Oceanic basin

Diagrammatic cross-section of an ocean basin, showing the various geographic features

In hydrology, an oceanic basin may be anywhere on Earth that is covered by seawater, but geologically, ocean basins are large geologic basins that are below sea level. Geologically, there are other undersea geomorphological features such as the continental shelves, the deep ocean trenches, and the undersea mountain ranges (for example, the Mid-Atlantic Ridge and the Emperor Seamounts) which are not considered to be part of the ocean basins; while hydrologically, oceanic basins include the flanking continental shelves and the shallow epeiric seas.


Three types of plate boundary

The Earth is composed of a magnetic central core, a mostly liquid mantle and a hard rigid outer shell (or lithosphere), which is composed of the Earth's rocky crust and the deeper mostly solid outer layer of the mantle. On land the crust is known as the continental crust while under the sea it is known as the oceanic crust. The latter is composed of relatively dense basalt and is some five to ten kilometres (three to six miles) thick. The relatively thin lithosphere floats on the weaker and hotter mantle below and is fractured into a number of tectonic plates.[1] In mid-ocean, magma is constantly being thrust through the seabed between adjoining plates to form mid-oceanic ridges and here convection currents within the mantle tend to drive the two plates apart. Parallel to these ridges and nearer the coasts, one oceanic plate may slide beneath another oceanic plate in a process known as subduction. Deep trenches are formed here and the process is accompanied by friction as the plates grind together. The movement proceeds in jerks which cause earthquakes, heat is produced and magma is forced up creating underwater mountains, some of which may form chains of volcanic islands near to deep trenches. Near some of the boundaries between the land and sea, the slightly denser oceanic plates slide beneath the continental plates and more subduction trenches are formed. As they grate together, the continental plates are deformed and buckle causing mountain building and seismic activity.[2][3]

The Earth's deepest trench is the Mariana Trench which extends for about 2,500 kilometres (1,600 mi) across the seabed. It is near the Mariana Islands, a volcanic archipelago in the West Pacific. Its deepest point is 10.994 kilometres (nearly 7 miles) below the surface of the sea.[4] An even longer trench runs alongside the coast of Peru and Chile, reaching a depth of 8,065 metres (26,460 ft) and extending for approximately 5,900 kilometres (3,700 mi). It occurs where the oceanic Nazca Plate slides under the continental South American Plate and is associated with the upthrust and volcanic activity of the Andes.[5]


Older references (e.g., Littlehales 1930)[6] consider the oceanic basins to be the complement to the continents, with erosion dominating the latter, and the sediments so derived ending up in the ocean basins. More modern sources (e.g., Floyd 1991)[7] regard the ocean basins more as basaltic plains, than as sedimentary depositories, since most sedimentation occurs on the continental shelves and not in the geologically-defined ocean basins.[8]

Hydrologically some geologic basins are both above and below sea level, such as the Maracaibo Basin in Venezuela, although geologically it is not considered an oceanic basin because it is on the continental shelf and underlain by continental crust.

Earth is the only known planet in the solar system where hypsography is characterized by different kinds of crust, oceanic crust and continental crust.[9] Oceans cover 70% of the Earth's surface. Because oceans lie lower than continents, the former serve as sedimentary basins that collect sediment eroded from the continents, known as clastic sediments, as well as precipitation sediments. Ocean basins also serve as repositories for the skeletons of carbonate- and silica-secreting organisms such as coral reefs, diatoms, radiolarians, and foraminifera.

Geologically, an oceanic basin may be actively changing size or may be relatively, tectonically inactive, depending on whether there is a moving plate tectonic boundary associated with it. The elements of an active - and growing - oceanic basin include an elevated mid-ocean ridge, flanking abyssal hills leading down to abyssal plains. The elements of an active oceanic basin often include the oceanic trench associated with a subduction zone.

The Atlantic ocean and the Arctic ocean are good examples of active, growing oceanic basins, whereas the Mediterranean Sea is shrinking. The Pacific Ocean is also an active, shrinking oceanic basin, even though it has both spreading ridge and oceanic trenches. Perhaps the best example of an inactive oceanic basin is the Gulf of Mexico, which formed in Jurassic times and has been doing nothing but collecting sediments since then.[10] The Aleutian Basin[11] is another example of a relatively inactive oceanic basin. The Japan Basin in the Sea of Japan which formed in the Miocene, is still tectonically active although recent changes have been relatively mild.[12]

See also


  1. ^ Pidwirny, Michael (28 March 2013). "Structure of the Earth". The Encyclopedia of Earth. Retrieved 20 September 2013.
  2. ^ Pidwirny, Michael (28 March 2013). "Plate tectonics". The Encyclopedia of Earth. Retrieved 20 September 2013.
  3. ^ "Plate Tectonics: The Mechanism". University of California Museum of Paleontology. Retrieved 20 September 2013.
  4. ^ "Scientists map Mariana Trench, deepest known section of ocean in the world". The Telegraph. 7 December 2011. Retrieved 24 September 2013.
  5. ^ "Peru-Chile Trench". Encyclopedia Britannica. Britannica Online Encyclopedia. Retrieved 24 September 2013.
  6. ^ Littlehales, G. W. (1930) The configuration of the oceanic basins Graficas Reunidas, Madrid, Spain, OCLC 8506548
  7. ^ Floyd, P. A. (1991) Oceanic basalts Blackie, Glasgow, Scotland, ISBN 978-0-216-92697-4
  8. ^ Biju-Duval, Bernard (2002) Sedimentary geology: sedimentary basins, depositional environments, petroleum formation Editions Technip, Paris, ISBN 978-2-7108-0802-2
  9. ^ Ebeling, Werner and Feistel, Rainer (2002) Physics of Self-Organization and Evolution Wiley-VCH, Weinheim, Germany, page 141, ISBN 978-3-527-40963-1
  10. ^ Huerta, Audrey D. and Harry, Dennis L. (2012) "Wilson cycles, tectonic inheritance, and rifting of the North American Gulf of Mexico continental margin" Geosphere 8(2): pp. 374–385, first published on March 6, 2012, doi:10.1130/GES00725.1
  11. ^ Verzhbitsky, E. V.; M. V. Kononov; V. D. Kotelkin (5 February 2007). "Plate Tectonics of the Northern Part of the Pacific Ocean". Oceanology (In Translation from Okeanologiya ). 47 (5): 705–717. Bibcode:2007Ocgy...47..705V. doi:10.1134/S000143700705013X. S2CID 140689505.
  12. ^ Clift, Peter D. (2004) Continent-Ocean Interactions Within East Asian Marginal Seas American Geophysical Union, Washington, D.C., pages 102–103, ISBN 978-0-87590-414-6

Further reading

External links

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