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Highresolution regional gravity field recovery from Poisson wavelets using heterogeneous observational techniques
Earth, Planets and Space volume 69, Article number: 34 (2017)
Abstract
We adopt Poisson wavelets for regional gravity field recovery using data acquired from various observational techniques; the method combines data of different spatial resolutions and coverage, and various spectral contents and noise levels. For managing the illconditioned system, the performances of the zero and firstorder Tikhonov regularization approaches are investigated. Moreover, a direct approach is proposed to properly combine Global Positioning System (GPS)/leveling data with the gravimetric quasigeoid/geoid, where GPS/leveling data are treated as an additional observation group to form a new functional model. In this manner, the quasigeoid/geoid that fits the local leveling system can be computed in one step, and no postprocessing (e.g., corrector surface or least squares collocation) procedures are needed. As a case study, we model a new reference surface over Hong Kong. The results show solutions with firstorder regularization are better than those obtained from zeroorder regularization, which indicates the former may be more preferable for regional gravity field modeling. The numerical results also demonstrate the gravimetric quasigeoid/geoid and GPS/leveling data can be combined properly using this direct approach, where no systematic errors exist between these two data sets. A comparison with 61 independent GPS/leveling points shows the accuracy of the new geoid, HKGEOID2016, is around 1.1 cm. Further evaluation demonstrates the new geoid has improved significantly compared to the original model, HKGEOID2000, and the standard deviation for the differences between the observed and computed geoidal heights at all GPS/leveling points is reduced from 2.4 to 0.6 cm. Finally, we conclude HKGEOID2016 can be substituted for HKGEOID2000 for engineering purposes and geophysical investigations in Hong Kong.
Background
Highresolution regional gravity field recovery is of considerable importance not only for surveying and mapping, but also for research fields, such as oceanography (understanding ocean circulation and currents), geophysics (investigating the structure of seismic activities and the lithosphere), and geodynamics (Kuroishi 2009; Panet et al. 2011; Shih et al. 2015).
Typically, middle and shortwavelength gravity field signals down to a few kilometers are extracted from highresolution groundbased measurements, e.g., terrestrial and shipborne gravity data, which are only available in geographically limited regions (Wang et al. 2012; Odera and Fukuda 2014; Lieb et al. 2016). In contrast, longwavelength signals from tens of kilometers or larger are often recovered using global geopotential models (GGMs) derived from satellite observations. Over the last 10 years, launches of the Gravity Field and Climate Experiment (GRACE) (Tapley et al. 2004) and Gravity Field and SteadyState Ocean Circulation Explorer (GOCE) (Rummel et al. 2002) missions have greatly contributed to improving the spatial resolution and accuracy of GGMs. Moreover, developing various observational techniques, e.g., GPS, airborne gravimetric measurements, and satellite altimetry missions, can further improve regional gravity fields (Hwang et al. 2006; Jiang and Wang 2016; Wu and Luo 2016). Combined, these data sets form a solid basis for modeling highresolution and highquality regional gravity fields. However, these data have heterogeneous spatial coverage and resolutions, various error characteristics, and different spectral contents, which make their use an open issue. Thus, the aim of this study is to adopt an approach that combines heterogeneous data and extracts different spectral contents from various observational techniques for regional gravity field recovery.
The Stokes/Molodensky integral makes it difficult to combine heterogeneous data, while the least squares collocation (LSC) is numerically inefficient in managing cases that involve a large number of pointwise data (Wittwer 2009). The new gravity field described in this study is parameterized using Poisson wavelets. Poisson wavelets are radially symmetric basis functions that have localizing properties in both the spatial and frequency domains, which have been used extensively in regional gravity field modeling and potential field analysis (Tenzer and Klees 2008; Hayn et al. 2012; Bentel et al. 2013).
We also investigate several aspects that affect the solution quality derived from Poisson wavelets. To begin with, as heterogeneous data have different spatial coverage and resolutions, the derived least squares system from Poisson wavelets is typically illconditioned, where regularization is mandatory for deriving reliable results (Wittwer 2009). One of the key points that affect the quality of regularization is the choice of regularization matrices (Chambodut et al. 2005). Unlike using diagonal regularization matrices in global gravity field modeling from spherical harmonics (Kusche and Klees 2002), the regularization matrices derived from various constraints in regional scale are no longer entirely diagonal. The choice of regularization matrices may affect the solution quality, which is investigated in this study.
Moreover, mainly due to commission errors in the GGMs and uncorrected systematic errors in the data, the computed gravimetric quasigeoid/geoid usually deviates from local values observed from GPS/leveling data by a centimeter level or larger (Wu et al. 2016). Generally speaking, corrector surface (Featherstone 2000; Fotopoulos 2005; Nahavandchi and Soltanpour 2006) or more complicated algorithms, e.g., least squares collocation (Tscherning 1978) and boundaryvalue methodology (Klees and Prutkin 2008; Prutkin and Klees 2008), can be applied to reduce systematic errors and properly combine GPS/leveling data and gravimetric solutions. However, given the difficulty in choosing a proper corrector surface, as well as the associated algorithmic complexity for the leastsquares collocation and boundaryvalue approach, we propose a direct methodology for removing the inconsistency between these two data sets. The GPS/leveling data are treated as an independent observation group and added to the functional model for the gravity field computation. Using this method, the quasigeoid/geoid that fits the local leveling system is computed in one step, no systematic errors exist between the data, and postprocessing procedures, e.g., corrector surface or LSC approaches, for calibrating systematic errors are not required.
