Earth:Volcanic explosivity index

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Short description: Qualitative scale for explosiveness of volcanic eruptions
VEI and ejecta volume correlation

The volcanic explosivity index (VEI) is a relative measure of the explosiveness of volcanic eruptions. It was devised by Christopher G. Newhall of the United States Geological Survey and Stephen Self in 1982.

Volume of products, eruption cloud height, and qualitative observations (using terms ranging from "gentle" to "mega-colossal") are used to determine the explosivity value. The scale is open-ended with the largest eruptions in history given a magnitude of 8. A value of 0 is given for non-explosive eruptions, defined as less than 10,000 m3 (350,000 cu ft) of tephra ejected; and 8 representing a mega-colossal explosive eruption that can eject 1.0×1012 m3 (240 cubic miles) of tephra and have a cloud column height of over 20 km (66,000 ft). The scale is logarithmic, with each interval on the scale representing a tenfold increase in observed ejecta criteria, with the exception of between VEI-0, VEI-1 and VEI-2.[1]

Classification

With indices running from 0 to 8, the VEI associated with an eruption is dependent on how much volcanic material is thrown out, to what height, and how long the eruption lasts. The scale is logarithmic from VEI-2 and up; an increase of 1 index indicates an eruption that is 10 times as powerful. As such, there is a discontinuity in the definition of the VEI between indices 1 and 2. The lower border of the volume of ejecta jumps by a factor of one hundred, from 10,000 to 1,000,000 m3 (350,000 to 35,310,000 cu ft), while the factor is ten between all higher indices. In the following table, the frequency of each VEI indicates the approximate frequency of new eruptions of that VEI or higher.

VEI Ejecta
volume
(bulk) 		Classification Description Plume Periodicity Tropospheric
injection 		Stratospheric
injection[2]
Examples
0 < 104 m3 Hawaiian Effusive < 100 m constant negligible none
Kīlauea (current), Mawson Peak (current), Dallol (2011), Holuhraun (2014-2015), Fagradalsfjall (2021-2023), Mauna Loa (1975, 1984, 2022)
> 104 m3 Hawaiian / Strombolian Gentle 100 m – 1 km daily minor none
Yakedake (1995), Raoul Island (2006), Havre Seamount (2012), Dieng Volcanic Complex (1964, 1979, 2017), Nyiragongo (1977, 2002, 2021)
> 106 m3 Strombolian / Vulcanian Explosive 1–5 km 2 weeks moderate none
Stromboli (since 1934), Etna (current), Unzen (1792), Ruang (1871), Ritter Island (1888), Galeras (1993), Whakaari / White Island (2019)
> 107 m3 Strombolian / Vulcanian / Peléan / Sub-Plinian Severe 3–15 km 3 months substantial possible
Surtsey (1963-1967), Nevado del Ruiz (1985), Redoubt (1989-1990), Soufrière Hills (1997), Ontake (2014), Fuego (2018), Cumbre Vieja (2021)
> 0.1 km3 Peléan / Plinian / Sub-Plinian Catastrophic > 10 km 18 months substantial definite
Laki (1783), Bandai (1888), Pelée (1902), Lamington (1951), Eyjafjallajökull (2010), Merapi (2010), Taal (2020), Semeru (2021)
> 1 km3 Peléan / Plinian Cataclysmic > 10 km 12 years substantial significant
Vesuvius (79), Fuji (1707), Tarawera (1886), St. Helens (1980), El Chichón (1982), Puyehue (2011), Hunga Tonga–Hunga Haʻapai (2022)
> 10 km3 Plinian / Ultra-Plinian Colossal > 20 km 50–100 years substantial substantial
Santorini (1620 BC), Lake Ilopango (450), Huaynaputina (1600), Krakatoa (1883), Santa Maria (1902), Novarupta (1912), Pinatubo (1991)
> 100 km3 Ultra-Plinian Super-colossal > 20 km 500–1,000 years substantial substantial
Long Valley (760 kyr), Campi Flegrei (37 kyr), Aira (22 kyr), Mazama (5700 BC), Kikai (4300 BC), Samalas (1257), Tambora (1815)
> 1,000 km3 Ultra-Plinian Mega-colossal > 20 km > 50,000 years[3][4] vast vast
Flat Landing Brook (Ordovician), Wah Wah Springs (30 Mya), La Garita (26.3 Mya), Yellowstone (2.1 Mya, 640 kyr), Toba (74 kyr), Taupō (26.5 kyr)

