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Anton Dohrn Seamount

Coordinates: 57°30′N 11°00′W / 57.500°N 11.000°W / 57.500; -11.000[1]
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Anton Dohrn Seamount
Anton Dohrn Seamount is located in Oceans around British Isles
Anton Dohrn Seamount
Anton Dohrn Seamount is located in North Atlantic
Anton Dohrn Seamount
Anton Dohrn Seamount (North Atlantic)
Summit depth600 metres
Height1,500 m
Location
LocationNorth Atlantic Ocean
Coordinates57°30′N 11°00′W / 57.500°N 11.000°W / 57.500; -11.000[1]
CountryUnited Kingdom (EEZ)
Geology
TypeGuyot
Last eruption~40 million years

The Anton Dohrn Seamount is a guyot in the Rockall Trough in the northeast Atlantic. It is 1.8 kilometres (1.1 mi) high and is topped with pinnacles, one of which reaches a depth of 530 metres (1,740 ft). Away from the flat top upon which the pinnacles rest, the slopes fall off steeply into the Rockall Trough and a moat in the sediment that surrounds the seamount.

It appears to be a volcano formed by basaltic lava and tuff. It formed during the Cretaceous and Paleogene and was proposed to be a source for bentonite layers across the British Isles. After the Cretaceous, subsidence and erosion lowered its top until it sank below sea level. The seamount was discovered in 1958.

Anton Dohrn Seamount hosts a diverse ecosystem characterized by reefs formed by cold water corals, sponges and xenophyophorans, which themselves host a number of animals. It has been affected by human fishing operations, however.

Name and research history

Anton Dohrn Seamount is also known as Anton Dohrn Kuppe, a name used by German charts,[2] and as Anton Dohrn bank.[3] It was discovered in September 22, 1958 by the survey vessel Gauss during the Polarfront programme and later surveyed in April 18–19, 1959 by the fishery research vessel FFS Anton Dohrn.[4]

Geography and geomorphology

Anton Dohrn Seamount is located in the northeast Atlantic Ocean west of Scotland,[5] approximately halfway between St Kilda (Hebrides) and Rockall,[6] about 155 kilometres (96 mi) west of the former.[7] It lies in the Rockall Trough, an over 2,000 metres (6,600 ft) deep submarine depression of unclear origin. North-northeast lies the Rosemary Bank and Hebrides Terrace Seamount is found south-southeast from the seamount.[6] The seamount is located inside the exclusive economic zone of the United Kingdom.[8]

Anton Dohrn Seamount is a 1.8 kilometres (1.1 mi) high[9] and about 45 kilometres (28 mi)[10]–40 kilometres (25 mi) wide circular[9] guyot[6] with a flat top at 1,100–530 kilometres (680–330 mi) depth.[11] Flat-topped seamounts are unusual in the North Atlantic.[12] The shallowest point of the seamount lies at about 530 metres (1,740 ft) depth[9] and is formed by a pinnacle that protrudes from the c. 600 metres (2,000 ft) deep summit platform.[10] A 100 metres (330 ft) thick layer of sediment covers the flat top[13] and appears to be reworked by storms and sea currents.[9] Mounds,[14] slope breaks and other volcanic pinnacles are located on the flat top.[15] The seamount tilts southeastward.[16]

Beyond the margin of the flat top, the slopes of Anton Dohrn Seamount drop down to 2,400 metres (7,900 ft) depth.[17] The steep slopes have been variously described as either lacking a sediment cover[1] or featuring gravelly sediments along with outcropping bedrock.[7] There are cliffs, ridges[11] and rockfalls[14] but no gullies or canyons.[8] Parasitic cones lie on the northwestern slope. A moat surrounds the seamount[15] and reaches depths of about 2,300 metres (7,500 ft).[10] It might have formed either through erosion of surrounding sediments by ocean currents or through isostatic subsidence.[18]

Geology

The crust underneath Anton Dohrn Seamount is much thinner than underneath the British Isles and the Rockall Plateau east and west of the seamount, respectively, and the Mohorovičić discontinuity is located at a shallower depth.[6] It may be either stretched continental crust or oceanic crust, and is covered by sediments.[1] At Anton Dohrn Seamount it appears to be unusually shallow, perhaps due to the Iceland plume's buoyancy. The Iceland plume has uplifted terrain as far as 1,000 kilometres (620 mi) from the plume.[19] A 100 kilometres (62 mi) long crustal lineament known as the Anton Dohrn Lineament crosses through the seamount; it may extend into Scotland and Rockall Bank[20] and runs in northwest–southeast direction.[21]

