| Ōkataina Caldera | |
| Other Name: | Ōkataina Volcanic Centre, Okataina Caldera, Okataina Volcanic Centre |
| Map: | New Zealand#North Island |
| Location: | North Island |
| Country: | New Zealand |
| Region: | Bay of Plenty |
| Coordinates: | -38.1667°N 206°W |
| Type: | Caldera |
| Width: | 15km (09miles) |
| Length: | 28km (17miles) |
| Volcanic Arc/Belt: | Taupō Rift |
| Volcanic Region: | Taupō Volcanic Zone |
| Last Eruption: | 1886 Tarawera, 1973 Hydrothermal in Waimangu Volcanic Rift Valley |
| Access: | State Highway 5 (New Zealand) |
Ōkataina Caldera (Ōkataina Volcanic Centre, also spelled Okataina) is a volcanic caldera and its associated volcanoes located in Taupō Volcanic Zone of New Zealand's North Island. It has several actual or postulated sub calderas. The Ōkataina Caldera is just east of the smaller separate Rotorua Caldera and southwest of the much smaller Rotomā Embayment which is usually regarded as an associated volcano. It shows high rates of explosive rhyolitic volcanism although its last eruption was basaltic. The postulated Haroharo Caldera contained within it has sometimes been described in almost interchangeable terms with the Ōkataina Caldera or volcanic complex or centre and by other authors as a separate complex defined by gravitational and magnetic features.[1] .[2] Since 2010 other terms such as the Haroharo vent alignment, Utu Caldera, Matahina Caldera, Rotoiti Caldera and a postulated Kawerau Caldera are often used,[3] rather than a Haroharo Caldera classification.[1]
The caldera covers an area of about 450km2, stretching from Lake Rotoehu in the north to Lake Rotomahana in the south.[4] The north east boundary bisects Lake Rotoiti and the north east includes all of Lake Rotomā. The south west corner is defined by the domes of the Ōkareka Embayment and the Waimangu Volcanic Rift Valley while the south east aspect is dominated by Mount Tarawera and the volcanic badlands of the Puhipuhi Basin. The caldera also contains several lakes, including part or all of Lake Ōkareka, Lake Ōkataina, Lake Rotoehu, Lake Rotomā, Lake Rotoiti, Lake Rotomahana, Lake Tarawera and Lake Tikitapu.[4]
The overwhelming volcanic deposits are rhyolite, with some basalt and one area of dacite. The caldera is now thought to contain the Utu Caldera, the major event Matahina Caldera, the Rotoiti Caldera, and the Kawerau Caldera with three associated geologically collapse structure embayments.[3] These are Rotomā Embayment, historically regarded as a caldera, the Ōkareka Embayment as another, now in-filled caldera and the Puhipuhi Embayment. The oldest parts of the caldera basement are now over 5km (03miles) deep and the younger Rotoiti and Kawerau calderas are still 2.5km (01.6miles) deep and largely infilled by eruptives.[5] [3]
The caldera has seen six eruptions in the past 10,000 years, most recently the 1886 Mount Tarawera eruption in the caldera's southeastern corner. The caldera contains two major lava dome complexes, the Haroharo vent alignment in the north and Tarawera vent alignment in the south. These two vent alignments are associated with current subsidence in the last 20 years of about 1.5cm/year which is assumed to be because of mainly cooling and contraction of previous magma melt.[6] Other volcanoes connected with the caldera include Putauaki (Mount Edgecumbe) [7] and the maar crater of Lake Rotokawau which is most likely to have formed from a basaltic dike extrusion associated with the common magma mush body.[8]
While most currently active New Zealand volcanoes produce small eruptions relatively frequently, Ōkataina's volcanoes tend to erupt very violently after intervals of centuries. As such, they pose significant potential threats to the Bay of Plenty Region but are also the most significant volcanic risk in New Zealand.[7] During the last 20,000 years, pyroclastic and lava eruptions have occurred of several types; low-silicate basalt eruptions, high-silicate rhyolite eruptions, and the rarer intermediate andesite and dacite eruptions. The most common magma type at Ōkataina is rhyolite.[7] The warning time before eruptions is currently suspected to be potentially hours as volcanic unrest signals are very non specific, historic composition analysis is consistent with this speed from magma reservoir to surface and this was all the warning given by the only rhyolitic eruption of the modern era.[9]
The underlying arc volcanism is driven initially by large inputs of basaltic melt from the subducted Pacific Plate. These basaltic melts often never reach the surface due to a relatively high density of the magma compared to the surrounding Australian Plate crust, but may trigger earthquake swarms.[10] Usually, these intrusions cool in the crust and then either solidify to a gabbroic igneous intrusion (also known as a pluton) at depth or are associated with the generation of more evolved magmas with higher silicate content that separate. They may then as evolved intrusions, cool further without erupting to form a felsic intrusion or can ascend to then erupt as rhyolite, dacite, or andesite. Sometimes such eruptions are believed to be primed by a basaltic melt predecessor. In the case of the Ōkataina Caldera the sub-surface architecture is known to be made up of discrete melt-mush pockets, and with one dacite exception already mentioned, these are rhyolitic. The melt-mush pockets are mainly between 5kmand8kmkm (03milesand05mileskm) in depth but one has been characterised at 3km (02miles) depth.[5] The pockets have erupted compositionally distinct magmas in single eruptions.[3] The composition is related to heat and volatiles transferred between the parent basalts and such rhyolites over the time the sub pocket has been maturing. Basaltic-rhyolitic magma interaction definitely happens from local and world wide studies, and will also be a factor in the many different eruption styles that have occurred.[3] Sometimes basalt appears to lead the eruption, at other times it has been postulated that tectonic earthquakes are the final enabler of an eruption.[3]
Any basaltic magmas that do reach the surface will have traversed this complicated crustal region and may erupt as a dyke. This is believed to have happened with the 1886 Mount Tarawera eruption.[3]
It is likely that the volcanic history of the area began some 625,000 years ago.[11] The caldera was formed by at least five huge eruptions between 400,000 and 50,000 years ago.
