# 3D inversion of full gravity gradient tensor data in spherical coordinate system using local north-oriented frame

**Part of the following topical collections:**

## Abstract

## Keywords

Gravity gradient tensor Inversion Density distribution Spherical coordinate system Local north-oriented frame## Abbreviations

- GGT
gravity gradient tensor

- SCS
spherical coordinate system

- CCS
Cartesian coordinate system

- SVD
singular value decomposition

- FEM
finite element method

- GSF
geocentric spherical frame

- LNOF
local north-oriented frame

## Introduction

The gravity gradient tensor (GGT) is the second derivative of the gravity potential. Compared to the general gravity field *T*_{ z }, GGT contains nine components and has much higher resolution in inverting the spatial position of target anomaly bodies, which means it will offer more information to better understand the interior structure of the earth or some other planets (Li 2001; Bouman et al. 2016).

In 1886, a torsion balance gradiometer was first developed by Lorand Eotvos, becoming a useful tool for mining and hydrocarbon exploration (Pedersen and Rasmussen 1990; Bell and Hansen 1998). 3D inversion of GGT data was originally introduced by Vasco (1989) and Vasco and Taylor (1991), who focused on the covariance and resolution measures of the solution appraisal. More recently, several algorithms were developed to inverse GGT data (e.g., Li 2001; Zhdanov et al. 2004; Uieda and Barbosa 2012; Oliveira and Barbosa 2013; Martinez et al. 2012; Geng et al. 2015; Meng 2016). The differences among these algorithms are related to the choice of model object functions in the inversion procedure; all the model object functions can be retraced back to the inversion methods used in the inversion of the general gravity field (e.g., Last and Kubik 1983; Guillen and Menichetti 1984; Barbosa and Silva 1994; Li and Oldenburg 1996, 1998; Farquharson 2008).

In addition to the choice of model object functions, there is little agreement on best component of GGT for the inversion. Li (2001) combined five independent components excluding *T*_{ zz }. Zhdanov et al. (2004) used the horizontal components *T*_{ xy } and *T*_{ uv } = (*T*_{ xx } − *T*_{ yy })/2. Martinez et al. (2012) combined the horizontal components and *T*_{ zz }. Capriotti et al. (2015) employed a combination of the GGT and general gravity field *T*_{ z }. Pilkington (2012) used an eigenvalue spectra method to evaluate the utility of combining different GGT components, preferring the *T*_{ zz } component, indicating that the source-model information is improved by adding more components only at close distance to the anomaly sources. Later, Pilkington (2013) used estimated parameter errors from parametric inversions, concluding that the *T*_{ zz } component gave the best performance, while the horizontal components *T*_{ xx } and *T*_{ yy } performed poorly. Paoletti et al. (2016) used a singular value decomposition (SVD) tool to analyze both synthetic data and gradiometer measurements. This research showed that the main factors controlling the reliability of the inversion are algebraic ambiguity (the difference between the number of unknowns and the number of available data points) and signal-to-noise ratio.

All these inversion methods mentioned are implemented in the Cartesian coordinate system (CCS). For small-scale problems such as mining or hydrocarbon exploration on earth, the target area is usually relatively small compared to the radius of the earth and can be considered as a flat surface, so inversion in CCS works fine and obtains reliable inversion results with high accuracy. However, for large-scale inversion problems, such as density imaging of the lunar mascon with the satellite gravity datasets, the target area of the lunar mascon was usually large and covered an area with hundreds or thousands of kilometers in both longitude and latitude directions. Moreover, the radius of the moon was relatively small (1738 km), and this meant the inversion area of the mascon was no longer a flat area; hence, inversion methods cannot ignore the influences of the lunar curvature. To deal with this problem, the inversion method in the SCS must be considered. Liang et al. (2014) extended Li and Oldenburg’s (1996, 1998) inversion method to the SCS using the general gravity field.

