利用多种地震数据联合反演剪切波速度结构的可靠性检测

郑现 赵翠萍 郑斯华

郑现, 赵翠萍, 郑斯华. 2019: 利用多种地震数据联合反演剪切波速度结构的可靠性检测. 地震学报, 41(2): 194-206. doi: 10.11939/jass.20180100
引用本文: 郑现, 赵翠萍, 郑斯华. 2019: 利用多种地震数据联合反演剪切波速度结构的可靠性检测. 地震学报, 41(2): 194-206. doi: 10.11939/jass.20180100
Zheng Xian, Zhao Cuiping, Zheng Sihua. 2019: Reliability tests of shear wave velocity structure from joint inversion of multiple types of seismic data. Acta Seismologica Sinica, 41(2): 194-206. doi: 10.11939/jass.20180100
Citation: Zheng Xian, Zhao Cuiping, Zheng Sihua. 2019: Reliability tests of shear wave velocity structure from joint inversion of multiple types of seismic data. Acta Seismologica Sinica, 41(2): 194-206. doi: 10.11939/jass.20180100

利用多种地震数据联合反演剪切波速度结构的可靠性检测

doi: 10.11939/jass.20180100
基金项目: 国家自然基金青年项目(41704048)和中国地震局地震预测研究所部门任务专项(2018IEF0305)共同资助
详细信息
    通讯作者:

    郑现,e-mail:zhengx@cea-ies.ac.cn

  • 中图分类号: P315.2

Reliability tests of shear wave velocity structure from joint inversion of multiple types of seismic data

  • 摘要: 本文模拟使用青藏高原东南缘区域台网及国家台网的170个宽频台站基于背景噪声、天然地震面波、P波接收函数反演时的实际数据,对青藏高原东南缘假定的初始模型进行恢复,通过计算初始模型台站下方纯路径频散、提取各台站对间的瑞雷波频散曲线、计算理论接收函数以及反演剪切波速度结构来测试使用不同单项数据与联合使用多种数据反演对初始模型的恢复程度。结果表明,同时使用接收函数、基于噪声经验格林函数的群速度、相速度频散以及基于天然地震面波的相速度频散联合反演的剪切波速度结构,充分利用了几种数据的分辨率优势,清晰地分辨出中下地壳及上地幔顶部的低速层。此外,本文也分析了实际数据处理中出现的计算误差、随机噪声干扰对计算结果稳定性的影响。结果显示:对于面波频散,加入1%的误差后,联合反演的结果仍可很好地反映低速层的形态,但是当误差提升至5%后,对最终结果则产生了一定程度的影响;而在接收函数中加入4%的随机噪声时,虽然地幔低速层的上界面和下界面会略微受到随机噪声的影响,但是低速层的深度范围和速度值均得到了较好的恢复。

     

  • 图  1  青藏高原东南缘台站(a)及剪切波速度分布(b)示意图

    Figure  1.  Images of station locations (a) and shear wave velocity (b) in the southeastern margin of the Tibetan Plateau

    图  2  成像分辨率检测试验中各周期实际使用的频散数目

    红色圆点与绿色圆点分别表示基于背景噪声经验格林函数和基于天然地震面波的频散数目;蓝色圆点表示在重叠周期21—60 s内基于两种数据最终提取的频散数目

    Figure  2.  Number of dispersion measurements used in resolution test at each periods

    The red dots and green dots represent the number of dispersion measurements retrieved from empirical Green’s functions based on ambient noise,two-station analysis using teleseismic sur-face wave data,respectively;blue dots represent the number of final dispersion measurements retrieved from the two types of data in the overlapping periods (21−60 s)

    图  3  格点(102°E,25°N)下方的联合反演结果

    (a) 初始模型和由面波频散曲线及接收函数联合反演的输出模型;(b) 根据图(a)中模型计算的P波接收函数;(c) 基于初始模型的瑞雷波相速度、群速度频散曲线

    Figure  3.  Joint inversion results beneath the grid (102°E,25°N)

