Hudson Mountains

The Hudson Mountains are a mountain range in western Ellsworth Land just east of Pine Island Bay at the Walgreen Coast of the Amundsen Sea. They are of volcanic origin, consisting of low scattered mountains and nunataks that protrude through the West Antarctic Ice Sheet. The Hudson Mountains are bounded on the north by Cosgrove Ice Shelf and on the south by Pine Island Glacier. The mountains were volcanically active during the Miocene and Pliocene, but there is evidence for an eruption about two millennia ago and uncertain indications of activity in the 20th century.

Hudson Mountains
Aerial view of the southern Hudson Mountains.
Highest point
PeakMount Moses
Elevation750 m (2,460 ft)
Coordinates72°25′S 99°30′W[1]
Geography
Hudson Mountains is located in Antarctica
Hudson Mountains
Hudson Mountains
Geology
Mountain typeStratovolcanoes
Last eruption210 BCE[2]
Hudson Mountains
Highest point
Elevation749 m (2,457 ft) Edit this on Wikidata

Geography and geomorphology

The Hudson Mountains rise in western Ellsworth Land[3] of West Antarctica[4] and were discovered in 1940 by the United States Antarctic Service Expedition.[5] The mountains lie at some distance from the Amundsen Sea's Walgreen Coast,[6] facing Pine Island Bay.[7] The Cosgrove Ice Shelf lies north of the Hudson Mountains.[8] The mountains are remote and visits are rare.[9] In 1991, they were prospected as a potential aircraft landing site.[10]

The mountains are a volcanic field formed by parasitic vents and stratovolcanoes[1] covered in snow and ice,[11] forming a cold desert landscape[12] with an area of about 8,400 square kilometres (3,200 sq mi).[9] About 20 mountains emerge above the Antarctic Ice Sheet in the form of nunataks,[11][13] with the largest rocky outcrops found at Mount Moses and Maish Nunatak.[14] The stratovolcanoes Mount Manthe, Mount Moses, and Teeters Nunatak constitute the bulk of the volcanic field and are heavily eroded. Better preserved are some parasitic cones and volcanic craters[15] which appear to have formed on these three volcanoes.[16] To their south lies the Pine Island Glacier, while the Larter Glacier traverses the Hudson Mountains between Mount Moses and Mount Manthe[17] and other glaciers from the Hudson Mountains join the Pine Island Glacier.[18] The glaciers are rapidly thinning owing to global warming.[19]

Mount Moses reaches an elevation of 749 metres (2,457 ft) above sea level, Teeters Nunatak 617 metres (2,024 ft), and Mount Manthe 576 metres (1,890 ft). Other named structures are:[20]

  • Inman Nunatak east-southeast, Meyers Nunatak southeast, Shepherd Dome south, 495 metres (1,624 ft) high Webber Nunatak (which has a crater on its northern side[21]) west and Evans Knoll west-southwest of Mount Manthe; there are additional unnamed features southeast of Inman Nunatak and south/southwest of Webber Nunatak.[20]
  • Mount Moses is almost due north of Mount Manthe; Siren Rock lies far east of Mount Moses, while 536 metres (1,759 ft) high Slusher Nunatak and 574 metres (1,883 ft) high Velie Nunatak are found north of Mount Moses and 232 metres (761 ft) high Maish Nunatak southwest of Mount Moses. Unnamed features exist between Maish and Moses and east-northeast from Moses.[20]
  • West-northwest of Mount Moses is the 212 metres (696 ft) high Tighe Rock, followed to its north by Hodgson Nunatak and then Teeters Nunatak. To the northwest of Teeters is first an unnamed feature, then Mount Nickens. Northeast of Mount Nickens are Pryor Cliff and Kenfield Nunatak.[20]
  • There may be about three to eleven volcanoes buried under ice in the Hudson Mountains.[18]

The volcanoes are made up by breccia, palagonite tuff,[1] scoriaceous lava flows and tuffs. At Mount Nickles [22] and Mount Moses there are pillow lavas. Lava fragments are dispersed on the slopes of Mount Moses.[23] Volcanic rock sequences that were emplaced under water and under ice are overlaid by volcanic products that were deposed under the atmosphere,[15] there are deposits of volcanic ash and breccia produced by hydromagmatic activity[4] and tuya-like shapes associated with subglacial growth of the volcanoes.[24] At Mount Moses, erosion has exposed dykes.[23] Glaciers have deposited granite boulders and erratic blocks on the Hudson Mountains,[25] and left glacial striations on the pillow lavas of Mount Moses.[23] Physical weathering has yielded soils in some areas.[26] Volcanic glass found in the Pine Island Glacier probably originates in the Hudson Mountains.[27]

Geology

Neighbouring Marie Byrd Land was volcanically active during the Cenozoic, forming a number of volcanoes, some of which are buried under ice, while others emerge above the ice sheet. The Hudson Mountains are part of the Thurston Island[28] or Bellingshausen Volcanic Province, and are its largest and best preserved volcanic field.[29] The volcanism at the mountains may have either been caused by a mantle plume under Marie Byrd Land or by the presence of anomalies (slab windows) in the mantle left over by subduction.[30] Seismic tomography has found evidence of low velocity anomalies under the Hudson Mountains, which may reflect the presence of the Marie Byrd Land mantle plume.[31]

