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A glaciated valley in the Altai Mountains showing the characteristic U shape.
Malyovitsa U-shaped valley, Rila Mountain, Bulgaria

U-shaped valleys, trough valleys or glacial troughs, are formed by the process of glaciation. They are characteristic of mountain glaciation in particular.[1] They have a characteristic U shape, with steep, straight sides and a flat or rounded bottom (by contrast, valleys carved by rivers tend to be V-shaped in cross-section). Glaciated valleys are formed when a glacier travels across and down a slope, carving the valley by the action of scouring.[2] When the ice recedes or thaws, the valley remains, often littered with small boulders that were transported within the ice, called glacial till or glacial erratic.

Examples of U-valleys are found in mountainous regions like the Andes, Alps, Caucasus Mountains, Himalaya, Rocky Mountains, New Zealand and the Scandinavian Mountains. They are found also in other major European mountains including the Carpathian Mountains, the Pyrenees, the Rila and Pirin mountains in Bulgaria, and the Scottish Highlands. A classic glacial trough is in Glacier National Park in Montana, USA in which the St. Mary River runs. Another famous U-shaped valley is the Nant Ffrancon Valley in Snowdonia, Wales.


Glacier Valley formation
Illustration of a U-shaped valley being formed


Formation of a U-shaped valley happens over geologic time, meaning not during a human's lifespan. It can take anywhere between 10,000 and 100,000 years for a V-shaped valley to be carved into a U-shaped valley.[3] These valleys can be several thousand feet deep and tens of miles long.[1] Glaciers will spread out evenly in open areas, but tend to carve deep into the ground when confined to a valley.[1] Ice thickness is a major contributing factor to valley depth and carving rates. As a glacier moves downhill through a valley, usually with a stream running through it, the shape of the valley is transformed. As the ice melts and retreats, the valley is left with very steep sides and a wide, flat floor. This parabolic shape is caused by glacial erosion removing the contact surfaces with greatest resistance to flow, and the resulting section minimises friction.[4] There are two main variations of this U-shape. The first is called the Rocky Mountain model and it is attributed to alpine glacial valleys, showing an overall deepening effect on the valley. The second variation is referred to as the Patagonia-Antarctica model, attributed to continental ice sheets and displaying an overall widening effect on its surroundings.[4]

Valley floorEdit

The floors of these glacial valleys is where the most evidence can be found regarding glaciation cycles. For the most part, the valley floor is wide and flat, but there are various glacial features that signify periods of ice transgression and regression. The valley can have various steps, known as valley steps, and over-deepenings anywhere from ten to hundreds of meters deep.[3] These then fill in with sediments to create plains or water to create lakes, sometimes referred to as "string-of-pearl" or ribbon lakes.[3] Such water filled U-valley basins are also known as "fjord-lakes" or "valley-lakes" (Norwegian: fjordsjø or dalsjø). Gjende and Bandak lakes in Norway are examples of fjord-lakes. Some of these fjord-lakes are very deep for instance Mjøsa (453 meters) and Hornindalsvatnet (514 m). The longitudinal profile of a U-shaped, glaciated valley is often stepwise where flat basins are interrupted by thresholds. Rivers often dig a V-shaped valley or gorge through the threshold.[5][6][7]

Surrounding smaller tributary valleys will often join the main valleys during glaciation periods, leaving behind features known as hanging valleys high in the trough walls after the ice melts.

After deglaciation, snow and ice melt from the mountain tops can create streams and rivers in U-shaped valleys. These are referred to as misfit streams. The streams that form in hanging valleys create waterfalls that flow into the main valley branch. The glacial valleys can also have natural dam-like structures cutting through them, these are called terminal moraines. They are created due to excess sediment and glacial till moved and deposited by the glacier.

In volcanic mountain ranges, such as the Principal Cordillera of the Andes, glacial valley floors may be covered by thick lava flows.[8]

Trough endEdit

A glacial trough or glaciated mountain valley often ends in an abrupt head known as the 'trough end' or 'trough head'.[9] This may have almost sheer rock walls and spectacular waterfalls.[9][10] They are believed to have been formed where a number of small glaciers merge to produce a much larger glacier.[9] Examples include: Warnscale Bottom in the Lake District, Yosemite Valley, and the Rottal and Engstlige valleys in Switzerland.[9][10]

Marine troughsEdit

Submarine glacial troughs may also exist on continental shelves, such as the Laurentian Channel. These geomorphic features significantly influence sediment distribution and biological communities through their modification of current patterns.[11]


Geologists did not always believe that glaciers were responsible for U-shaped valleys and other glacial erosional features. Ice is quite soft and it was unbelievable to many that it could be responsible for the severe carving of bedrock characteristic of glacial erosion. German geologist Penck and American geologist Davis were vocal supporters of this unprecedented glacial erosion.[12]

Progress was made in the 1970s and 1980s on the possible mechanisms of glacial erosion and U-shaped valleys via models proposed by various scientists. Numerical models have been created to explain the phenomenon of carving U-shaped valleys.[3]

See alsoEdit


  1. ^ a b c "glacial valley | geological formation". Encyclopedia Britannica. Retrieved 2017-05-23.
  2. ^ "Glacial Trough/U-Shaped Valley". Illustrated Glossary of Alpine Glacial Landforms. Department of Geography, Central Michigan University. Retrieved 8 August 2019.
  3. ^ a b c d Waddington, E. D.; Anderson, S. P.; Anderson, R. S.; MacGregor, K. R. (November 2000). "Geology". 28 (11): 1031–1034. doi:10.1130/0091-7613(2000)28<1031:NSOGLP>2.0.CO;2. Cite journal requires |journal= (help)
  4. ^ a b "Wiley Online Library". doi:10.1002/esp.3290130805. Cite journal requires |journal= (help)
  5. ^ Karlsen, Ole G. (1981). Delta: naturgeografi for den videregående skolen. Oslo: TANO. ISBN 8251814782.
  6. ^ Hamblin, P. F., & Carmack, E. C. (1978). River‐induced currents in a Fjord Lake. Journal of Geophysical Research: Oceans, 83(C2), 885–899.
  7. ^ Gjessing, Just (1978). Norges landformer. Oslo: Universitetsforl. ISBN 8200017729.
  8. ^ Charrier, Reynaldo; Iturrizaga, Lafasam; Charretier, Sebastién; Regard, Vincent (2019). "Geomorphologic and Glacial Evolution of the Cachapoal and southern Maipo catchments in the Andean Principal Cordillera, Central Chile (34°-35º S)". Andean Geology. 46 (2): 240–278. doi:10.5027/andgeoV46n2-3108. Retrieved June 9, 2019.
  9. ^ a b c d Blackie, Blackie's Dictionary of Geography, Mumbai: Blackie, 2000, p. 344.
  10. ^ a b Monkhouse, F.J., Dictionary of Geography, London: AldineTransaction, 1970, p.359.
  11. ^ Buhl-Mortensen L, et al. (2012). "51 – Banks, Troughs, and Canyons on the Continental Margin off Lofoten, Vesterålen, and Troms, Norway". Seafloor Geomorphology as Benthic Habitat. pp. 703–715. doi:10.1016/B978-0-12-385140-6.00051-7. ISBN 978-0-12-385140-6.
  12. ^ Bierman; et al. Key Concepts in Geomorphology.

Further readingEdit