Tropic Seamount

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Tropic Seamount
Tropic Seamount is located in North Atlantic
Tropic Seamount
Tropic Seamount
Tropic Seamount (North Atlantic)
Location offshore Africa
Summit depth970 m (3,180 ft)
Location
LocationNorth Atlantic
GroupCanary Islands Seamount Province
Coordinates23°53′N 20°43′W / 23.89°N 20.72°W / 23.89; -20.72[1]Coordinates: 23°53′N 20°43′W / 23.89°N 20.72°W / 23.89; -20.72[1]

Tropic Seamount is a Cretaceous[a] seamount southwest of the Canary Islands and north of Cape Verde, one of a number of seamounts (a type of underwater volcanic mountain) in this part of the Atlantic Ocean. It was probably formed by volcanic processes triggered by the proximity to the African continent. Tropic Seamount is located at a depth of 970 metres (3,180 ft) and has a summit platform with an area of 120 square kilometres (46 sq mi).

Limalok is formed by volcanic rocks including basalt and trachyte and was probably an island at first; for reasons unknown it sunk to its present day depth. Large landslides and late volcanic activity affected the seamount, cutting large scars into its flanks and forming cones on its summit plateau, respectively. Volcanic activity at Tropic Seamount commenced almost 120 million years ago and ended about 60 million years ago. Later, sedimentation commenced on the seamount leading to the deposition of manganese crusts and pelagic sediments; iron and manganese accumulated in crusts over time beginning a few tens of millions of years ago.

Name[edit]

Tropic Seamount lies close to the Tropic of Cancer, thus the name.[3] It is also known as "Tropical Bank" or "Carmenchu Peak",[4] the latter named after Me. del Carmen Piernavieja y Oramas of Las Palmas, Spain; this nomenclature reflected the idea that Carmenchu Peak was a separate summit.[5] The seamount is recognized by the International Hydrographic Organization.[1] An alternative name "Tropic Guyot" has been proposed[6] and the diminutive "Tropiquito" was applied to another smaller seamount in the region.[7]

Geography and geomorphology[edit]

Tropic Seamount lies 470 kilometres (290 mi) west of Cape Blanc[8] and 400 kilometres (250 mi) south of the Canary Islands[9] off the coast of Mauretania,[10] Northwestern Africa.[11] The seamount is part of the exclusive economic zone of Spain.[12]

Regional[edit]

Tropic Seamount is the southernmost member[13] of the Canary Islands Seamount Province, which reaches from north of Lanzarote in the Canary Islands to southwest of the archipelago[14] and contains over a hundred seamounts in a space 1,000 kilometres (620 mi) long.[12] This province aside from Tropic Seamount in the south includes The Paps Seamount, Ico Seamount, Echo Bank and Drago Seamount but also Essaouira Seamount north of Lanzarote. Especially the southern among these underwater mountains are poorly studied.[14] Aside from the seamounts, submarine canyons and large debris flows occur in the region[15] such as the Sahara Slide which has run around Echo Bank.[16]

Local[edit]

The isolated[17] seamount lies about halfway between the Canary Islands and Cape Verde, 480 kilometres (260 nmi) west of West Sahara/Mauritania.[4] It is a 42 by 37 kilometres (26 mi × 23 mi) wide guyot[1] with the shape of a square and a summit area with a four-point star form.[18] The seafloor around Tropic Seamount has an age of about 150 million years and is covered by Quaternary silt, pelagic ooze and aeolian sediments.[4]

The seamount rises 3.2 kilometres (2.0 mi) from a depth of 4,200 metres (13,800 ft) to a depth of 1,000 metres (3,300 ft) and a flat summit[1] that has a surface area of about 120 square kilometres (46 sq mi)[4] and is covered with sediments;[17] the shallowest sector of the seamount lies at 970 metres (3,180 ft) depth.[12] This flat summit is covered by 10–20 metres (33–66 ft) high volcanic cones and features terraces at the margin of the summit[1] as well as ridges that point due north, east, south and west. Volcanic cones are concentrated in the southern and eastern parts of the summit platform.[18]

The outer slopes of the seamount become steeper to the summit[4] perhaps due to geochemical differences between the rocks that form the lower slopes and these of the upper slopes.[19] They are cut by curved flank collapses that open to the northeast, southeast, southwest and northwest;[1] these collapses have cut into the volcanic edifice and have left ridges between the individual collapses which give the seamount its four-point star form[20] and deposited debris around the seamount,[21] although the deposits are not recongizable probably because they are old and buried beneath sediments.[13] In addition there are 3–10 kilometres (1.9–6.2 mi) long gullies[1] formed either by erosional or volcanic processes.[16]

Geology[edit]