The rest of the paper is organized as follows: the main principle of regional gravity modeling from Poisson wavelets is first introduced, and heterogeneous gravityrelated observations are linked to the functional model parameterized by Poisson wavelets. The weights for different observation groups are determined through the variance component estimation (VCE) approach, and unknown coefficients are estimated through the least squares adjustment. Further, the Tikhonov regularization method is introduced to deal with the illconditioned system, where a rapid synthesis method for computing zero and firstorder regularization matrices is provided. In the following section, Hong Kong is selected as the study area and heterogeneous data are introduced. The numerical results are also shown in this part, where the new height reference surface, HKGEOID2016, is determined. In addition, HKGEOID2016 is compared with existing models, e.g., HKGEOID2000 (Luo et al. 2005) and recently published GGMs, such as EIGEN6C4 (European Improved Gravity Model of the Earth by New Techniques 6C4) and EIGEN6C3STAT (Förste et al. 2012, 2014), for crossvalidation. The last section contains the main summary and conclusions.
Methods
Functional model and parameters estimation
Following Holschneider and IglewskaNowak (2004), we denote Ω _{ R } as the sphere of radius R, Ω _{ R } = {(u _{1}, u _{2}, u _{3}): u ^{2}_{1} + u ^{2}_{2} + u ^{2}_{3} = R ^{2}}, and we also denote IntΩ _{ R } as the interior and ExtΩ _{ R } as the exterior:
Consider two points \( \varvec{y} \), \( \varvec{z} \), \( \left \varvec{y} \right < R < \left \varvec{z} \right \), and then the exterior Poisson wavelet of degree d in position \( \varvec{y} \) evaluated at \( \varvec{z} \) is defined by (Holschneider and IglewskaNowak 2004)
where \( \varvec{z = }\left( {z_{1} ,z_{2} ,z_{3} } \right)^{\text{T}} \), \( \varvec{y = }\left( {y_{1} ,y_{2} ,y_{3} } \right)^{\text{T}} \), and \( \varvec{\hat{z} = }\frac{\varvec{z}}{{\left \varvec{z} \right}} \) and \( \hat{y} = \frac{\varvec{y}}{{\left \varvec{y} \right}} \) are the unit vectors of \( \varvec{z} \) and \( \varvec{y} \), respectively. \( P_{l} \left( {\hat{\varvec{z}}^{T} \hat{\varvec{y}}} \right) \) is the Legendre function.
In the framework of removecomputerestore (RCR) methodology, only the residual disturbing potential is parameterized by Poisson wavelets, while the long and shortwavelength parts of the gravity field are recovered using the global geopotential model (GGM) and residual terrain model (RTM), respectively (Omang and Forsberg 2000). Based on the Runge–Krarup theory, the residual disturbing potential, T _{res}, is estimated using a linear combination of Poisson wavelets (Klees et al. 2008):
where \( \varvec{z} \) and \( \varvec{y} \) are interpreted as the 3D coordinates of the observations and position of a Poisson wavelet, respectively. K is the number of Poisson wavelets, β _{ i } is an unknown coefficient, which should be estimated from the data. Moreover, Ω _{ R } is chosen as a sphere that is entirely located within the Earth, e.g., a Bjerhammar sphere. We note that the depth of the Poisson wavelet under the Bjerhammar sphere, computed as \( d = R  \left \varvec{y} \right \), is the key point to determining its property in the frequency domain (Wittwer 2009).
After the linearization and spherical approximation, the residual gravity anomalies, Δg _{res}, can be linked to Poisson wavelets through (Klees et al. 2008)
The computed model, together with the RTM reduction, derives the quasigeoid instead of geoid, and the residual height anomaly, ς_{res}, is derived from Poisson wavelets using the Bruns formula (Heiskanen and Moritz 1967):
where γ is the normal gravity value.
In order to properly combine the gravimetric quasigeoid/geoid and GPS/leveling data, parts of the GPS/leveling data, ς ^{p}_{res} , are treated as observations, which are added in the functional model for the regional gravity field computation:
where η is the 7parameter model, which is used to absorb systematic errors between these two data sets, and χ is a vector of unknown parameters. More specifically, η and χ are expressed as (Eshagh and Zoghi 2016)
where φ and λ are the latitude and longitude of the GPS/leveling data, e is the second eccentricity of the reference ellipsoid.
Typically, observations \( \varvec{l}_{p} \) in group p are linked to the residual disturbing potential \( T_{\text{res}} \left( \varvec{z} \right) \) through
where \( \varvec{\varDelta}_{p} \) are observation errors, b _{ p } is an unknown bias parameter, \( \varvec{L}_{p} \) is the specific function linking observations to the residual disturbing potential, J is the number of observation groups.
Assuming that the observation noise is white Gaussian with zero mean, Eq. (8) is rewritten as
where \( \varvec{x} \) is the K′ × 1 vector of unknown coefficients, which consists of unknown parameters of Poisson wavelets and bias parameters. For example, \( \varvec{x} = \left[ {\beta_{1} ,\beta_{2} , \ldots ,\beta_{K} ,b_{1} ,b_{2} , \ldots ,b_{J} } \right]^{\prime } \) and K′ = K + J, \( \varvec{A}_{p} \) is the m _{ p } × K′ design matrix of group p, \( \varvec{l}_{p} \) is the m _{ p } × 1 corresponding observation vector, \( \varvec{e}_{p} \) is the m _{ p } × 1 vector of corresponding stochastic errors, and m _{ p } is the number of observations in group p. E{·} and D{·} are the expectation and dispersion operators, respectively. \( \varvec{C}_{p} \) is the error variance–covariance matrix of group p, and σ ^{2}_{ p } and \( \varvec{Q}_{p} \) are the variance factor and cofactor matrix, respectively.
The observations in different groups are assumed to be uncorrelated, and the error variance–covariance matrix of all observation groups is expressed as
Pointwise data can be directly linked to Poisson wavelets through the functional model described above. However, as these data are not homogeneously distributed and data gaps may exist in locally, the associated least squares system is typically illconditioned, and regularization is mandatory (Wittwer 2009). Usually, the Tikhonov regularization method is applied for tackling the illconditioned issues, because it does not need a priori information (Xu 1992). For a given α (regularization parameter) and κ (regularization matrix), the leastsquares solution of Eq. (9) is (Klees et al. 2008)
The widely used Lcurve approach, which is the log–log scale plot of the residual norm versus solution norm, is used to estimate the regularization parameter in this study. For discrete illconditioned problems, this plot displays an ‘Lshape’ with a corner point, where a certain balance between the regularized solution and fit to the data is achieved (Hansen et al. 2007). Moreover, the variance component estimation (VCE) approach can be applied to determine the optimal variance factors of different observation groups (Koch and Kusche 2002; Kusche 2003):
