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Atoll

For other uses, see Atoll (disambiguation).

An atoll (/ˈæt.ɒl, -ɔːl, -oʊl, əˈtɒl, -ˈtɔːl, -ˈtoʊl/)[1] is a ring-shaped island, including a coral rim that encircles a lagoon. There may be coral islands or cays on the rim.[2][3]: 60  Atolls are located in warm tropical or subtropical parts of the oceans and seas where corals can develop. Most of the approximately 440 atolls in the world are in the Pacific Ocean.

The atoll of Tetiʻaroa in French Polynesia

Two different, well-cited models, the subsidence model and the antecedent karst model, have been used to explain the development of atolls.[4] According to Charles Darwin's subsidence model,[5] the formation of an atoll is explained by the sinking of a volcanic island around which a coral fringing reef has formed. Over geologic time, the volcanic island becomes extinct and eroded as it subsides completely beneath the surface of the ocean. As the volcanic island subsides, the coral fringing reef becomes a barrier reef that is detached from the island. Eventually, reef and the small coral islets on top of it are all that is left of the original island, and a lagoon has taken the place of the former volcano. The lagoon is not the former volcanic crater. For the atoll to persist, the coral reef must be maintained at the sea surface, with coral growth matching any relative change in sea level (sinking of the island or rising oceans).[4]

An alternative model for the origin of atolls is called the antecedent karst model. In the antecedent karst model, the first step in the formation of an atoll is the development of a flat top, mound-like coral reef during the subsidence of an oceanic island of either volcanic or nonvolcanic origin below sea level. Then, when relative sea level drops below the level of the flat surface of coral reef, it is exposed to the atmosphere as a flat topped island which is dissolved by rainfall to form limestone karst. Because of hydrologic properties of this karst, the rate of dissolution of the exposed coral is lowest along its rim and the rate of dissolution increases inward to its maximum at the center of the island. As a result, a saucer shaped island with a raised rim forms. When relative sea level submerges the island again, the rim provides a rocky core on which coral grow again to form the islands of an atoll and the flooded bottom of the saucer forms the lagoon within them.[4][6]

Usage

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The word atoll comes from the Dhivehi word atholhu (އަތޮޅު, pronounced [ˈat̪oɭu]). Dhivehi is an Indo-Aryan language spoken in the Maldives. The word's first recorded English use was in 1625 as atollon. Charles Darwin coined the term in his monograph, The Structure and Distribution of Coral Reefs. He recognized the word's indigenous origin and defined it as a "circular group of coral islets", synonymously with "lagoon-island".[5]: 2 

More modern definitions of atoll describe them as "annular reefs enclosing a lagoon in which there are no promontories other than reefs and islets composed of reef detritus"[7] or "in an exclusively morphological sense, [as] a ring-shaped ribbon reef enclosing a lagoon".[8]

Distribution and size

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There are approximately 440 atolls in the world.[9] Most of the world's atolls are in the Pacific Ocean (with concentrations in the Caroline Islands, the Coral Sea Islands, the Marshall Islands, the Tuamotu Islands, Kiribati, Tokelau, and Tuvalu) and the Indian Ocean (the Chagos Archipelago, Lakshadweep, the atolls of the Maldives, and the Outer Islands of Seychelles). In addition, Indonesia also has several atolls spread across the archipelago, such as in the Thousand Islands, Taka Bonerate Islands, and atolls in the Raja Ampat Islands. The Atlantic Ocean has no large groups of atolls, other than eight atolls east of Nicaragua that belong to the Colombian department of San Andres and Providencia in the Caribbean.

Reef-building corals will thrive only in warm tropical and subtropical waters of oceans and seas, and therefore atolls are found only in the tropics and subtropics. The northernmost atoll in the world is Kure Atoll at 28°25′ N, along with other atolls of the Northwestern Hawaiian Islands. The southernmost atolls in the world are Elizabeth Reef at 29°57′ S, and nearby Middleton Reef at 29°27′ S, in the Tasman Sea, both of which are part of the Coral Sea Islands Territory. The next southerly atoll is Ducie Island in the Pitcairn Islands Group, at 24°41′ S. The atoll closest to the Equator is Aranuka of Kiribati. Its southern tip is just 13 km (8 mi) north of the Equator.

