Open Access

Bathymetric stripping corrections to gravity gradient components

Earth, Planets and Space201264:640070021

https://doi.org/10.5047/eps.2012.07.001

Received: 11 April 2012

Accepted: 2 July 2012

Published: 16 August 2012

Abstract

To allow for geophysical interpretation of observed gravity gradients, several corrections must be applied. In this article expressions for gravimetric forward modeling of bathymetric (ocean density contrast) stripping corrections to GOCE gravity gradient observables are evaluated numerically. The generic expression for the bathymetric gravitational potential utilizes a depth-dependent seawater density distribution model. The expressions are defined in their spectral representation by means of the bathymetric spherical functions which describe the global geometry of the ocean bottom relief. Numerical examples are given for the bathymetric stripping corrections to selected gravity field parameters computed with a spectral resolution complete to degree 360 of spherical harmonics. All computations are realized globally on the 1 arc-deg geographical grid at the mean satellite elevation of 250 km. The results reveal that the bathymetric stripping corrections to gravity gradients globally vary within ±5 × 10−9 s−2. Extreme values apply mainly along the continental margins where the largest spatial bathymetric gravitation signal variations occur.

Key words

Bathymetryforward modelingGOCEgravitational gradiometryocean density contrast

1. Introduction

In gravimetric inverse methods for studying the lithosphere structure, the topographic, bathymetric, and additional corrections of all known anomalous mass density structures within the Earth’s crust are applied to observed gravity data in order to model the unknown (and sought) density structure or density interface. In geophysics, this step is well known as gravity stripping (e.g., Hammer, 1963). The gravitational field generated by the ocean density contrast (relative to an adopted mean Earth’s density) represents a significant amount of the gravitational signal to be modeled and subsequently removed from observed gravity data. Currently available global gravitational models (GGM) as well as global topographic and bathymetric data sets allow for relatively accurate numerical evaluation of topography-corrected and bathymetry-stripped gravity field parameters to a very high spatial resolution.

The GOCE gravity gradiometry satellite mission provides global and homogeneous data sets with well-known stochastic properties. It is thus expected that GOCE gravity field solutions will improve our knowledge about the Earth’s inner density structure especially beneath oceanic and continental areas where seismic data are not yet available or their accuracy and spatial coverage is insufficient.

Novák and Grafarend (2006) evaluated numerically external gravitational fields of topographic and atmospheric masses by using spherical harmonic expansions. Tenzer et al. (2008, 2009, 2010) then computed globally the bathymetry-generated gravity field parameters by using the apparatus of the spherical harmonic analysis and synthesis. Novák (2010) computed globally the gravitational potential generated by the global ocean masses with a very high spatial resolution. In these studies a constant value of the ocean density contrast was adopted.

The actual seawater density variations due to salinity, temperature, and pressure typically range within 1020 and 1050 kg m−3, with most of this variation being due to pressure (Garrison, 2001). When the actual seawater density is approximated only by its mean value, relative inaccuracies up to about 2% were estimated in computed values of the bathymetric stripping corrections (Tenzer et al., 2011). Since global bathymetric models are currently available to a very high accuracy and spatial resolution, the errors caused by approximating the actual seawater density by the mean value represent the largest contribution to the total error budget. These errors can reach up to 200 m2 s−2 and 16 mGal in terms of the gravitational potential and its radial derivative, respectively. The extreme values apply particularly to the computation areas situated over deepest oceans.

Gladkikh and Tenzer (2011) analyzed the oceanographic data of the World Ocean Atlas 2009 (WOA09) and the World Ocean Circulation Experiment 2004 (WOCE04). WOA09 products are made available by the NOAA’s National Oceanographic Data Center (Johnson et al., 2009). WOCE04 oceanographic data were provided by the German Federal Maritime and Hydrographic Agency (Gouretski and Koltermann, 2004). They used experimental data of salinity, temperature, and pressure to calculate the seawater density values based on the thermodynamic equation of state TEOS-10 for seawater (Millero et al., 2008). The density values were then used to formulate an empirical model of the global seawater density distribution defined as a function of the ocean depth to account for density variations due to pressure. The comparison of the experimental and theoretical seawater density values revealed that the new empirical model approximates the above referenced seawater density distributions with the maximum relative error better than 0.6%, while the corresponding average error is about 0.1%. Tenzer et al. (2012a) utilized this empirical seawater density model for computing the bathymetric stripping gravity correction. In this study we adopt this empirical density model to compute accurately the bathymetric stripping corrections to gravity gradient components.

2. Theory

Tenzer et al. (2012a) derived the expression for the gravitational potential V generated by the ocean density contrast in the following form
(1)
where R = 6371 × 103 m is the adopted mean Earth’s radius, GM = 3986005 × 108 m3 s−2 is the geocentric gravitational constant, Y nm stands for the spherical harmonic function of degree n and order m, and nax is the maximum available degree of spherical harmonics. The 3-D position is defined in the spherical coordinate system; where r is the geocentric radius and denotes the geocentric direction with spherical latitude and longitude γ. Bathy-metric potential coefficients V nm in Eq. (1) read
(2)
The nominal value of the ocean density contrast is defined as the difference between the reference crustal density and the seawater density, . The value of the surface seawater density = 1027.91 kg m−3 (Gladkikh and Tenzer, 2011) was adopted as the nominal seawater density. For the adopted value of the reference crustal density of 2670 kg m−3 (Hinze, 2003), the nominal ocean density contrast (at the zero depth) equals = 1642.09 kg m−3. The adopted value of the Earth’s mean homogeneous density in Eq. (2) is = 5500 kg m−3 (e.g., Novák, 2010). The parameters of the depth-dependent density term in Eq. (2) are: β = 0.00637 kg m−3, a1 = 0.7595 m−1 and a2 = −4.3984 × 10−6 m−2. The numerical coefficients F nm , and in Eq. (2) are defined as (Tenzer et al, 2011)
(3)
(4)
(5)
The coefficients D nm of the global bathymetric model (GBM) describe the geometry of the ocean bottom relief. The series defines the surface spherical bathymetric function D n of degree n. It reads (Tenzer et al., 2010)
(6)
where D is the ocean depth and P n is the Legendre polynomial. Higher-order terms read
(7)
where the symbol denotes the full spatial angle. The components of the gravitational vector and Marussi gravitational gradient tensor, both generated by the ocean density contrast, can be readily derived from the expressions in Eqs. (1)(7).