The geological origin of the Canary Islands Seamounts are unclear, with various hotspot processes as well as crustal and mantle phenomena proposed.[15] The age progression from either Essaouira Seamount or Lanzarote-Fuerteventura to El Hierro-La Palma has been interpreted as indicating a hotspot process[22] but the considerably higher ages of the submarine volcanism both in the Canaries and at the Canary Islands Seamounts are not compatible with a hotspot origin. An alternative theory posits that mantle convection is driven by the close distance between the seamounts and the African continent[23] and generated these volcanoes beginning in the Cretaceous.[12] Volcanic activity at Echo and Tropic seamounts was probably focused and generated a circular volcanic structure, while at Drago and The Paps it was controlled by lineaments and thus formed elongated edifices.[20]

Composition[edit]

Dredging has produced basaltic and carbonatic rocks that are partly covered by ferromanganese crusts or chemically altered by phosphate.[4] In addition, shallow water calcarenites, conglomerates,[12] coral debris,[24] hemipelagic sediments, breccia, limestones, felsite,[25] reefal limestones and sediments have been recovered.[10]

The volcanic rocks include alkali basalts,[26] basanite, hyaloclastite, palagonite, pumices, basaltic tuffs, trachybasalt[27][28] and trachyte[17] and define an alkaline ocean island basalt suite although the existence of tholeiites as in Hawaii is possible[29] and substantial amounts of evolved volcanic rocks have been recovered; these were probably generated by basaltic melts in magma chambers.[30] Minerals contained in the rocks include mafic clots, amphibole,[31] apatite, clinopyroxene including augite, olivine, plagioclase, spinel and titanomagnetite.[4] Non-hydrothermal chemical alteration has taken place and has formed carbonate, celadonite, chlorite, hematite, prehnite, quartz, smectite and rare zeolites.[32]

Thick ferromanganese deposits were recovered from the seamount in 1992 by the RV Sonne[8] and are found especially on the western flank[17] but also in the summit region, often over partly consolidated sediments.[33] Components include carbonate fluorapatite, goethite and manganese dioxide as well as minor calcite and quartz;[34] the crusts which occur on the Canary Islands Seamounts including at Tropic Seamount reach thicknesses of 20 centimetres (7.9 in) and are rich in cobalt[35] and other elements of industrial importance.[36] At Tropic Seamount they formed from water but were also influenced by material coming from Africa.[37]

Environment[edit]

Water temperatures and salinity of the water masses around Tropic Seamount decrease with increasing depth[37] and ripples indicate that strong ocean currents affect the seamount.[10] A number of separate water masses surround the seamount, which originate from regions such as the North Atlantic, the South Atlantic and Antarctica and are stacked over each other.[15]

Corals and sponges and more generally sessile fauna cover parts of the eastern and western spurs of Tropic Seamount.[33] The bivalve Rhinoclama teres[38] and the echinoids Echinocyamus scaber,[39] Palaeotropus josephinae,[40] Peripatagus cinctus[41] and Selenocidaris varispina have been found on this seamount.[42]

Geologic history[edit]

Tropic Seamount appears to be the oldest among the Canary Islands Seamounts.[20] Ages of samples from its southwestern slopes range from 119.3 ± 0.3 to 113.9 ± 0.2 million years ago[43] while the northern slopes have produced ages of 84 to 59 million years ago; this has been interpreted as meaning that Tropic Seamount was active mainly between 119 and 114 million years ago but later volcanic activity continued until about 60 million years ago.[44] When Tropic Seamount was active the Atlantic Ocean was much narrower than today and dinosaurs still roamed the Earth.[7]

Tropic Seamount once formed an island before it was eroded down to its current depth.[12][45] Flat topped summits can form through diverse mechanisms;[20] erosion of an island is the preferred theory in the case of Tropic Seamount[45] as there is little evidence of caldera-forming volcanic activity.[4] How this former island subsided to a depth of 1 kilometre (0.62 mi) however is unclear.[46]

The growth of ferromanganese crusts began probably no earlier than 76 million years ago[47] and would be one among the oldest such crusts recovered if it is that old.[48] Other crusts began developing about 30 million years ago, with a younger generation of crusts developing starting from 12 ± 2 million years ago.[49]

Notes[edit]

  1. ^ Between ca. 145 and 66 million years ago.[2]

References[edit]

