Aufeis (/ˈaʊfaɪs/OW-fysse) (German for "ice on top") is a sheet-like mass of layered ice that forms from successive flows of ground or river water during freezing temperatures. This form of ice is also called overflow, icings,[1] or the Russian term, naled (Russian: наледь). The term "Aufeis" was first used in 1859 by Alexander von Middendorff following his observations of the phenomenon in northern Siberia.
When thawed, aufeis leave footprints in the form of aufeis glades or, perhaps more accurately in tundra habitats, aufeis barrens, because of the near absence of vascular plants due to ice cover during much of the growing season.
Aufeis literally translates from German to “on-ice”. In 1859 the Baltic German scientist and explorer Alexander von Middendorff used this term to describe his observations of the phenomenon in northern Siberia.[2][3][4]
Aufeis accumulates during winter along stream and river valleys in arctic and subarctic environments. It forms by upwelling of river water behind ice dams, or by ground-water discharge. The latter mechanism prevails in high-gradient alpine streams as they freeze solid. Ground-water discharge is blocked by ice, perturbing the steady-state condition and causing a small incremental rise in the local water table until discharge occurs along the bank and over the top of the previously formed ice. Successive ice layers can grow and expand, attaining areas of ~25+ km2 and thicknesses of 6+ m.[5] Aufeis typically melts out during summer and will often form in the same place year after year.[6]
River aufeis form when the cross-sectional area of a stream channel becomes locally restricted as ice accumulates during winter. Such restrictions or “choke-points” result in bulk overflow and local increases in hydrostatic pressure, causing water to move upward through fissures onto the original ice layer.[7][8][1] This overflowing water subsequently freezes to produce additional ice layers, thus explaining the origin of the term aufeis.[2] This process, repeated through the long arctic winter, can generate large volumes of ice, with some aufeis in arctic Alaska—where they are also known as “icings”—attaining areas of 20+ km2[1][9] and localized thicknesses of 6+ m.[10] The cumulative area of late-winter aufeis in the Sagavanirktok River drainage alone, for example, ranges from 102 to 103 km2.[11]
Backpackers cross a sheet of aufeis in the Anaktuvuk River Valley of Alaska
Sheets of aufeis may block stream channels and cause their flood plains to widen as spring floodwaters are forced to flow around the ice.[12] Research on aufeis has to a large extent been motivated by the variety of engineering problems the ice sheets can cause (e.g. blocking drainages and causing flooding of roads).[13]
Aufeis can present an extreme danger to recreational boaters even during summer months, who can find themselves trapped between walls of ice or pulled under aufeis by the current of the river. Breaking dams of aufeis can cause flash floods downriver.[14]
When thawed, aufeis leave footprints in the form of “aufeis glades”[7] or more accurately in tundra habitats, aufeis barrens, because of the near absence of vascular plants due to ice cover during much of the growing season. Aufeis barrens are distinctive landscape features of the arctic tundra and provide reliable indicators of aufeis locations[8][7][15]".[5]
In late 2011, Mongolia planned to test the use and storage of artificial naleds as a way of cooling Ulan Bator in the hot Mongolian summer, and reducing the use of energy-intensive air conditioning.[16]
River aufeis are common and widespread features of the arctic cryosphere, particularly in northern Alaska and Siberia.[8][7] In eastern Siberia, where aufeis are known as naleds, 10,000 aufeis with a cumulative area of ~ 50,000 km2 containing 30 km3 of water have been documented in 2015.[7][17]
Analysis of satellite imagery from 2000 to 2015 has shown that the extent and duration of many Alaskan river icings has decreased due to climate change.[26]
^Veillette, J.J.; Thomas, R.D. (November 1979). "Icings and seepage in frozen glacio-fluvial deposits, District of Keewatin, NWT". Canadian Geotechnical Journal. 16 (4): 789–798. doi:10.1139/t79-084.
^Reedyk, Sharon; Woo, Ming-Ko; Prowse, Terry D. (1995). "Contribution of icing ablation to streamflow in a discontinuous permafrost area". Canadian Journal of Earth Sciences. 32 (1): 13–20. Bibcode:1995CaJES..32...13R. doi:10.1139/e95-002.
^Clark, Ian D.; Lauriol, Bernard (1997). "Aufeis of the Firth River Basin, Northern Yukon, Canada: Insights into Permafrost Hydrogeology and Karst". Arctic and Alpine Research. 29 (2): 240–252. doi:10.2307/1552053. JSTOR1552053.
^Priesnitz, Kuno; Schunke, Ekkehard (2002). "The fluvial morphodynamics of two small permafrost drainage basins, northwestern Canada". Permafrost and Periglacial Processes. 13 (3): 207–217. doi:10.1002/ppp.424. S2CID130985786.
^Alekseev, V.; Savko, N. (1975). The theory of naled processes. Nayka. pp. 1–205.
Wanty, Richard B.; Wang, Bronwen; Vohden, Jim; et al. (2007). Gough, Larry P.; Day, Warren C. (eds.). Aufeis Accumulations in Stream Bottoms in Arctic and Subarctic Environments as an Indicator of Geologic Structure(PDF). Recent U.S. Geological Survey Studies in the Tintina Gold Province, Alaska, United States, and Yukon, Canada — Results of a 5-Year Project (Report). Vol. Scientific Investigations Report 2007–5289–F. U.S. Department of the Interior and U.S. Geological Survey.
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