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Dutter R 1986/1987: Mathematische Methoden in der Montangeologie. Vorlesungsnotizen, Manuscript, Leoben Mathematische Methoden in der Montangeologie

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Methoden in der Montangeologie. Vorlesungsnotizen, Manuscript, Leoben Huber P J 1981: Robust Statistics, Wiley, New York Steiner F 1990: Introduction to Geostatistics (in Hungarian

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Balla Z 1994: Deep Structure and seismic hazard of the Gabcikovo-Nagymaros region. Manuscript, Archive of MáFI Balla Z, Schweitzer F, Szabó Z 1993: Summary map of the ruptures and ruptured belts active in Pleistocene, M=1

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Determination of the gravimetric geoid is based on inversion of observed values of gravity into the disturbing gravity potential, i.e., the unknown potential is sought from discrete values of its vertical gradient. This transformation is often solved using boundary-value problems of the potential theory defined in terms of the Laplace differential equation and corresponding boundary conditions. However, this apparatus requires the potential function to be harmonic everywhere outside the boundary on which the unknown potential is solved for. For geoid determination, the boundary represents the geoid that is usually approximated for derivation of the solution by a geocentric sphere or reference ellipsoid. Since there are topographical and atmospheric masses outside the geoid, the potential function is not harmonic everywhere outside the geoid and the so-called reduction of the gravity potential and its functionals must be applied. This manuscript investigates the generalized method of Helmert’s condensation, namely its numerical implications for the standard procedure of geoid determination. An optimum location of the condensation layer is investigated from the point of relative smoothness of the gravity field and numerical difficulties with gravity inversion. The test area in the Canadian Rocky Mountains with a highly variable gravity field and topography is used for numerical investigations. Numerical results indicate that the condensation layer buried approximately 20–30 km inside the geoid gives the best results in terms of the gravity field smoothness as well as the complexity of gravity inversion. However, larger values of the primary indirect effect on the geoid for this depth of the condensed masses seem to overcome these numerical advantages.

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Oros E 2003: Seismological Bulletin of Banat Region, Timisoara, Romania (manuscript) Süle B 2010: Central European J. Geosci. , 2, 475–480. Süle B

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: Cartography in France, 1660–1848. Science, engineering and statecraft. University of Chicago Press Márton M 1985: The relief of oceans and seas. The representation of undersea features in small scale maps. Manuscript (in

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Bremer J 2000: Manuscript not published yet COST 251 RALVI Ionospheric Database 1997. Rutherford-Appleton Laboratory, Chilton, Didcot, UK Manuscript not published yet COST 251 RALVI Ionospheric Database 1997

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Maślanka J (without date): Austrian cadaster (in Polish). Manuscript with internet availability (URL: http://gps.put.mielec.pl/new_page_1.htm ) Mugnier C J 2004: Photogrammetric Engineering and Remote Sensing

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. Hung 35 149 175 Szarka L, Ádám A, Menvielle M 2004: Geophysical Prospecting , Manuscript 3166 (in press

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Kiss J 2005: Magyar Geofizika (in press) Németh G 2005: Report on the geological experiments along the CEL-7 profile. Manuscript Posgay K, Bodoky T, Hegedös E, Kovácsvölgyi S, Lenkey L

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