Jump to content

Oruanui eruption

Coordinates: 38°48′S 175°54′E / 38.800°S 175.900°E / -38.800; 175.900
From Wikipedia, the free encyclopedia

Oruanui eruption
VolcanoTaupō Volcano
DateAbout 25,700 year BP
TypeUltra-Plinian
LocationNorth Island, New Zealand
38°48′S 175°54′E / 38.800°S 175.900°E / -38.800; 175.900
Volume1,170 km3 (280 cu mi)
VEI8
ImpactDevastated much of North Island with detectable ash fall 5,000 km (3,100 mi) away
Recent vents and caldera structures Taupō Volcano. Present active geothermal systems are in light blue. A key to the vents is in the diagram.

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, and largest phreatomagmatic eruption characterised to date.

Geography

[edit]

At the time of the eruption sea level was much lower than at present and the Taupō Volcano had been for over 100,000 years mainly located under a larger lake than the present Lake Taupō called Lake Huka.[1]: 6  Lake Huka was destroyed in the eruption and other features of the local geography were changed significantly as outlined below.

Eruption

[edit]
Oruanui eruption impact
Oruanui eruption impact North Island in terms of approximate 10cm ash deposit (white shading) and approximate ignimbrite from pyroclastic flow (yellow shading).[2]: 529  The central red area is the Oruanui caldera with surrounding collapse crater in lighter red. It is superimposed on present day New Zealand although at the time New Zealand land mass was larger, as sea level was much lower.

With a Volcanic Explosivity Index of 8, it is one of the largest eruptions ever to occur in New Zealand and the most recent supereruption.[3] It occurred 25675±90 years BP[4][5][a] 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 rhyolitic magma, totalling 1,170 km3 (280 cu mi) of total deposits. As such it is the largest phreatomagmatic eruption characterised to date.[1]: 8  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.[8][2]: 528 [9][10]

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

[edit]

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.[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 adjoining Mount Tauhara whose magma chamber is under Wairakei 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 contain volcanic ash aggregates.[13]

Eruption process

[edit]

The timescale for the growth of the assumed Oruanui mush zone, which has a distinctive chemical and isotopic composition and zircon model-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 between 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 along dykes 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 the Maroa 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 later Hatepe 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 sea bed as wind direction varied, the eruptive columns were so high, and the volumes of ash were so large.

Eruption Timetable[15][11][16]: 40   pre-eruption   syn-eruption   biotite-bearing in high-SiO2 rhyolite   99% high-SiO2 rhyolite.
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 of Cretaceous to Jurassic basement greywacke and Quaternary 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 dissolved orthopyroxene 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 with accretionary 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 Oruanui eruption, containing spherical accretionary lapilli as in phase 8

Local impact

[edit]
Map
Approximate maximum lake size at 22,500 years ago after the Oruanui eruption (dark blue shading). This is before the volcanic material dam near the present lake outlet failed, and has the lake flowing via its old Waihora outlet into the Mangakino Stream and on to the Waikato River.

Tephra from the eruption covered much of the central North Island and is termed Kawakawa-Oruanui tephra, or KOT.[17] The Oruanui ignimbrite 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 the Chatham 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 the South 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 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.[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 as Mangakino.[18] The impact has been summarised as:[2]: 530 

  1. A new landscape with up to hundreds of metres thick ignimbrite that ponded in valleys around the volcano. 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 volume created by the caldera collapse acted both as a sedimentation sink for 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. Destruction of vegetation over most of the central North Island.
  5. Remobilisation of the pyroclastic material as alluvium with rainfall changed the drainage pattern of the Waikato River. The large amount of material mobilised particularly impacted the Waikato Plains and Hauraki Plains.