Bermuda is sometimes claimed as the "northernmost atoll" at a latitude of 32°18′ N. At this latitude, coral reefs would not develop without the warming waters of the Gulf Stream. However, Bermuda is termed a pseudo-atoll because its general form, while resembling that of an atoll, has a very different origin of formation.

In most cases, the land area of an atoll is very small in comparison to the total area. Atoll islands are low lying, with their elevations less than 5 metres (16 ft). Measured by total area, Lifou (1,146 km2, 442 sq mi) is the largest raised coral atoll of the world, followed by Rennell Island (660 km2, 250 sq mi).[10] More sources, however, list Kiritimati as the largest atoll in the world in terms of land area. It is also a raised coral atoll (321 km2, 124 sq mi land area; according to other sources even 575 km2, 222 sq mi), 160 km2 (62 sq mi) main lagoon, 168 km2 (65 sq mi) other lagoons (according to other sources 319 km2, 123 sq mi total lagoon size).

The geological formation known as a reef knoll refers to the elevated remains of an ancient atoll within a limestone region, appearing as a hill. The second largest atoll by dry land area is Aldabra, with 155 km2 (60 sq mi). Huvadhu Atoll, situated in the southern region of the Maldives, holds the distinction of being the largest atoll based on the sheer number of islands it comprises, with a total of 255 individual islands.

 
Map from Charles Darwin's 1842 The Structure and Distribution of Coral Reefs showing the world's major groups of atolls and coral reefs

List of atolls

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Largest atolls by total area (lagoon plus reef and dry land)[11]
Name Position Location Land area (km2) Total area (km2) Notes
Great Chagos Bank 6°10′S 72°00′E / 6.17°S 72.00°E / -6.17; 72.00 Indian Ocean 4.5 12,642
Reed Bank 11°27′N 116°54′E / 11.45°N 116.90°E / 11.45; 116.90 Spratly Islands 8,866 Submerged, at shallowest 9 m
Macclesfield Bank 16°00′N 114°30′E / 16.00°N 114.50°E / 16.00; 114.50 South China Sea 6,448 Submerged, at shallowest 9.2 m
North Bank 9°04′S 60°12′E / 9.07°S 60.20°E / -9.07; 60.20 North of Saya de Malha Bank 5,800 Submerged, at shallowest <10 m
Rosalind Bank 16°26′N 80°31′W / 16.43°N 80.52°W / 16.43; -80.52 Caribbean 4,500 Submerged, at shallowest 7.3 m
Thiladhunmathi 6°44′N 73°02′E / 6.73°N 73.04°E / 6.73; 73.04 Maldives 51 3,850
Chesterfield Islands 19°21′S 158°40′E / 19.35°S 158.66°E / -19.35; 158.66 New Caledonia <10 3,500
Huvadhu Atoll 0°30′N 73°18′E / 0.50°N 73.30°E / 0.50; 73.30 Maldives 38.5 3,152
Chuuk Lagoon 7°25′N 151°47′E / 7.42°N 151.78°E / 7.42; 151.78 Chuuk, Micronesia 3,152
Sabalana Islands 6°45′S 118°50′E / 6.75°S 118.83°E / -6.75; 118.83 Indonesia 2,694
Lihou Reef 17°25′S 151°40′E / 17.42°S 151.67°E / -17.42; 151.67 Coral Sea 1 2,529
Bassas de Pedro 13°05′N 72°25′E / 13.08°N 72.42°E / 13.08; 72.42 Lakshadweep, India 2,474 Submerged, at shallowest 16.4 m
Ardasier Bank 7°43′N 114°15′E / 7.71°N 114.25°E / 7.71; 114.25 Spratly Islands 2,347
Kwajalein Atoll 9°11′N 167°28′E / 9.19°N 167.47°E / 9.19; 167.47 Marshall Islands 16.4 2,304
Diamond Islets Bank 17°25′S 150°58′E / 17.42°S 150.96°E / -17.42; 150.96 Coral Sea <1 2,282
Namonuito Atoll 8°40′N 150°00′E / 8.67°N 150.00°E / 8.67; 150.00 Chuuk, Micronesia 4.4 2,267
Ari Atoll 3°52′N 72°50′E / 3.86°N 72.83°E / 3.86; 72.83 Maldives 69 2,252
Maro Reef 25°25′N 170°35′W / 25.42°N 170.59°W / 25.42; -170.59 Northwestern Hawaiian Islands 1,934
Rangiroa 15°08′S 147°39′W / 15.13°S 147.65°W / -15.13; -147.65 Tuamotus 79 1,762
Kolhumadulu Atoll 2°22′N 73°07′E / 2.37°N 73.12°E / 2.37; 73.12 Maldives 79 1,617
Kaafu Atoll 4°25′N 73°30′E / 4.42°N 73.50°E / 4.42; 73.50 Maldives 69 1,565
Ontong Java Atoll 5°16′S 159°21′E / 5.27°S 159.35°E / -5.27; 159.35 Solomon Islands 12 1500
Lifou 20°58′S 167°14′E / 20.97°S 167.23°E / -20.97; 167.23 New Caledonia 1146 Raised atoll with no lagoon
Rennell 11°40′S 160°10′E / 11.67°S 160.17°E / -11.67; 160.17 Solomon Islands 660 Raised atoll with no lagoon
Kiritimati 1°51′N 157°24′W / 1.85°N 157.4°W / 1.85; -157.4 Kiribati 312 640
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Formation

