AbstractBecause of inhospitable terrain, there are practical difficulties in the acquisition of gravity or satellite data for determining the earth's gravity field in high mountain regions. Also, because of the limitations of both gravimetric and astrogeodetic-gravimetric methods in the absence of observational data and the difficulties in direct application of satellite techniques using satellite altimetry, laser ranging, Doppler etc. due to geographic inaccessibility, a geodynamic method with a higher degree geopotential coefficient solution appears to be the only alternative in determining the earth's gravity field without recourse to actual ground observations. In addition, the terrestrial free-air gravity anomaly data as used in existing geopotential coefficient solutions, appear to be defective on various counts noted in [3].Apart from providing improved formulae for the computation of 1°×1°mean free-air gravity anomalies through extended forms of regression equations having both station elevations and positional coordinates as arguments to account for possible layer-wise crustal density variations inside the large 1°×1°squares as detailed in [4], the relevant corrections to reduce the ground level 1°×1°mean free-air gravity anomaly values to the geoid, have been computed and provided in tabular forms in [6], for general use in geopotential coefficients solutions.The 1°×1°mean free-air anomaly values obtained, on being converted into corresponding isostatic anomalies using relevant Airy isostatic corrections, were then utilised in filling the present 1°×1°mean isostatic anomaly gaps at places over mountainous regions by making use of the same methodology as in the case of 1°×1°mean free-air anomaly values [4]. The 1°×1°mean isostatic anomalies predicted, are then converted back into 1°×1°mean free-air anomalies for use in the precise geopotential coefficients solutions, in order to obtain the 10 global geoid and mean free-air gravity anomalies more precisely for geodetic and geophysical determinations.