Volcanism of New Zealand

The volcanism of New Zealand has been responsible for many of the country's geographical features, especially in the North Island and the country's outlying islands.

While the land's volcanism dates back to before the Zealandia microcontinent rifted away from Gondwana 60–130 million years ago, activity continues today with minor eruptions occurring every few years. This recent activity is primarily due to the country's position on the boundary between the Indo-Australian and Pacific Plates, a part of the Pacific Ring of Fire, and particularly the subduction of the Pacific Plate under the Indo-Australian Plate.

New Zealand's rocks record examples of almost every kind of volcanism observed on Earth, including some of the world's largest eruptions in geologically recent times.

None of the South Island's volcanoes are active.

Map of selected surface volcanic features in the northern North Island which includes features from volcanic activity in recorded historic times in New Zealand. Clicking on the map enlarges it, and enables panning and mouseover of volcano name/wikilink and ages before present. Key for the volcanics that are shown with panning is:   basalt (shades of brown/orange),   monogenetic basalts,

  undifferentiated basalts of the Tangihua Complex in Northland Allochthon,

  arc basalts,   arc ring basalts,

  dacite,

  andesite (shades of red),   basaltic andesite,

  rhyolite, (ignimbrite is lighter shades of violet),

and   plutonic. White shading is selected caldera features.

New Zealand has been the site of many large explosive eruptions during the last two million years, including several of supervolcano size.^[1] These include eruptions from Macauley Island and the Taupō, Whakamaru, Mangakino, Reporoa, Rotorua, and Haroharo calderas.

Two relatively recent eruptions from the Taupō Volcano are perhaps the best known. Its Oruanui eruption was the world's largest known eruption in the past 70,000 years, with a Volcanic Explosivity Index (VEI) of 8. It occurred around 26,500 years ago and deposited approximately 1,200 km³ of material.^[2][3] Tephra from the eruption covered much of the central North Island with ignimbrite up to 200 metres (650 feet) deep, and most of New Zealand was affected by ash fall, with even an 18 cm (7 inch) ash layer left on the Chatham Islands, 1,000 km (620 mi) away. Later erosion and sedimentation had long-lasting effects on the landscape, causing the Waikato River to shift from the Hauraki Plains to its current course through the Waikato to the Tasman Sea.^[4] New Zealand's largest lake, Lake Taupō, fills the caldera formed in this eruption.

Taupō's most recent major eruption, the Taupō or Hatepe eruption, took place around 232 CE, and is New Zealand's largest eruption since Oruanui.^[5] It ejected some 120 km³ of material (rating 7 on the VEI scale),^[6] with around 30 km³ ejected in just a few minutes. It is believed that the eruption column was 50 kilometres (31 mi) high, twice as high as the eruption column from Mount St. Helens in 1980. This makes it one of the most violent eruptions in the last 5000 years (alongside the Tianchi eruption of Baekdu at around 1000 and the 1815 eruption of Tambora). The resulting ash turned the sky red over Rome and China.^[7]

Mount Tarawera's eruption around 1310 CE, while not nearly as large, was still substantial, producing 2.5 km³ of lava and 5 km³ of tephra (VEI 5).^[8] Because its deposits, stretching from Gisborne to the Bay of Islands, were emplaced around the time that Māori permanently settled New Zealand, they have provided a useful archaeological marker. Tarawera erupted again on 10 June 1886, spewing ash and debris over 16,000 km² (6,200 sq mi), destroying the Pink and White Terraces and three villages, including Te Wairoa, and claiming the lives of perhaps 120 people.^[9] Approximately 2 km³ of tephra was erupted (VEI 5).^[8]

Part of the 17-kilometre (11 mi) long rift created in Mount Tarawera's 1886 eruption

As well as the direct effects of explosions, lava, and pyroclastic flows, volcanoes pose various hazards to the New Zealand populace. These include tsunamis, break-out floods and lahars from volcanically dammed lakes, ashfall, and other far field effects.

For instance, the Tangiwai disaster occurred on 24 December 1953 when the Tangiwai railway bridge across the Whangaehu River collapsed from a lahar in full flood, just before an express train was about to cross it. The train could not stop in time, and 151 people died. This was ultimately caused by Ruapehu's 1945 eruption, which had emptied the crater lake and dammed the outlet with tephra.

An eruption of the Whakaari / White Island stratovolcano occurred on 8 December 2019 while there was a group of 47 visitors on the island. Twenty-two people died, either in the explosion or from injuries sustained, including two whose bodies were never found and were later declared dead. A further 25 people suffered injuries, with the majority needing intensive care for severe burns.^[10]

Effects can be widespread even for eruptions of only moderate size. Ash plumes from Ruapehu's 1996 eruption forced the closure of eleven airports, including Auckland International Airport.^[11]

Insurance against volcanic damage (along with other natural disasters) is provided by the country's Earthquake Commission.

The Māori had many myths and legends regarding the land's volcanic mountains. Perhaps the most well known regards the relative locations of Taranaki, Tongariro and Pihanga. It holds that the two first-named volcanoes competed for the love of the beautiful Pihanga and, after Tongariro succeeded, the defeated Taranaki moved to its lonely location near New Plymouth.