The oldest eruptive sub caldera is called the Utu caldera and is located in the south central portion. The basement of this sub caldera is about 5km (03miles) below present ground level.[3]
The most significant collapse event, with an eruptive volume of was 280,000 years ago. This collapse was associated with eruption of the Matahina Ignimbrite which covers over 2000km2 of the central North Island. The second major phase Matahina sub caldera is to the south east and its basement is also about 5km (03miles) below present ground level.[3] The original shape of the Matahina caldera has been modified (and buried/destroyed) by various events including at least eight smaller eruptions between 70,000 and 24,000 years ago. For example the dacite Puripuri basin/embayment is a subsidence related feature. This subsidence is related to the lateral movement of the underlying magma towards the eastern caldera margins.[3]
The paired eruptions approximately 50,000 years ago[12] of Rotoiti and at Earthquake Flat at far northern and southern ends of the caldera respectively had eruptive volumes of and . The resulting Rotoiti sub caldera is to the north of the Utu Caldera.[3]
Between this eruption and 21,000 years ago over 81km3 of Mangaone silicic plinian tephras or pyroclastic flow deposits occurred but it is unknown where the eruptions were centered. One of these events can be assigned to the Kawerau ignimbrite eruption of 33,000 years ago, with its location within the central part of the Matahina Caldera at level of the Puhipuhi Basin. An area of low gravity on gravimetric studies is consistent with the fourth phase Kawerau Caldera being here and its basement being about 2km (01miles) below present ground level.[3]
Although the latest caldera models include the Haroharo vent alignment they do not allow for the separate existence of a Haroharo caldera as many had historically postulated existed.[3]
More recently volcanoes within the caldera are known to have erupted eleven times in the last 21,000 years, with all but two of those eruptions being rhyolite.[13] [7] The Rotoma eruptions occurred in a north eastern embayment, and again like with the case of the Puripuri basin, the magma erupted from a lateral reservoir is associated with subsidence back to the eastern Rotoiti caldera margin. The Ōkareka Embayment to the west is also associated with caldera rim subsidence, this time the western shared rims of the Utu, Matahina and Rotoiti calderas.[3]
Two of these eruptions, both at Tarawera, occurred within the last 2000 years (in 1886 and). The most explosive of the eruptions in the last 21,000 years is likely to have been on the Haroharo vent alignment at about 5500 BCE. This ejected some 17km3 of magma.[7] During the last 21,000 years the Ōkataina volcano has contributed a total magma eruptive volume of about 80km3 in all its eruptions.[13] [14]
In summary the more significant eruptions have been:[15] [11] [16]
| Year before present | Calendar date | Eruptive name | Vent / Vent alignment / Caldera | Volume erupted | Notes | |
|---|---|---|---|---|---|---|
| cal.yr | 10 June 1886 CE | Basaltic eruption[17] | ||||
| ± 12 cal.yr | 1314 ± 12 CE | 5km3 DRE | [18] This eruption was immediately preceded by a rupture on the Edgecumbe fault.[19] | |||
| 3710 ± 10 cal.yr | ± 10 BCE | Rotokawau | - | Basaltic eruption[20] [21] [22] | ||
| 5526 ± 145 cal.yr | ± 145 BCE | Whakatane | 13km3 DRE | |||
| 7940 ± 257 cal.yr | ± 257 BCE | Mamaku | 17km3 DRE | [23] | ||
| 9423 ± 120 cal.yr | ± 120 BCE | Rotoma | 8km3 DRE | |||
| 14,009 ± 155 cal.yr | ± 155 BCE | Waiohau tephra | 10km3 DRE | |||
| 15,635 ± 412 cal.yr | ±412 BCE | Rotorua tephra | 4km3 DRE | |||
| 17,496 ± 462 cal.yr | ± 462 BCE | Rerewhakaaitu tephra | 5km3 DRE | [24] | ||
| 23,525–370+230 cal.yr | BCE | Okareka | 8km3 DRE | |||
