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Map of the hotspots on Earth. Arago is #59

Coordinates: 23°26′S 150°44′W / 23.44°S 150.73°W / -23.44; -150.73[1]

Arago hotspot is a hotspot in the Pacific Ocean, presently located below the Arago seamount close to the island of Rurutu, French Polynesia.

Arago is part of a family of hotspots in the southern Pacific, which include the Society hotspot and the Macdonald hotspot among others. These are structures beneath Earth's crust which generate volcanoes and which are in part formed by mantle plumes, although Arago itself might have a shallower origin. As the Pacific plate moves over the hotspots, new volcanoes form and old volcanoes are carried away; sometimes an older volcano is carried over the hotspot and is then uplifted as happened with Rurutu.

The Arago hotspot is responsible for the formation of Arago seamount and uplift on Rurutu; however reconstructions of the past positions of tectonic plates and geochemistry suggest that other islands and seamounts were constructed by the Arago hotspot during the past 120 million years. These potentially include Tuvalu, Gilbert Islands, the Ratak Chain of the Marshall Islands as well as part of the Austral Islands and Cook Islands.

NameEdit

The hotspot is named after the Arago seamount 130 kilometres (81 mi) southeast of Rurutu. The seamount is named after the French Navy ship Arago, which discovered the seamount in 1993.[2] The ship itself is named after astronomer François Arago.[3] Polynesians knew of the existence of the shallow (27 metres (89 ft) beneath sea level) seamount and named it Tinomana.[2] Before the link to Arago seamount was discovered, the hotspot was also known as "Rurutu hotspot",[4][5] a name sometimes still used,[6] which is a name also used for an older volcanic chain that starts at Raivavae[7] or President Thiers Bank.[8] Other names are "Young Rurutu"[6] and "Atiu trend".[5][9]

Geography and geologyEdit

 
Location in the southern Pacific Ocean
 
The islands in the southern Pacific Ocean

The southern Pacific Ocean is the site of the South Pacific Superswell, an area where the ocean is anomalously shallow (by about 700 metres (2,300 ft))[10][11] and which covers an area of about 3,000 by 3,000 kilometres (1,900 mi × 1,900 mi).[12] Underneath this superswell a large mantle plume might give rise to secondary plumes which in turn form the surface hotspots.[13] Hotspots in the region are the Macdonald hotspot, Marquesas hotspot, Pitcairn hotspot and Society hotspot;[10] of which the first and the last appear to be rooted deep in the mantle.[14] The nature of the volcanism in the area is not completely understood.[15]

Arago Seamount is part of the volcanic chain that forms the Austral Islands and Cook Islands. The 2,200 kilometres (1,400 mi) long chain consists of two separate trends that form two atolls and eleven islands; of these systems one (Macdonald seamount) is a still active volcano.[16] The ages of these islands follow an approximate age progression typical of a hotspot volcano but the occurrence of younger ages on Aitutaki and Rurutu and the chemistry of these younger rocks indicated that there must be more than one hotspot involved.[2] Recent models envisage the presence of a number of separate hotspot tracks in what has been dubbed a "hotspot highway".[17] Further, some hotspots such as the Hawaii hotspot show evidence of movement but the Arago hotspot appears to be static.[18]

The Arago and other hotspots probably are not deep mantle plumes but rather more shallow structures that are also influenced by the lithosphere;[19] in the case of the Arago hotspot the absence of an oceanic plateau that could have been formed by the head of the mantle plume supports such a shallow origin.[20] The upper mantle might be the source of the Arago hotspot.[21] Data on the presence of seismic velocity anomalies and whether they are positive (higher) or negative (lower) beneath Arago are contradictory.[22] Seismic imaging published in 2009 indicates only a slight seismic velocity anomaly shallower than 100 kilometres (62 mi),[23] with no indication of a deep mantle root.[24] More recent research however has endorsed a deep mantle origin for the Arago hotspot.[25] Presently, Arago and the Macdonald hotspot are the two active hotspots of the Austral Islands,[26] but a hotspot that formed Rarotonga may also still be active; additional hotspots in the area are Tubuai, Taukina and Ngatemato.[27]