Anton Dohrn Seamount is probably formed mostly by basaltic lava[10] and tuffs[12] which define a transitional to alkaline suite.[22] The rocks contain feldspar and olivine phenocrysts as well as plagioclase. They are covered with ferromanganese crusts[23] and vesicles contain carbonates, clay and zeolites which formed through alteration.[24] Chalks of Maastrichtian age,[23] Eocene nearshore conglomerates[25] and Miocene muds and sands have also been recovered.[26] A granite rock has been dredged as well; it may be a dropstone from icebergs[27] and such exotic rocks have been found in other dredge samples.[12]

Geologic history

Anton Dohrn Seamount is a former volcano.[9] Radiometric dating of volcanic rocks dredged from it has yielded ages of 70 ± 1, 62 ± 1, 47 ± 1 and 41 ± 1 million years ago,[28] indicating episodic activity over 29 million years.[9] Pulses of volcanic activity of similar age have been identified at other volcanoes in the region and may reflect fluctuations of the Iceland plume.[29] The onset of volcanic activity may have been the consequence of crustal extension in the region.[12] The activity during the Cretaceous implies that rifting in the North Atlantic was already underway at that time.[30] At that time, the Rockall Trough was at least 1 kilometre (0.62 mi) deep.[31]

Xenoliths found in volcanic rocks indicate that at Anton Dohrn volcanic activity involved interactions between magma and sediments, resulting in phreatomagmatic eruptions that could have dispersed volcanic ash in the region.[32] This volcanic ash erupted by Anton Dohrn may be the source of post-Cenomanian bentonites of the British Isles[33] but the age and composition of the bentonites do not support this theory.[34] The seamount was once proposed to be the source of Turonian tephra deposits in Western Europe before its Maastrichtian age was established.[35]

During the Cretaceous the seamount was about 2 kilometres (1.2 mi) higher than present,[19] perhaps even reaching 2,000 metres (6,600 ft) height above sea level;[16] presumably it was then eroded during the Paleocene when a wave of erosion took place in western Britain and stripped much of the volcanic centres of northwest Scotland.[19] An episode of crustal subsidence in the Cretaceous-Oligocene also played a role in lowering Anton Dohrn Seamount.[36] The pinnacles on the seamount may be leftover volcanic conduits that resisted erosion.[12] Sedimentation covered the seamount and its flanks in the Eocene and continued afterwards.[9]

Ecology

Barnacles and brachiopods grow on the top of the seamount, and echinoderms,[37] corals[38] and cirripedes also occur there.[39] On the sandy or gravelly substrate serpulids and sponges are found.[8] The seamount may be a shark nursery.[40] Finally, the bivalve Xylophaga anselli has been found at Anton Dohrn Seamount and the Hebrides slope.[41]

A number of ecosystems have been found on Anton Dohrn Seamount, including coral gardens, cold water coral reefs and sponge and xenophyophore communities;[42][43] this seamount is the first place in the United Kingdom where coral gardens have been discovered.[44] The sandy and cobbly terrain of the slopes with occasional bedrock outcrops is populated by reefs that grow on bedrock or on cobbles.[45] They mostly occur on the sides of the seamount, on mounds on the flat top[46] and its margin,[8] perhaps for hydrodynamic reasons or because substrates favourable for the development of the reefs are found there.[47] There is a vertical stratification, with Lophelia found at shallower depths than Solenosmilia.[48] Corals such as antipatharians like Leiopathes sp., small bamboo corals, large gorgonians and soft corals like as Anthomastus sp. have also been found at parasitic vents.[7] The cold water coral cover can become so thick that the underground disappears underneath it.[49]

Dropframe camera surveys[43] have seen anemones, anthozoans, ascidians, the asteroid (starfish) Henricia sp., bamboo corals, caryophyllids, cerianthids, antipatharian corals with various shapes, the corals Desmophyllum dianthus, Lophelia pertusa and Solenosmilia variabilis, echinoderms including brisingids and crinoids, glass sponges, gorgonians, holothurians, the ophiuroids Ophiactis balli and Ophiomusium lymani, the pencil urchin Cidaris cidaris, pycnogonids, the scleractinian Madrepora oculata, the seapen Pennatula phosphorea, sea urchins, sea whips, serpulids, soft corals such as Gersemia sp. and Anthomastus sp., lobose, large and encrusting sponges, stylasterids and xenophyophores. Decapods, fish including Lepidion eques, the eel Synaphobranchus kaupi and squat lobsters Munida sp. have also been encountered.[45][50][51]

Seamounts are considered to be biodiversity hotspots,[52] and there are proposals to make Anton Dohrn Seamount a Special Area of Conservation.[8] The region is considered to be "the cradle of deep-sea biology" as Victorian-era scientists sampled the regional fauna.[8] Ocean currents around Anton Dohrn Seamount are complicated and formed by various water masses.[10] Internal tides at the seamount appear to be important for its ecosystem.[53]