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See also: Coral reef § Formation
 
Aerial view of Bora Bora, French Polynesia
 
Tarawa Atoll, Federated States of Micronesia
 
Bikini Atoll, Marshall Islands

In 1842, Charles Darwin[5] explained the creation of coral atolls in the southern Pacific Ocean based upon observations made during a five-year voyage aboard HMS Beagle from 1831 to 1836. Darwin's explanation suggests that several tropical island types: from high volcanic island, through barrier reef island, to atoll, represented a sequence of gradual subsidence of what started as an oceanic volcano. He reasoned that a fringing coral reef surrounding a volcanic island in the tropical sea will grow upward as the island subsides (sinks), becoming an "almost atoll", or barrier reef island, as typified by an island such as Aitutaki in the Cook Islands, and Bora Bora and others in the Society Islands. The fringing reef becomes a barrier reef for the reason that the outer part of the reef maintains itself near sea level through biotic growth, while the inner part of the reef falls behind, becoming a lagoon because conditions are less favorable for the coral and calcareous algae responsible for most reef growth. In time, subsidence carries the old volcano below the ocean surface and the barrier reef remains. At this point, the island has become an atoll.

As formulated by J. E. Hoffmeister,[13] F. S. McNeil,[14] E. G. Prudy,[6] and others, the antecedent karst model argues that atolls are Pleistocene features that are the direct result of the interaction between subsidence and preferential karst dissolution that occurred in the interior of flat topped coral reefs during exposure during glacial lowstands of sea level. The elevated rims along an island created by this preferential karst dissolution become the sites of coral growth and islands of atolls when flooded during interglacial highstands.

The research of A. W. Droxler and others[4] supports the antecedent karst model as they found that the morphology of modern atolls are independent of any influence of an underlying submerged and buried island and are not rooted to an initial fringing reef/barrier reef attached to a slowly subsiding volcanic edifice. In fact, the Neogene reefs underlying the studied modern atolls overlie and completely bury the subsided island are all non-atoll, flat-topped reefs. In fact, they found that atolls did not form doing the subsidence of an island until MIS-11, Mid-Brunhes, long after the many the former islands had been completely submerged and buried by flat topped reefs during the Neogene.

