Isostatic depression is the sinking of large parts of the Earth's crust into the asthenosphere caused by a heavy weight placed on the Earth's surface, often glacial ice during continental glaciation.[2] Isostatic depression and isostatic rebound occur at rates of centimeters per year. Greenland is an example of an isostatically depressed region.
Glacial isostatic depression
editIsostatic depression is a phase of glacial isostasy, along with isostatic rebound.[3] Glacial isostasy is the Earth's response to changing surface loads of ice and water during the expansion and contraction of large ice sheets. The Earth's asthenosphere acts viscoelastically, flowing when exposed to loads and non-hydrostatic stress, such as ice sheets, for an extended period of time. The Earth's crust is depressed by the product of thickness of ice and the ratio of ice and mantle densities. This large ice load results in elastic deformation of the entire lithospheric mantle over the span of 10,000-100,000 years, with the load eventually supported by the lithosphere after the limit of local isostatic depression has been attained.[2] Historically, isostatic depression has been used to estimate global ice volume by relating the magnitude of depression to the density of ice and upper mantle material.[4]
Glacial megalakes can form in regional depressions under the influence of glacial load.[2]
Isostatic depression in Greenland
editGreenland is isostatically depressed by the Greenland ice sheet. However, due to deglaciation induced by climate change, the regions near the shrinking ice sheet have begun to uplift, a process known as post-glacial rebound. Modeling these glacial isostatic adjustments has been an area of interest for some time now as the entire topography of Greenland is affected by these movements.[1] These movements are unique in that they can be observed on a human time scale unlike other geological processes. Models have been created to assess what future equilibrium states of the Greenland ice sheet will look like.[4]
See also
editReferences
edit- ^ a b Robinson, Alexander; Calov, Reinhard; Ganopolski, Andrey (June 2012). "Multistability and critical thresholds of the Greenland ice sheet". Nature Climate Change. 2 (6): 429–432. Bibcode:2012NatCC...2..429R. doi:10.1038/nclimate1449. ISSN 1758-678X.
- ^ a b c Lambeck, Kurt (2009), "Glacial Isostasy", in Gornitz, Vivien (ed.), Encyclopedia of Paleoclimatology and Ancient Environments, Encyclopedia of Earth Sciences Series, Dordrecht: Springer Netherlands, pp. 374–380, doi:10.1007/978-1-4020-4411-3_93, ISBN 978-1-4020-4551-6
- ^ Milne, G.; Shennan, I. (2013), "Isostasy: Glaciation-Induced Sea-Level Change", Encyclopedia of Quaternary Science, Elsevier, pp. 452–459, doi:10.1016/b978-0-444-53643-3.00135-7, ISBN 978-0-444-53642-6
- ^ a b Whitehouse, Pippa L. (2018). "Glacial isostatic adjustment modelling: historical perspectives, recent advances, and future directions" (PDF). Earth Surface Dynamics. 6 (2): 401–429. Bibcode:2018ESuD....6..401W. doi:10.5194/esurf-6-401-2018. ISSN 2196-632X. S2CID 54666588.
 | This glaciology article is a stub. You can help Wikipedia by expanding it. |