شعب حلقي

(تم التحويل من أتولا)
صورة ساتلية لآتول أتافو في توكلاو في المحيط الهادي.
شعب مورورا الحلقي

الشعاب الحلقية أو الآتولات Atoll هي جزر تكونت نتيجة لتراكم الشعاب المرجانية على جزر بركانية غارقة في مياه المحيط ويستمر نموها وتراكمها حتى تكون جزيرة جديدة. يظهر الشعب الحلقي في هيئة حلقة محيطة ببحيرة شاطئية (لاغون) مستديرة وسطه. مياه تلك البحيرة الشاطئية قد تكون مياه عذبة أو مسوسية ولكن في الغالب تكون مياهها مالحة.

صورة ساتلية لآتولات المالديڤ التقطتها ناسا. A total of 1200 islands arranged into 22 atolls make up the country.

Two different, well-cited models, the subsidence and antecedent karst models, have been used to explain the development of atolls.[1] According to Charles Darwin's subsidence model,[2] 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).[1]

An alternative model for the origin of atolls, called the antecedent karst model, was first proposed by J. E. Hoffmeister,[3][4] later revised by E. G. Prudy,[5] and evaluated and modified using a compilation of seismic reflection and drillhole data from various atolls by A. W. Droxler and others.[1] 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.[1][5]

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Usage

The word atoll comes from the Dhivehi word atholhu (Dhivehi: އަތޮޅު, dv). 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".[2](p. 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"[6] or "in an exclusively morphological sense, [as] a ring-shaped ribbon reef enclosing a lagoon".[7]


Distribution and size

There are approximately 440 atolls in the world.[8]

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). 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).[9] 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 remains of an ancient atoll as a hill in a limestone area is called a reef knoll. The second largest atoll by dry land area is Aldabra, with 155 km2 (60 sq mi). The largest atoll in terms of island numbers is Huvadhu Atoll in the south of the Maldives, with 255 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

Largest atolls by total area (lagoon plus reef and dry land)[10]
Name
Position
Location
Area (km2)
Remarks
Great Chagos Bank 6°10′S 72°00′E / 6.17°S 72.00°E / -6.17; 72.00
Indian Ocean
12,642
 Land area 4.5 km2
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 (Ritchie Bank, north of
the Saya de Malha 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 (Boduthiladhunmathi) 6°44′N 73°02′E / 6.73°N 73.04°E / 6.73; 73.04
Maldives
3,850
 Land area 51 km2
Chesterfield Islands 19°21′S 158°40′E / 19.35°S 158.66°E / -19.35; 158.66
New Caledonia
3,500
 Land area <10 km2
Huvadhu Atoll 0°30′N 73°18′E / 0.50°N 73.30°E / 0.50; 73.30
Maldives
3,152
 Land area 38.5 km2
Truk Lagoon 7°25′N 151°47′E / 7.42°N 151.78°E / 7.42; 151.78
Chuuk, FSM
3,152
 [11]
Sabalana Islands 6°45′S 118°50′E / 6.75°S 118.83°E / -6.75; 118.83
Indonesia
2,694
Nukuoro Atoll 3°51′N 154°56′E / 3.85°N 154.94°E / 3.85; 154.94
Pohnpei, FSM
40
 Land area 1.7 km2 in 40 islets
Lihou Reef 17°25′S 151°40′E / 17.42°S 151.67°E / -17.42; 151.67
Coral Sea
2,529
 Land area 1 km2
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
 Cay on the south side?
Kwajalein Atoll 9°11′N 167°28′E / 9.19°N 167.47°E / 9.19; 167.47
Marshall Islands
2,304
 Land area 16.4 km2
Diamond Islets Bank 17°25′S 150°58′E / 17.42°S 150.96°E / -17.42; 150.96
Coral Sea
2,282
 Land area <1 km2
Namonuito Atoll 8°40′N 150°00′E / 8.67°N 150.00°E / 8.67; 150.00
Chuuk, FSM
2,267
 Land area 4.4 km2
Ari Atoll 3°52′N 72°50′E / 3.86°N 72.83°E / 3.86; 72.83
Maldives
2,252
 Land area 69 km2
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
Tuamotu Islands
1,762
 Land area 79 km2
Kolhumadulhu Atoll 2°22′N 73°07′E / 2.37°N 73.12°E / 2.37; 73.12
Maldives
1,617
 Land area 79 km2
Kaafu Atoll (North Malé Atoll) 4°25′N 73°30′E / 4.42°N 73.50°E / 4.42; 73.50
Maldives
1,565
 Land area 69 km2
Ontong Java Atoll 5°16′S 159°21′E / 5.27°S 159.35°E / -5.27; 159.35
Solomon Islands
1500
 Land area 12 km2


