There are 184 oceanic plateaus covering an area of 18,486,600 km2 (7,137,700 sq mi), or about 5.11% of the oceans. The South Pacific region around Australia and New Zealand contains the greatest number of oceanic plateaus (see map).
Oceanic plateaus produced by large igneous provinces are often associated with hotspots, mantle plumes, and volcanic islands — such as Iceland, Hawaii, Cape Verde, and Kerguelen. The three largest plateaus, the Caribbean, Ontong Java, and Mid-Pacific Mountains, are located on thermal swells. Other oceanic plateaus, however, are made of rifted continental crust, for example Falkland Plateau, Lord Howe Rise, and parts of Kerguelen, Seychelles, and Arctic ridges. Plateaus formed by large igneous provinces were formed by the equivalent of continental flood basalts such as the Deccan Traps in India and the Snake River Plain in the United States.
In contrast to continental flood basalts, most igneous oceanic plateaus erupt through young and thin (6–7 km (3.7–4.3 mi)) mafic or ultra-mafic crust and are therefore uncontaminated by felsic crust and representative for their mantle sources. These plateaus often rise 2–3 km (1.2–1.9 mi) above the surrounding ocean floor and are more buoyant than oceanic crust. They therefore tend to withstand subduction, more-so when thick and when reaching subduction zones shortly after their formations. As a consequence, they tend to "dock" to continental margins and be preserved as accreted terranes. Such terranes are often better preserved than the exposed parts of continental flood basalts and are therefore a better record of large-scale volcanic eruptions throughout Earth's history. This "docking" also means that oceanic plateaus are important contributors to the growth of continental crust. Their formations often had a dramatic impact on global climate, such as the most recent plateaus formed, the three, large, Cretaceous oceanic plateaus in the Pacific and Indian Ocean: Ontong Java, Kerguelen, and Caribbean.
Role in crust–mantle recycling
Geologists believe that igneous oceanic plateaus may well represent a stage in the development of continental crust as they are generally less dense than oceanic crust while still being denser than normal continental crust.
Density differences in crustal material largely arise from different ratios of various elements, especially silicon. Continental crust has the highest amount of silicon (such rock is called felsic). Oceanic crust has a smaller amount of silicon (mafic rock). Igneous oceanic plateaus have a ratio intermediate between continental and oceanic crust, although they are more mafic than felsic.
However, when a plate carrying oceanic crust subducts under a plate carrying an igneous oceanic plateau, the volcanism which erupts on the plateau as the oceanic crust heats up on its descent into the mantle erupts material which is more felsic than the material which makes up the plateau. This represents a step toward creating crust which is increasingly continental in character, being less dense and more buoyant. If an igneous oceanic plateau is subducted underneath another one, or under existing continental crust, the eruptions produced thereby produce material that is yet more felsic, and so on through geologic time.
List of oceanic plateaus
Continental oceanic plateaus
Igneous oceanic plateaus
- Agulhas Plateau (Southwest Indian)
- Azores Plateau (North Atlantic)
- Broken Ridge Plateau (Indian)
- Caribbean-Colombian Plateau (Caribbean)
- Exmouth Plateau (Indian)
- Hikurangi Plateau (Southwest Pacific)
- Iceland Plateau (North Atlantic)
- Kerguelen Plateau (Indian)
- Magellan Rise (Pacific)
- Manihiki Plateau (Southwest Pacific)
- Mascarene Plateau (Indian)
- Naturaliste Plateau (Indian)
- Ontong Java Plateau (Southwest Pacific)
- Shatsky Rise (North Pacific)
- Vøring Plateau (North Atlantic)
- Wrangellia Terrane (Northeast Pacific)
- Yermak Plateau (Arctic)
- IHO 2013, pp. 2–12
- Harris et al. 2014, Plateaus (Supplementary Table 20), p. 16
- Mooney, Laske & Masters 1998, Anomalous Crust: Oceanic Plateaus, Hotspots, and Rifts, pp. 754–755
- Kerr 2013, p. 632
- Harris et al. 2014, Supplementary table 20
- Boldreel & Andersen 1994, p. 163
- Uenzelmann-Neben, Gohl & Ehrhardt 1999
- Hildenbrand, Anthony; Weis, Dominique; Madureira, Pedro; Margues, Fernando Ornelas (2014). "Recent plate re-organization at the Azores Triple Junction: Evidence from combined geochemical and geochronological data on Faial, S. Jorge and Terceira volcanic islands". Lithos. 210: 27. Bibcode:2014Litho.210...27H. doi:10.1016/j.lithos.2014.09.009. ISSN 0024-4937.
- Boldreel, L. O.; Andersen, M. S. (1994). "Tertiary development of the Faeroe-Rockall Plateau based on reflection seismic data". Bulletin of the Geological Society of Denmark. 41 (2): 162–180. Retrieved 1 May 2017.
- Harris, P. T.; Macmillan-Lawler, M.; Rupp, J.; Baker, E. K. (2014). "Geomorphology of the oceans". Marine Geology. 352: 4–24. Bibcode:2014MGeol.352....4H. doi:10.1016/j.margeo.2014.01.011. Retrieved 30 April 2017.
- IHO (September 2013). Standardization of Undersea Feature Names B-6 (PDF) (Report) (4.1.0 ed.). Monaco: International Hydrographic Organization. Retrieved 30 April 2017. (updated February 2017)
- Kerr, A. C. (2013). "Oceanic plateau". In Holland, H. D.; Turekian, K. K. (eds.). Treatise on Geochemistry (2nd ed.). Amsterdam; San Diego, CA, USA: Elsevier. pp. 631–667. doi:10.1016/B978-0-08-095975-7.00320-X. ISBN 9780080983004. OCLC 864682251. Retrieved 30 April 2017.
- Mooney, W. D.; Laske, G.; Masters, T. G. (1998). "CRUST 5.1: A global crustal model at 5°×5°". Journal of Geophysical Research: Solid Earth. 103 (B1): 727–747. Bibcode:1998JGR...103..727M. doi:10.1029/97JB02122. Retrieved 30 April 2017.
- Uenzelmann-Neben, G.; Gohl, K.; Ehrhardt, A.; Seargent, M. (1999). "Agulhas Plateau, SW Indian Ocean: New Evidence for Excessive Volcanism" (PDF). Geophysical Research Letters. 26 (13): 1941–1944. Bibcode:1999GeoRL..26.1941U. doi:10.1029/1999gl900391.