Erebus hotspot

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The Erebus hotspot is a volcanic hotspot responsible for the high volcanic activity on Ross Island in the western Ross Sea of Antarctica. Its current eruptive zone, Mount Erebus, has erupted continuously since its discovery in 1841. Magmas of the Erebus hotspot are similar to those erupted from hotspots at the active East African Rift in eastern Africa. Mount Bird at the northernmost end of Ross Island and Mount Terror at its eastern end are large basaltic shield volcanoes that have been potassium-argon dated 3.8–4.8 and 0.8–1.8 million years old. [1]

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There is currently disagreement over the cause of volcanic activity on Ross Island. The traditional view is that the area is underlain by a mantle plume which has given rise to volcanism and, in conjunction with a second plume thought to be under Marie Byrd Land on the mainland to the east, a system of rifts known as the West Antarctic Rift System. Support for a plume origin includes petrological, geochemical, and isotopic evidence for a deep-mantle source, [2] [3] high heat flow in the area, [4] high volcanic output, [5] domal uplift, [6] [7] and seismic anomalies in the upper mantle consistent with a plume approximately 250 to 300 km (160 to 190 mi) in diameter extending 200 km (120 mi) below the surface where it changes into a narrow column that extends at least a further 400 km (250 mi) [8] [9] and according to some studies as deep as 1,000 km (620 mi). [10] [11] The area lacks the time-progressive volcanism typically associated with mantle plumes. This has been explained by the Antarctic Plate being stationary since the late Cretaceous.

Other observations appear to be inconsistent with the plume model. Uplift in the region lacks the circular symmetry typically associated with mantle plumes. Rifting occurred mainly in the late Cretaceous, whereas uplift occurred mainly in the middle Eocene, so uplift followed extension rather than preceding it as would be expected with a mantle plume. The volume of magmatism, when the long duration of volcanic activity is taken into account, appears lower than would be expected to result from a mantle plume. Seismic imaging does not show the circular symmetry expected for a mantle plume but indicates rather a linear, tectonic feature extending from Tasmania to the Ross Sea. [12] [13] [14]

Owing to these issues, some scientists have questioned the plume model and propose instead a shallow, tectonic mechanism. In this view, lithospheric extension and rifting during the late Cretaceous stretched the lithosphere, giving rise to partial melts. Though insufficient to break the surface, fertile, low-liquidus material was distributed throughout the lithospheric mantle. During the middle Eocene, tectonic changes in the Southern Ocean gave rise to further lithospheric deformation, causing strike-slip faulting which enabled decompression melting and extrusion of the fertile material emplaced during the late Cretaceous. [12] [13] [14]

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The plate theory is a model of volcanism that attributes all volcanic activity on Earth, even that which appears superficially to be anomalous, to the operation of plate tectonics. According to the plate theory, the principal cause of volcanism is extension of the lithosphere. Extension of the lithosphere is a function of the lithospheric stress field. The global distribution of volcanic activity at a given time reflects the contemporaneous lithospheric stress field, and changes in the spatial and temporal distribution of volcanoes reflect changes in the stress field. The main factors governing the evolution of the stress field are:

  1. Changes in the configuration of plate boundaries.
  2. Vertical motions.
  3. Thermal contraction.

Intraplate volcanism is volcanism that takes place away from the margins of tectonic plates. Most volcanic activity takes place on plate margins, and there is broad consensus among geologists that this activity is explained well by the theory of plate tectonics. However, the origins of volcanic activity within plates remains controversial.