The bedrock around the Hudson Mountains lies below sea level.[32] The basement on which the volcanoes formed is not exposed in the Hudson Mountains, but crops out in the neighbouring Jones Mountains.[22] It forms the so-called Thurston Island tectonic block.[11] Below the Hudson Mountains, the crust is about 21–27 kilometres (13–17 mi) thick.[33] A proposal by Lopatin and Polyakov 1974 is that east and north-trending fractures have controlled the position of the volcanoes.[34]

Composition

The main volcanic rocks include alkali basalt,[35] basalt, hawaiite and tephrite.[16] They define an alkaline suite, some samples trend towards subalkaline.[36] Ultramafic nodules have been reported from some rocks.[37] The magmas erupted by the volcanoes may have originated in a mantle that had been influenced by subduction,[38] and underwent fractionation of olivine as they ascended.[39]

Life and climate

Sparse lichens grow on most of the nunataks,[40] including Usnea species.[41] Mosses have been found growing in gaps between or cracks in boulders.[40] Petrels have been observed.[42] There are no data on the local climate.[14] An automated weather station was installed on Evans Knoll in 2011 and records air temperatures and wind speeds.[43]

Geologic history

The volcanoes were active during the late Miocene and Pliocene. Dates range between 8.5±1.0 and 3.7±0.2 million years ago,[1] an older date is 20±4 million years.[44] There is no evidence of an age progression in any direction.[5]

Ice cover was thicker on the Hudson Mountains during the last glacial maximum, perhaps by about 150 metres (490 ft).[45] Retreat commenced about 14,000[46]-10,000 years ago;[47] however, glaciers were still thicker than today during the early Holocene and deposited rocks on the Hudson Mountains.[25] Another thinning step began about 8,000 years ago and was very fast, perhaps lasting only a century.[48]

Radar data have found a tephra deposit buried under the ice, which may have originated during an eruption of the Hudson Mountains around 207±240 BCE;[4] the eruption may correspond to an electrical conductivity anomaly in an ice core at Siple Dome[49] and a tephra layer dated to 325 BCE in the Byrd Station ice core. The eruption may have had a volcanic explosivity index of 3-4[50] and originated in an area east of the main Hudson Mountains.[50][20] LeMasurier et al. 1990 referenced reports of activity in the Hudson Mountains.[51] These include a report of steaming at one of the nunataks and of satellite data of a potential eruption in 1985 of Webber Nunatak,[16] but the report of this eruption is questionable.[49] There is no evidence of increased heat flow or morphological changes at Webber Nunatak since then,[52] but anomalies in helium isotope ratios from the Pine Island Glacier ice have been attributed to volcanic activity in the Hudson Mountains.[53]

References
  1. LeMasurier et al. 1990, p. 259.
  2. "Hudson Mountains". Global Volcanism Program. Smithsonian Institution.
  3. Gohl 2007, p. 68.
  4. Corr & Vaughan 2008, p. 122.
  5. LeMasurier et al. 1990, p. 293.
  6. LeMasurier et al. 1990, p. 258.
  7. Johnson et al. 2014, p. 999.
  8. Djoumna & Holland 2021, p. 3.
  9. Smellie & Edwards 2016, p. 21.
  10. Swithinbank 1991, p. 11.
  11. Wilch, McIntosh & Panter 2021, p. 564.
  12. Abakumov 2010, p. 298.
  13. Bockheim 2015, p. 187.
  14. Abakumov 2010, p. 299.
  15. LeMasurier et al. 1990, p. 261.
  16. LeMasurier et al. 1990, p. 289.
  17. Nichols et al. 2023, p. 2.
  18. Loose et al. 2018, p. 5.
  19. Johnson et al. 2014, pp. 999–1000.
  20. LeMasurier et al. 1990, p. 290.
  21. LeMasurier et al. 1990, p. 291.
  22. WADE & La PRADE 1969, p. 93.
  23. Gohl 2007, p. 69.
  24. Wilch, McIntosh & Panter 2021, p. 565.
  25. Johnson et al. 2014, p. 1000.
  26. Abakumov 2010, p. 300.
  27. Herbert et al. 2023, p. 10.
  28. Wilch, McIntosh & Panter 2021, p. 515.
  29. LeMasurier et al. 1990, pp. 259, 261.
  30. Hole, Storey & LeMasurier 1994, p. 91.
  31. Lucas et al. 2020, p. 11.
  32. LeMasurier et al. 1990, p. 12.
  33. O'Donnell et al. 2019, p. 5025.
  34. LeMasurier et al. 1990, p. 260.
  35. Panter et al. 2021, p. 4.
  36. Panter et al. 2021, p. 7.
  37. Panter et al. 2021, p. 10.
  38. LeMasurier et al. 1990, p. 264.
  39. Panter et al. 2021, p. 28.
  40. GILBERT, EARLY & KING 1969, p. 95.
  41. Bockheim 2015, p. 191.
  42. GILBERT, EARLY & KING 1969, p. 96.
  43. Lenaerts et al. 2018, p. 31.
  44. Rutford, Craddock & Bastien 1968, p. 22.
  45. Larter et al. 2014, p. 73.
  46. Ivins et al. 2013, p. 3129.
  47. Larter et al. 2014, p. 75.
  48. Johnson et al. 2014, p. 1001.
  49. Quartini, Blankenship & Young 2021, p. 25.
  50. Corr & Vaughan 2008, p. 123.
  51. LeMasurier et al. 1990, p. 265.
  52. Patrick & Smellie 2013, p. 482.
  53. Loose et al. 2018, p. 7.

Sources
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