| 25,171 ± 964 cal.yr | BCE | Te Rere | Kawerau Caldera (Haroharo) | 13km3 DRE | 33,000 years ago Kawerau (previously called Kaingaroa and miss-assigned to be 200,000 years older) now corrected to 25,171 years ago | |
| 31,500 cal.yr | BCE | Unit L | Unknown | 8.1km3 Tephra | [25] | |
| 32,500 cal.yr | BCE | Omataroa | Unknown | 16.2km3 Tephra | ||
| 32,800 cal.yr | BCE | Awakeri | Unknown | 0.77km3 Tephra | ||
| 33,000 cal.yr | BCE | Mangaone | Unknown | 19.1km3 Tephra | ||
| 34,500 cal.yr | BCE | Unit H | Unknown | 0.1km3 Tephra | ||
| 35,000 cal.yr | BCE | Unit G | Unknown | 2.5km3 Tephra | ||
| 36,100 cal.yr | BCE | Hauparu | Unknown | 15.2km3 Tephra | ||
| 36,700 cal.yr | BCE | Te Mahoe | Unknown | 0.9km3 Tephra | ||
| 36,800 cal.yr | BCE | Maketu | Unknown | 11km3 Tephra | ||
| 38,000 approx. cal.yr | BCE | Unit C (Pupuwharau then Pongakawa) | Unknown | 0.7km3 Tephra | ||
| 39,000 approx. cal.yr | BCE | Ngamotu | Unknown | 4.6km3 Tephra | ||
| 40,000 approx. cal.yr | BCE | Unit A | Unknown | 0.44km3 Tephra | ||
| 49,000 approx. cal.yr | BCE | Earthquake Flat | Earthquake Flat | |||
| about 50,000 cal.yr | BCE | Rotoiti/Rotoehu tephra | Rotoiti Caldera (Haroharo)' | 130km3 DRE | Basalt was emplaced on the floor of the rhyolitic reservoir. [26] [27] [28] [29] | |
| 50,000 + cal.yr | BCE | Matahi Scoria | Suspected to be Rotoiti Caldera | Basaltic immediately pre-Rotoiti | ||
| about 51,000 | BCE | Puhipuhi Dacite | 48,000+ ie is definitely before Rotoiti but age depends on actual Rotoiti age. | |||
| 96,000 approx. cal.yr | BCE | Moerangi | Moerangi Dome | |||
| 188,000 approx. cal.yr | BCE | Tutaeheke/Hap-Kapenga | Tutaeheke Dome | |||
| 240,000 + cal.yr | BCE | Pokopoko pyroclastics | Unknown | |||
| 240,000 + cal.yr | BCE | Onuku pyroclastics | Unknown | |||
| 280,000 cal.yr | 278000 BCE | Matahina | Matahina Caldera | 150km3 DRE | Recharging basalt found on top igmibrite layer. The latest age (not literature peer reviewed) is claimed at 322,000 ± 7,000 [30] which appears to be a reversion to the initial uncorrected timing. Also previously timed 230,000. - large as caldera collapse | |
| 280,000 + cal.yr | BCE | Matawhaura | Matawhaura Dome | |||
| 280,000 + cal.yr | BCE | Murupara pyroclastics | Unknown | |||
| 280,000 + cal.yr | BCE | Wairua | Wairua Dome | |||
| 280,000 + cal.yr | BCE | Maunawhakamana | Maunawhakamana Dome | |||
| 280,000 + cal.yr | BCE | Whakapoungakau | Lost volume with Matahini eruption | |||
| 557,000 cal.yr | 555000 BCE | Utu | Utu Caldera | |||
| 625,000 cal.yr | 623000 BCE | Ōkataina | Ōkataina |
Faults are not defined under this very active caldera. The active Paeroa Fault terminates at the caldera edge and the active Ngapouri-Rotomahana Fault is just to the south. The two recently active main vent alignments in the Ōkataina Caldera, the Horahora and Tarawera vents, are parallel with these identifiable faults outside the caldera, although the faults are not on the exact vent line.[16] In the last 9,500 years, four of the seven major ruptures of the Manawahe Fault have been associated in time with a volcanic eruption of the Okataina volcanic centre. This fault is just to the east of Lake Rotoma at the boundary between the tectonic Whakatāne Graben and the magmatic Ōkataina segments of the Taupō Rift. These are the Whakatane eruption of about 5500 years ago, the Mamaku eruption of about 8000 years ago and at least two fault ruptures in before or during the Rotoma eruption of 9500 years ago.[15] Similarly the Ngapouri-Rotomahana Fault and Paeroa Fault have multiple ruptures associated in time with volcanism including immediately prior to the Mamaku and Rotoma rhyolite eruptions in the case of the Paeroa Fault and of the Ngapouri-Rotomahana Fault immediately prior to the Kaharoa eruption.[31] At least 30% of major Taupō Volcanic Zone eruptions have now been associated with significant local fault ruptures within 30km (20miles) of the eruption.[15]