- Martinec Z (2004) Time-domain, spectral-finite element method to viscoelastic relaxation of a self-gravitating, incompressible, Maxwell-viscoelastic, radially symmetric sphere. Computers and Geosciences, submitted.Google Scholar
- Lambeck K, Smither C and Ekman M (1998) Tests of glacial rebound models for Fennoscandinavia based on instrumented sea-and lake-level records. Geophys J Int 135: 375–387.CrossRefGoogle Scholar
- Mitrovica JX and Peltier WR (1989) Pleistocene deglaciation and the global gravity field. J Geophys Res 94: 13,651–13,671.Google Scholar
- Tushingham AM and Peltier WR (1998) Ice 3G: a new global model of late Pleistocene deglaciation based on geophysical predictions of postglacial relative sea level change. J Geophys Res 96: 4,497–4,523.Google Scholar
- Fleming K and Lambeck K (2004) Constraints on the Greenland Ice Sheet since the Last Glacial Maximum from sea-level observations and glacial rebound models. Quat Sci Rev, in press.Google Scholar
- Krabill W, Abdalati W, Frederick E, Manizade S, Martin C, Sonntag J, Swift R, Thomas R, Wright W and Yungel J (2000) Greenland Ice Sheet: high-elevation balance and peripheral thinning. Science 289: 428–430.CrossRefGoogle Scholar
- Thomas R, Akins T, Csatho B, Fahnestock M, Gogineni P, Kim C and Sonntag J (2000) Mass balance of the Greenland Ice Sheet at high elevations. Science 289: 426–428.CrossRefGoogle Scholar
- Velicogna I and Wahr J (2002) Postglacial rebound and Earth's viscosity structure from GRACE. J Geophys Res 107: 2,376–2,387.Google Scholar
- Rignot E and Thomas R (2002) Mass balance of polar ice sheets. Science 297:1,502–1,506.CrossRefGoogle Scholar
Geoid height anomalies around the Iceland hotspot in an area extending between 50°W to 14°E and 45°N to 72°N have been investigated to search for evidence of an upper mantle thermal anomaly. After removing wavelengths longer than 3800 km, the effect of the cooling lithosphere was eliminated by low-pass filtering of age data and applying the boundary model. The effects of the various platforms and swells in the North Atlantic were removed by an Airy model, since the geoid-to-topography ratio is lower than 1.5 m km-1 for all areas of elevated topography independent of their origin. The residual geoid shows a large positive anomaly with a steep constant slope towards a location (north)west of Iceland beneath Greenland. The amplitude of the anomaly can be estimated to at least 8 m. The geoid-to-topography ratio reaches a value of 7 m km-1 which is in good agreement with a plume-related anomaly.
![Geoid Download Greenland Geoid Download Greenland](http://earth-info.nga.mil/GandG/wgs84/gravitymod/egm2008/GIS/world_geoid/EGM08_Geoid.gif)
![Geoid model download Geoid model download](https://www.researchgate.net/profile/N_Pavlis/publication/255608816/figure/tbl1/AS:668503350714373@1536395027450/Terrain-Types-of-the-30-DTM2002-Data_Q320.jpg)
Since 2010, we have been working on a self-consistent dataset of the Greenland Ice Sheet based on the conservation of mass that is now freely available at NSIDC.The new version (v3) now includes ocean bathymetry.