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Hotspot (geology)

In geology, hotspots (or hot spots) are volcanic locales thought to be fed by underlying mantle that is anomalously hot compared with the surrounding mantle.[1] Examples include the Hawaii, Iceland, and Yellowstone hotspots. A hotspot's position on the Earth's surface is independent of tectonic plate boundaries, and so hotspots may create a chain of volcanoes as the plates move above them.

Diagram showing a cross section through Earth at the Hawaii hotspot. Magma originating in the mantle rises into the asthenosphere and lithosphere. A chain of volcanoes is created as the lithosphere moves over the source of magma.

There are two hypotheses that attempt to explain their origins. One suggests that hotspots are due to mantle plumes that rise as thermal diapirs from the core–mantle boundary.[2] The alternative plate theory is that the mantle source beneath a hotspot is not anomalously hot, rather the crust above is unusually weak or thin, so that lithospheric extension permits the passive rising of melt from shallow depths.[3][4]

Origin

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Schematic diagram showing the physical processes inside the Earth that lead to the generation of magma. Partial melting begins above the fusion point.
 
Map showing approximate location of many current hotspots and the relationship to current tectonic plates and their boundaries and movement vectors

The origins of the concept of hotspots lie in the work of J. Tuzo Wilson, who postulated in 1963 that the formation of the Hawaiian Islands resulted from the slow movement of a tectonic plate across a hot region beneath the surface.[5] It was later postulated that hotspots are fed by streams of hot mantle rising from the Earth's core–mantle boundary in a structure called a mantle plume.[6] Whether or not such mantle plumes exist has been the subject of a major controversy in Earth science,[4][7] but seismic images consistent with evolving theory now exist.[8]

At any place where volcanism is not linked to a constructive or destructive plate margin, the concept of a hotspot has been used to explain its origin. A review article by Courtillot et al.[9] listing possible hotspots makes a distinction between primary hotspots coming from deep within the mantle and secondary hotspots derived from mantle plumes. The primary hotspots originate from the core/mantle boundary and create large volcanic provinces with linear tracks (Easter Island, Iceland, Hawaii, Afar, Louisville, Reunion, and Tristan confirmed; Galapagos, Kerguelen and Marquersas likely). The secondary hotspots originate at the upper/lower mantle boundary, and do not form large volcanic provinces, but island chains (Samoa, Tahiti, Cook, Pitcairn, Caroline, MacDonald confirmed, with up to 20 or so more possible). Other potential hotspots are the result of shallow mantle material surfacing in areas of lithospheric break-up caused by tension and are thus a very different type of volcanism.

Estimates for the number of hotspots postulated to be fed by mantle plumes have ranged from about 20 to several thousand, with most geologists considering a few tens to exist.[8] Hawaii, Réunion, Yellowstone, Galápagos, and Iceland are some of the most active volcanic regions to which the hypothesis is applied. The plumes imaged to date vary widely in width and other characteristics, and are tilted, being not the simple, relatively narrow and purely thermal plumes many expected.[8] Only one, (Yellowstone) has as yet been consistently modelled and imaged from deep mantle to surface.[8]

Composition

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Most hotspot volcanoes are basaltic (e.g., Hawaii, Tahiti). As a result, they are less explosive than subduction zone volcanoes, in which water is trapped under the overriding plate. Where hotspots occur in continental regions, basaltic magma rises through the continental crust, which melts to form rhyolites. These rhyolites can form violent eruptions.[10][11] For example, the Yellowstone Caldera was formed by some of the most powerful volcanic explosions in geologic history. However, when the rhyolite is completely erupted, it may be followed by eruptions of basaltic magma rising through the same lithospheric fissures (cracks in the lithosphere). An example of this activity is the Ilgachuz Range in British Columbia, which was created by an early complex series of trachyte and rhyolite eruptions, and late extrusion of a sequence of basaltic lava flows.[12]

The hotspot hypothesis is now closely linked to the mantle plume hypothesis.[13][8] The detailed compositional studies now possible on hotspot basalts have allowed linkage of samples over the wider areas often implicate in the later hypothesis,[14] and it's seismic imaging developments.[8]

Contrast with subduction zone island arcs

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Hotspot volcanoes are considered to have a fundamentally different origin from island arc volcanoes. The latter form over subduction zones, at converging plate boundaries. When one oceanic plate meets another, the denser plate is forced downward into a deep ocean trench. This plate, as it is subducted, releases water into the base of the over-riding plate, and this water mixes with the rock, thus changing its composition causing some rock to melt and rise. It is this that fuels a chain of volcanoes, such as the Aleutian Islands, near Alaska.

Hotspot volcanic chains

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Over millions of years, the Pacific Plate has moved over the Hawaii hotspot, creating a trail of underwater mountains that stretches across the Pacific.
 