In the history of the Moon exploration, one of the most amazing discoveries was the concentrated areas of mass found on the near side of the moon (Muller and Sjogren 1968; Melosh et al. 2013; Freed et al. 2014). These concentrated areas of mass, referred to as mascons, usually have a positive gravity anomaly peak and surrounded by negative gravity anomalies with low geographical elevation. The knowledge of the interior density structure of mascons will help to understand its origin mechanism (Wang et al. 2015; Jansen et al. 2017). There has a significant improvement on lunar gravity field model development (Matsumoto et al. 2010; Yan et al. 2012), and the recent high solution gravity field model GL1500E derived from GRAIL mission (The Planetary Data System 2016) makes it possible to investigate the interior density structure of the mascons (Zuber et al. 2013a, b) using lunar gradient data.

The high-resolution lunar gradient data produced from GRAIL gravity was applied by Andrews-Hanna et al. (2014) to investigate the structure and evolution of the lunar Procellarum region. The fault geometry, thermal structure, and material content were considered to generate rectilinear patterns of the gradient data in this region. A forward modeling method coupling with finite element method (FEM) was employed this work. GGT is the difference of gravity in different directions, which helps to remove the influence of the long-wave part in the lunar gravity, and it is easier to highlight the lunar gravity’s shortwave effect and to get a better resolution for density imaging. In this work, we will focus on inversion of the lunar gradient data, which is different from the previous work (Andrews-Hanna et al. 2013).

The remainder of this paper is as follows: a brief introduction of this inversion method is presented in second section. Third section details two different models and experiments with synthetic GGT datasets and inversion of GGT observation datasets of moon. The interior density structure of the Mare Smythii mascon is discussed in fourth section. Finally, in fifth section we present the conclusions of this study.

## Methodology

### GGT in the spherical coordinate system

*U*in the

*r*,

*λ*, and \(\varphi\) directions of GSF, where

*r*,

*λ*, and \(\varphi\) refer to the radial, longitude, and latitude, respectively (Eq. 1).

*z*has the geocentric radial downward direction,

*x*points to the north, and

*y*is directed to the east with a right-handed system, relationship between the LNOF and GSF can be described as in Eq. (2) (Reed 1973; Petrovskaya and Vershkov 2006).

In this paper, we choose to use LNOF, which will not be singular when calculating GGT components from a gravity spherical harmonics model (Eshagh 2008, 2010) and because the GGT is symmetric and the trace of the GGT equals zero; hence, there are only five independent components.

### Forward modeling

In Eq. (3), *m* and *G*_{ ij } refer to the model and kernel matrix, respectively.

*G*as the linear combination of the five independent components of GGT:

*k*_{ ij } here refers to the weighting factor of each component, and it can be considered as the data accuracies (or the reliabilities) of each component.

Due to the relationship of *T*_{ xx } + *T*_{ yy } + *T*_{ zz } = 0, the linear combination of the components *T*_{ xx } and *T*_{ yy } can be described by the vertical components *T*_{ zz }; hence, we do not employ the components *T*_{ xx } and *T*_{ yy } in Eq. (4).

*d*

_{ s }can be also adopted into the linear combination of the independent components:

*T*

_{ ij }, the error standard deviation is

*σ*

_{ ij }. According to error theory, the error standard deviation of the GGT will be:

In Eq. (6), *Cov* represents the sum of the error covariance of all components. On the assumption that the error of the GGT follows the Gaussian random distribution and one independent component has no connection with each other, then *Cov* = 0.

### Inversion method

In general, because of an insufficient observed dataset, the multiple solutions problem becomes a serious issue for the 3D gravity inversion. To deal with the problem, a suitable model objective function is required.

*m*and

*m*

_{ ref }refer to the recovered and reference model, respectively.

*α*

_{ i }(

*i*=

*s*,

*r*,

*λ*, \(\varphi\)) are length scales, which control the balance of the smoothness versus smallness for the whole model,

*α*

_{ s }for smallness, and

*α*

_{ r },

*α*

_{ λ }, and \(a_{\varphi}\) for smoothness (Oldenburg and Li 2005; Williams 2008). In practice,

*α*

_{ s }usually can be assigned to a value of 1.0 or other suitable value; however, different to those in CCS (Williams 2008),

*α*

_{ λ }, and \(a_{\varphi}\) are variable because of the different tesseroid body sizes along the radial direction.