About 40 eruptions of VEI-8 magnitude within the last 132 million years (Mya) have been identified, of which 30 occurred in the past 36 million years. Considering the estimated frequency is on the order of once in 50,000 years,[3] there are likely many such eruptions in the last 132 Mya that are not yet known. Based on incomplete statistics, other authors assume that at least 60 VEI-8 eruptions have been identified.[5][6] The most recent is Lake Taupō's Oruanui eruption, more than 27,000 years ago, which means that there have not been any Holocene eruptions with a VEI of 8.[5]

There have been at least 10 eruptions of VEI-7 in the last 11,700 years. There are also 58 Plinian eruptions, and 13 caldera-forming eruptions, of large, but unknown magnitudes. By 2010, the Global Volcanism Program of the Smithsonian Institution had cataloged the assignment of a VEI for 7,742 volcanic eruptions that occurred during the Holocene (the last 11,700 years) which account for about 75% of the total known eruptions during the Holocene. Of these 7,742 eruptions, about 49% have a VEI of 2 or lower, and 90% have a VEI of 3 or lower.[7]

Limitations

Under the VEI, ash, lava, lava bombs, and ignimbrite are all treated alike. Density and vesicularity (gas bubbling) of the volcanic products in question is not taken into account. In contrast, the DRE (dense-rock equivalent) is sometimes calculated to give the actual amount of magma erupted. Another weakness of the VEI is that it does not take into account the power output of an eruption, which makes the VEI extremely difficult to determine with prehistoric or unobserved eruptions.

Although VEI is quite suitable for classifying the explosive magnitude of eruptions, the index is not as significant as sulfur dioxide emissions in quantifying their atmospheric and climatic impact.[8]

Lists of notable eruptions

  • Timeline of volcanism on Earth (mostly VEI-6, within 2 kya)
  • List of volcanic eruptions 1500–1999
  • List of volcanic eruptions in the 21st century
  • List of volcanic eruptions by death toll
  • List of large Holocene volcanic eruptions (VEI-5–7)
  • List of large volcanic eruptions (VEI-5–8, within 450+ Mya)
  • List of largest volcanic eruptions (VEI-7–8, mostly within 500 Mya)

See also

References

  1. ↑ Newhall, Christopher G.; Self, Stephen (1982). "The Volcanic Explosivity Index (VEI): An Estimate of Explosive Magnitude for Historical Volcanism". Journal of Geophysical Research 87 (C2): 1231–1238. doi:10.1029/JC087iC02p01231. Bibcode: 1982JGR....87.1231N. http://www.agu.org/books/hg/v002/HG002p0143/HG002p0143.pdf. 
  2. ↑ "Volcanic Explosivity Index (VEI)". Global Volcanism Program. Smithsonian National Museum of Natural History. http://www.volcano.si.edu/world/eruptioncriteria.cfm#VEI. 
  3. ↑ 3.0 3.1 Dosseto, A. (2011). Timescales of Magmatic Processes: From Core to Atmosphere. Wiley-Blackwell. ISBN 978-1-4443-3260-5. 
  4. ↑ Rothery, David A. (2010), Volcanoes, Earthquakes and Tsunamis, Teach Yourself 
  5. ↑ 5.0 5.1 Mason, Ben G.; Pyle, David M.; Oppenheimer, Clive (2004). "The size and frequency of the largest explosive eruptions on Earth". Bulletin of Volcanology 66 (8): 735–748. doi:10.1007/s00445-004-0355-9. Bibcode: 2004BVol...66..735M. 
  6. ↑ Bryan, S.E. (2010). "The largest volcanic eruptions on Earth". Earth-Science Reviews 102 (3–4): 207–229. doi:10.1016/j.earscirev.2010.07.001. Bibcode: 2010ESRv..102..207B. https://eprints.qut.edu.au/40259/1/c40259.pdf. 
  7. ↑ Siebert, L.; Simkin, T.; Kimberly, P. (2010). Volcanoes of the World (3rd ed.). University of California Press. pp. 28–38. ISBN 978-0-520-26877-7. 
  8. ↑ Miles, M. G.; Grainger, R. G.; Highwood, E. J. (2004). "Volcanic Aerosols: The significance of volcanic eruption strength and frequency for climate". Quarterly Journal of the Royal Meteorological Society 130 (602): 2361–2376. doi:10.1256/qj.03.60. Bibcode: 2004QJRMS.130.2361M. http://eodg.atm.ox.ac.uk/eodg/papers/2004Miles1.pdf. 

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