The seamount has been impacted by deep water fishing.[8] Lost fishing gear and trawl marks have been found on Anton Dohrn Seamount,[54] and animals found at its foot have ingested microplastics.[55]

References

  1. ^ a b c Jones et al. 1994, p. 239.
  2. ^ Rogalla 1962, p. 60.
  3. ^ Bott, Martin H. P.; Saxov, Svend; Talwani, Manik; Thiede, Jörn, eds. (1983). Structure and Development of the Greenland-Scotland Ridge. Boston, MA: Springer US. p. 679. doi:10.1007/978-1-4613-3485-9. ISBN 978-1-4613-3487-3.
  4. ^ Rogalla 1962, p. 59.
  5. ^ Stewart et al. 2009, p. 10.
  6. ^ a b c d Jones et al. 1994, p. 238.
  7. ^ a b c Stewart et al. 2009, p. 9.
  8. ^ a b c d e f g Morato, T.; Kvile, K. Ø; Taranto, G. H.; Tempera, F.; Narayanaswamy, B. E.; Hebbeln, D.; Menezes, G. M.; Wienberg, C.; Santos, R. S.; Pitcher, T. J. (May 6, 2013). "Seamount physiography and biology in the north-east Atlantic and Mediterranean Sea". Biogeosciences. 10 (5): 3047. Bibcode:2013BGeo...10.3039M. doi:10.5194/bg-10-3039-2013. ISSN 1726-4170.
  9. ^ a b c d e f g Stewart et al. 2009, p. 12.
  10. ^ a b c d e Davies et al. 2015, p. 4.
  11. ^ a b Stewart et al. 2009, p. 31.
  12. ^ a b c d e Jones et al. 1974, p. 129.
  13. ^ Jones et al. 1994, p. 244.
  14. ^ a b Stewart et al. 2009, p. 34.
  15. ^ a b Stewart et al. 2009, p. 14.
  16. ^ a b Jones et al. 1974, p. 130.
  17. ^ Stewart et al. 2009, p. 130.
  18. ^ Heezen, Bruce C.; Johnson, G. Leonard (November 1, 1963). "A moated knoll in the Canary Passage". Deutsche Hydrografische Zeitschrift. 16 (6): 270. Bibcode:1963DeHyZ..16..269H. doi:10.1007/BF02025932. ISSN 1616-7228.
  19. ^ a b c Jones et al. 1994, p. 245.
  20. ^ Roberts, Alan M.; Alvey, Andrew D.; Kusznir, Nick J. (May 1, 2019). "Crustal structure and heat-flow history in the UK Rockall Basin, derived from backstripping and gravity-inversion analysis". Petroleum Geoscience. 25 (2): 146. doi:10.1144/petgeo2017-063. ISSN 1354-0793.
  21. ^ Stoker, Martyn S.; Holford, Simon P.; Hillis, Richard R. (March 1, 2018). "A rift-to-drift record of vertical crustal motions in the Faroe–Shetland Basin, NW European margin: establishing constraints on NE Atlantic evolution". Journal of the Geological Society. 175 (2): 270. Bibcode:2018JGSoc.175..263S. doi:10.1144/jgs2017-076. ISSN 0016-7649.
  22. ^ Dietrich, V. J; Jones, E. J. W (April 1, 1980). "Volcanic rocks from Rosemary Bank (Rockall Trough, NE Atlantic)". Marine Geology. 35 (4): 295. Bibcode:1980MGeol..35..287D. doi:10.1016/0025-3227(80)90122-X. ISSN 0025-3227.
  23. ^ a b Jones et al. 1994, p. 240.
  24. ^ Jones et al. 1994, p. 241.
  25. ^ Stoker, Weering & Svaerdborg 2001, p. 411.
  26. ^ Stoker, Weering & Svaerdborg 2001, p. 431.
  27. ^ Rogalla 1962, p. 62.
  28. ^ O'Connor et al. 2000, p. 955.
  29. ^ O'Connor et al. 2000, p. 957.
  30. ^ Gordon, John E.; Brooks, Anthony J.; Chaniotis, Peter D.; James, Ben D.; Kenyon, Neil H.; Leslie, Alick B.; Long, David; Rennie, Alistair F. (December 1, 2016). "Progress in marine geoconservation in Scotland's seas: assessment of key interests and their contribution to Marine Protected Area network planning". Proceedings of the Geologists' Association. 127 (6): 724. doi:10.1016/j.pgeola.2016.10.002. hdl:10023/12093. ISSN 0016-7878.
  31. ^ Scrutton, Roger A. (1986). "The geology, crustal structure and evolution of the Rockall Trough and the Faeroe-Shetland Channel". Proceedings of the Royal Society of Edinburgh, Section B: Biological Sciences. 88: 24. doi:10.1017/S0269727000004437. ISSN 2053-5910.
