Taupo Volcano

Lake Taupō, in the centre of New Zealand’s North Island, is the caldera of a large rhyolitic supervolcano called the Taupō Volcano. This huge volcano has produced two of the world’s most violent eruptions in geologically recent times.

Volcano, lake, and caldera locations in the Taupō Volcanic Zone

The Taupō Volcano forms part of the Taupō Volcanic Zone, a region of volcanic activity that extends from Ruapehu in the South, through the Taupō and Rotorua districts, to White Island, in the Bay of Plenty region.

Taupō began erupting about 300,000 years ago, but the main eruptions that still affect the surrounding landscape are the Oruanui eruption, about 26,500 years ago, which is responsible for the shape of the modern caldera, and the Hatepe eruption, dated 232 ± 5 CE.[1] However, there have been many more eruptions, with major ones every thousand years or so (see timeline of last 10,000 years of eruptions).[2][3][4]

Considering recent history alone, the volcano has been inactive for an unusually long period of time, but considering its long-term activity, it was inactive for much longer between 8100 and 5100 BC (3,000 year inactivity, compared to the current 1,800 years). Some volcanoes within the Taupō Volcanic Zone have erupted far more recently, however, notably a violent VEI-5 eruption of Mount Tarawera in 1886, and frequent activity of Whakaari/White Island, which erupted most recently in December 2019.

Rhyolitic eruptions

The Taupō Volcano erupts rhyolite, a viscous magma, with a high silica content.

If the magma does not contain much gas, rhyolite tends to just form a lava dome. However, when mixed with gas or steam, rhyolitic eruptions can be extremely violent. The magma froths to form pumice and ash, which is thrown out with great force.

If the volcano creates a stable plume, high in the atmosphere, the pumice and ash is blown sideways, and eventually falls to the ground, draping the landscape like snow.

If the material thrown out cools too rapidly, and becomes denser than the air, it cannot rise as high, and suddenly collapses back to the ground, forming a pyroclastic flow, hitting the surface like water from a waterfall, and spreading sideways across the land at enormous speed. When the pumice and ash settles, it is sufficiently hot to stick together as a rock called ignimbrite. Pyroclastic flows can travel hundreds of kilometres an hour.

Earlier eruptions

Earlier ignimbrite eruptions occurred further north than Taupō. Some of these were enormous, and two eruptions around 1.25 and 1.0 million years ago were big enough to generate an ignimbrite sheet that covered the North Island from Auckland to Napier.

While Taupō has been active for 300,000 years, explosive eruptions became more common 65,000 years ago.

Oruanui eruption
Main article: Oruanui eruption
A large eruption column during the Oruanui eruption as it may have appeared from space

The Oruanui eruption of the Taupō Volcano was the world's largest known eruption in the past 70,000 years, with a Volcanic Explosivity Index of 8. It occurred around 26,500 years ago and generated approximately 430 km³ of pyroclastic fall deposits, 320 km³ of pyroclastic density current (PDC) deposits (mostly ignimbrite) and 420 km³ of primary intracaldera material, equivalent to 530 km³ of magma.[5][6][7]

Modern Lake Taupō partly fills the caldera generated during this eruption.

Tephra from the eruption covered much of the central North Island with ignimbrite up to 200 metres deep. Most of New Zealand was affected by ashfall, with even an 18 cm ash layer left on the Chatham Islands, 1,000 km away. Later erosion and sedimentation had long-lasting effects on the landscape, and caused the Waikato River to shift from the Hauraki Plains to its current course through the Waikato to the Tasman Sea.

Hatepe eruption
Main article: Hatepe eruption
The Taupō eruption's three main vents ran parallel to Lake Taupō's current southeastern shore.

The Taupō eruption (also known as the Hatepe eruption) represents the most recent major eruption of the Taupō Volcano, and occurred about 1,800 years ago. It represents the most violent eruption in the world in the last 5,000 years.[8][9]

Stages of eruption

The eruption went through several stages.

  • A minor eruption occurred beneath the ancestral Lake Taupō.
  • A dramatic increase in activity produced a high eruption column from a second vent, and pumice was deposited over a wide area.
  • Water entered the first vent, and mixed with the magma, producing a white ash-rich pumice fall.
  • A new vent formed, and produced a dark ash- and obsidian-rich fall deposit.
  • A larger eruption ensued, producing pumice over a huge area, and a small ignimbrite deposit.
  • The most destructive part of the eruption then occurred. Part of the vent area collapsed, unleashing about 30 km³ of material, that formed a fast moving (600–900 km/h) pyroclastic flow.
  • Rhyolitic lava domes were extruded some years later, forming the Horomatangi reefs and Waitahanui bank.[10]

The main pyroclastic flow devastated the surrounding area, climbing over 1500 metres (5000 ft) to overtop the nearby Kaimanawa Ranges and Mount Tongariro, and covering the land within 80 kilometres (50 mi) with ignimbrite from Rotorua to Waiouru. Only Ruapehu was high enough to divert the flow.

