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Isostasy (Greek ''ísos'' "equal", ''stásis'' "standstill") is the state of gravitational equilibrium between Earth's crust and mantle such that the crust "floats" at an elevation that depends on its thickness and density of underlying roots of the low density of the mountain. This concept is invoked to explain how different topographic heights can exist at Earth's surface. When a certain area of Earth's crust reaches the state of isostasy, it is said to be in ''isostatic equilibrium''. Isostasy is not a process that upsets equilibrium, but instead is one which restores it (a negative feedback). It is generally accepted 〔A.B. Watts, Isostasy and flexure of the lithosphere,Cambridge Univ. Press., 2001〕 that Earth is a dynamic system that responds to loads in many different ways. However, isostasy provides an important 'view' of the processes that are happening in areas that are experiencing vertical movement. Certain areas (such as the Himalayas) are ''not'' in isostatic equilibrium, which has forced researchers to identify other reasons to explain their topographic heights (in the case of the Himalayas, which are still rising, by proposing that their elevation is being "propped-up" by the force of the impacting Indian plate; The Basin and Range Province of the Western US is another example of a region not in isostatic equilibrium.) Although originally defined in terms of continental crust and mantle, it has subsequently been interpreted in terms of lithosphere and asthenosphere, particularly with respect to oceanic island volcanoes such as the Hawaiian Islands. In the simplest example, isostasy is the principle of buoyancy wherein an object immersed in a fluid is buoyed with a force equal to the weight of the displaced fluid. On a geological scale, isostasy can be observed where Earth's strong crust or lithosphere exerts stress on the weaker mantle or asthenosphere, which, over geological time, flows laterally such that the load is accommodated by height adjustments. The general term 'isostasy' was coined in the year 1889 by the American geologist Clarence Dutton.〔(【引用サイトリンク】 title=Clarence Edward Dutton )〕 == Isostatic models == Three principal models of isostasy are used: # The Airy–Heiskanen model – where different topographic heights are accommodated by changes in crustal thickness, in which the crust has a constant density # The Pratt–Hayford model – where different topographic heights are accommodated by lateral changes in rock density. # The Vening Meinesz, or flexural isostasy model – where the lithosphere acts as an elastic plate and its inherent rigidity distributes local topographic loads over a broad region by bending. Airy and Pratt isostasy are statements of buoyancy, whereas flexural isostasy is a statement of buoyancy when deflecting a sheet of finite elastic strength. 抄文引用元・出典: フリー百科事典『 ウィキペディア（Wikipedia）』 ■ウィキペディアで「Isostasy」の詳細全文を読む スポンサード リンク
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