Kilauea is the most active shield volcano in the world. The volcano erupted from 1983 to 2018 and is part of the Hawaiian–Emperor seamount chain.
 
Mauna Loa is a large shield volcano. Its last eruption was in 2022 and it is part of the Hawaiian–Emperor seamount chain.
 
Bowie Seamount is a dormant submarine volcano and part of the Kodiak-Bowie Seamount chain.
 
Axial Seamount is the youngest seamount of the Cobb–Eickelberg Seamount chain. Its last eruption was in 2015.
 
Mauna Kea is the tallest volcano in the Hawaiian–Emperor seamount chain. Many cinder cones have been emplaced around its summit.
 
Hualalai is a massive shield volcano in the Hawaiian–Emperor seamount chain. Its last eruption was in 1801.

The joint mantle plume/hotspot hypothesis originally envisaged the feeder structures to be fixed relative to one another, with the continents and seafloor drifting overhead. The hypothesis thus predicts that time-progressive chains of volcanoes are developed on the surface. Examples are Yellowstone, which lies at the end of a chain of extinct calderas, which become progressively older to the west. Another example is the Hawaiian archipelago, where islands become progressively older and more deeply eroded to the northwest.

Geologists have tried to use hotspot volcanic chains to track the movement of the Earth's tectonic plates. This effort has been vexed by the lack of very long chains, by the fact that many are not time-progressive (e.g. the Galápagos) and by the fact that hotspots do not appear to be fixed relative to one another (e.g. Hawaii and Iceland).[15] That mantle plumes are much more complex than originally hypothesised and move independently of each other and plates is now used to explain such observations.[8]

In 2020, Wei et al. used seismic tomography to detect the oceanic plateau, formed about 100 million years ago by the hypothesized mantle plume head of the Hawaii-Emperor seamount chain, now subducted to a depth of 800 km under eastern Siberia.[16]

Postulated hotspot volcano chains

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An example of mantle plume locations suggested by one recent group.[9] Figure from Foulger (2010).[4]

List of volcanic regions postulated to be hotspots

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Distribution of hotspots in the list to the left, with the numbers corresponding to those in the list. The Afar hotspot (29) is misplaced.
Map all coordinates using OpenStreetMap

Download coordinates as:

Eurasian Plate

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African Plate

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Antarctic Plate

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South American Plate

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North American Plate

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Australian Plate

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Nazca Plate

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Pacific Plate

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Over millions of years, the Pacific Plate has moved over the Bowie hotspot, creating the Kodiak–Bowie Seamount chain in the Gulf of Alaska.
 
