Volcanic explosivity index

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VEI and ejecta volume correlation

The volcanic explosivity index (VEI) is a relative measure of the explosiveness of volcanic eruptions. It was devised by Chris Newhall of the United States Geological Survey and Stephen Self at the University of Hawaii 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 volcanoes in history given magnitude 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 (12 mi). 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[edit]

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 100 from 10,000 to 1,000,000 m3 (350,000 to 35,310,000 cu ft) while the factor is 10 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 Frequency Tropospheric
injection
Stratospheric
injection[2]
Examples
0 < 10^4 m³ Hawaiian Effusive < 100 m continuous negligible none
Kīlauea, Piton de la Fournaise, Erebus
1 > 10^4 m³ Hawaiian / Strombolian Gentle 100 m–1 km fortnightly minor none
Nyiragongo (2002), Raoul Island (2006), Stromboli (continuous since Roman times to present)
2 > 10^6 m³ Strombolian / Vulcanian Explosive 1–5 km monthly moderate none
Unzen (1792), Cumbre Vieja (1949), Galeras (1993), Sinabung (2010)
3 > 10^7 m³ Vulcanian / Peléan/Sub-Plinian Catastrophic 3–15 km 3 months substantial possible
Nevado del Ruiz (1985), Lassen Peak (1915), Soufrière Hills (1995), Nabro (2011)
4 > 10^8 m³ Peléan / Plinian/Sub-Plinian Cataclysmic > 10 km (Plinian or sub-Plinian) 18 months substantial definite
Mayon (1814), Pelée (1902), Galunggung (1982), Eyjafjallajökull (2010)
5 >10^9 m³ Peléan/Plinian Paroxysmic > 10 km (Plinian) 12 years substantial significant
Vesuvius (79), Fuji (1707), Mount Tarawera (1886), St. Helens (1980), Puyehue (2011)
6 > 10^10 m³ Plinian / Ultra-Plinian Colossal > 20 km 50 - 100 yrs substantial substantial
Laacher See (c. 12,900 BC), Veniaminof (c. 1750 BC), Huaynaputina (1600), Krakatoa (1883), Novarupta (1912), Pinatubo (1991)
7 > 10^11 m³ Ultra-Plinian Super-colossal > 20 km 500 - 1,000 yrs substantial substantial
Mazama (c. 5600 BC), Thera (c. 1620 BC), Taupo (180), Baekdu (1000), Samalas (Mount Rinjani) (1257), Tambora (1815)
8 > 10^12 m³ Supervolcanic[citation needed] Apocalyptic[citation needed] > 20 km > 50,000 yrs[3][4] vast vast
La Garita Caldera (26.3 Ma), Yellowstone (640,000 BC), Toba (74,000 BC), Taupo (24,500 BC)

A total of 47 eruptions of VEI 8 magnitude or above, ranging in age from Ordovician to Pleistocene, have been identified, of which 42 occurred in the past 36 million years. The most recent is Lake Taupo's Oruanui eruption, 26,500 years ago, which means that there have not been any Holocene (within the last 10,000 years) eruptions with a VEI of 8.[5] There have been at least five identified Holocene eruptions with a VEI of 7. There are also 58 plinian eruptions, and 13 caldera-forming eruptions, of large, but unknown magnitudes. There are likely many other eruptions that are not identified.[citation needed]

By 2010, the Global Volcanism Program of the Smithsonian Institution had catalogued 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 eruptions known to have occurred during the Holocene. About 90% of these 7,742 eruptions have a VEI of 3 or less. About 49% of these 7,742 eruptions have a VEI of 2.[6]

Limitations of VEI[edit]

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 sulphur dioxide emissions in quantifying their atmospheric and climatic impact, as a 2004 paper by Georgina Miles, Roy Grainger and Eleanor Highwood points out.

“Tephra, or fallout sediment analysis, can provide an estimate of the explosiveness of a known eruption event. It is, however, not obviously related to the amount of SO2 emitted by the eruption. The volcanic explosivity index (VEI) was derived to catalogue the explosive magnitude of historical eruptions, based on the order of magnitude of erupted mass, and gives a general indication as to the height the eruptive column reached. The VEI itself is inadequate for describing the atmospheric effects of volcanic eruptions. This is clearly demonstrated by two eruptions, Agung (1963) and El Chichón (1982). Their VEI classification separates them by an order of magnitude in explosivity, although the volume of SO2 released into the stratosphere by each was measured to be broadly similar, as shown by the optical depth data for the two eruptions.”[7]

Lists of large eruptions[edit]

2011 Puyehue-Cordón Caulle eruption 1980 eruption of Mount St. Helens 1912 eruption of Novarupta Yellowstone Caldera AD 79 Eruption of Mount Vesuvius 1902 eruption of Santa María 1280 eruption of Quilotoa 1600 eruption of Huaynaputina 2010 eruptions of Eyjafjallajökull Yellowstone Caldera 1783 eruption of Laki 1477 eruption of Bárðarbunga 1650 eruption of Kolumbo Volcanic activity at Santorini Toba catastrophe theory Kuril Islands Baekdu Mountain Kikai Caldera 1991 eruption of Mount Pinatubo Long Island (Papua New Guinea) 1815 eruption of Mount Tambora 1883 eruption of Krakatoa 2010 eruptions of Mount Merapi Billy Mitchell (volcano) Taupo Volcano Taupo Volcano Taupo Volcano Crater Lake
Clickable imagemap of notable volcanic eruptions. The apparent volume of each bubble is linearly proportional to the volume of tephra ejected, colour-coded by time of eruption as in the legend. Pink lines denote convergent boundaries, blue lines denote divergent boundaries and yellow spots denote hotspots.

See also[edit]

References[edit]

  1. ^ Newhall, Christopher G.; Self, Stephen (1982). "The Volcanic Explosivity Index (VEI): An Estimate of Explosive Magnitude for Historical Volcanism" (PDF). Journal of Geophysical Research. 87 (C2): 1231–1238. Bibcode:1982JGR....87.1231N. doi:10.1029/JC087iC02p01231. 
  2. ^ "Volcanic Explosivity Index (VEI)". Global Volcanism Program. Smithsonian National Museum of Natural History. Archived from the original on Nov 10, 2011. Retrieved August 21, 2014. 
  3. ^ Dosseto, A. (2011). Turner, S. P.; Van-Orman, J. A., eds. "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. ^ 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. Bibcode:2004BVol...66..735M. doi:10.1007/s00445-004-0355-9. 
  6. ^ 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. 
  7. ^ Miles, M. G.; Grainger, R. G.; Highwood, E. J. (2004). "Volcanic Aerosols: The significance of volcanic eruption strength and frequency for climate" (pdf). Quarterly Journal of the Royal Meteorological Society. 130 (602): 2361–2376. doi:10.1256/qj.30.60. 

External links[edit]