References

  1. ↑ Morgan, W.J.; Phipps Morgan, J. (2007) "Plate velocities in hotspot reference frame: electronic supplement".
  2. ↑ Hole, M.J.; LeMasurier, W.E. (1994). "Tectonic controls on the geochemical composition of Cenozoic, mafic alkaline volcanic rocks from West Antarctica". Contributions to Mineralogy and Petrology. 117 (2): 187–202. Bibcode:1994CoMP..117..187H. doi:10.1007/BF00286842. S2CID   129078098.
  3. ↑ Sims, K.W.W.; Blichert-Toft, J.; Kyle, P.R.; Pichat, S.; Gauthier, P-J.; Blusztajn, J.; Kelly, P.; Ballf, L.; Layne, G. (2008). "A Sr, Nd, Hf, and Pb isotope perspective on the genesis and long-term evolution of alkaline magmas from Erebus volcano, Antarctica". Journal of Volcanology and Geothermal Research. 177 (3): 606–618. Bibcode:2008JVGR..177..606S. doi:10.1016/j.jvolgeores.2007.08.006.
  4. ↑ Storey, B.; Leat, P.T.; Weaver, S.D.; Pankhurst, R.J.; Bradshaw, J.D.; Kelley, S. (1999). "Mantle plumes and Antarctica-New Zealand rifting: Evidence from mid-Cretaceous mafic dykes". Journal of the Geological Society, London. 156 (4): 659–671. Bibcode:1999JGSoc.156..659S. doi:10.1144/gsjgs.156.4.0659. S2CID   129513402.
  5. ↑ Esser, R.P.; Kyle, P.R.; McIntosh, W.C. (2004). "40Ar/39Ar dating of the eruptive history of Mount Erebus, Antarctica: volcano evolution". Bulletin of Volcanology. 66 (8): 671–686. Bibcode:2004BVol...66..671E. doi:10.1007/s00445-004-0354-x. S2CID   129118037.
  6. ↑ Kyle, P.R.; Moore, J.A.; Thirlwall, M.F. (1992). "Petrologic evolution of anorthoclase phonolite lavas at Mount Erebus, Ross Island, Antarctica". Journal of Petrology. 33 (4): 849–875. doi:10.1093/petrology/33.4.849.
  7. ↑ LeMasurier, W.E.; Landis, C.A. (1996). "Mantle-plume activity recorded by low-relief erosion surfaces in West Antarctica and New Zealand". GSA Bulletin. 108 (11): 1450–1466. Bibcode:1996GSAB..108.1450L. doi:10.1130/0016-7606(1996)108<1450:MPARBL>2.3.CO;2.
  8. ↑ Zhao, D (2007). "Seismic images under 60 hotspots: Search for mantle plumes". Gondwana Research. 12 (4): 335–355. Bibcode:2007GondR..12..335Z. doi:10.1016/j.gr.2007.03.001.
  9. ↑ Gupta, S.; Zhao, D; Raia, S.S. (2009). "Seismic imaging of the upper mantle under the Erebus hotspot in Antarctica". Gondwana Research. 16 (1): 109–118. Bibcode:2009GondR..16..109G. doi:10.1016/j.gr.2009.01.004.
  10. ↑ Sieminski, A.; Debayle, E.; Lévêque, J-J. (2003). "Seismic evidence for deep low-velocity anomalies in the transition zone beneath West Antarctica". Earth and Planetary Science Letters. 216 (4): 645–661. Bibcode:2003E&PSL.216..645S. doi:10.1016/S0012-821X(03)00518-1.
  11. ↑ Montelli, R.; Nolet, G.; Dahlen, F.A.; Masters, G. (2006). "A catalogue of deep mantle plumes: New results from finite‐frequency tomography". Geochemistry, Geophysics, Geosystems. 7 (11): n/a. Bibcode:2006GGG.....711007M. doi: 10.1029/2006GC001248 .
  12. 1 2 Rocchi, S.; Armienti, P.; D’Orazio, M.; Tonarini, S.; Wijbrans, J.R.; Di Vincenzo, G. (2002). "Cenozoic magmatism in the western Ross Embayment: Role of mantle plume versus plate dynamics in the development of the West Antarctic Rift System". Journal of Geophysical Research. 107 (B9): ECV 5-1-ECV 5-22. Bibcode:2002JGRB..107.2195R. doi: 10.1029/2001JB000515 .
  13. 1 2 Rochi, S.; Storti, F.; Di Vincenzo, G.; Rossetti, F. (2003). "Intraplate strike-slip tectonics as an alternative to mantle plume activity for the Cenozoic rift magmatism in the Ross Sea region, Antarctica". In Storti, F; Holdsworth, R.E.; Salvini, F. (eds.). Intraplate strike-slip deformation belts: Geological Society, London, Special Publications, 210. Vol. 210. Geological Society of London. pp. 145–158. doi:10.1144/GSL.SP.2003.210.01.09. S2CID   134316807.{{cite book}}: |journal= ignored (help)
  14. 1 2 Rocchi, S.; Armienti, P.; Di Vincenzo, G. (2005). "No plume, no rift magmatism in the West Antarctic Rift". In Foulger, G.R.; Natland, J.H.; Presnall, D.C.; Anderson, D.L. (eds.). Plates, plumes and paradigms: Geological Society of America Special Paper 388. Geological Society of America. pp. 435–447. doi:10.1130/0-8137-2388-4.435. ISBN   9780813723884.
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