are same as those in Fig. 1
图 5
计算接收函数(a)和ZH振幅比(b)所用到的远震事件的震中分布
Figure 5.
Epicentral distribution of teleseismic events for receiver functions (a) and ZH ratio (b) in this study
图 8
(a) 计算深度敏感核所使用的一维速度模型，该模型是由Shen等(2016)的速度模型在本文区范围内进行平均所得；(b) 周期为5 s、20 s、35 s和50 s的Rayleigh波相速度对VS随深度的敏感核函数；(c) 周期为12 s、20 s、30 s和40 s的Rayleigh波ZH振幅比对VS随深度的敏感核函数
Figure 8.
The 1D velocity model used to calculate depth sensitivity is obtained by averaging the velocity model of Shen et al. (2016) in the study region; (b) Depth sensitivity to VS for Rayleigh wave phase velocity at periods of 5 s, 20 s, 35 s, and 50 s; (c) Depth sensitivity to VS for Rayleigh wave ZH ratio at periods of 12 s, 20 s, 30 s, and 40 s
图 9
研究区在20 s和40 s周期的Rayleigh波ZH振幅比(a和c)及误差(b和d)分布图
Figure 9.
Example maps of the Rayleigh wave ZH ratio in the study region at 20 s (a) and 40 s (c) period. Associated uncertainties in ZH ratio are also presented in (b) and (d)
图 12
不同深度绝对VS值的水平分布
Figure 12.
Horizontal variation in the absolute VS at different depths
图 13
沿5条剖面的绝对VS垂直切片，剖面位置如(a)中的黑色虚线所示
Figure 13.
Vertical cross-sections of absolute VS along five profiles, and the position of sections are marked by black dashed lines in (a)
图 14
本文与Wang等(2020)在4 km深度的VS水平异常分布
Figure 14.
Maps of horizontal VS perturbation between ours and Wang et al. (2020)′s results at 4 km depth
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