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The removal of mass from a region will be [[Isostasy|isostatically compensated]] by crustal rebound. If we take into consideration typical crustal and mantle densities, erosion of an average 100 meters of rock across a broad, uniform surface will cause the crust to isostatically rebound about 85 meters and will cause only a 15-meter loss of mean surface elevation.<ref>Burbank, Douglas W., and Anderson, Robert S. Tectonic Geomorphology. Chichester, West Sussex: J. Wiley & Sons, 2011. Print.</ref> An example of isostatic uplift would be [[post-glacial rebound]] following the melting of [[continental glacier]]s and [[ice sheet]]s. The [[Hudson Bay]] region of [[Canada]], the [[Great Lakes]] of Canada and the [[United States]], and [[Fennoscandia]] are currently undergoing gradual rebound as a result of the melting of ice sheets 10,000 years ago.
Crustal thickening, which for example is currently occurring in the [[Himalaya]] due to the [[continental collision]] between the [[Indian Plate|Indian]] and the [[Eurasian Plate|Eurasian]] plates, can also lead to surface uplift; but due to the isostatic sinking of thickened crust, the magnitude of surface uplift will only be about one-sixth of the amount of crustal thickening. Therefore, in most [[Convergent plate boundary|convergent settings]] isostatic uplift plays a relatively small role and high peak formation can be more attributed to tectonic processes.<ref>Gilchrist, A. R., M. A. Summerfield, and H. A. P. Cockburn. "Landscape Dissection, Isostatic Uplift, and the Morphologic Development of Orogens." Geology 22.11 (1994): 963-966. Print.</ref> Direct measures of the elevation change of the land surface can only be used to estimate erosion or bedrock uplift rates when other controls (such as changes in mean surface elevation, volume of eroded material, timescales and lags of isostatic response, variations in crustal density) are known.
==Coral islands==
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