Sandurs are found in glaciated areas, such as Svalbard, Kerguelen Islands, and Iceland. Glaciers and icecaps contain large amounts of silt and sediment, picked up as they erode the underlying rocks when they move slowly downhill, and at the snout of the glacier, meltwater can carry this sediment away from the glacier and deposit it on a broad plain. The material in the outwash plain is often size-sorted by the water runoff of the melting glacier with the finest materials, like silt, being the most distantly re-deposited, whereas larger boulders are the closest to the original terminus of the glacier.
An outwash plain might contain surficial braided stream complexes that rework the original deposits. They may also contain kettle lakes, locations where blocks of ice have melted, leaving a depression that fills with water. The flow pattern of glacial rivers across sandar is typically diffuse and unchannelized, but in situations where the glacial snout has retreated from the terminal moraine, the flow is more channelized.
Sandurs are most common in Iceland, where geothermal activity beneath ice caps speeds up the deposition of sediment by meltwater. As well as regular geothermal activity, volcanic activity gives rise to large glacial bursts several times a century, which carry down large volumes of sediment.
The prototype sandur
The original sandur from which the general name is derived is Skeiðarársandur, a broad sandy wasteland along Iceland's south-eastern coast, between the Vatnajökull icecap and the sea. Skeiðarársandur is the largest sandur in the world, covering an area of 1,300 km2 (500 sq mi). Volcanic eruptions under the icecap have given rise to many large glacial bursts (jökulhlaups in Icelandic), most recently in 1996, when the Ring Road was washed away (minor floods have also occurred since then). This road, which encircles Iceland and was completed in 1974, has since been repaired. The 1996 jökulhlaup was caused by the eruption of the Grímsvötn volcano, with peak flow estimated to be 50,000 m3/s (1,800,000 cu ft/s) compared to the normal summer peak flow of 200 to 400 m3/s (7,100–14,100 cu ft/s). Net deposition of sediment was estimated to be 12,800,000 m3 (450,000,000 cu ft).
The main braided channels of Skeiðarársandur are the Gígjukvísl and Skeiðará rivers, which incurred net gains of 29 and 24 cm (11.4 and 9.4 in) respectively during the 1996 jökulhlaup. In the Gígjukvísl there was massive sediment deposition of up to 12 m (39 ft), which occurred closest to the terminus of the glacier. The erosional patterns of Skeiðarársandur can be seen by looking at the centimetre-scale elevation differences measured with repeat-pass laser altimetry (LIDAR) flown in 1996 (pre-flood), 1997, and 2001. Of the overall deposition during the 1996 jökulhlaup, nearly half of the net gain had been eroded 4 years after the flood. These two rivers on the sandur display drastically different erosional patterns. The difference in sediment erosion can be attributed to the 2 km (1.2 mi) wide trench near the terminus where the Gígjukvísl flows, in contrast with the Skeiðará, which has braided flows directly onto the outwash plain. The Gígjukvísl river is where some of the highest level of sediment deposit occurred and also where the largest erosion happened afterward. This indicates that these massive jökulhlaup deposits may have a large geomorphic impact in the short term, but the net change on the surface relief could be minimal after a couple years to a decade.
The observed change of Skeiðarársandur from a diffuse to a channelized distributary system where it has the most observed sediment deposit has a significant impact on the development of the fluvial succession in the proximal zone. However in order to have sustained active accretion across the entire sandur there needs to be a diffuse, multipoint distribution system. The system of accumulation on Skeiðarársandur, which is a product of glacier retreat, can be seen as multiple regions of differing channel patterns that distribute sediment across the plain in dynamic configurations.
- Ritter, Dale F., R. Craig Kochel, & Jerry Russell Miller. 1995. Process geomorphology. Dubuque, IA: Wm C. Brown, p. 349.
- Whittow, John (1984). Dictionary of Physical Geography. London: Penguin, 1984, p. 467. ISBN 0-14-051094-X.
- Gornitz, Vivien (ed.). 2009. Encyclopedia of Paleoclimatology And Ancient Environments. Springer: Dordrecht, p. 665.
- Leffman, David; Proctor, James (2004). The Rough Guide to Iceland. Rough Guides. p. 28.
- Church, Michael A. (1972), Baffin Island sandurs: a study of arctic fluvial processes.
- Garvin J.B. (2001), Topographic Dynamics of Kerguelen Island: A Preliminary SRTM Analysis, American Geophysical Union, Fall Meeting 2001
- Gomez B., Russell A.J., Finnegan D.C., Smith L.C., Knudsen O. (2001), Sediment Distribution on Skeidararsandur, Southeast Iceland, American Geophysical Union, Fall Meeting 2001
- Hardardottir J., Snorrason A., Zophoniasson S., Jonsson P., Sigurdsson O., Elefsen S.O. (2003), Glacial Outburst Floods (Jökulhlaups) in Iceland, EGS - AGU - EUG Joint Assembly, Abstracts from the meeting held in Nice, France, 6–11 April 2003
- Magilligan F.J., Gomez B., Mertes L.A.K., Smith, L.C. Smith N.D., Finnegan D., Garvin J.B., Geomorphic effectiveness, sandur development, and the pattern of landscape response during jökulhlaups: Skeiðarársandur, southeastern Iceland, Geomorphology 44 (2002) 95–113
- Hétu, B., La déglaciation de la région de Rimouski, Bas-Saint-Laurent (Québec): Indices d'une récurrence glaciaire dans la mer de Goldthwait entre 12400 et 12000 BP, Géographie physique et Quaternaire, 1998, vol. 52, n.3, p. 325-347
- Smith L.C., Sheng Y., Magilligan F.J., Smith N.D., Gomez B., Mertes L., Krabill W.B., Garven J.B., Geomorphic impact and rapid subsequent recovery from the 1996 Skeiðarársandur jökulhlaup, Iceland, measured with multi-year airborne lidar. Geomorphology vol. 75 Is. 1-2 (2006) 65-75
Lua error in Module:Coordinates at line 668: callParserFunction: function "#coordinates" was not found.