where \( \varvec{v}_{p} = \varvec{A}_{p} \hat{\varvec{x}}  \varvec{l}_{p} \) is the vector of residuals for group p and r _{ p } is the corresponding redundancy number. The estimation of the variance factor is iteratively computed until convergence is achieved.
The final quasigeoid, ς, is computed by combining the residual part with the long and shortwavelength components derived from the GGM (ς_{GGM}) and RTM (ς_{RTM}), respectively (Omang and Forsberg 2000):
However, the geoid (N) instead of a quasigeoid is needed in some cases, where their relationship is described by
where \( \bar{g} \) and \( \bar{\gamma } \) are the mean value of gravity and normal gravity, respectively, Δg _{ B } is the Bouguer anomaly, and h is topographical height.
Choice of regularization matrix
The regularization matrix is the key element controlling the quality of the regularized solutions, which describes the signal energy decreasing from large to small scale (Chambodut et al. 2005). For selecting the optimal regularization matrix, the zero and firstorder regularization matrices are investigated.
Zeroorder Tikhonov regularization
With the addition theorem of spherical harmonics, the Poisson wavelets are rewritten as (Wittwer 2009)
where \( \bar{Y}_{lm} \) are the fully normalized spherical harmonics, l and m are their degree and order, respectively.
If we assume Poisson wavelets are the target functions on the sphere, i.e., \( s = W_{\varvec{y}}^{{{\text{ext}},d}} (\varvec{z}) \), then the entries of the zeroorder regularization matrix κ ^{0}_{ P,Q } are expressed as the inner product of different Poisson wavelets (Heiskanen and Moritz 1967):
Equation (16) is also rapidly synthesized by Holschneider and IglewskaNowak (2004)
where \( \varvec{y}_{P}^{*} = \frac{{R^{2} }}{{\left {\varvec{y}_{P} } \right^{2} }}\varvec{y}_{P} \) and \( \varvec{y}_{Q}^{*} = \frac{{R^{2} }}{{\left {\varvec{y}_{Q} } \right^{2} }}\varvec{y}_{Q} \).
Firstorder Tikhonov regularization
The zeroorder Tikhonov regularization derived above is suitable for functions restricted to a sphere σ _{U} belonging to L _{2}(σ _{U}). However, this function space is quite large and includes many unsmooth functions. To introduce a scalar product suitable for smoother functions, a target function is selected as the firstorder derivative of the Poisson wavelets, and the inner products of the target functions are used to derive the entries of the firstorder regularization matrix.
Assuming the target function is a firstorder radial derivative of the Poisson wavelets, the entries of the radially constrained regularization matrix κ ^{r}_{ P,Q } are (Heiskanen and Moritz 1967)
As \( \frac{\partial }{{\partial \left \varvec{z} \right}}\psi_{l} =  \frac{l + 1}{{\left \varvec{z} \right}}\psi_{l} \), in Eqs. (15), (18) is rewritten as
According to Holschneider and IglewskaNowak (2004), κ ^{r}_{ P, Q } is rapidly computed as
Similarly, the entries of the horizontal constrained regularization matrix R ^{h}_{ P,Q } read
Results and discussion
Study area and data
The study area is bounded by 113.83° to 114.5° in longitude and from 22.15° to 22.58° in latitude, as shown in the region enclosed in a black rectangle in Fig. 1, which covers the entire Hong Kong mainland, parts of Shenzhen, as well as the South China Sea. Figure 1 also shows the distribution of heterogeneous gravity data; the red dots represent terrestrial data, including measurements both in Hong Kong and parts of Shenzhen. The green dots indicate locations of shipborne data coverage, which are sparsely distributed. As a result, we also incorporate satellite altimetryderived gravity data to fill these data gaps, indicated with yellow dots, obtained from DTU13 (DTU = Technical University of Denmark) that uses multisatellite altimetry data (e.g., TOPEX/Poseidon, Jason1, Jason2, ERS2) over 20 years. DTU13 has a spatial resolution of 1′ × 1′, and the altimetry gravity data precision is approximately several mGal globally (Andersen et al. 2013). We note that even the terrestrial data are not homogeneously distributed and data gaps exist, especially for mainland Hong Kong. This makes the study area a good location to test the feasibility of our adopted approach for managing data gaps. Because the currently used leveling system, Hong Kong Principal Datum (HKPD) over Hong Kong, is an orthometric height system (Chen and Luo 2004), the modeled quasigeoid from Eq. (13) is converted to a geoid for further validation and comparison.
Global geopotential model and digital terrain model
Earth Gravity Model 2008 (EGM2008) with a full degree and order (d/o) of 2190 (Pavlis et al. 2008, 2012) is chosen to recover longwavelength signals of the regional gravity field. EGM2008 was developed by combining satellite gravity observations, groundbased gravity measurements and radar altimetry data; the accuracy of EGM2008 is 0.239 m when compared to globally distributed GPS/leveling data, which is one of the most accurate GGMs published in the recent years http://icgem.gfzpotsdam.de/ICGEM/evaluation/evaluation.html. A highresolution and highquality DTM (digital terrain model) is needed for applying RTM corrections to smooth the regional gravity field at short scales (Forsberg and Tscherning 1981). Two data sources, SRTM (Shuttle Radar Topography Mission) and GEBCO (General Bathymetric Chart of the Oceans), are combined to generate a DTM with a spatial resolution of three arcseconds over land and sea. In order to reduce edge effects, a larger RTM computational area than study region is need; the derived DTM is shown in Fig. 2a. The mean elevation surface (MES) used in the RTM is computed from a highorder spherical harmonic expansion of Earth’s topography, the DTM2006.0 topography model (Pavlis et al. 2007, 2008). The truncated degree of DTM2006.0 is consistent with the GGM used in this study, EGM2008 with a full d/o of 2190. The derived mean elevation surface is shown as Fig. 2b. Considering the curvature of Earth, tesseroids instead of prisms are chosen as the integral elements (Heck and Seitz 2007). The density parameter is selected as ρ _{land} = 2.67 g/cm^{3} and ρ _{sea} = 1.64 g/cm^{3} given the difference between the mean crustal density and seawater (Forsberg 1984). We also show detailed topographical information over Hong Kong (Fig. 3).
GPS/leveling data