Atolls are the product of the growth of tropical marine organisms, and so these islands are found only in warm tropical waters. Volcanic islands located beyond the warm water temperature requirements of hermatypic (reef-building) organisms become seamounts as they subside, and are eroded away at the surface. An island that is located where the ocean water temperatures are just sufficiently warm for upward reef growth to keep pace with the rate of subsidence is said to be at the Darwin Point. Islands in colder, more polar regions evolve toward seamounts or guyots; warmer, more equatorial islands evolve toward atolls, for example Kure Atoll. However, ancient atolls during the Mesozoic appear to exhibit different growth and evolution patterns.[15][16]

  •  
    Darwin's theory starts with a volcanic island which becomes extinct
  •  
    As the island and ocean floor subside, coral growth builds a fringing reef, often including a shallow lagoon between the land and the main reef
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    As the subsidence continues the fringing reef becomes a larger barrier reef farther from the shore with a bigger and deeper lagoon inside
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    Ultimately the island sinks below the sea, and the barrier reef becomes an atoll enclosing an open lagoon

Coral atolls are important as sites where dolomitization of calcite occurs. Several models have been proposed for the dolomitization of calcite and aragonite within them. They are the evaporative, seepage-reflux, mixing-zone, burial, and seawater models. Although the origin of replacement dolomites remains problematic and controversial, it is generally accepted that seawater was the source of magnesium for dolomitization and the fluid in which calcite was dolomitized to form the dolomites found within atolls. Various processes have been invoked to drive large amounts of seawater through an atoll in order for dolomitization to occur.[17][18][19]

Investigation by the Royal Society of London

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Aerial overview of the Wake Island atoll, part of the Pacific Remote Islands Marine National Monument

In 1896, 1897 and 1898, the Royal Society of London carried out drilling on Funafuti atoll in Tuvalu for the purpose of investigating the formation of coral reefs. They wanted to determine whether traces of shallow water organisms could be found at depth in the coral of Pacific atolls. This investigation followed the work on the structure and distribution of coral reefs conducted by Charles Darwin in the Pacific.

The first expedition in 1896 was led by Professor William Johnson Sollas of the University of Oxford. Geologists included Walter George Woolnough and Edgeworth David of the University of Sydney. Professor Edgeworth David led the expedition in 1897.[20] The third expedition in 1898 was led by Alfred Edmund Finckh.[21][22][23]

