Abstract
Long-term changes in sea level are dominated by tectono-eustasy due to alternations in the volume of the ocean basins (i.e. the hypsographic land/ sea distribution), by geoidal eustasy due to redistribution of mass within the Earth and rotational changes, and by local or regional crustal movements. Glacio-eustasy had, of course, only effect during periods of glaciations; namely the Upper Cenozoic, the Permian, the Ordovician, the Upper Precambrian and at around 2.3 Ga. Morner (1983a, 1985a) estimated the rates and amplitudes possible for the different eustatic factors. Tectono-eustasy is a slow process (operating at maximum rates of 0.5-0.7 mm a–1) whilst geoidal eustasy (as well as glacial eustasy) also includes very rapid processes (some 10-30 mm a–1).
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