Gravity at sea

Dehlinger, Peter; Chiburis, E. F.

doi:10.1016/0025-3227(72)90027-8

Cited by 7 publications

(1 citation statement)

References 34 publications

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“…In addition, any mass has power over the entire spherical harmonic spectrum (e.g., Pollack 1973;Sutton et al 1991). The point-mass approximation then suggests a maximum depth of the anomaly of sorts (Dehlinger 1978;Goossens & Smith 2023). Thus, anomalies assigned to a depth based on degree can in principle also be caused by density anomalies that are shallower.…”

Section: Introductionmentioning

confidence: 99%

Constraining the Structure under Lunar Impact Basins with Gravity

Smith,

Goossens,

Neumann

et al. 2023

Planet. Sci. J.

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The lunar gravity field is used to estimate and constrain the depth of mass anomalies under 19 major lunar impact basins. We use radial gravitational spectra, consisting of accelerations computed either per spherical harmonic degree or cumulatively, at surface locations to obtain the distribution of the gravity signal with spherical harmonic degree and, by implication, to the likely depth below the surface. The results provide estimates for the maximum likely depths of the primary component to the mass anomalies under 19 basins. We find that the maximum depths of the primary source of mascon gravity on the lunar nearside are deeper than the depths for those on the farside when South Pole–Aitken (SPA) is excluded. All basin mass anomalies on the lunar nearside are in the mantle. The maximum depth of the primary source of the mass anomalies is <80 km, with the exception of SPA, whose dominant mass signature lies at a maximum depth of >200 km beneath the surface. The upper 20 km under all basins is largely devoid of anomalies, reflecting predominantly mixing and relaxation associated with impact melt combined with ejecta fallback, as well as homogenization associated with post-basin formation impact bombardment. Except for SPA, all basin anomalies merge with the deep interior at ∼150 km or below, indicating the depth penetration of disruption of the density structure of the lunar interior associated with impact bombardment.

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Section: Introductionmentioning

confidence: 99%

Constraining the Structure under Lunar Impact Basins with Gravity

Smith,

Goossens,

Neumann

et al. 2023

Planet. Sci. J.

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show abstract

3.6 References for 3

Kahle¹

Landolt-Börnstein - Group v Geophysics

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The Earth's gravity field

Rapp

1975

Geophysical Surveys

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Abstract. The Earth's gravity field can be determined from gravity measurements made on the surface of the Earth, and through the analysis of the motion of Earth satellites. Gravity data can be used to solve the boundary value problem of gravimetric geodesy in various ways, from the classical formulation using a geoid to the concept of a reference surface interior to the masses of the Earth to a statistical method. We now have gravity information for 1 ~ data blocks over 46700 of the Earth's surface and more than several million point measurements available.Satellite observations such as range, range-rate, and optical data have been analyzed to determine potential coefficients used to describe the Earth's gravitational potential field. Coefficients, in a spherical harmonic expansion to degree 12, can be determined from satellite data alone, and to at least degree 20 when the satellite data is combined with surface gravity material. Recent solutions for potential coefficients agree well to degree 4, but with increasing disagreement at higher degrees.

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Gravity at sea

Cited by 7 publications

References 34 publications

Constraining the Structure under Lunar Impact Basins with Gravity

Constraining the Structure under Lunar Impact Basins with Gravity

3.6 References for 3

The Earth's gravity field

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