Taupo Volcanic Zone

Mount Ngauruhoe
Satellite photo of the Lake Taupo caldera
Volcano and lake/caldera locations in the Taupo Volcanic Zone. The distance between the town of Rotorua and the town of Taupo is 80 km. (White Island is not shown.)
Whakaari/White Island

The Taupo Volcanic Zone is a highly active volcanic V shaped area in the North Island of New Zealand that is spreading east -west at the rate of about 8mm per year. It is named after Lake Taupo, the flooded caldera of the largest volcano in the zone.

Activity

There are numerous volcanic vents and geothermal fields in the zone, with Mount Ruapehu, Mount Ngauruhoe and White Island erupting most frequently. The zone's largest eruption since the arrival of Europeans was that of Mount Tarawera in 1886, which killed over 100 people. Early Maori would also have been affected by the much larger Kaharoa eruption from Tarawera around 1300 AD.[1]

The last major eruption from Lake Taupo, the Hatepe eruption, occurred in 181 AD. It is believed to have first emptied the lake then followed that feat with a pyroclastic flow that covered about 20,000 square kilometres (7,722 sq mi) of land with volcanic ash. A total of 120 km3 (29 cu mi) of material is believed to have been ejected, and over 30 km3 (7.2 cu mi) of material is estimated to have been ejected in just a few minutes. The date of this activity is known since the ash expulsion was sufficiently large to turn the sky red over Rome and China (as documented in Hou Han Shu).

Taupo erupted an estimated 1,170 km3 (280 cu mi) of material in its Oruanui eruption 26,500 years ago. This was Earth's most recent eruption reaching VEI-8, the highest level on the Volcanic Explosivity Index.

The Rotorua caldera has been dormant longer, with its main eruption occurring about 240,000 years ago, although lava dome extrusion has occurred within the last 25,000 years.[2]

Extent and geological context

The Taupo Volcanic Zone is approximately 350 kilometres (217 mi) long by 50 kilometres (31 mi) wide. Mount Ruapehu marks its southwestern end, while the submarine Whakatane volcano (85 kilometres (53 mi) beyond White Island) is considered its northeastern limit.[3]

It forms a southern portion of the active Lau-Havre-Taupo back-arc basin, which lies behind the Kermadec-Tonga subduction zone.[4] Volcanic activity continues to the north-northeast, along the line of the Taupo Volcanic Zone, through several undersea volcanoes (known as Clark, Tangaroa, the Silents and the Rumbles), then shifts eastward to the parallel volcanic arc of the Kermadec Islands and Tonga. Although the back-arc basin continues to propagate to the southwest, with the South Wanganui Basin forming an initial back-arc basin, volcanic activity has not yet begun in this region.[5]

South of Kaikoura the plate boundary changes to a transform boundary with oblique continental collision uplifting the Southern Alps in the South Island. A subduction zone reappears southwest of Fiordland, at the southwestern corner of the South Island, although here the subduction is in the opposite direction. Solander Island is an extinct volcano associated with this subduction zone, and the only one that protudes above the sea.

Scientific study

Recent scientific work indicates that the Earth's crust below the Taupo Volcanic Zone may be as little as 16 kilometres thick. A film of magma 50 kilometres (30 mi) wide and 160 kilometres (100 mi) long lies 10 kilometres under the surface.[6][7] The geological record indicates that some of the volcanoes in the area erupt infrequently but have large, violent and destructive eruptions when they do. There is also some possible rifting in the Taupo Volcanic Zone.

Volcanoes, lakes and geothermal fields

See also List of volcanoes in New Zealand#Taupo Volcanic Zone.

The following Volcanic Centers belong to the Taupo Volcanic Zone:

Rotorua, Okataina, Maroa, Taupo, Tongariro and Mangakino.[8][9]

In 1886, Mount Tarawera produced New Zealand's largest historic eruption
Lady Knox Geyser, Waiotapu geothermal area
Craters of the Moon geothermal area
Composite satellite image of Mount Ruapehu
Satellite view of the Lake Rotorua Caldera. Mount Tarawera is in the lower right corner.
Southwest side of Mount Tarawera, Mount Edgecumbe on the background.

        Other important features of the TVZ include the Whakatane, Ngakuru and Ruapehu grabens.