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Gallery

التكون

انظر أيضاً: Coral reef § Formation
This dynamic animation shows the dynamic process of coral atoll formation. Corals (represented in tan and purple) settle and grow around an oceanic island, forming a fringing reef. In favorable conditions, the reef will expand, and the interior island will subside. Eventually the island completely subsides beneath the water, leaving a ring of growing coral with an open lagoon in its center. The process of atoll formation may take as long as 30,000,000 years to occur.
Aerial view of Bora Bora
Tarawa Atoll
Bikini Atoll

In 1842, Charles Darwin[2] 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,[3] F. S. McNeil,[13] E. G. Prudy,[5] 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[1] 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.[14][15]

  • Darwin's theory starts with a volcanic island which becomes extinct

    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

    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

  • As the subsidence continues the fringing reef becomes a larger barrier reef farther from the shore with a bigger and deeper lagoon inside

    As the subsidence continues the fringing reef becomes a larger barrier reef farther from the shore with a bigger and deeper lagoon inside

  • Ultimately the island sinks below the sea, and the barrier reef becomes an atoll enclosing an open lagoon

    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.[16][17][18]

Investigation by the Royal Society of London

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.[19] The third expedition in 1898 was led by Alfred Edmund Finckh.[20][21][22]

انظر أيضاً

المصادر

  1. ^ أ ب ت ث ج 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.
  2. ^ أ ب ت خطأ استشهاد: وسم <ref> غير صحيح؛ لا نص تم توفيره للمراجع المسماة darwincr1
  3. ^ أ ب Hoffmeister, J.E., 1930. Erosion of elevated fringing coral reefs. Geological Magazine, 67(12), pp.549-554.
  4. ^ Hoffmeister, J.E., and Ladd, H.S., 1935. "The foundations of atolls: a discussion." The Journal of Geology, 43, no. 6, 653-665.
  5. ^ أ ب ت 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.
  6. ^ McNeil (1954, p. 396).
  7. ^ Fairbridge (1950, p. 341).
  8. ^ Watts, T. (2019). "Science, Seamounts and Society". Geoscientist. August 2019: 10–16.
  9. ^ "Misinformation about Islands". worldislandinfo.com.
  10. ^ "Atoll Area, Depth and Rainfall" (spreadsheet). The Geological Society of America. 2001.
  11. ^ "A Blueprint for Conserving the Biodiversity of the Federated States of Micronesia". conserveonline.org. Micronesia Program Office. Archived from the original on 2011-09-27. Retrieved 2007-12-05.
  12. ^ خطأ استشهاد: وسم <ref> غير صحيح؛ لا نص تم توفيره للمراجع المسماة inparques1
  13. ^ MacNeil, F.S., 1954. The shape of atolls; an inheritance from subaerial erosion forms. American Journal of Science, 252(7), pp.402-427.
  14. ^ 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.
  15. ^ 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. doi:10.1111/bre.12670. hdl:10044/1/98098. S2CID 248223664.
  16. ^ Budd, D.A., 1997. Cenozoic dolomites of carbonate islands: their attributes and origin. Earth-Science Reviews, 42(1-2), pp.1-47.
  17. ^ 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.
  18. ^ 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.
  19. ^ خطأ استشهاد: وسم <ref> غير صحيح؛ لا نص تم توفيره للمراجع المسماة davidcm1
  20. ^ خطأ استشهاد: وسم <ref> غير صحيح؛ لا نص تم توفيره للمراجع المسماة finckhae1
  21. ^ خطأ استشهاد: وسم <ref> غير صحيح؛ لا نص تم توفيره للمراجع المسماة cantrellc1
  22. ^ خطأ استشهاد: وسم <ref> غير صحيح؛ لا نص تم توفيره للمراجع المسماة rodgerska1

قراءات اضافية

مشاع المعرفة فيه ميديا متعلقة بموضوع Atoll.
  • Darwin, C. 1842. The structure and distribution of coral reefs. London.
  • 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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