Oruanui eruption

From Wikipedia, the free encyclopedia
Jump to navigation Jump to search
Oruanui eruption
Taupo 2.png
A large eruption column during the Oruanui eruption as it may have appeared from space
VolcanoTaupo Volcano
DateAbout 26,500 BC
TypeUltra-Plinian
LocationNorth Island, New Zealand
38°48′S 175°54′E / 38.800°S 175.900°E / -38.800; 175.900Coordinates: 38°48′S 175°54′E / 38.800°S 175.900°E / -38.800; 175.900
VEI8

The Oruanui eruption of New Zealand's Taupo Volcano, the world's most recent supereruption, had a Volcanic Explosivity Index of 8. It is one of the largest eruptions in the history of New Zealand. It occurred at about 26,500 BC in the Late Pleistocene and generated approximately 430 km3 (100 cu mi) of pyroclastic fall deposits, 320 km3 (77 cu mi) of pyroclastic density current (PDC) deposits (mostly ignimbrite) and 420 km3 (100 cu mi) of primary intracaldera material, equivalent to 530 km3 (130 cu mi) of magma, totaling 1,170 km3 (280 cu mi) of total deposits. The eruption is divided into 10 different phases on the basis of nine mappable fall units and a tenth, poorly preserved but volumetrically dominant fall unit.[1][2][3][4]

Modern-day Lake Taupo (616 km2, 238 sq mi in area and 186 m, 610 ft deep) partly fills the caldera generated during this eruption. A 140 km2 (54 sq mi) structural collapse is concealed beneath Lake Taupo, while the lake outline at least partly reflects volcano-tectonic collapse. Early eruption phases saw shifting vent positions; development of the caldera to its maximum extent (indicated by lithic lag breccias) occurred during phase 10.

The Oruanui eruption shows many unusual features: its episodic nature, wide range of magma-water interaction, and complex interplay of pyroclastic fall and flow deposits.[1] As the eruption occurred through a lake system overlying the vent, many of the deposits contain volcanic ash aggregates.[5]

Tephra from the Oruanui eruption, containing spherical accretionary lapilli

Tephra from the eruption covered much of the central North Island, with ignimbrite up to 200 metres (660 ft) deep. Ashfall affected most of New Zealand, with an ash layer as thick as 18 centimetres (7 in) deposited on the Chatham Islands, 1,000 km (620 mi) away. Later erosion and sedimentation had long-lasting effects on the landscape, and may have caused the Waikato River to shift from the Hauraki Plains to its current course through the Waikato to the Tasman Sea. Less than 22,500 years ago, Lake Taupo, having filled to about 75 m (246 ft) above its current level, cut through its Oruanui ignimbrite dam at a rate which left no terraces around the lake. About 60 km3 (14 cu mi) of water was released, leaving boulders of up to 10 m (33 ft) at least as far down the Waikato River as Mangakino.[6]

See also[edit]

References[edit]

  1. ^ a b Wilson, C. J. N. (2001). "The 26.5ka Oruanui eruption, New Zealand: An introduction and overview". Journal of Volcanology and Geothermal Research. 112 (1–4): 133–174. doi:10.1016/S0377-0273(01)00239-6.
  2. ^ Manville, V.; Wilson, C. J. N. (2004). "The 26.5 ka Oruanui eruption, New Zealand: A review of the roles of volcanism and climate in the post‐eruptive sedimentary response". New Zealand Journal of Geology and Geophysics. 47 (3): 525. doi:10.1080/00288306.2004.9515074.
  3. ^ Wilson, C. J. N. (2005). "The 26.5 ka Oruanui Eruption, Taupo Volcano, New Zealand: Development, Characteristics and Evacuation of a Large Rhyolitic Magma Body". Journal of Petrology. 47: 35–69. doi:10.1093/petrology/egi066.
  4. ^ Richard Smith, David J. Lowe and Ian Wright. 'Volcanoes - Lake Taupo', Te Ara - the Encyclopedia of New Zealand, updated 16 April 2007.
  5. ^ Van Eaton, Alexa R.; Wilson, Colin J. N. (2013). "The nature, origins and distribution of ash aggregates in a large-scale wet eruption deposit: Oruanui, New Zealand". Journal of Volcanology and Geothermal Research. 250: 129–154. doi:10.1016/j.jvolgeores.2012.10.016.
  6. ^ Manville, V.; Hodgson, K. A.; Nairn, I. A. (June 2007). "A review of break‐out floods from volcanogenic lakes in New Zealand". New Zealand Journal of Geology and Geophysics. 50 (2): 131–150. doi:10.1080/00288300709509826. ISSN 0028-8306. S2CID 129792354.