By Zdenek Martinec

This publication deals a simultaneous remedy of the speculation and numerical software of boundary-value difficulties with regards to the choice of an actual geoid from gravimetric facts. the next matters are mentioned: topographical results and their computations in targeted gravimetric geoid selection, the downward continuation of a harmonic functionality, Stokes' challenge formulated on an ellipsoid of revolution, round Stokes' challenge with ellipsoidal corrections interested by boundary stipulations for an anomalous capability, and the altimetry-gravimetry boundary-value challenge. the reply to a few clinical difficulties, raised and mentioned in geodetic literature over the last years, are available right here. The booklet is meant for scientists and complicated graduate students.

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Additional resources for Boundary-Value Problems for Gravimetric Determination of a Precise Geoid

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65) exists except for the geoidal wavelength of an infinitesimally short wavelength that must be completely suppressed prior to downward continuation. 6; jr~] = 10000, and j,~a, = 11600). 65). The main disadvantage of this approach is that the boundary operator is referred to the Earth's surface which cannot be approximated by a smooth boundary. 65) is not available. 65) is again different from the nature of the original Stokes two-boundaryvalue problem. 7 demonstrates this fact in a transparent way.

2 19 Axisymmetric geometry Let the height H(0, A) of the Earth's surface above the geoid is modelled by zonal as well as tesseral and sectoral spherical harmonies of the global digital terrain model TUG87 (Wieser, 1987) cut at degree 180. To create a rotational symmetric body, axisymmetric height H(0) will be generated by height H(O~ A) taken along a fixed meridian A = A0. 57) +e~j~=( R )J+~ =o sin 0 cos 0 dPj(cosO)_ -~ /~j, (cos,O)sinOd 0 R + H(O) Note that the elements Aj~j can only be evaluated by a method of numerical quadrature.

Ltl] tE-4 1E-3 1E-2 IIIIIII 1E-1 1E+O angular distance (degree) The integration kernels for the indirect and direct topographical effects grid step size rather than that with a sparse grid size. 2 we will show, for instance, that densifying a 5' x 5' grid of topographical heights in the Canadian Rocky Mountains to a 1 km x 1 kin grid causes an increase of the maximal amplitude of the indirect topographical effect from 3 cm to 18 cm. 59). 0001 ° to ¢ = 1°. This confirms the well known-fact that the gravitational potential of topographical masses of a finite thickness behaves like the potential of a thin layer when it is observed from a larger distance.

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