球坐标系密度界面反演方法及在华南大陆的应用

doi:10.11720/wtyht.2020.0067

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Abstract

The density interface inversion method has been playing an important role in the oil and gas exploration, regional structure inference studies as well as crustal crystal basement surface and Moho undulations researches. Most of the density interface inversion methods are generally based on the Cartesian coordinate system. When large regional or even global scale data are dealt with, the influence of earth curvature cannot be ignored, and the density interface inversion method based on Tesseroid model of spherical coordinate system needs to be considered. However, due to the limitations of calculation accuracy and efficiency, the existing density interface inversion method based on Tesseroid cannot be well applicable to the surface gravity observation data. In this paper, on the basis of previous studies, a density interface inversion method of spherical coordinate system suitable for surface observation data is proposed. Firstly, the gravity Gauss-Legendre integral formula in the spherical coordinate system is simplified to improve the forward calculation efficiency. Then, an optimized adaptive subdivision algorithm is introduced to enhance the calculation accuracy. According to the previous forward calculation and by using Cordell iterative optimization algorithm, the authors propose a density interface inversion method for the surface observation data in the spherical coordinate system. The proposed inversion method in this paper can be verified through the synthetic data test. The inversion results show that the proposed method can overcome the limitation of calculating precision and efficiency of the surface observation data. In addition, the inversion results based on spherical coordinate system are better than those based on cartesian coordinate system. Finally, tests on real data from South China mainland verify the feasibility of the presented methods. The results show that Moho depth rises gradually from the west to the east, with the western part uplifting dramatically and the eastern part uplifting gently. Between Wuling Mountain and Guizhou-Guangxi border, there is an obvious NNE-Moho step.

Key words： gravity spherical coordinate system density interface inversion method Tesseroid South China mainland

Received: 17 February 2020 Published: 26 October 2020

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	Xiang WANG
	Liang-Hui GUO

Cite this article:

Xiang WANG,Liang-Hui GUO. Density interface inversion method in spherical coordinates and its application in the South China mainland[J]. Geophysical and Geochemical Exploration, 2020, 44(5): 1161-1171.

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https://www.wutanyuhuatan.com/EN/10.11720/wtyht.2020.0067 OR https://www.wutanyuhuatan.com/EN/Y2020/V44/I5/1161

The sketch of Tesseroid model

Sketch of discretization of Tesseroid
a—routine discretization shown that the tesseroid had a uniform division. L_φ, L_λ are the dimensions of the tesseroid’s top surface;b—adaptive discretization shown that a fine division of the tesseroid close the computation point and a coarser division further away

The forward model of tesseroid

The flow chart for Cordell iterative approach

The images of spherical shell models
a—inside view of a shell;b—side view of a shell

The gravity anomaly calculated by the Taylor on the different cell size and 2D-GLQ methods based on the different height of observation surface

The improvement of efficiency of computation by using the method of this paper
a—the Briggs logarithm of Er based on the different value of nφ and nλ;b—the changing trend of T₁/T₂ when Er get reduced

The depth of academic interface and its forward result
a—the density interface model graph; b— the gravity anomaly graph of density interface model forward result by the GQL-Plus method of this paper

Figure 8(b)
a—Cartesian coordinates;b—two order Taylor;c—2D-GLQ inversion results; d,e,f—respectively are errors of (a), (b), and (c); g—shown the diagonal section comparisons of (a), (b) and (c);h—depth RMS;i—bouguer RMS
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Comparisons of the inversion results from the data of Figure 8(b)
a—Cartesian coordinates;b—two order Taylor;c—2D-GLQ inversion results; d,e,f—respectively are errors of (a), (b), and (c); g—shown the diagonal section comparisons of (a), (b) and (c);h—depth RMS;i—bouguer RMS

39];g—The difference of (c) and (e)
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Comparisons of the inversion results from measured data in South China
a— The Bouguer anomaly in South China;b—The Moho gravity anomaly in South China by using the low-pass filter;c—The Moho depth in South China by the inversion method of this paper;d—The trend chart of depth RMS;f—The Moho depth in South China^[39];g—The difference of (c) and (e)

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