  1. ^ a b c d e f g Palomino et al. 2016, p. 128.
  2. ^ "International Chronostratigraphic Chart" (PDF). International Commission on Stratigraphy. August 2018. Retrieved 22 October 2018.
  3. ^ "Thirteenth Meeting of the GEBCO Sub-Committeeon Undersea Feature Names" (PDF). International Hydrographic Organization. 1999. p. 44. Retrieved 10 February 2019.
  4. ^ a b c d e f g h Blum, Halbach & Münch 1996, p. 3.
  5. ^ Atlantic Oceanographic and Meteorological Laboratories; Pacific Oceanographic Laboratories; United States. Environmental Science Services Administration. Research Laboratories; Environmental Research Laboratories (U.S.) (1968). Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Penn State University. US Department of Commerce. p. 324.
  6. ^ SCUFN (2003). Summary Report (PDF). Sixteenth meeting of the GEBCO Subcommittee on Undersea Feature Names. International Hydrographic Organization. p. 4.
  7. ^ a b "Logbuch METEOR M146". Center for Marine Environmental Sciences (in German). Bremen University. Retrieved 10 February 2019.
  8. ^ a b Koschinsky et al. 1996, p. 567.
  9. ^ Yeo, I. A.; Vardy, M. E.; Holwell, D.; North, L.; Murton, B. J. (2017-12-01). "Mapping beneath the seafloor: AUV sub-bottom profilers, sediment thickness and resource potential". AGU Fall Meeting Abstracts. 21: OS21C–02. Bibcode:2017AGUFMOS21C..02Y.
  10. ^ a b c Glasby, Geoffrey P.; Mountain, Bruce; Vineesh, Theckethottathil C.; Banakar, Virupaxa; Rajani, Ramesh; Ren, Xiangwen (June 2010). "Role of Hydrology in the Formation of Co-rich Mn Crusts from the Equatorial N Pacific, Equatorial S Indian Ocean and the NE Atlantic Ocean". Resource Geology. 60 (2): 172–173. doi:10.1111/j.1751-3928.2010.00123.x.
  11. ^ Blum, Halbach & Münch 1996, p. 2.
  12. ^ a b c d e f Marino et al. 2017, p. 42.
  13. ^ a b Schmincke & Graf 2000, p. 34.
  14. ^ a b Palomino et al. 2016, p. 125.
  15. ^ a b c Palomino et al. 2016, p. 126.
  16. ^ a b Palomino et al. 2016, p. 135.
  17. ^ a b c d Koschinsky et al. 1996, p. 569.
  18. ^ a b Palomino et al. 2016, p. 130.
  19. ^ Blum, Halbach & Münch 1996, p. 17.
  20. ^ a b c d Palomino et al. 2016, p. 133.
  21. ^ Palomino et al. 2016, p. 137.
  22. ^ van den Bogaard 2013, p. 1.
  23. ^ van den Bogaard 2013, p. 6.
  24. ^ Schmincke & Graf 2000, p. 73.
  25. ^ Schmincke & Graf 2000, pp. 20-21.
  26. ^ Schmincke & Graf 2000, p. 88.
  27. ^ Schmincke & Graf 2000, pp. 25-26.
  28. ^ Blum, Halbach & Münch 1996, p. 3,5.
  29. ^ Blum, Halbach & Münch 1996, pp. 8-9.
  30. ^ Schmincke & Graf 2000, p. 46.
  31. ^ Schmincke & Graf 2000, p. 24.
  32. ^ Blum, Halbach & Münch 1996, p. 5.
  33. ^ a b Murton, B. J.; Lusty, P.; Yeo, I. A.; Howarth, S. (2017-12-01). "Detailed seamount-scale studies of ferromanganese crusts reveal new insights into their formation and resource assessment". AGU Fall Meeting Abstracts. 34: OS34A–05. Bibcode:2017AGUFMOS34A..05M.
  34. ^ Marino et al. 2017, p. 47.
  35. ^ Torres Pérez-Hidalgo, Trinidad José; Ortiz Menéndez, José Eugenio; González, F.J.; Somoza, L.; Lunar, R.; Martínez-Frías, J.; Medialdea, T.; León, R.; Martín-Rubí, J.A.; Marino, E. (2014). Polymetallic ferromanganese deposits research on the Atlantic Spanish continental margin. Harvesting Seabed Minerals Resources in Harmony with Nature UMI 2014. Lisboa. p. 7 – via Academia.edu.CS1 maint: Date and year (link)
  36. ^ Marino et al. 2017, pp. 57-58.
  37. ^ a b Koschinsky et al. 1996, p. 571.
  38. ^ Krylova, Elena M. (2006). "Bivalves of seamounts of the north-eastern Atlantic" (PDF). In Mironov, A.N.; Gebruk, A.V.; Southward, A.J. Biogeography of the North Atlantic seamounts. p. 92.
  39. ^ Mironov 2006, p. 114.
  40. ^ Mironov 2006, p. 117.
  41. ^ Mironov 2006, p. 119.
  42. ^ Mironov 2006, p. 106.
  43. ^ van den Bogaard 2013, p. 2.
  44. ^ van den Bogaard 2013, p. 3.
  45. ^ a b Palomino et al. 2016, p. 134.
  46. ^ Schmincke & Graf 2000, p. 26.
  47. ^ Marino et al. 2017, p. 49.
  48. ^ Marino et al. 2017, p. 53.
  49. ^ Koschinsky et al. 1996, p. 575.

Sources[edit]