    (a) The initial model and output model after joint inversion of surface wave dispersion measurements and receiver function; (b) The P wave receiver functions calculated according to the initial models in Fig.(a); (c) Rayleigh wave phase velocity and group velocity dispersion measurements calculated according to the initial model respectively

    图  4  由图1初始模型计算得到的不同周期T瑞雷波的相速度、群速度图像

    Figure  4.  Rayleigh wave phase velocity and group velocity images at different periods T calculated from the initial model shown in Fig.1

    图  5  使用不同数据反演所得沿25°N剖面的剪切波速度结构

    (a) 仅使用基于背景噪声的瑞雷波群速度频散反演;(b) 仅使用基于天然地震面波的瑞雷波相速度频散反演;(c) 同时使用基于背景噪声及天然地震面波的瑞雷波群速度、相速度频散反演;(d) 仅使用接收函数反演;(e) 同时使用3种数据联合反演

    Figure  5.  Cross sections of shear wave velocity structure along 25°N from inversion by using different seismic data

    (a) The output model inverted from Rayleigh wave group velocity dispersions based on ambient noise;(b) The output model inverted from Rayleigh wave phase velocity dispersions based on teleseismic wave;(c) The output model jointly inverted from Rayleigh wave group velocity and phase velocity dispersions based on ambient noise and teleseismic wave;(d) The output model inverted from receiver function;(e) The output model jointly inverted from three types of seismic wave data

    图  6  沿25°N剖面使用不同数据反演后模型与初始模型的速度扰动分布

    (a) 仅使用基于背景噪声的瑞雷波群速度频散反演;(b) 仅使用基于天然地震面波的瑞雷波相速度频散反演;(c) 同时使用基于背景噪声及天然地震面波的瑞雷波群速度、相速度频散反演;(d) 同时使用3种数据联合反演

    Figure  6.  Cross sections of shear wave velocity perturbation along 25°N using different types of seismic data

    (a) Cross sections of shear wave velocity perturbation calculated based on Rayleigh wave group velocity dispersion measurements;(b) Similar to Fig.(a) but calculated based on Rayleigh wave phase velocity dispersion measurements from teleseismic wave;(c) Similar to Fig.(a) but calculated based on both Rayleigh wave group velocity and phase velocity dispersion measurements from ambient noise and tele-seismic wave;(d) Similar to Fig.(a) but calculated based on three types of seismic data

    图  7  初始模型纯路径频散加入1%初始误差后反演的瑞雷波相速度、群速度图像

    Figure  7.  Rayleigh wave phase velocity and group velocity images at different periods by inversion with 1% initial error added to the pure path dispersions based on the the initial model

    图  8  初始模型纯路径频散加入1% (a)和5% (b)初始误差后反演所得到的剪切波速度结构

    Figure  8.  Cross sections of shear wave velocity along 25°N inverted using pure path dispersion measurements with 1% (a) and 5% (b) initial error added to the pure path dispersions based on the the initial model

    图  9  格点(102°E,25°N)下方100组基于加入随机噪声的接收函数联合反演的结果

    (a) 初始模型和联合反演输出模型;(b) 联合反演使用的P波接收函数;(c) 瑞雷波相速度、群速度频散曲线

    Figure  9.  The 100 joint inversion results beneath the grid (102°E, 25°N) based on receiver functions with different random noise

    (a) The initial model and the output models based on joint inversion;(b) The P wave receiver functions used in joint inversions;(c) The Rayleigh wave phase velocity and group velocity dispersion measurements used in joint inversions

    图  10  沿25°N剖面加入随机噪声后反演所获得的剪切波速度图

    Figure  10.  Shear wave velocity image from inversion with random noise along 25°N vertical cross section

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出版历程
  • 收稿日期:  2018-07-18
  • 修回日期:  2018-09-20
  • 网络出版日期:  2019-03-18
  • 刊出日期:  2019-03-01

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