Note


There is nowadays a somewhat different classification:[16][17]

Panorama across Lake Taupo

See also

References

  1. ↑ David, Lowe. "Polynesian settlement and impacts of volcanism on early Maori society". In Lowe, D.J. Guidebook for ‘Land and Lakes’ field trip, New Zealand Society of Soil Science Biennial Conference, Rotorua, held in 27–30 November 2006 (PDF). Lincoln: New Zealand Society of Soil Science. pp. 50–55.
  2. ↑ "Rotorua". Global Volcanism Program. Smithsonian Institution. Retrieved 2010-08-31.
  3. ↑ Gamble, J. A.; Wright, I. C.; Baker, J. A. (1993). "Seafloor geology and petrology in the oceanic to continental transition zone of the Kermadec-Havre-Taupo Volcanic Zone arc system, New Zealand". New Zealand Journal of Geology and Geophysics. 36 (4): 417–435. doi:10.1080/00288306.1993.9514588.
  4. ↑ Parson, L. M.; Wright, I. C. (1996). "The Lau-Havre-Taupo back-arc basin: A southward-propagating, multi-stage evolution from rifting to spreading". Tectonophysics. 263: 1–22. Bibcode:1996Tectp.263....1P. doi:10.1016/S0040-1951(96)00029-7.
  5. ↑ Villamor, P.; Berryman, K. R. (2006). "Evolution of the southern termination of the Taupo Rift, New Zealand". New Zealand Journal of Geology and Geophysics. 49: 23–37. doi:10.1080/00288306.2006.9515145.
  6. ↑ Easton, Paul (15 September 2007). "Central North Island sitting on magma film". The Dominion Post. Retrieved 16 March 2008.
  7. ↑ Heise, W.; Bibby, H.M.; Caldwell, T.G. (2007). "Imaging magmatic Processes in the Taupo Volcanic Zone (New Zealand) with Magnetotellurics" (PDF). Geophysical Research Abstracts. 9. 01311.
  8. ↑ Cole, J.W. (1990). "Structural control and origin of volcanism in the Taupo volcanic zone, New Zealand". Bulletin of Volcanology. 52 (6): 445–459. Bibcode:1990BVol...52..445C. doi:10.1007/BF00268925.
  9. ↑ "New Zealand".
  10. 1 2 3 4 5 6 7 http://www.volcano.si.edu/world/largeeruptions.cfm
  11. ↑ Newhall, Christopher G.; Dzurisin, Daniel (1988). "Historical unrest at large calderas of the world". USGS Bulletin. 1855: 1108. Citing Scott, B.J. (1986). Gregory, J.G.; Watters, W.A., eds. "Volcanic hazards assessment in New Zealand". New Zealand Geol. Surv. Rec. 10: 49–54. |chapter= ignored (help)
  12. ↑ Okataina Volcanic Center, New Zealand
  13. ↑ Nairn, I.A. (2002). "Geology of the Okatania Volcanic Centre". Geological Map 25. Institute of Geological and Nuclear Sciences: 156.
  14. 1 2 Hodgson, K. A.; Nairn, I. A. (August 2004). "The Sedimentation and Drainage History of Haroharo Caldera and The Tarawera River System, Taupo Volcanic Zone, New Zealand" (PDF). Operations Publication 2004/03. Environment Bay of Plenty: 7. ISSN 1176-5550.
  15. ↑ Krippner, Stephen J. P.; Briggs, Roger M.; Wilson, Colin J. N.; Cole, James W. (1998). "Petrography and geochemistry of lithic fragments in ignimbrites from the Mangakino Volcanic Centre: implications for the composition of the subvolcanic crust in western Taupo Volcanic Zone, New Zealand". New Zealand Journal of Geology and Geophysics. 41 (2): 187–199. doi:10.1080/00288306.1998.9514803.
  16. ↑ Cole, J. W.; Spinks, K. D. (2009). "Caldera volcanism and rift structure in the Taupo Volcanic Zone, New Zealand". Special Publications. London: Geological Society. 327 (1): 9–29. Bibcode:2009GSLSP.327....9C. doi:10.1144/SP327.2.
  17. ↑ Hiess, J; Cole, JW; Spinks, KD (2007). High-Alumina Basalts of the Taupo Volcanic Zone, New Zealand: Influence of the Crust and Crustal Structure (PDF). p. 36. Part of a BSc Project by Hiess, J. (University of Canterbury).
  18. ↑ Gravley, D. M.; Wilson, C. J. N.; Rosenberg, M. D.; Leonard, G. S. (2006). "The nature and age of Ohakuri Formation and Ohakuri Group rocks in surface exposures and geothermal drillhole sequences in the central Taupo Volcanic Zone, New Zealand". New Zealand Journal of Geology and Geophysics. 49 (3): 305–308. doi:10.1080/00288306.2006.9515169.
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