Distal impact

[edit]

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 and they provide a convenient marker for the last glacial 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 

Afterwards

[edit]

The first characterised eruption from the Taupō Volcano after the Oruanui eruption took place about 5000 years later.[1]: 10  The first three eruptions were dacitic as was the Puketarata 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 focussed vent locations, and a wide range of eruption volumes, with nine explosive events producing tephra deposits.[1]: 10 

See also

[edit]

Notes

[edit]
  1. ^ The age given here is the most recent identified in a number of review articles,[4] and may be subject to further correction. A previous age of 26.5 ka,[6] was updated in 2020 by IntCal20 correction to 25.675 ± 0.09 ka BP. In 2022, the ice core date of 25.318 ± .25 ka BP using the WD2014 timescale was corrected to 25.718 ka.[4][7]
  2. ^ The use of years in this way in this table is because it is sortable. One day is 0.003 of a year so the eruption has arbitrarily been given a length just less than 3 months when it might have lasted from start to finish twice this. Many of the eruption stages were continuous and lasted just hours. The syn-eruption processes happened all together.
  3. ^ a b These are not Dense-rock equivalent(DRE) which is more standardised way of expressing the size of an eruption.
  4. ^ a b c The numbering of Fig. 15 of Allen et al for geological processes is perhaps not logical given likely time of initiation. This is one reason the table has been made sortable.