The power of the pyroclastic flow was so strong that in some places it eroded more material off the ground surface than it replaced with ignimbrite. Valleys were filled with ignimbrite, evening out the shape of the land.

All vegetation within the area was flattened. Loose pumice and ash deposits formed lahars down all the main rivers.

The eruption further expanded the lake, which had formed after the much larger Oruanui eruption. The previous outlet was blocked, raising the lake 35 metres above its present level until it broke out in a huge flood, flowing for more than a week at roughly 200 times the Waikato River's current rate.

Dating the Taupō eruption

Many dates have been given for the Taupō eruption. One estimated date is 181 CE from ice cores in Greenland and Antarctica.[11] It is possible that the meteorological phenomena described by Fan Ye in China and by Herodian in Rome[12] were due to this eruption, which would give a date of exactly 186.[13] However, ash from volcanic activity does not normally cross hemispheres,[14] and recent radiocarbon dating by R. Sparks has put the date at 233 CE +/- 13 (95% confidence).[15]

There was no local population at this time, so the nearest humans would have been those in Australia, more than 2000 km to the west.

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See also

References
  1. Alan Hogg, David J. Lowe, Jonathan Palmer, Gretel Boswijk and Christopher Bronk Ramsey (2011). "Revised calendar date for the Taupō eruption derived by 14C wiggle-matching using a New Zealand kauri 14C calibration data set". The Holocene. 22: 439–449. Bibcode:2012Holoc..22..439H. doi:10.1177/0959683611425551. hdl:10289/5936.CS1 maint: multiple names: authors list (link)
  2. A continent on the move: New Zealand geoscience into the 21st century. Graham, Ian J. et al.; The Geological Society of New Zealand in association with GNS Science, 2008. ISBN 978-1-877480-00-3. page 66, 168.
  3. "Taupo the volcano" (a single sheet pamphlet), C.J.N. Wilson and B.F. Houghton, Institute of Geological & Nuclear Sciences, c2004.
  4. Information from GNS Science on the Taupo Volcano
  5. Wilson, Colin J. N. (2001). "The 26.5 ka Oruanui eruption, New Zealand: an introduction and overview". Journal of Volcanology and Geothermal Research. 112 (1–4): 133–174. Bibcode:2001JVGR..112..133W. doi:10.1016/S0377-0273(01)00239-6.
  6. Manville, Vern & Wilson, Colin 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 & Geophysics. 47 (3): 525–547. doi:10.1080/00288306.2004.9515074. Archived from the original on 2008-09-08.CS1 maint: multiple names: authors list (link)
  7. Wilson, Colin J. N.; et al. (2006). "The 26.5 ka Oruanui Eruption, Taupō Volcano, New Zealand: Development, Characteristics and Evacuation of a Large Rhyolitic Magma Body". Journal of Petrology. 47 (1): 35–69. Bibcode:2005JPet...47...35W. doi:10.1093/petrology/egi066.
  8. "Taupo the eruption" (a single sheet pamphlet), C.J.N. Wilson and B.F. Houghton, Institute of Geological & Nuclear Sciences, c2004.
  9. Wilson, C.J.N. and Walker, G.P.L., 1985. The Taupō eruption, New Zealand I. General aspects. Philosophical Transactions of the Royal Society of London, A314: 199-228.
  10. Houghton, B.F. (2007). Field Guide - Taupo Volcanic Zone.
  11. Lake Taupo Official Site Archived 2007-03-12 at the Wayback Machine
  12. Herodian of Antioch. "Chapter 14". History of the Roman Empire. Book 1. Stars remained visible during the day; other stars, extending to an enormous length, seemed to be hanging in the middle of the sky.
  13. Barton, John (2001). The First New Zealand Book? — an Eyewitness account of the Taupō eruption of AD 186. New Plymouth: Trustees of the Dalberton Library. ISBN 0-473-08268-3.
  14. Iridium: tracking down the extraterrestrial element in sedimentary clays "New Scientist". 1989: 58. Cite journal requires |journal= (help)
  15. Sparks, R.J.; Melhuish, W.H.; McKee, J.W.A.; Ogden, J.; Palmer, J.G. (1995). "14C calibration in the Southern Hemisphere and the date of the last Taupō eruption: evidence from tree-ring sequences". Radiocarbon. 37: 155–163. doi:10.1017/s0033822200030599.

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