There are 168 highquality GPS stations in Hong Kong, the ellipsoidal heights are referenced to the WGS84 ellipsoid (ITRF 96 @ 1998:121), and their heights were determined with precise geometric leveling and trigonometric leveling. The entire GPS/leveling dataset is divided into three groups (Fig. 4). The leveling heights of GPS/leveling data in the first group were derived from precise leveling measurement, while the heights of the next two groups were surveyed from precise leveling and trigonometric height measurements. Based on recent leveling network adjustments, the accuracy of the overall GPS/leveling data is approximately 1 cm. The first two groups, i.e., group I (58 points) and II (49 points), are used as observations, aimed at reducing inconsistency between the gravimetric solution and GPS/leveling data. The third group (61 points), group III, is applied to evaluating the quality of the computed model.
Gravity data
The original gravity database in Hong Kong has 507 terrestrial and 133 shipborne pointwise gravity observations, the spacing on land is 2 and 2–4 km at sea. They were collected using a Lacoste and Romberg model ‘G’ land gravity meter and model ‘H/U’ seabed gravity meter from Electronic and Geophysical Services Ltd (Luo et al. 2005). The local gravity base is connected to International Gravity Standardization Net 1971 (IGSN 71) with an accuracy of 0.03 mGal (Evans 1990). Moreover, recent gravity measurements also provide 623 discrete terrestrial gravity observations. The heights of gravity data in Hong Kong are referenced to the Hong Kong Principal Datum. In addition, gravity measurements in the neighboring Shenzhen region are also available, 1312 points on land and 876 points at sea, with 1 km spatial resolution. They were measured with a Lacoste & Romberg model ‘G’ and ‘D’ land gravimeter and model ‘S’ sea gravimeter in 2001, and the accuracy of observed data is better than 0.1 mGal. The heights of gravity measurements over Shenzhen are referenced to the National Vertical Datum 1956 (Chen and Luo 2004). Further, due to poor coverage of the marine gravity observations, DTU13derived altimetry gravity anomalies are also introduced. The DTU13 model uses the EGM2008derived geoid as the vertical datum (Andersen et al. 2013). To unify these heterogeneous gravity data from various sources, transforming parameters are used for height datum unification, and the heights of gravity data from Shenzhen and the DTU13 model are unified to the local heights based on the Hong Kong Principal Datum. To quantify the DTU13 model quality in the target region, DTU13derived gravity anomalies are compared with marine gravity data (Fig. 5). The comparison indicates large differences in the coastal areas, where the quality of the altimetry data is suspect (Hwang et al. 2006). The statistics in Table 1 show the accuracy of the DTU13 model for the seas around Hong Kong is approximately 4.3 mGal. The bias of the DTU13 model versus marine gravity data is at the level of 4.8 mGal, which needs to be estimated as unknown bias parameters in the functional model, as shown in Eq. (8). The imperfection in height transforming parameters and uncorrected systematic errors in the data may result in unreduced biases in the data after height unification. Thus, except for the terrestrial gravity data over Hong Kong, terrestrial data in Shenzhen and all shipborne and altimetry data are supposed to have biases. For data derived from specific source, we assume a constant bias parameter in the functional model, and three bias parameters in total are estimated using the least square adjustment.
Based on RCR methodology, residual gravity data are computed by subtracting the long and shortwavelength parts from the original observations. Figure 6 shows the residual gravity data, where (a) and (d) represent the residual terrestrial data, (b) and (e) display the residual marine data, and (c) and (f) show the residual altimetry data. The top panels, (a), (b) and (c), show the residual observations obtained by only subtracting EGM2008derived quantities from the original data. The bottom panels, (d), (e) and (f), demonstrate the residual data derived by subtracting EGM2008derived quantities and RTM corrections. After incorporating RTM corrections, the residual gravity field is much smoother, and the most significant improvements are found southeast of Shenzhen, in New Territory, Lan Tau and Hong Kong land, regions with a tendency toward topographical variation (Fig. 3). As shown in Table 2, the standard deviation (SD) of the residual terrestrial data is reduced from 11.9 to 4.4 mGal, with approximately 63% improvement after incorporating the RTM reductions. For marine data, the improvement is not as much as the terrestrial data, the SD of shipborne data is only reduced from 7.2 to 6.0 mGal, mainly due to the low resolution of the bathymetry model, the GECBO model has a spatial resolution of 30″ × 30″, and the small variation in local bathymetry (Fig. 3). Similarly, the SD of altimetry data is only reduced from 2.3 to 1.4 mGal with RTM reductions.
Numerical results
Determination the regularization matrix and regularization parameter
We put the Poisson wavelets on a Fibonacci grid beneath the topography, keeping it parallel with the topography (Tenzer et al. 2012). However, as mentioned above, data gaps in the observations usually lead to an illconditioned least squares system. Thus, before computing a highquality model, the reliability of the Lcurve approach and performances of various regularization matrices need to be evaluated. The numerical experiment is designed as follows, the grid depth is selected as 40 km, and the number of Poisson wavelets is approximately chosen as 1600. Terrestrial, shipboard and altimetry gravity data, as well as the two groups of GPS/leveling data (i.e., group I and II), are combined for modeling. The normal matrix with this parameterization is highly illconditioned, which is the proper case study for investigating the performances of the Tikhonov regularization technique. Figure 7 shows Lcurve plots for various regularization matrices, where the optimal regularization parameter is between 10^{−11} and 10^{−10} when zeroorder regularization is applied. For the firstorder regularization, both for the radial and horizontal constrained matrices, the optimal parameter is situated between 10^{−12} and 10^{−11}. To further demonstrate the Lcurve corner, the regularization parameters are densified around the intervals where optimal parameters are located (red circles in Fig. 7); the corresponding information can be found in Tables 3 and 4. The estimated optimal regularization parameters for zero and firstorder regularization matrices are α = 10^{−10.6} and α = 10^{−11.3}, respectively. However, the Lcurve method may lead to obtain an oversmoothed solution (Xu 1998). Therefore, we also provide the quality of various solutions