References

[edit]
  1. ^ a b c d e f g h i j k l m Barker, SJ; Wilson, CJN; Illsley-Kemp, F; Leonard, GS; Mestel, ERH; Mauriohooho, K; Charlier, BLA (2020). "Taupō: an overview of New Zealand's youngest supervolcano". New Zealand Journal of Geology and Geophysics. 64 (2–3): 320–346. doi:10.1080/00288306.2020.1792515. S2CID 225424075. Retrieved 2023-11-28.
  2. ^ a b c d e f g Manville, V.; Wilson, C. J. N. (2004). "The 26.7 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): 525–546. Bibcode:2004NZJGG..47..525M. doi:10.1080/00288306.2004.9515074.
  3. ^ Lowe, D. J.; Balks, M. R. (2019). "Introduction to Tephra-Derived Soils and Farming, Waikato-Bay of Plenty, North Island, New Zealand" (PDF).
  4. ^ a b c Dong, Xiyu; Kathayat, Gayatri; Rasmussen, Sune O.; Svensson, Anders; Severinghaus, Jeffrey P.; Li, Hanying; Sinha, Ashish; Xu, Yao; Zhang, Haiwei; Shi, Zhengguo; Cai, Yanjun; Pérez-Mejías, Carlos; Baker, Jonathan; Zhao, Jingyao; Spötl, Christoph (2022-10-04). "Coupled atmosphere-ice-ocean dynamics during Heinrich Stadial 2". Nature Communications. 13 (1): 5867. Bibcode:2022NatCo..13.5867D. doi:10.1038/s41467-022-33583-4. ISSN 2041-1723. PMC 9532435. PMID 36195764.
  5. ^ Muscheler, Raimund; Adolphi, Florian; Heaton, Timothy J; Bronk Ramsey, Christopher; Svensson, Anders; van der Plicht, Johannes; Reimer, Paula J (2020). "Testing and Improving the IntCal20 Calibration Curve with Independent Records". Radiocarbon. 62 (4): 1079–1094. Bibcode:2020Radcb..62.1079M. doi:10.1017/RDC.2020.54. ISSN 0033-8222.
  6. ^ Dunbar, Nelia W.; Iverson, Nels A.; Van Eaton, Alexa R.; Sigl, Michael; Alloway, Brent V.; Kurbatov, Andrei V.; Mastin, Larry G.; McConnell, Joseph R.; Wilson, Colin J. N. (25 September 2017). "New Zealand supereruption provides time marker for the Last Glacial Maximum in Antarctica". Scientific Reports. 7 (1): 12238. Bibcode:2017NatSR...712238D. doi:10.1038/s41598-017-11758-0. PMC 5613013. PMID 28947829.
  7. ^ Muscheler, Raimund; Adolphi, Florian; Heaton, Timothy J; Bronk Ramsey, Christopher; Svensson, Anders; van der Plicht, Johannes; Reimer, Paula J (2020). "Testing and Improving the IntCal20 Calibration Curve with Independent Records". Radiocarbon. 62 (4): 1079–1094. Bibcode:2020Radcb..62.1079M. doi:10.1017/RDC.2020.54. ISSN 0033-8222.: Volcanic Time Markers 
  8. ^ 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. Bibcode:2001JVGR..112..133W. doi:10.1016/S0377-0273(01)00239-6.
  9. ^ 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.
  10. ^ Richard Smith, David J. Lowe and Ian Wright. 'Volcanoes – Lake Taupo', Te Ara – the Encyclopedia of New Zealand, updated 16 April 2007.
  11. ^ a b c d e f g h i Allan, AS; Barker, SJ; Millet, MA; Morgan, DJ; Rooyakkers, SM; Schipper, CI; Wilson, CJ (2017). "A cascade of magmatic events during the assembly and eruption of a super-sized magma body" (PDF). Contributions to Mineralogy and Petrology. 172 (7): 1–34. Bibcode:2017CoMP..172...49A. doi:10.1007/s00410-017-1367-8. S2CID 73613346.: Discussion 
  12. ^ Rosenberg, MD; Wilson, CJ; Bignall, G; Ireland, TR; Sepulveda, F; Charlier, BL (15 January 2020). "Structure and evolution of the Wairakei–Tauhara geothermal system (Taupo Volcanic Zone, New Zealand) revisited with a new zircon geochronology". Journal of Volcanology and Geothermal Research. 390 (106705). Bibcode:2020JVGR..39006705R. doi:10.1016/j.jvolgeores.2019.106705.: 6.3.3. Origins of the modern Wairakei-Tauhara geothermal system 
  13. ^ 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. Bibcode:2013JVGR..250..129V. doi:10.1016/j.jvolgeores.2012.10.016.
  14. ^ a b Bindeman, I.N. (2024). "Reinterpretation of the post-26 ka Taupō Rhyolitic Magmatic System (New Zealand) as Deep and Vertically Extensive Based on Isotope Thermometry and Measured and Modeled Zircon Destinies". Journal of Petrology. 65 (6). egae055. doi:10.1093/petrology/egae055.: Discussion 
  15. ^ a b c Myers, ML; Wallace, PJ; Wilson, CJ (2019). "Inferring magma ascent timescales and reconstructing conduit processes in explosive rhyolitic eruptions using diffusive losses of hydrogen from melt inclusions". Journal of Volcanology and Geothermal Research. 369: 95–112. Bibcode:2019JVGR..369...95M. doi:10.1016/j.jvolgeores.2018.11.009.
  16. ^ a b Wilson, CJ; Blake, S; Charlier, BL; Sutton, AN (2006). "The 26·5 ka Oruanui Eruption, Taupo Volcano, New Zealand: Development, Characteristics and Evacuation of a Large Rhyolitic Magma Body". Journal of Petrology. 47 (1): 35–69. doi:10.1093/petrology/egi066.
  17. ^ a b c Dunbar, N.W.; Iverson, N.A.; Van Eaton, A.R.; Sigl, M.; Alloway, B.V.; Kurbatov, A.V.; Mastin, L.G.; McConnell, J.R.; Wilson, C.J.N. (2017). "New Zealand supereruption provides time marker for the Last Glacial Maximum in Antarctica". Scientific Reports. 7 (12238): 12238. Bibcode:2017NatSR...712238D. doi:10.1038/s41598-017-11758-0. PMC 5613013. PMID 28947829.
  18. ^ 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. Bibcode:2007NZJGG..50..131M. doi:10.1080/00288300709509826. ISSN 0028-8306. S2CID 129792354.
  19. ^ Harper, MA; Pledger, SA; Smith, EG; Van Eaton, AR; Wilson, CJ (2015). "Eruptive and environmental processes recorded by diatoms in volcanically dispersed lake sediments from the Taupo Volcanic Zone, New Zealand". Journal of Paleolimnology. 54 (263–77): 1–15. Bibcode:2015JPall..54..263H. doi:10.1007/s10933-015-9851-5. S2CID 127263257.
Retrieved from "https://en.wikipedia.org/w/index.php?title=Oruanui_eruption&oldid=1259902815"