*w*(

*r*) here represents the depth weighting function, and it can be used to avoid the skin effect in the inversion (Li and Oldenburg 1996; Li 2001). The depth weighting functions match the decay of the gravity or magnetic kernel functions, and they are in proportion to 1/

*r*

^{2}in gravity and 1/

*r*

^{3}in magnetic inversion problem. Without them, the inversion will get results concentrated on the surface of the target area (Li 2001). Unlike the uniform prism cells in CCS, the tesseroid cells become smaller along the radial direction from surface to the core, so it must rescale them into the same level. Liang’s et al. (2014) main contribution is the modification of the depth weighting function in SCS by rescaling the cell volume to the surface (see Additional file 1).

In Eq. (8), *R* is the radius of the reference sphere and *H* is the average height of observed dataset above the reference sphere, while *r*_{0} and *r* are the radial distance of the surface and for computing tesseroid cells, respectively.

In addition, geological and geophysical constraints play an important role in the gravity inversion. The geological and geophysical constraints are varied, and they can be classified into two different kinds: (1) geometry constraints like structure boundaries, orientations, and locations information; (2) physical property constraints such as surface material content and information from drill holes. All these constraints can be described as the function of the physical property and positions. In our inversion method, as we divided the subspace into different tesseroid cells, the constraints become the function of the physical property and index number of the tesseroid cells.

Different from the model objective function, which aims to solve the non-uniqueness in ill-posed inverse problems, the purpose of using a prior geological and geophysical information during the inversion is to improve the inversion result. In this paper, we use the Lagrangian multipliers method, introduced by Zhang et al. (2015), to fit for the different prior geological or geophysical information during the inversion procedure; the additional penalty function of the density bound constraints makes the recovered model more reliable.

## Examples of synthetic GGT data

In this section, we will give two examples of the artificial synthetic model used to validate our inversion method.

### Single model

3D mesh and dataset for inversion

Direction | Inversion range | Model | Data | ||
---|---|---|---|---|---|

Grid size | Grid number | Data size | Data number | ||

Longitude | 30.0°–40.0° | 0.25° | 40 | 0.25° | 41 |

Latitude | 30.0°–40.0° | 0.25° | 40 | 0.25° | 41 |

Depth/elevation | 0–100 km | 5 km | 20 | 0.5 km |

^{3}and covers an area of 33°–37° in both the longitude and latitude directions as well as 1648–1698 km in radial direction. The background density was set to 0 g/cm

^{3}. Figure 2 shows the horizontal slice and vertical profile of the artificial synthetic model used for inversion.

*G*

_{ s }=

*G*

_{ xy }+

*G*

_{ xz }+

*G*

_{ yz }+

*G*

_{ zz }and the GGT dataset

*d*

_{ s }=

*d*

_{ xy }+

*d*

_{ xz }+

*d*

_{ yz }+

*d*

_{ zz }, as shown in Fig. 4c.

^{3}to each inverted cell. The L-curve method (Calvetti et al. 2000) was used to search for the best Tikhonov regularization parameter (Tikhonov and Arsenin 1977), and the recovered model is shown in Fig. 7. Tikhonov regularization parameter here is the trade-off between the model objective function and data objective function (also named data misfit). The Tikhonov regularization parameter we chose is 10, which is located at the corner of L-curve, but slightly offset to the right with a smaller data misfit (Zhang et al. 2015). The black lines in Fig. 7 indicate the boundary of the artificial synthetic model, and the recovered model was fitted well. The recovered model with minimum-structure inversions using

*L*

_{2}-norm measures usually has blurred boundaries, and if sharp boundaries and blocky features are needed, the non-

*L*

_{2}inversions may provide an alternative method (Sun and Li 2014).

### Composite models

^{3}. The residual density of the other model was 0.7 g/cm

^{3}, and its geological setting was 34°–36°, 36°–38°, and 1658–1698 km in latitude and longitude as well as radial direction, respectively. The 3D mesh and dataset settings we used are shown in Table 1. The horizontal slice and vertical profile of the artificial synthetic models are shown in Fig. 8.

