Solifluction


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solifluction

[¦säl·ə′flək·shən]
(geology)
A rapid soil creep, especially referring to downslope soil movement in periglacial areas. Also known as sludging; soil flow; soil fluction.

Solifluction

 

the flow of wet, finely dispersed soil down a slope resulting from the perennial freezing and thawing of the ground. The flow rate is usually a few centimeters a year; sometimes, in the case of disastrous flows, the flow rate reaches hundreds of meters an hour. The development of solifluction results from decreased ground stability caused by meltwaters and rain and by freezing and thawing. Solifluction occurs primarily in permafrost regions and in regions characterized by seasonal freezing. It is most common on slopes of medium steepness (8°-15°) that have a layer of dispersed beds at least 1.0–2.0 m thick. Slow solifluction develops primarily above the timberline and creates characteristic forms of microrelief, for example, flows and terraces having a tonguelike (parabolic) shape. The classical regions of development of solifluction are the polar and subpolar regions, the Urals, the Chukchi Peninsula, Spitsbergen, and Alaska.

REFERENCES

Kaplina,T. N. Kriogennyesklonovyeprotsessy. Moscow, 1965.
Zhigarev, L. A. Prichiny i mekhanizm razvitiia solifluiuktsü. Mos cow, 1967.

T. N. KAPLINA

References in periodicals archive ?
(2390 m a.s.1.), where we set out to investigate the internal structure of a solifluction lobe.
This rapid establishment of forest and reduction in solifluction resulted in a stabilization of the surrounding slopes, causing an abrupt drop in erosion and surface runoff, as indicated by the sharp decline in mineral influx at Splan Pond and the return to organic sediment evident at all three sites.
He has reconstructed the palaeoecological evolution in the present periglacial belt of this high semiarid Mediterranean massif studying two sedimentary records: solifluction lobes and mountain lakes.
The most typical processes were thawing of frozen soils, glaciokarst (in Poozerye), thermokarst, and solifluction (in periglacial areas) processes, and descent of periglacial water reservoirs.
The Early and Middle Pleistocene covers include a large proportion of angular clasts, pointing to the role of intensive solifluction within glacial stages.
However, the bowhead whale bones described by Atkinson and England (2004) are anomalously old compared with dated driftwood and marine shells collected from the same shoreline, suggesting that the animal either sank prior to being exposed by falling sea level, or experienced post-stranding redeposition, likely due to solifluction. The usefulness of this bowhead whale in reconstructing the postglacial emergence history of Ellef Ringnes Island was therefore limited, and Atkinson and England (2004) did not discuss these remains further.
Coastal profiles and their Pleistocene evolution correspond to the slope-over-wall model (Bird, 2000), where the cliffs were degraded by periglacial processes during the Glacial period, with the altered mantle moving downslope by solifluction and translational landsliding.
There are no indications of mass movement or solifluction and the differing surface features appear to relate to natural variation in depositional conditions during ice retreat.
Wind erosion following salinization, solifluction, and deflation are greater for particles 0.1-0.5 mm in diameter, depending on the intensity of the energy source and its turbulence.
Periglacial effects (e.g., solifluction) may, however, have limited the extent of vegetated area during glacial maximum (Veit and Garleff 1995).
The rest is shared by landslides, avalanches, glaciers, solifluction movements, and wind erosion.
A solifluction sheet directly buried level IA without affecting levels II or III.