| Oruanui eruption | |
|---|---|
| Volcano | Taupō Volcano |
| Date | c. 25,700 yearsBP |
| Type | Ultra-Plinian |
| Location | North Island,New Zealand 38°48′S175°54′E / 38.800°S 175.900°E /-38.800; 175.900 |
| Volume | 1,170 km3 (280 cu mi) |
| VEI | 8 |
| Impact | Devastated much ofNorth Island with detectable ash fall 5,000 km (3,100 mi) away |
| Maps | |
 Recent vents and caldera structures Taupō Volcano. Present active geothermal systems are in light blue. A key to the vents is in the diagram. | |
TheOruanui eruption (also known as theKawakawa eruption orKawakawa/Oruanui event) ofTaupō Volcano inNew Zealand around 25,700 yearsbefore present was the world's most recentsupereruption, and its largestphreatomagmatic eruption characterised to date.
At the time of the eruption, the sea level was much lower than at present, and for over 100,000 years the Taupō Volcano had been mainly underLake Huka, a larger lake than the presentLake Taupō.[1]: 6 Lake Huka was destroyed in the eruption, and other features of the local geography were changed significantly as outlined below.
With aVolcanic Explosivity Index of 8, it is one of the largest eruptions ever to occur in New Zealand and the most recentsupereruption.[3] It occurred25,675±90 years BP[4][5][a] in theLate Pleistocene. It generated approximately 430 km3 (100 cu mi) ofpyroclastic fall deposits, 320 km3 (77 cu mi) ofpyroclastic density current (PDC) deposits (mostlyignimbrite), and 420 km3 (100 cu mi) of primary intracaldera material, equivalent to 530 km3 (130 cu mi) ofrhyoliticmagma, totalling 1,170 km3 (280 cu mi) of total deposits. As such it is the largestphreatomagmatic eruption characterised to date.[1]: 8 The eruption is divided into 10 different phases on the basis of ninemappable fallunits and a tenth, poorly preserved but volumetrically dominant fall unit.[8][2]: 528 [9][10]
Modern-dayLake Taupō, 616 km2 (238 sq mi) in area and 186 m (610 ft) deep, partly fills thecaldera 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 lagbreccias) occurred during phase 10.
The Oruanui eruption shows many unusual features: its episodic nature, a wide range of magma–water interaction, and complex interplay of pyroclastic fall andflow deposits.[8] The erupted magma was very uniform in composition and this composition has not been seen since, but had been seen before the eruption.[1]: 8 Detailed compositional analysis has revealed the early phases of the eruption had a small amount of magma from outside the Taupō Volcano and are most consistent with a tectonic trigger.[11][1]: 8 The eruption occurred through a lake system which was either the southern section of Lake Huka, recently separated by pre-eruption upwarping shortly before the eruption itself,[2]: 528 or some have suggested Lake Taupō had separated with a higher level than the remaining Lake Huka about a thousand years earlier, due solely to eruptive activity of the Poihipi volcano adjoiningMount Tauhara whose magma chamber is underWairakei and that had erupted at Trig 9471 and the Rubbish Tip Domes about 27,000 years ago, filling that portion of Lake Huka.[1]: Fig. 4 [12] Accordingly, many of the deposits containvolcanic ash aggregates.[13]
The timescale for the growth of the assumed Oruanuimush zone, which has a distinctive chemical andisotopic composition andzirconmodel-age spectra, is now known to be from about 40,000 years ago from earlier Taupō Volcano eruptions.[11] During crystal-liquid separation in this mush, large volumes of melt and crystals were carried upwards into a melt-dominant magma body that formed at 3.5–6 km (2.2–3.7 mi) depth.[11] There is emerging evidence that much of the silicic magma produced was formed deeper than this in the middle or lower crust (some have suggested as deep as the upper mantle) and ascending rapidly to this magma reservoir with only brief storage there.[14] The relative uniformity of the eruptives (99% high-SiO2 rhyolite),[1]: 8 suggests the Oruanui magma body had been vigorously convecting by the time of the eruption.[11] Nonetheless composition analysis shows that three different rhyolites contributed, with the initial two phases of the eruption having contributions from a leak of biotite-bearing rhyolite, presumably alongdykes at more than 2 km (1.2 mi) depth,[15] associated with tectonic faulting from a magma chamber to the north.[11] The biotite-bearing rhyolite composition is like that found within theMaroa Caldera adjacent to the Taupō Volcano.[11]
These initial stages were from magma at relatively low overpressure and if stored and matured in a shallow magma chamber had a temperature of about 780 ± 20 °C,[11] with between a week to two weeks ascent of magma before eruption.[15] It is possible that if the later majority of the magma formed deeper, the maturing temperature was about 900 °C.[14] About 0.5% of the eruptives was low-SiO2 rhyolite believed to have been tapped from isolated pockets in the underlying crystal mush.[1]: 8 Two distinct mafic magmas were involved in the eruption, and a total volume of 3–5 km3 (0.72–1.20 cu mi) of mafic magma is atypically high compared to other nearby rhyolitic eruptions.[11]
The timescales involved in the final eruption priming appear to be only decades long at most. The eruption itself lasted only a few months, with most of the stages as described below being continuous. The location of the eruptive vents are only known for the first four stages of the eruption. Vents during stage 1 and 2 were in the north-east portion of present Lake Taupō, a third vent (or more likely several vents) was closer to the eastern alignment of the laterHatepe eruption,[1]: 8 and the 4th vent was more central. The later stages of the eruption may have had venting from much of what is now the northern part of Lake Taupō.[16]: 39
While pyroclastic density currents were generated throughout the eruption, the peak distance reached in ignimbrite deposits was about 90 km (56 mi) during phase 8.[1]: 8 This phase, as well as several others, before phase 10, were not that much smaller than the later Hatepe eruption of the Taupō Volcano. Ash (Kawakawa tephra) distributed during the various stages created a stratigraphic layer found over much of New Zealand and its surrounding seabed as wind direction varied.