using an external validation from the GPS/leveling data from group III, (Tables 3, 4). These results indicate that the optimal parameters estimated from the Lcurve method are consistent with the direct evaluation results, suggesting the Lcurve method in this study is reliable. In addition, there are no differences in the performances of different firstorder regularization matrices, i.e., the radial and horizontal constrained matrices, and thus we do not distinguish these matrices in the following discussion. However, when comparing the quality of solutions derived from zero and firstorder regularization, we conclude the application of firstorder regularization produces better results, and the accuracy of the corresponding model reaches 1.6 cm. In comparison, for solutions computed from zeroorder regularization, the accuracy decreases to 1.8 cm. These results show the choice of regularization matrices has a nonnegligible effect on the solutions, and the firstorder regularization may be more preferable for local gravity field modeling.
Optimal network design for Poisson wavelets
Another key point affecting the final solution quality is the network design of the Poisson wavelets, where the optimal depth and number of Poisson wavelets need to be carefully estimated (Wu et al. 2016). The depth should not be chosen too shallow, which may lead to overfitting problem. However, too deep Poisson wavelets may cause a heavily illconditioned normal matrix, where strong regularization is need, and the associated regularization errors may corrupt the solution. A good depth choice should be a tradeoff between data fit and smoothness of the solution (Slobbe 2013). In addition to depth, the number of Poisson wavelets also affects the stability and the quality of the solution. To obtain the optimal network design, we use a trialanderror approach, i.e., preselected depths and number of Poisson wavelets are combined to form various networks; based on these networks, different solutions are computed. For selecting the best solution, GPS/leveling points serve as evaluation data, where the combination of the depth and number that obtains the best fit to the evaluation data is the optimal parameterization. Through trial and error, the depth of the grid was found to increase from 10 to 40 km with an interval of 5 km, and the number of Poisson wavelets in the computational domain changed from 400 to 2000 with an increment of 400. Similar to the case study designed in the previous section, the first two GPS/leveling groups, together with the heterogeneous gravity data, are incorporated for gravity field modeling. The third group of GPS/leveling serves as evaluation data for validating the different solutions. Finally, the Lcurve approach with firstorder Tikhonov regularization is applied for managing the illconditioned system. Figure 8 shows the quality of the different models parameterized using various networks, where a minimum SD of 1.1 cm is obtained when the depth is 10 km and the number is 1600. Adding more Poisson wavelets only increases the computational load, without gaining improvement, e.g., the accuracy of the geoid decreases to 1.2 cm when the depth is unchanged, but the number increases to 2000. We also note that there are other choices that provide slightly worse solutions with a SD value a few millimeters larger than 1.1 cm, which indicates the solution is quite robust with respect to minor changes in network parameterization.
A new height reference surface over Hong Kong
Based on the optimal network designed above, a new height reference surface, HKGEOID2016, over Hong Kong is estimated. Figure 9 provides the estimated biases for the gravity data, with magnitudes of −0.6, −0.7 and −4.5 mGal for terrestrial, shipborne and altimetry data, respectively. However, the estimated bias in the altimetry data is not exactly consistent with the results shown in Table 1, where the bias between shipborne measurements and altimetry data is roughly −4.8 mGal. This also indicates the biases estimated from the functional model parameterized in this study may deviate from the true value, and additional efforts are needed for further improvements in the near future. Figure 10 displays the residuals of the gravity observations after the least squares adjustment. As shown in Table 5, the functional model fits the terrestrial and marine data much better than the altimetry data, and the SD of the residuals for terrestrial and marine data is approximately 1.2 and 1.1 mGal, respectively, while for altimetry data this value significantly increases to 4.8 mGal. In addition, the most prominent residuals in the altimetry data are located at coastal areas, which further demonstrates the poor DTU13 quality over these regions. Moreover, we conclude that the parameterization of the functional model with constant unknown bias parameters does not thoroughly remove systematic errors in the data. Future work should also incorporate densification of shipborne gravity measurements, which may further improve the solution quality over marine areas. Further, for the two groups of GPS/leveling data used to combine the gravimetric solution and GPS/leveling data, i.e., groups I and II, the residuals are displayed in Fig. 11, and the corresponding statistics are provided in Table 6. These results show the internal agreement between the model and GPS/leveling data. For comparison, we also provide results derived from the purely gravimetric geoid, i.e., the solution modeled only from gravity data using Poisson wavelets. The corresponding results display differences between the purely gravimetric solution and GPS/leveling data at the decimeter level, ranging from 6.7 to 22.3 cm. SD values are 4.1 and 3.6 cm, and mean values are 15.1 and 15.4 cm for groups I and II, respectively. These statistics indicate systematic errors exist between these two data sets. Because the GPS/leveling data are acquired using highquality GPS measurements and spirit leveling observations, it is usually hypothesized that errors in the computed gravimetric model primarily account for the observed systematic errors; these are usually due to commission errors in the GGM, as well as uncorrected systematic errors in the data. However, as shown in Table 6, the incorporation of two groups of GPS/leveling data leads to a significant reduction in SD values for differences between the modeled geoid heights and observed ones, to 0.2 and 0.3 cm for groups I and II, respectively. More important, introducing these GPS/leveling data substantially reduces the mean difference between the model and GPS/leveling data. The zero mean values for both groups of data also indicate that the gravimetric model and GPS/leveling data can be properly combined through the direct approach we proposed. Furthermore, systematic errors, especially in the computed model, have been significantly reduced when compared to the case derived from a purely gravimetric solution.
