A submarine canyon is a steep-sided valley cut into the sea floor of the continental slope, sometimes extending well onto the continental shelf and having relief comparable to even the largest of land canyons. About 3% of submarine canyons are joined to shelf valleys that connect with large rivers; the largest canyons (equal to about 29% by number) incise into the continental shelf but the largest number of canyons (about 69%) terminate on the slope, making so-called “blind” or “headless” canyons. Canyons cutting the continental slopes have been found at depths greater than 2 km below sea level. Many submarine canyons continue as submarine channels across continental rise areas and may extend seawards for hundreds of kilometres onto the abyssal plain. Ancient examples have been found in rocks dating back to the Neoproterozoic. Turbidites are formed in submarine canyons.
Submarine canyons are more common on the steep slopes found on active margins compared to those on the gentler slopes found on passive margins. They show erosion through all substrates, from unlithified sediment to crystalline rock. Canyons are steeper, shorter, more dendritic and more closely spaced on active than on passive continental margins. The walls are generally very steep and can be near vertical. The walls are subject to erosion by bioerosion, or slumping. There are an estimated 9,477 submarine canyons on earth, covering about 11% of the continental slope.
- Avilés Canyon, the deepest submarine canyon in the world, southern Bay of Biscay, Spain. Up to 4,750 m from the slope.
- Amazon Canyon, extending from the Amazon River
- Baltimore and Wilmington Canyons, East Coast of Maryland and Delaware States
- Bering Canyon, in the Bering Sea
- Congo Canyon, the largest river canyon, extending from the Congo River, is 800 km (497 mi) long, and 1,200 m (3,900 ft) deep.
- Hudson Canyon, extending from the Hudson River
- Ganges Canyon, extending from the Ganges
- Indus Canyon, extending from the Indus River
- Kaikoura Canyon, extending offshore from the Kaikoura Peninsula, New Zealand
- La Jolla and Scripps Canyon, off the coast of La Jolla, southern California
- Monterey Canyon, off the coast of central California
- Pribilof Canyon, in the Bering Sea
- Whittard Canyon, Atlantic Ocean off southwest Ireland
- Zhemchug Canyon the largest submarine canyon in the world, in the Bering sea
Many mechanisms have been proposed for the formation of submarine canyons, and during the 1940s and 1950s the primary causes of submarine canyons were subject to active debate.
An early and obvious theory was that the canyons present today were carved during glacial times, when sea level was about 125 meters below present sea level, and rivers flowed to the edge of the continental shelf. However, while many (but not all) canyons are found offshore from major rivers, subaerial river erosion cannot have been active to the water depths as great as 3000 meters where canyons have been mapped, as it is well established (by many lines of evidence) that sea levels did not fall to those depths.
The major mechanism of canyon erosion is now thought to be turbidity currents and underwater landslides. Turbidity currents are dense, sediment-laden currents which flow downslope when an unstable mass of sediment that has been rapidly deposited on the upper slope fails, perhaps triggered by earthquakes. There is a spectrum of turbidity- or density-current types ranging from "muddy water" to massive mudflow, and evidence of both these end members can be observed in deposits associated with the deeper parts of submarine canyons and channels, such as lobate deposits (mudflow) and levees along channels.
Mass wasting, slumping, and submarine landslides are forms of slope failures (the effect of gravity on a hillslope) observed in submarine canyons. Mass wasting is the term used for the slower and smaller action of material moving downhill. Slumping is generally used for rotational movement of masses on a hillside. Landslides, or slides, generally comprise the detachment and displacement of sediment masses.
It is now understood that many mechanisms of submarine canyon creation have had effect to greater or lesser degree in different places, even within the same canyon, or at different times during a canyon's development. However, if a primary mechanism must be selected, the downslope lineal morphology of canyons and channels and the transportation of excavated or loose materials of the continental slope over extensive distances require that various kinds of turbidity or density currents act as major participants.
In addition to the processes described above, submarine canyons that are especially deep may form by another method. In certain cases, a sea with a bed significantly below sea level is cut off from the larger ocean to which it is usually connected. The sea which is normally repleted by contact and inflow from the ocean is now no longer replenished and hence dries up over a period of time, which can be very short if the local climate is arid. In this scenario, rivers that previously flowed into the sea at a sea level elevation now can cut far deeper into the bottom of the bed now exposed. The Messinian Salinity Crisis is an example of this phenomenon; between five and six million years ago, the Mediterranean Sea became isolated from the Atlantic Ocean and evaporated away in roughly a thousand years. During this time, the Nile River delta, among other rivers, extended far beyond its present location, both in depth and length. In a cataclysmic event, the Mediterranean sea basin was flooded. One relevant consequence is that the submarine canyons eroded are now far below the present sea level.
- Shepard, F.P., 1963. Submarine Geology. Harper & Row, New York
- Harris, P.T., Whiteway, T., 2011. Global distribution of large submarine canyons: geomorphic differences between active and passive continental margins. Marine Geology 285, 69–86.
- Giddings, J.A.; Wallace M.W.; Haines P.W.; Mornane K. (2010). "Submarine origin for the Neoproterozoic Wonoka canyons, South Australia". Sedimentary Geology. Elsevier. 223 (1-2): 35–50. Bibcode:2010SedG..223...35G. doi:10.1016/j.sedgeo.2009.10.001. Retrieved 26 January 2012.
- Harris, P.T. (2011). "Seafloor Geomorphology–Coast, Shelf, and Abyss". In Harris P.T. & Baker E.K. Seafloor Geomorphology as Benthic Habitat: GeoHAB Atlas of Seafloor Geomorphic Features and Benthic Habitats. Elsevier. pp. 125–127. ISBN 978-0-12-385141-3. Retrieved 26 January 2012.
- Harris, P.T., MacMillan-Lawler, M., Rupp, J., Baker, E.K., 2014. Geomorphology of the oceans. Marine Geology 352, 4-24.
- Arthur Newell Strahler, Physical Geography. New York: John Wiley & Sons, Inc., 1960, Second Edition, p. 290