See also

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References

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Inline citations

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  1. ^ "atoll". Dictionary.com Unabridged (Online). n.d.
  2. ^ Migoń, Piotr, ed. (2010). Geomorphological Landscapes of the World. Springer. p. 349. ISBN 978-90-481-3055-9. Retrieved 12 February 2013.
  3. ^ Blake, Gerald Henry, ed. (1994). World Boundary Series. Vol. 5 Maritime Boundaries. Routledge. ISBN 978-0-415-08835-0. Retrieved 12 February 2013.
  4. ^ a b c d Droxler, A.W. and Jorry, S.J., 2021. The Origin of Modern Atolls: Challenging Darwin's Deeply Ingrained Theory. Annual Review of Marine Science, 13, pp.537–573.
  5. ^ a b c Darwin, Charles R (1842). The structure and distribution of coral reefs. Being the first part of the geology of the voyage of the Beagle, under the command of Capt. Fitzroy, R.N. during the years 1832 to 1836. London: Smith Elder and Co – via Darwin Online.
  6. ^ a b Purdy, E. G., 1974. Reef configurations, cause and effect. In Laporte, L. F. (ed.), Reefs in Time and Space. Society of Economic Palaeontologists and Mineralogists Special Publication 18, pp. 9–76.
  7. ^ McNeil (1954, p. 396).
  8. ^ Fairbridge (1950, p. 341).
  9. ^ Watts, T. (2019). "Science, Seamounts and Society". Geoscientist. August 2019: 10–16.
  10. ^ "Misinformation about Islands". worldislandinfo.com.
  11. ^ "Atoll Area, Depth and Rainfall" (spreadsheet). The Geological Society of America. 2001.
  12. ^ "Archipiélago de Los Roques" (in Spanish). Caracas, Venezuela: Instituto Nacional de Parques (INPARQUES). 2007. Archived from the original on 2008-04-24. Retrieved 27 February 2013.
  13. ^ Hoffmeister, J.E., 1930. Erosion of elevated fringing coral reefs. Geological Magazine, 67(12), pp.549–554.
  14. ^ MacNeil, F.S., 1954. The shape of atolls; an inheritance from subaerial erosion forms. American Journal of Science, 252(7), pp.402–427.
  15. ^ Bialik, Or M.; Samankassou, Elias; Meilijson, Aaron; Waldmann, Nicolas D.; Steinberg, Josh; Karcz, Kul; Makovsky, Yizhaq (January 2021). "Short-lived early Cenomanian volcanic atolls of Mt. Carmel, northern Israel". Sedimentary Geology. 411: 105805. Bibcode:2021SedG..41105805B. doi:10.1016/j.sedgeo.2020.105805. S2CID 228873675.
  16. ^ El-Yamani, Mahmoud S.; John, Cédric M.; Bell, Rebecca (16 May 2022). "Stratigraphic evolution and karstification of a Cretaceous Mid-Pacific atoll (Resolution Guyot) resolved from core-log-seismic integration and comparison with modern and ancient analogues". Basin Research. 34 (5): 1536–1566. Bibcode:2022BasR...34.1536E. doi:10.1111/bre.12670. hdl:10044/1/98098. S2CID 248223664.
  17. ^ Budd, D.A., 1997. Cenozoic dolomites of carbonate islands: their attributes and origin. Earth-Science Reviews, 42(1–2), pp.1–47.
  18. ^ Wheeler, C.W., Aharon, P. and Ferrell, R.E., 1999. Successions of late Cenozoic platform dolomites distinguished by texture, geochemistry, and crystal chemistry; Niue, South Pacific. Journal of Sedimentary Research, 69(1), pp.239–255.
  19. ^ Suzuki, Y., Iryu, Y., Inagaki, S., Yamada, T., Aizawa, S. and Budd, D.A., 2006. Origin of atoll dolomites distinguished by geochemistry and crystal chemistry: Kita-daito-jima, northern Philippine Sea. Sedimentary Geology, 183(3–4), pp.181–202.
  20. ^ David, Cara (Caroline Martha) (1899). Funafuti or Three Months On A Coral Atoll: an unscientific account of a scientific expedition. London: John Murray. ISBN 978-1-151-25616-4.
  21. ^ Finckh, Dr. Alfred Edmund (11 September 1934). "TO THE EDITOR OF THE HERALD". The Sydney Morning Herald. NSW: National Library of Australia. p. 6. Retrieved 20 June 2012.
  22. ^ Cantrell, Carol (1996). "Alfred Edmund Finckh (1866–1961)". Finckh, Alfred Edmund (1866–1961). National Centre of Biography. Retrieved 23 December 2012 – via Australian Dictionary of Biography at Australian National University.
  23. ^ Rodgers, K A; Cantrell, Carol (1987). "Alfred Edmund Finckh 1866–1961: Leader of the 1898 Coral Reef Boring Expedition to Funafuti". Historical Records of Australian Science. 7 (4): 393–403. doi:10.1071/HR9890740393. PMID 11617111.

Sources

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  • Dobbs, David. 2005. Reef Madness: Charles Darwin, Alexander Agassiz, and the Meaning of Coral. Pantheon. ISBN 0-375-42161-0
  • Fairbridge, R. W. 1950. "Recent and Pleistocene coral reefs of Australia". J. Geol., 58(4): 330–401.
  • McNeil, F. S. 1954. "Organic reefs and banks and associated detrital sediments". Amer. J. Sci., 252(7): 385–401.
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