Results from the GPS/leveling data for groups I and II only provide the internal agreement between the modeled geoid and GPS/leveling data, and cannot be used for assessing the solution quality because they are used as observations for modeling. Thus, the third group of GPS/leveling data, with independent 61 pointwise measurements, is used for external validation and the result is displayed in Fig. 12. All residuals are within 2.0 cm (Table 7), the SD of the differences between the HKGEOID2016 and GPS/leveling points is approximately 1.1 cm, and the zero mean value also confirms the geoid model and GPS/leveling data have been combined properly. For further evaluation, we also compare HKGEOID2016 with the existing model, HKGEOID2000 (Luo et al. 2005). Figure 13 shows the differences between the observed and computed geoidal heights at all GPS/leveling points based on the various geoids. Compared to the solution derived from HKGEOID2000, as shown in the Table 8, the SD of these differences is reduced from 2.4 to 0.6 cm when HKGEOID2016 is incorporated. We mainly attribute these improvements to the incorporation of more gravityrelated observations, as well as recent leveling network adjustments to reduce the systematic errors in the leveling system over Hong Kong. We also note that the mean value of the residuals is 0.8 cm when HKGEOID2000 is used, which indicates systematic errors may exist in the original GPS/leveling data used by Luo et al. (2005).
The performances of the recently published GGMs are also investigated in Hong Kong, i.e., EGM2008 with d/o 2190 (Pavlis et al. 2012), EIGEN6C3STAT (d/o 1949) and EIGEN6C4 (d/o 2190) (Förste et al. 2012, 2014) (Fig. 14). The statistics in Table 9 show the accuracy of these GGMs is not better than 4 cm, and the mean deviation between GGM and local geoid is larger than 17 cm, which is undesirable for engineering purposes or geophysical investigation. The main reason for the poor performances of these GGMs is their development was implemented without confidential gravity data from China, and the quality of these models in regions such as China is suspect, and local refinements are necessary. Moreover, differences between the HKGEOID2016 and GGMderived geoids are shown in Fig. 15, these differences are at the decimeter level, and the incorporation of locally distributed data primarily contributes to improving the fine structures of the regional gravity field at short scales.
Conclusions
Poisson wavelets are used for modeling the regional gravity field using data from various observational techniques. The method combines data with different spatial coverage, various noise levels, and spectral contents. As a case study, terrestrial, shipborne, and satellite altimetry gravity data, as well as GPS/leveling measurements, are incorporated in the Poisson wavelet model for regional gravity field recovery over Hong Kong.
The Tikhonov regularization is introduced to manage the illconditioned least squares system; in particular, the performances of various regularization matrices are investigated. The numerical results show solutions with firstorder regularization provide better results, where the accuracy of the local solution increases by 0.2 cm compared to that obtained from zeroorder regularization. These results also indicate that firstorder regularization may be more preferable in regional gravity field recovery using Poisson wavelets. Moreover, a direct approach is proposed to properly combine the gravimetric quasigeoid/geoid and GPS/leveling data; a subset of the GPS/leveling data is treated as an independent observation group to formulate the new functional model, and the quasigeoid/geoid that fits the local leveling system can be modeled in a single step. The results show the SD is approximately 0.3 cm for the residuals on the first two GPS/leveling groups, regarded as observations. The zero mean value indicates the gravimetric model and GPS/leveling data can be properly combined through this direct approach. In addition, an external validation with 61 independent GPS/leveling points shows that the accuracy of the new geoid, HKGEOID2016, is approximately 1.1 cm. Compared with the original solution, HKGEOID2000, the SD of the differences between observed and computed geoidal heights at all GPS/leveling points is reduced from 2.4 to 0.6 cm when HKGEOID2016 is incorporated. This is a significant improvement. In addition, the performances of three recently published GGMs, EGM2008, EIGEN6C3STAT and EIGEN6C4, are investigated in Hong Kong. The corresponding results show the accuracies of these GGMs are all below 4 cm. The deviation from the local geoid at the decimeter level also indicates the GGM alone cannot recover a highquality gravity field in this region, and local refinement is necessary.
Several issues should be carefully considered to make further improvements to the local geoid. Usually, the geoid is poorly modeled in the coastal areas due to unfavorable data coverage (Hipkin et al. 2004; Filmer and Featherstone 2012). In the study region, the distribution of shipborne data is quite sparse, and the quality of the altimetry data degrades in the vicinity of coastal areas. Therefore, the densification of shipborne data would further improve the local geoid in future work. In addition, the developments of appropriate altimeter waveform retracking approaches may also contribute to improving the geoid over coastal areas (Hwang et al. 2006; Andersen and Knudsen 2009). Errors in the GGM inevitably propagate into regional solutions because we usually consider the GGM as errorfree data implemented in the removerestore framework. The magnitude of these commission errors in the GGMs reaches the centimeter scale or larger (Pavlis et al. 2012), which should be carefully considered when computing the quasigeoid/geoid at centimeter accuracy. These commission errors are actually calibrated with GPS/leveling data using the direct approach proposed in this study. However, the errors in the GGM could also be quantified if the full error variance–covariance matrix of the spherical coefficients is known, and a more realistic error variance–covariance matrix of the data could be estimated through error propagation. In this manner, the weights of different observation groups may be more properly determined, and the accuracy of the quasigeoid/geoid, especially for the purely gravimetric one, may be further improved.
Abbreviations
 GPS:

