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Desert geomorphology or the geomorphology of arid and semi-arid lands shares many landforms and processes with more humid regions. One distinctive feature is the sparse or lacking vegetation cover, which influences fluvial and slope processes, related to wind and salt activity. [4]
It is a response to the development of this GIS technology to gather and process DEM data (e.g. remote sensing, the Landsat program and photogrammetry). Recent applications proceed with the integration of geomorphometry with digital image analysis variables obtained by aerial and satellite remote sensing . [ 7 ]
An early popular geomorphic model was the geographical cycle or cycle of erosion model of broad-scale landscape evolution developed by William Morris Davis between 1884 and 1899. [11] It was an elaboration of the uniformitarianism theory that had first been proposed by James Hutton (1726–1797). [24]
Nivation is the set of geomorphic processes associated with snow patches.The primary processes are mass wasting and the freeze and thaw cycle, [1] in which fallen snow gets compacted into firn or névé.
If the tensile stress exceeds the magnitude of the least principal compressive stress the rock will fail in a brittle manner and these cracks propagate in a process called hydraulic fracturing. Hydraulic joints occur as both nonsystematic and systematic joints, including orthogonal and conjugate joint sets.
Sediments underlying fluvial terrace exposed in cutbanks along the Manú River, Peru. In geology, a terrace is a step-like landform. A terrace consists of a flat or gently sloping geomorphic surface, called a tread, that is typically bounded on one side by a steeper ascending slope, which is called a "riser" or "scarp".
Understanding the principle of isostasy is a key element to understanding the interactions and feedbacks shared between erosion and tectonics. The principle of isostasy states that when free to move vertically, lithosphere floats at an appropriate level in the asthenosphere so that the pressure at a depth of compensation in the asthenosphere well below the base of the lithosphere is the same. [3]
Deposits of slow periglacial solifluction compromise poorly stratified diamicton and diamicton where stratification is wholly lacking. When stratification can be seen it is often distinguished by a buried organic soil. [3]