Arago SeamountEdit

The eponymous Arago Seamount is a composite volcano with three rift zones, similar to Rurutu.[2] The seamount was formed by three volcanoes with one overlapping the other two; potassium-argon dating on Arago has yielded ages of 230,000 ± 4,000 before present and an imprecise age of 0 years before present.[19] There is some evidence of submarine landslide activity, a typical occurrence on ocean volcanoes,[26] with one landslide scar each on the northern, eastern and western flank.[28] This seamount is considered to be the present location of the hotspot, given its young age;[16] however, unlike Macdonald, Arago Seamount has no recorded historical eruptions.[29]

Hotspots other than the Arago hotspot may have contributed to the growth of the Arago Seamount; a hotspot associated with Raivavae and potentially the President Thiers Bank has been associated through isotope analysis with 8.2 million year old samples taken from Arago Seamount.[30] Other volcanoes in the region also show evidence that they were built by more than one hotspot; this might indicate that their formation is controlled by lithospheric features.[13]

Other islands and seamountsEdit

 
Hotspot provinces in the Pacific Ocean; Arago belongs to the "Macdonald" province

As the Pacific Plate drifted over the hotspot several volcanoes were formed on the hotspot where weaknesses in the crust allowed the penetration of magma, and were subsequently carried away,[19][18] at a rate of about 120 millimetres per year (4.7 in/year).[31] Isotope ratios of lead in the volcanic rocks tie the younger volcanics of Rurutu to the Arago hotspot,[19] the ratio in this case is characterized by high radiogenic lead isotope composition ("HIMU").[32] Some volcanic material from the Arago hotspot may have been recycled in the mantle and mixed into the magmas erupted in the northeastern Lau basin;[33] rocks shed from seamounts created by the Arago hotspot may have been subducted in the Tonga trench which is close to the reconstructed path of the Arago hotspot and then erupted onto the Lau basin.[34] HIMU xenoliths have been found in Tubuai just ahead of Arago Seamount as well.[35]

Rurutu already existed before the interaction with the Arago hotspot, having been formed by an older volcanic episode; when it moved over the Arago hotspot a volcanic episode occurred and emplaced lava flows that are formed by basanite and hawaiite. Also, the island and surrounding coral reef were uplifted,[36] and these uplifted coral reefs (known as makatea) caught the attention of early geologists, who were speculating as to what might have lifted the reefs out of the sea already in 1840.[37] Other uplifted atolls occur northwest from Rurutu and may have formed in the same way when they passed over the Arago hotspot.[38]

Map all coordinates using: OpenStreetMap 
Download coordinates as: KML · GPX

The following volcanics are at least tentatively attributed to the Arago hotspot:

The oldest volcanic structures potentially formed by the Arago hotspot are 120 million years old. If their attribution is correct, the Arago hotspot may be the oldest still active hotspot in the Pacific Ocean, ahead of the Hawaii hotspot and the Louisville hotspot.[57] A contrasting viewpoint believes that Arago is a short-lived hotspot with few dated volcanoes along its predicted path.[1]

The island of Tubuai is located ahead of the hotspot, and the island will be transported over it in a few million years. As with Rurutu, this interaction will lead to uplift in Tubuai and possibly to renewed volcanism.[36]

ReferencesEdit

  1. ^ a b c Clouard & Bonneville 2001, p. 697.
  2. ^ a b c d Bonneville et al. 2002, p. 1024.
  3. ^ "Arago (P 675)". Ministère des Armées (in French). 3 February 2015. Retrieved 26 October 2017.
  4. ^ Bonneville, Dosso & Hildenbrand 2006, p. 252.
  5. ^ a b Konrad et al. 2018, p. 2.
  6. ^ a b c Finlayson et al. 2018, p. 171.
  7. ^ Neall & Trewick 2008, p. 3299.
  8. ^ Morgan & Morgan 2007, pp. 65–67.
  9. ^ Price et al. 2016, p. 1696.
  10. ^ a b Isse et al. 2016, p. 1.
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  12. ^ Suetsugu et al. 2009, p. 2.
  13. ^ a b c Bonneville, Dosso & Hildenbrand 2006, p. 266.
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  16. ^ a b Bonneville et al. 2002, p. 1023.
  17. ^ Finlayson et al. 2018, p. 170.
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  20. ^ Clouard & Bonneville 2001, p. 695.
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