Global Positioning System
 GGM:

global geopotential model
 GRACE:

Gravity Field and Climate Experiment
 GOCE:

Gravity Field and SteadyState Ocean Circulation Explorer
 LSC:

least squares collocation
 VCE:

variance component estimation
 EIGEN:

European Improved Gravity Model of the Earth by New Techniques
 RCR:

removecomputerestore
 RTM:

residual terrain model
 3D:

three dimensional
 DTU:

Technical University of Denmark
 d/o:

degree and order
 DTM:

digital terrain model
 SRTM:

Shuttle Radar Topography Mission
 GEBCO:

General Bathymetric Chart of the Oceans
 MES:

mean elevation surface
References
Andersen OB, Knudsen P (2009) The DNSC08 mean sea surface and mean dynamic topography. J Geophys Res 114(C11):327–343. doi:10.1029/2008JC005179
Andersen OB, Knudsen P, Stenseng L (2013) The DTU13 global mean sea surface from 20 years of satellite altimetry. In: OSTST Meeting, Boulder, Colo
Bentel K, Schmidt M, Gerlach C (2013) Different radial basis functions and their applicability for regional gravity field representation on the sphere. Int J Geomath 4(1):67–96. doi:10.1007/s1313701200461
Chambodut A, Panet I, Mandea M, Diament M, Holschneider M, Jamet O (2005) Wavelet frames: an alternative to spherical harmonic representation of potential fields. Geophys J Int 163(3):875–899. doi:10.1111/j.1365246X.2005.02754.x
Chen Y, Luo Z (2004) A hybrid method to determine a local geoid modelCase study. Earth Planets Space 56(4):419–427. doi:10.1186/BF03352495
Eshagh M, Zoghi S (2016) Local error calibration of EGM08 geoid using GNSS/levelling data. J Appl Geophys 130(5):209–217. doi:10.1016/j.jappgeo.2016.05.002
Evans RB (1990) Hong Kong gravity observations in July 1990 with BGS Lacoste and Romberg meter No. 97 and international connections to IGSN 71. Report, British and Geology Survey, Hong Kong, China
Featherstone WE (2000) Refinement of a gravimetric geoid using GNSS and levelling data. J Surv Eng 126(2):27–56. doi:10.1061/(ASCE)07339453(2000)126:2(27)
Filmer MS, Featherstone WE (2012) A reevaluation of the offset in the Australian Height Datum between mainland Australia and Tasmania. Mar Geod 35(1):107–119. doi:10.1080/01490419.2011.634961
Forsberg R (1984) A study of terrain reductions, density anomalies and geophysical inversion methods in gravity field modeling. Report No. 355, Department of Geodetic Science and Surveying, The Ohio State University, Columbus, Ohio, USA
Forsberg R, Tscherning CC (1981) The use of height data in gravity field approximation by collocation. J Geophys Res 86(B9):7843–7854
Förste C, Bruinsma SL, Flechtner F, Marty JC, Lemoine JM, Dahle C, Abrikosov O, Neumayer KH, Biancale R, Barthelmes F, Balmino G (2012) A preliminary update of the Direct approach GOCE Processing and a new release of EIGEN6C. AGU General Assembly, San Francisco
Förste C, Bruinsma SL, Abrikosov O, Lemoine JM, Schaller T, Götze HJ, Ebbing J, Marty JC, Flechtner F, Balmino G, Biancale R (2014) EIGEN6C4 The latest combined global gravity field model including GOCE data up to degree and order 2190 of GFZ Potsdam and GRGS Toulouse. The 5th GOCE User Workshop, Paris, France
Fotopoulos G (2005) Calibration of geoid error models via a combined adjustment of ellipsoidal, orthometric and gravimetric geoid height data. J Geod 79(1):111–123. doi:10.1007/s001900050449y
Hansen PC, Jensen TK, Rodriguez G (2007) An adaptive pruning algorithm for the discrete Lcurve criterion. J Comput Appl Math 198(2):483–492. doi:10.1016/j.cam.2005.09.026
Hayn M, Panet I, Diament M, Holschneider M, Mandea M, Davaille A (2012) Waveletbased directional analysis of the gravity field: evidence for largescale undulations. Geophys J Int 189(3):1430–1456. doi:10.1111/j.1365246X.2012.05455.x
Heck B, Seitz K (2007) A comparison of the tesseroid, prism and pointmass approaches for mass reductions in gravity field modelling. J Geod 81(2):121–136. doi:10.1007/s0019000600940
Heiskanen WA, Moritz H (1967) Physical geodesy. WH Freeman and Co., San Francisco
Hipkin RG, Haines K, Beggan C, Bingley R, Hernandez F, Holt J, Baker T (2004) The geoid EDIN2000 and mean sea surface topography around the British Isles. Geophys J Int 157(2):565–577. doi:10.1111/j.1365246X.2004.01989.x
Holschneider M, IglewskaNowak I (2004) Poisson wavelets on the sphere. J Fourier Anal Appl 13(4):405–419. doi:10.1007/s0004100669099
Hwang C, Guo J, Deng X, Hsu H, Liu Y (2006) Coastal gravity anomalies from retracked geosat/GM altimetry: improvement, limitation and the role of airborne gravity data. J Geod 80(4):204–216. doi:10.1007/s001900060052x
Jiang T, Wang YM (2016) On the spectral combination of satellite gravity model, terrestrial and airborne gravity data for local gravimetric geoid computation. J Geod. doi:10.1007/s0019001609327
Klees R, Prutkin I (2008) The combination of GNSSlevelling data and gravimetric (quasi) geoid heights in the presence of noise. J Geod 84(12):731–749. doi:10.1007/s0019001004062
Klees R, Tenzer R, Prutkin I, Wittwer T (2008) A datadriven approach to local gravity field modelling using spherical radial basis functions. J Geod 82(8):457–471. doi:10.1007/s0019000701963
Koch KR, Kusche J (2002) Regularization of geopotential determination from satellite data by variance components. J Geod 76(5):259–268. doi:10.1007/s001900020245x
Kuroishi Y (2009) Improved geoid model determination for Japan from GRACE and a regional gravity field model. Earth Planets Space 61(7):807–813. doi:10.1186/BF03353191
Kusche J (2003) A MonteCarlo technique for weight estimation in satellite geodesy. J Geod 76(11):641–652. doi:10.1007/s0019000203025
Kusche J, Klees R (2002) Regularization of gravity field estimation from satellite gravity gradients. J Geod 76(6):359–368. doi:10.1007/s0019000202576
Lieb V, Schmidt M, Dettmering D, Börger K (2016) Combination of various observation techniques for regional modeling of the gravity field. J Geophys Res Solid Earth 121(5):3825–3845. doi:10.1002/2015JB012586
