The Oruanui eruption of New Zealand's Taupō Volcano (also known as the Kawakawa eruption or Kawakawa/Oruanui event) was the world's most recent supereruption.[1]

Oruanui eruption
An artist's impression of the large eruption column during the Oruanui eruption as it may have appeared from space
Volcano	Taupō Volcano
Date	About 26,500 years ago
Type	Ultra-Plinian
Location	North Island, New Zealand 38°48′S 175°54′E
VEI	8
Impact	Devastated much of North Island with detectable ash fall 5,000 km (3,100 mi) away
The Oruanui caldera and collapse crater have been modified by the later smaller Hatepe eruption and other activity in the last 25,000 years. The vents in red have been active more recently. Present active geothermal systems are in light blue.

Eruption

With a Volcanic Explosivity Index of 8, it is one of the largest eruptions ever to occur in New Zealand. It occurred about 26,500 years ago 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.[3][2][4][5]

Modern-day Lake Taupō, 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 Taupō, 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.

Unusual features

The Oruanui eruption shows many unusual features: its episodic nature, a wide range of magma-water interaction, and complex interplay of pyroclastic fall and flow deposits.[3] As the eruption occurred through a lake system (Lake Huka)[2] overlying the vent, many of the deposits contain volcanic ash aggregates.[6]

Local impact

Tephra from the eruption covered much of the central North Island and is termed Kawakawa-Oruanui, or KOT, tephra.[7] The Oruanui ignimbrite is 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. The local biological impact must have been immense as 10 centimetres (4 in) of ash was deposited from just south of Auckland over the whole of the rest of the North Island and the top of the South Island, both of which were larger in land area as sea levels were considerably lower. The pyroclastic ignimbrite flows certainly destroyed all vegetation they reached.[2] 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 Taupō, having filled to about 75 m (246 ft) above its current level and draining initially via a Waihora outlet to the northwest, cut through its Oruanui ignimbrite dam near the present Taupō outlet to the northeast 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.[8] The impact has been summarised as:[2]

1. A wholly new landscape around the caldera, with ignimbrite accumulations that were landscape-burying up to hundreds of metres thick and ponding in valleys. The actual area of the ignimbrite is less than the subsequent smaller Hatepe eruption presumably because the later generated a more intense pyroclastic flow but much less accumulative tephra fall.
2. The area created by the caldera collapse acted both as a sink for sedimentation in the local catchment and as the basin in which a new Lake Taupō accumulated.
3. The former Lake Huka that had extended to the north and partially occupied the older Reporoa Caldera was destroyed and filled in with ignimbrite, which also created a temporary barrier between the Taupō and Reporoa watersheds that had to be eroded before a stable drainage of the new Lake Taupō was established.
4. Cumulative thicknesses of fall deposits and ignimbrite were likely sufficient to have wholly destroyed or buried vegetation over virtually all of the central North Island.
5. Remobilisation of the vast quantities of pyroclastic material as alluvium produced profound changes in the drainage pattern of the Waikato River, with an impact particularly on the Waikato Plains and Hauraki Plains.

Distal impact

The Oruanui eruption ash deposits from the final (tenth) phase have been geochemically matched to Western Antarctic ice core deposits 5,000 km (3,100 mi) away timed to 25,318 ± 250 years before 1950 and they provide a convenient marker for the last glacial maximum in Antarctica.[7] This ash cloud has been modelled to have taken about two weeks to encircle the Southern Hemisphere.[7]

See also

• North Island Volcanic Plateau
• Taupō volcano
• Hatepe eruption (The most recent major eruption of the Taupō volcano, dated to around 232 CE)

References

На других языках

[es] Erupción de Oruanui