The Hotspot highway in the south Pacific Ocean

Former hotspots

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See also

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References

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  1. ^ "The source of Yellowstone's heat". USGS. 16 April 2018. Retrieved 14 June 2021.
  2. ^ a b W. J. Morgan (5 March 1971). "Convection Plumes in the Lower Mantle". Nature. 230 (5288): 42–43. Bibcode:1971Natur.230...42M. doi:10.1038/230042a0. S2CID 4145715.
  3. ^ "Do plumes exist?". Retrieved 25 April 2010.
  4. ^ a b c Foulger, G.R. (2010). Plates vs. Plumes: A Geological Controversy. Wiley-Blackwell. ISBN 978-1-4051-6148-0.
  5. ^ Wilson, J. Tuzo (1963). "A possible origin of the Hawaiian Islands" (PDF). Canadian Journal of Physics. 41 (6): 863–870. Bibcode:1963CaJPh..41..863W. doi:10.1139/p63-094.
  6. ^ "Hotspots: Mantle thermal plumes". United States Geological Survey. 5 May 1999. Retrieved 15 May 2008.
  7. ^ Wright, Laura (November 2000). "Earth's interior: Raising hot spots". Geotimes. American Geological Institute. Retrieved 15 June 2008.
  8. ^ a b c d e f g Koppers, A.A.; Becker, T.W.; Jackson, M.G.; Konrad, K.; Müller, R.D.; Romanowicz, B.; Steinberger, B.; Whittaker, J.M. (2021). "Mantle plumes and their role in Earth processes" (PDF). Nature Reviews Earth & Environment. 2 (6): 382–401. Bibcode:2021NRvEE...2..382K. doi:10.1038/s43017-021-00168-6. Retrieved 21 November 2023.
  9. ^ a b Courtillot, V.; Davaillie, A.; Besse, J.; Stock, J. (2003). "Three distinct types of hotspots in the Earth's mantle". Earth Planet. Sci. Lett. 205 (3–4): 295–308. Bibcode:2003E&PSL.205..295C. CiteSeerX 10.1.1.693.6042. doi:10.1016/S0012-821X(02)01048-8.
  10. ^ Donald Hyndman; David Hyndman (1 January 2016). Natural Hazards and Disasters. Cengage Learning. pp. 44–. ISBN 978-1-305-88818-0.
  11. ^ Wolfgang Frisch; Martin Meschede; Ronald C. Blakey (2 November 2010). Plate Tectonics: Continental Drift and Mountain Building. Springer Science & Business Media. pp. 87–. ISBN 978-3-540-76504-2.
  12. ^ Holbek, Peter (November 1983). "Report on Preliminary Geology and Geochemistry of the Ilga Claim Group" (PDF). Archived from the original (PDF) on 12 January 2014. Retrieved 15 June 2008. {{cite journal}}: Cite journal requires |journal= (help)
  13. ^ Mainak Choudhuri; Michal Nemčok (22 August 2016). Mantle Plumes and Their Effects. Springer. pp. 18–. ISBN 978-3-319-44239-6.
  14. ^ a b c Bredow, E; Steinberger, B (16 January 2018). "Variable melt production rate of the Kerguelen hotspot due to long-term plume-ridge interaction". Geophysical Research Letters. 45 (1): 126–36. Bibcode:2018GeoRL..45..126B. doi:10.1002/2017GL075822. hdl:10852/70913.
  15. ^ Sager, William W. (4 June 2007). "Insight into Motion of the Hawaiian Hotspot from Paleomagnetism". www.MantlePlumes.org.
  16. ^ Wei, Songqiao Shawn; Shearer, Peter M.; Lithgow-Bertelloni, Carolina; Stixrude, Lars; Tian, Dongdong (20 November 2020). "Oceanic plateau of the Hawaiian mantle plume head subducted to the uppermost lower mantle". Science. 370 (6519): 983–987. Bibcode:2020Sci...370..983W. doi:10.1126/science.abd0312. ISSN 0036-8075. PMID 33214281. S2CID 227059993.
  17. ^ E. V. Verzhbitsky (2003). "Geothermal regime and genesis of the Ninety-East and Chagos-Laccadive ridges". Journal of Geodynamics. 35 (3): 289. Bibcode:2003JGeo...35..289V. doi:10.1016/S0264-3707(02)00068-6.
  18. ^ a b Carracedo, Juan Carlos; Troll, Valentin R. (1 January 2021). "North-East Atlantic Islands: The Macaronesian Archipelagos". Encyclopedia of Geology. pp. 674–699. doi:10.1016/B978-0-08-102908-4.00027-8. ISBN 9780081029091. S2CID 226588940.
  19. ^ a b c d e f g h i j k l m n o p q r s t u v w x y z aa ab ac ad ae af ag ah ai aj ak al am an ao ap aq ar as at au av aw ax ay az ba bb bc bd be bf bg bh bi W. J. Morgan and J. P. Morgan. "Plate velocities in hotspot reference frame: electronic supplement" (PDF). Retrieved 6 November 2011.
  20. ^ Nielsen, Søren B.; Stephenson, Randell; Thomsen, Erik (13 December 2007). "Letter:Dynamics of Mid-Palaeocene North Atlantic rifting linked with European intra-plate deformations". Nature. 450 (7172): 1071–1074. Bibcode:2007Natur.450.1071N. doi:10.1038/nature06379. PMID 18075591. S2CID 4428980.
  21. ^ O'Neill, C.; Müller, R. D.; Steinberger, B. (2003). "Revised Indian plate rotations based on the motion of Indian Ocean hotspots" (PDF). Earth and Planetary Science Letters. 215 (1–2): 151–168. Bibcode:2003E&PSL.215..151O. CiteSeerX 10.1.1.716.4910. doi:10.1016/S0012-821X(03)00368-6. Archived from the original (PDF) on 26 July 2011.
  22. ^ O'Connor, J. M.; le Roex, A. P. (1992). "South Atlantic hot spot-plume systems. 1: Distribution of volcanism in time and space". Earth and Planetary Science Letters. 113 (3): 343–364. Bibcode:1992E&PSL.113..343O. doi:10.1016/0012-821X(92)90138-L.
  23. ^ Smith, Robert B.; Jordan, Michael; Steinberger, Bernhard; Puskas, Christine M.; Farrell, Jamie; Waite, Gregory P.; Husen, Stephan; Chang, Wu-Lung; O'Connell, Richard (20 November 2009). "Geodynamics of the Yellowstone hotspot and mantle plume: Seismic and GPS imaging, kinematics and mantle flow" (PDF). Journal of Volcanology and Geothermal Research. 188 (1–3): 26–56. Bibcode:2009JVGR..188...26S. doi:10.1016/j.jvolgeores.2009.08.020.
  24. ^ "Catalogue of Canadian volcanoes- Anahim volcanic belt". Natural Resources Canada. Geological Survey of Canada. Archived from the original on 16 July 2011. Retrieved 14 June 2008.

Further reading

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Wikimedia Commons has media related to Hot spots (volcanism).
 
The Wikibook Historical Geology has a page on the topic of: Hotspots

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