Luo Z, Ning J, Chen Y, Yang Z (2005) High precision geoid models HKGEOID2000 for Hong Kong and SZGEOID2000 for Shenzhen, China. Mar Geod 28(2):191–200. doi:10.1080/01490410590953758
Nahavandchi N, Soltanpour A (2006) Improved determination of heights using a conversion surface by combining gravimetric quasigeoid/geoid and GNSSlevelling height differences. Stud Geophys Geod 50(2):165–180. doi:10.1007/s1120000600103
Odera PA, Fukuda Y (2014) Improvement of the geoid model over Japan using integral formulae and combination of GGMs. Earth Planets Space 66(1):1–7. doi:10.1186/188059816622
Omang OCD, Forsberg R (2000) How to handle topography in practical geoid determination: three examples. J Geod 74(6):458–466. doi:10.1007/s001900000107
Panet I, Kuroishi Y, Holschneider M (2011) Wavelet modelling of the gravity field by domain decomposition methods: an example over Japan. Geophys J Int 184(1):203–219. doi:10.1111/j.1365246X.2010.04840.x
Pavlis NK, Factor JK, Holmes SA (2007) Terrainrelated gravimetric quantities computed for the next EGM. Proceedings of the 1st international symposium of the international gravity field service, Istanbul, pp. 318–323
Pavlis NK, Holmes SA, Kenyon SC, Factor JF (2008) An Earth gravitational model to degree 2,160: EGM2008. Presented at the 2008 General Assembly of the European Geosciences Union, Vienna, April 13–18
Pavlis NK, Holmes SA, Kenyon SC, Factor JF (2012) The development and evaluation of Earth Gravitational Model (EGM2008). J Geophys Res 117:B04406. doi:10.1029/2011JB008916
Prutkin I, Klees R (2008) On the nonuniqueness of local quasigeoids computed from terrestrial gravity anomalies. J Geod 82(3):147–156. doi:10.1007/s0019000701611
Rummel R, Balmino G, Johannessen J, Visser P, Woodworth P (2002) Dedicated gravity field missionsPrinciple and aims. J Geodyn 33(1):3–20. doi:10.1016/S02643707(01)000503
Shih HC, Hwang C, Barriot JP, Mouyen M, Corréia P, Lequeux D, Sichoix L (2015) Highresolution gravity and geoid models in Tahiti obtained from new airborne and land gravity observations: data fusion by spectral combination. Earth Planets Space 67(1):1–16. doi:10.1186/s4062301502979
Slobbe DC (2013) Roadmap to a mutually consistent set of offshore vertical reference frames. Dissertation, Delft University of Technology, Delft
Tapley BD, Bettadpur S, Watkins M, Reigber C (2004) The gravity recovery and climate experiment: mission overview and early results. Geophys Res Lett 31:L09607. doi:10.1029/2004GL019920
Tenzer R, Klees R (2008) The choice of the spherical radial basis functions in local gravity field modeling. Stud Geophys Geod 52(3):287–304. doi:10.1007/s1120000800222
Tenzer R, Klees R, Wittwer T (2012) Local gravity field modelling in rugged terrain using spherical radial basis functions: case study for the Canadian rocky mountains. In: Kenyon S (eds) Geodesy for Planet Earth, International Association of Geodesy Symposia 136, Springer, Berlin, pp 401–409
Tscherning CC (1978) Introduction to functional analysis with a view to its application in approximation theory. In: Moritz H, Sünkel H (eds) Approximation methods in geodesy. Karlsruhe, Germany
Wang Y, Saleh J, Li X, Roman DR (2012) The US Gravimetric Geoid of 2009 (USGG2009): model development and evaluation. J Geod 86(3):165–180. doi:10.1007/s0019001105067
Wittwer T (2009) Regional gravity field modelling with radial basis functions, Dissertation, Delft University of Technology, Delft
Wu Y, Luo Z (2016) The approach of regional geoid refinement based on combining multisatellite altimetry observations and heterogeneous gravity data sets. Chin J Geophys (in Chinese) 59(5):1596–1607. doi:10.6038/cjg20160505
Wu Y, Luo Z, Zhou B (2016) Regional gravity modelling based on heterogeneous data sets by using Poisson wavelets radial basis functions. Chin J Geophys (in Chinese) 59(3):852–864. doi:10.6038/cjg20160308
Xu P (1992) The value of minimum norm estimation of geopotential fields. Geophys J Int 111(1):170–178. doi:10.1111/j.1365246X.1992.tb00563.x
Xu P (1998) Truncated SVD methods for discrete linear illposed problems. Geophys J Int 135(2):505–514. doi:10.1046/j.1365246X.1998.00652.x
Authors’ contributions
YW and ZL initiated the study, designed the numerical experiments, and wrote the manuscript. WC and YC provided the data and supplied beneficial suggestions. YW finalized the manuscript. All authors read and approved the final manuscript.
Acknowledgements
The authors would like to give our sincerest thanks to the two anonymous reviewers for their beneficial suggestions and comments, which helped us improve the manuscript. We would also like to thank the anonymous editor and the editorial office for their work on language editing. We acknowledge the assistance of Prof. Roland Klees and Dr. Cornelis Slobbe from Delft University of Technology for kindly providing the original software. This research was primarily supported by the National Natural Science Foundation of China (41374023), China Postdoctoral Science Foundation (No. 2016M602301), Key Laboratory of Geospace Environment and Geodesy, Ministry of Education, Wuhan University (150208), the State Scholarship Fund from Chinese Scholarship Council (201306270014) and project KZS0J, ‘Development of a Hong Kong Positioning Infrastructure based on GPS, Beidou, and Ground based Augmentation System.’ Generic Mapping Tools (GMT) was used to generate the figures.
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The authors declare that they have no competing interests.
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Wu, Y., Luo, Z., Chen, W. et al. Highresolution regional gravity field recovery from Poisson wavelets using heterogeneous observational techniques. Earth Planets Space 69, 34 (2017). https://doi.org/10.1186/s4062301706182
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DOI: https://doi.org/10.1186/s4062301706182