^{3}, the recovered model was obtained, as in Fig. 13; the recovered model was well fitted with the blank lines indicating the boundaries of the theoretical models.

Through the artificial theoretical models, we tested our inversion method in the SCS with LNOF. The results indicated that the method is possible to be employed in interior density structure model inversion. In the next section, we will make use of the actual lunar GGT datasets to validate our inversion method.

## Inversion of GGT data at lunar mascon

3D mesh and datasets for the inversion of Mare Smythii

Direction | Inversion range | Model | Data | ||
---|---|---|---|---|---|

Grid size | Grid number | Data size | Data number | ||

Longitude | 76.0°–97.0° | 0.25° | 84 | 0.25° | 85 |

Latitude | − 10.0°–9.0° | 0.25° | 76 | 0.25° | 77 |

Depth/elevation | 0–100 km | 5 km | 20 | 0.5 km |

The spherical harmonic coefficients below degree 6 were removed from the GGT datasets we used, and the gravity signal from the left degrees was assumed to be only affected by the lunar crust. The average density of the lunar crust we use here is generally 2.56 g/cm^{3}, at a range of 2.30–2.90 g/cm^{3} (Wieczorek et al. 2013). This was also considered as the geological constraint during the inverse process. The 3D mesh and datasets for the inversion of the Mare Smythii are described in Table 2.

The gravity gradient reflects the density anomaly; Figs. 16, 17 and 18 shows that there are multi-ring structures (Spudis 1993) at the Mare Smythii site. As the density distribution of the Mare Smythii we extracted through inversion showed some annulus density structures in the shallow stratums and these annulus density structures had the mascon center as the origin point, therefore we infer that there are significant density changes occurred from inside to outside. The formation of these annulus density structures is possibly explained by impacts and crater excavations (Melosh et al. 2013; Montesi 2013). When impacts occur, the kinetic energy is intense and is transformed into heat; this may cause melting and even vaporize the lunar crust, with cracked lunar crust rocks splashing out of the impact basin. After an impact, a rebalancing of the lunar crust and mantle will likely promote an uplifting of the deeper magma to fill in or eject around an impact basin. The density difference as well as the distance of an ejection could be the reason behind the annulus density structures in this area.

*T*

_{s}(Fig. 19a) is similar to the original

*T*

_{s}shown in Fig. 15c and the data residual in Fig. 19b, and the difference between original

*T*

_{s}and recovered

*T*

_{s}also meets our standard deviation expectation of about 5 E. From Fig. 19b, we can see that the residuals inside the Mare Smythii region are close to zero, and it means the good performance of our inversion method. The random big residual values at the verge are caused by the boundary effects.

## Conclusion

An inversion method is fundamental when developing an advanced understanding of the interior structure of planetary geological structures. We presented an effective algorithm that uses full gravity gradient tensor data in spherical coordinate system using local north-oriented frame. In the test case using simulated data, we used two different models, single and composite models. By checking the differences between the simulated and recovered models, we demonstrated the reliability of our method. We also tested the method on observed data from the Mare Smythii mascon area located on the lunar near side and obtained its interior density distribution. This method could also be applied more generally in magnetic data inversion and in exploratory studies of geological structures of large areas.

## Notes

### Authors’ contributions

YZ and JY conceived and designed the experiment; YZ performed the computation; YW analyzed the data; HW interpreted the results; and JAPR and YQ discussed the results and polished the manuscript. YZ and JY wrote the paper, and all the authors improved it. All authors read and approved the final manuscript.

### Acknowledgements

The authors thank Stephen McClure for fruitful and informative discussions.

### Competing interests

The authors declare that they have no competing interests.

### Data and resources

The source codes for this work can be obtained by contacting the corresponding author. Some of the figures were produced using Generic Mapping Tools (GMT).

### Funding

This work is supported by grant of the National Natural Science Foundation of China (41374024, 41704082), Director Foundation of the Institute of Seismology, China Earthquake Administration (IS201616249), Key Laboratory of Geospace Environment and Geodesy, Ministry of Education, Wuhan University (16-01-02), and Hubei Province Natural Science Foundation innovation group Project (2015CFA011).

### Publisher’s Note

Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

## Supplementary material

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