  32. ^ Pacey 1984, p. 57.
  33. ^ Pacey 1984, p. 58.
  34. ^ Wray, David S. (1999). "Identification and long-range correlation of bentonites in Turonian–Coniacian (Upper Cretaceous) chalks of northwest Europe". Geological Magazine. 136 (4): 367. Bibcode:1999GeoM..136..361W. doi:10.1017/S0016756899002836. ISSN 1469-5081.
  35. ^ Wray, David S.; Wood, Christopher J. (May 1, 1998). "Distinction between detrital and volcanogenic clay-rich beds in Turonian–Coniacian chalks of eastern England". Proceedings of the Yorkshire Geological Society. 52 (1): 95. doi:10.1144/pygs.52.1.95. ISSN 0044-0604.
  36. ^ Jones et al. 1974, pp. 130–131.
  37. ^ Stewart et al. 2009, p. 13.
  38. ^ Wilson, J. B. (1979). "The distribution of the coral Lophelia pertusa (L.) [L. prolifera (Pallas)] in the north-east Atlantic". Journal of the Marine Biological Association of the United Kingdom. 59 (1): 157. doi:10.1017/S0025315400046245. ISSN 1469-7769.
  39. ^ Gage, J. D. (1986). "The benthic fauna of the Rockall Trough: regional distribution and bathymetric zonation". Proceedings of the Royal Society of Edinburgh, Section B: Biological Sciences. 88: 169. doi:10.1017/S026972700000453X. ISSN 2053-5910.
  40. ^ Moore, D. M.; Neat, F. C.; McCarthy, I. D. (2013). "Population biology and ageing of the deep water sharks Galeus melastomus, Centroselachus crepidater and Apristurus aphyodes from the Rockall Trough, north-east Atlantic". Journal of the Marine Biological Association of the United Kingdom. 93 (7): 1947. doi:10.1017/S0025315413000374. ISSN 0025-3154.
  41. ^ Romano, Chiara; Voight, Janet Ruth; Pérez-Portela, Rocío; Martin, Daniel (July 25, 2014). "Morphological and Genetic Diversity of the Wood-Boring Xylophaga (Mollusca, Bivalvia): New Species and Records from Deep-Sea Iberian Canyons". PLOS One. 9 (7): 17. Bibcode:2014PLoSO...9j2887R. doi:10.1371/journal.pone.0102887. ISSN 1932-6203. PMC 4111485. PMID 25061913.{{cite journal}}: CS1 maint: unflagged free DOI (link)
  42. ^ Davies et al. 2015, pp. 14–15.
  43. ^ a b Henry et al. 2014, p. 1.
  44. ^ Davies et al. 2015, p. 24.
  45. ^ a b Stewart et al. 2009, pp. 38–46.
  46. ^ Davies et al. 2015, p. 16.
  47. ^ Davies et al. 2015, pp. 26–27.
  48. ^ Henry, Lea-Anne; Roberts, J. Murray (June 1, 2014). "Recommendations for best practice in deep-sea habitat classification: Bullimore et al. as a case study". ICES Journal of Marine Science. 71 (4): 896–897. doi:10.1093/icesjms/fst175. ISSN 1054-3139.
  49. ^ Stewart et al. 2009, p. 30.
  50. ^ Davies et al. 2015, pp. 12–13.
  51. ^ Copard, K.; Colin, C.; Henderson, G. M.; Scholten, J.; Douville, E.; Sicre, M. -A.; Frank, N. (January 1, 2012). "Late Holocene intermediate water variability in the northeastern Atlantic as recorded by deep-sea corals". Earth and Planetary Science Letters. 313–314: 35. Bibcode:2012E&PSL.313...34C. doi:10.1016/j.epsl.2011.09.047. ISSN 0012-821X.
  52. ^ Davies et al. 2015, p. 2.
  53. ^ Henry et al. 2014, p. 5.
  54. ^ Stewart et al. 2009, p. 74.
  55. ^ Courtene-Jones, Winnie; Quinn, Brian; Gary, Stefan F.; Mogg, Andrew O. M.; Narayanaswamy, Bhavani E. (December 1, 2017). "Microplastic pollution identified in deep-sea water and ingested by benthic invertebrates in the Rockall Trough, North Atlantic Ocean" (PDF). Environmental Pollution. 231 (Pt 1): 271–272. doi:10.1016/j.envpol.2017.08.026. ISSN 0269-7491. PMID 28806692.

Sources

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