3. Numerical Examples

The GBM coefficients were used to compute the bathymetric stripping corrections to the Earth’s gravitational potential and its first- and second-order derivatives with a spectral resolution complete to degree 360 of spherical harmonics. The computation was done globally on a 1 arc-deg grid at the mean elevation of 250 km. Statistics of all results are summarized in Table 1. The global maps of selected quantities: V, V r , V rr , and are shown in Figs. 13.
Table 1

Statistics of gravitational parameters generated by the ocean density contrast computed globally on a 1 arc-deg grid at the elevation of 250 km.

Parameter

Min

Max

Mean

RMS

V [m2 s−2]

16078

27173

21604

2907

V r [mGal]

−544

−128

−309

125

V φ [mGal]

−287

194

−14

77

V λ [mGal]

−221

246

0.0

66

V rr [E]

−2.0

4.7

0.9

1.4

V φ φ [E]

−2.6

2.2

0.0

0.7

V λ λ [E]

−3.5

3.1

0.0

0.7

V [E]

−3.5

4.1

−0.1

0.8

V [E]

−4.0

3.7

0.0

0.7

V φ λ [E]

−2.6

3.5

0.0

0.5

Fig. 1

Gravitational potential V (m2 s−2).

The bathymetric gravitational potential V, see Fig. 1, is everywhere positive. The maximum signal is over the largest ocean mass concentration (central Pacific Ocean).

The global map of V r , see Fig. 2, revealed major structures of the ocean bottom relief. It is everywhere negative, with its absolute maxima distributed over oceanic basins and (partially) subduction zones in Pacific Ocean. The spatial distribution of V r over oceanic areas also clearly revealed the features related to the oceanic divergent zones (i.e., mid-oceanic ridges). It was demonstrated in Tenzer et al. (2012b), that the application of this correction is essential for the interpretation of the age of oceanic lithosphere (characterized by the formation of oceanic lithosphere along the mid-oceanic ridges, its further speeding and consequent subduction under the oceanic or continental crust along the oceanic subduction zones) which is attributed to mantle convection. The (absolute) values of V r substantially decrease along the continental margins distinctively marking the boundary between the oceanic and continental lithosphere.
Fig. 2

Gravitational vector component V r (mGal = 10−5 m s−2).

Whereas V r is directly correlated with bathymetric depths, the maximum signal of V rr corresponds with the largest spatial variations of the ocean bottom relief. This is seen in Fig. 3(a). The map of V rr revealed major structures of the oceanic lithosphere. The small positive values are found along the oceanic divergent boundaries (mid-oceanic ridges). Over areas of the oceanic abyssal planes, these values further increase. The maxima correspond with locations of the oceanic subduction zones. Boundaries between oceanic and continental tectonic plates are also clearly distinguished (by small negative values) in the gravity map. The bathymetric corrections and , see Figs. 3(b, c), revealed a pattern of the largest horizontal variations of bathymetric gravitational field with respect to the meridional and prime-vertical directions. The maximum positive and negative values of are coupled along the continental margins with prevailing latitudinal directions. A similar pattern of the gravity signal is seen in the global map of , but in this case with prevailing meridional direction.
Fig. 3

Gravitational gradient components (a)V rr , (b) and (c) (E = 10−9 s−2).

4. Summary and Concluding Remarks

We have derived and applied spectral expressions for computing the bathymetric stripping corrections to gravity field parameters. The numerical examples were given globally on a 1 arc-deg grid computed at the mean satellite elevation of 250 km.

We demonstrated that the maxima of the bathymetric potential V and its radial derivative V r correspond with the largest seawater accumulation in Pacific Ocean. The map of V rr reproduces major structures of the oceanic lithosphere. The spatial distributions of the horizontal components and are more complex reflecting the largest bathymetric gravitational signal variations with respect to the coordinate directions. Their extreme values are found along the continental margins again with prevailing either south-north or east-west directions. Compared to and , the maximum signal of and along a particular continental margin comprises both, the positive as well as negative values.

Whereas the application of V r is important for modeling and interpretation of the refined gravity field obtained based on analysis of GRACE inter-satellite observables, the bathymetric stripping corrections V rr , and are applied to GOCE gravity gradient measurements. GOCE gravity gradiometry data provide the accurate information about the Earth’s gravity field especially at the medium spherical harmonics (somewhere between degrees 70–200). GRACE data provide the accurate information at the long-wavelength part of the gravitational field (up to degree of about 120). The combined inversion of GRACE and GOCE data (including additional geophysical constrains) is thus essential for a more robust and accurate recovery of the Earth’s inner density structures.

Declarations

Acknowledgments

Pavel Novák was supported by the Czech Science Foundation, project 209/12/1929.

Authors’ Affiliations

(1)
School of Surveying, University of Otago, Dunedin, New Zealand
(2)
NTIS—New Technologies for Information Society, University of West Bohemia, Plzeň, Czech Republic

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Copyright

© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB 2012