| Approximate start time process relative to eruption (years)[b] | Geological stage | Eruption stage | Geological event | Eruption relevance | Tephra volume<[c] (km3) | Ignimbrite volume<[c] (km3) |
|---|---|---|---|---|---|---|
| 10000 | 1 | – | Assimilation into melt ofCretaceous toJurassic basement greywacke andQuaternary igneous rocks | magma reservoir size and composition | – | – |
| 10000 | 2 | – | Mush crystallisation and development of interstitial melt | magma reservoir development and composition | – | – |
| 3000 | 3 | – | Melt-dominant magma body predominates | enables potential for eruption | – | – |
| 100 | 4 | – | Crystallisation of rim zones in melt-dominant body | allows timing of cooling | – | – |
| 100 | 5 | – | Recrystallisation of dissolvedorthopyroxene | allows timing | – | – |
| 100 | 6 | – | Crystal growth in isolated low-SiO2 rhyolite pockets | immature but tapped in eruption | – | – |
| 10 | 7 | – | Mafic magma interacting with mush | a potential primer event but did not cause the overpressure seen in other super eruptions | – | – |
| 0.01 | 8 | – | Mafic magma infiltration into high-SiO2 rhyolite | process just prior to and during eruption | – | – |
| 0.01 | 10[d] | – | Lateral, tectonically associated feeding in from north biotite-bearing rhyolite | The early phase 1 and 2 of the eruption were separated by several months, and this compositional signal is suggestive of a tectonic trigger. | – | – |
| 0.01 | 11[d] | – | Ascent, decompression and fragmentation of magma | Early melt average ascent was about 5 days, these processes are relevant to composition signals and the violence of the eruption, independent of it being under a lake | – | – |
| 0.001 | 9[d] | – | injection of low-SiO2 rhyolite into high-SiO2 rhyolite | late process during eruption | – | – |
| 0 | – | 1 | – | Single pumice fall, accompanied by wet low-velocity pyroclastics to northwest of vent | 0.8 | 0.01 |
| −0.215 | – | 2 | – | pumice and fine ash in 3 phases | 0·8 | 0.1 |
| −0.2151 | – | 3 | – | Wet with nearby pyroclastic and fall deposits, and distal multiple-bedded fall material postulated after mafic magma recharge | >5 | 10 |
| −0.2152 | – | 4 | – | Single pumice fall with thin but widespread pyroclastic deposit | 2.5 | 0.1 |
| −0.22 | – | 5 | – | Pumice fall with local pyroclastic deposit | 14 | 1 |
| −0.225 | – | 6 | – | Mixed dry and wet fall with widespread multiple pyroclastic deposits | 5.5 | 10 |
| −0.23 | – | 7 | – | Single pumice fall with widespread, voluminous pyroclastic deposit after mafic magma recharge of about 18 hours | 15 | 10 |
| −0.231 | – | 8 | – | Wet fall deposit, with widespread, voluminous pyroclastic deposit withaccretionary lapilli postulated after mafic magma recharge | 37 | 10 |
| −0.232 | – | 9 | – | Single ash and pumice fall bed, with mainly proximal, voluminous pyroclastic deposits | 85 | 10 |
| −0.24 | – | 10 | – | Fine-grained ash, with voluminous pyroclastic deposit in the Lake Taupo basin | 265 | 100 |
Tephra from the eruption covered much of the central North Island and is termed Kawakawa-Oruanui tephra, or KOT.[17] The Oruanuiignimbrite is up to 200 metres (660 ft) deep.[2]: 529 Ashfall affected most of New Zealand, with an ash layer as thick as 18 centimetres (7 in) deposited on theChatham Islands, 850 km (530 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 theSouth Island, both of which were larger in land area as sea levels were considerably lower than present. The pyroclastic ignimbrite flows destroyed all vegetation they reached.[2]: 530
Later erosion and sedimentation had long-lasting effects on the landscape and may have caused theWaikato River to shift from theHauraki Plains to its current course through the Waikato to theTasman 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 noterraces around the lake.[2]: 531–2 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 asMangakino.[18] The impact has been summarised as:[2]: 530
The Oruanui eruption ash deposits from the final (tenth) phase have beengeochemically matched toWestern Antarctic ice core deposits 5,000 km (3,100 mi) away and they provide a convenient marker for the lastglacial maximum in Antarctica.[17] This ash cloud has been modelled to have taken about two weeks to encircle the Southern Hemisphere.[17]Diatoms from erupted lake sediments have been found in the volcanic ash deposits about 850 km (530 mi) downwind on the Chatham Islands.[19]: 2
The first characterised eruption from the Taupō Volcano after the Oruanui eruption took place about 5000 years later.[1]: 10 The first three eruptions weredacitic as was thePuketarata eruption.[1]: 10 The other twenty-four rhyolitic events until the present, including the major Hatepe eruption, dated to around 232 CE, came from three distinct magma sources.[1]: 10 These have had geographically focused vent locations, and a wide range of eruption volumes, with nine explosive events producingtephra deposits.[1]: 10