Another legend recounts the exploits of Ngātoro-i-rangi, a tohunga (priest) who arrived from the ancestral Māori homeland, Hawaiki, on the Arawa waka (canoe). Travelling inland and then looking southward from Lake Taupō, he decided to climb the mountains he saw there. He reached and began to climb the first mountain along with his slave Ngāuruhoe, who had been travelling with him, and named the mountain Tongariro (the name literally means 'looking south'), whereupon the two were overcome by a blizzard carried by the cold south wind. Near death, Ngātoro-i-rangi called back to his two sisters, Kuiwai and Haungaroa, who had also come from Hawaiki but remained on Whakaari / White Island, to send him sacred fire, which they had brought from Hawaiki. This they did, sending the fire in the form of two taniwha (powerful spirits) named Te Pupu and Te Haeata by a subterranean passage to the top of Tongariro. The tracks of these two taniwha formed the line of geothermal fire that extends from the Pacific Ocean and beneath the Taupō Volcanic Zone, and is seen in the many volcanoes and hot springs extending from Whakaari to Tokaanu and up to the Tongariro massif. The fire arrived just in time to save Ngātoro-i-rangi from freezing to death, but Ngāuruhoe had already died by the time Ngātoro-i-rangi turned to give him the fire. For this reason the hole through which the fire ascended, the active cone of Tongariro, is now called Ngauruhoe.

Eruptions in the North Island, such as the Kaharoa eruption of Mt Tarawera in 1314, have been used to help determine the approximate date of arrival of the early Polynesian colonists to about 1280. Fossilized footprints of perhaps second- or third-generation Polynesian colonists have been found in volcanic ash on islands in the Hauraki Gulf.

Please see the main articles above because as already mentioned almost every kind of volcanism observed on Earth is found in New Zealand. For historic intrusive volcanism please see the section on older volcanism below. There is good evidence for continued intrusive volcanism activity in the central North Island.^[12][13][5] A quite recent, large dioritic pluton of the order of 550,000 years old has been dated from drill cores there.^[14]

While there are remnants of volcanic activity throughout most of New Zealand, there are several areas where they are more obvious, and somewhere activity continues. Since Taranaki's last activity in 1854, all eruptions have been in the Taupō Volcanic Zone or the Kermadec Arc.^[15]

The Kermadec Islands are an active volcanic island arc stretching north-northeast from New Zealand's North Island towards Tonga. While only a few volcanoes in the arc are tall enough to form islands, it includes about 30 sizeable submarine volcanoes with many in the South Kermadec Ridge Seamounts at the New Zealand end of the chain. The largest island, Raoul Island, produced a large eruption around 2200 years ago with a VEI of 6.^[16] Its activity has continued intermittently since, with its latest eruption occurring in 2006.^[17]

The Northland region contains two recently active volcanic fields, one centred around Whangarei,^[18] and the other is the Kaikohe-Bay of Islands volcanic field.^[19] The latest activity in the Kaikohe-Bay of Islands field, around 1300 to 1800 years ago, created four scoria cones at Te Puke (near Paihia).^[19]

Earlier, during the Miocene, a mainly andesitic volcanic arc ran through Northland and neighbouring regions (including the Three Kings Ridge and northern Coromandel Peninsula), with western and eastern belts active between 25—15 million years ago and 23–11 million years ago respectively.^[21] Although this produced substantial volcanic edifices, including New Zealand's largest known stratovolcano, the Waitakere volcano,^[22] most of these have been eroded away, buried, or submerged, especially in the west, where a series of volcanoes buried offshore stretches south almost to New Plymouth. This is called the Northland-Mohakatino Volcanic Belt.^[23] Remnants of these two ancient volcano belts are still exposed in many places, including Whangarei Heads, the Hen and Chickens Islands, around Whangaroa Harbour, Waipoua forest, and the Waitākere Ranges.

The basaltic Auckland volcanic field is a monogenetic volcanic field underlying much of the Auckland metropolitan area. The field's many vents have produced a diverse array of explosion craters, scoria cones, and lava flows. The largest and most recent is Rangitoto in the Hauraki Gulf, which last erupted 600–700 years ago. Currently dormant, the field is likely to erupt again within the next "hundreds to thousands of years" (based on past events), a short timeframe in geologic terms.^[24] Auckland's residents, however, face more danger from volcanoes farther south.^[24]

Auckland's volcanoes are believed to be the latest product of an unusual magma source related to local tectonics which is not a classic hot spot, as the earlier volcanic fields are to the south, the opposite expected from movement of the Australian Plate over a stationary mantle plume source.^[25]

Three volcanic fields erupted between 2.7 and 0.5 million years ago, migrating northwards from Mount Pirongia to the Bombay Hills. The earliest of these fields formed the Alexandra Volcanics^[26] which is distinguished by large arc volcano tholeiitic cones but did have associated Okete Volcanics which were traditionally more akaline and oxidised and were in the monogenetic volcanic field pattern seen in the later fields. The distinction between the Alexandra and Okete volcanics is not necessarily clear cut and is still being studied. Alexandra Volcanic Group rocks (mostly basalt) cover about 450 km² amounting to 55 km³ from at least 40 vents. Mount Pirongia and Mount Karioi are part of the main lineament in the group.^[27] The later fields are the smallest Ngatutura Volcanics which comprises about 16 volcanoes south of Port Waikato on the west coast and the South Auckland volcanic field with over 80 volcanoes.^[28] The magma body that created the Auckland volcanic field is considered to have been related to these outpourings also. Unlike typical hot spots such as the one underlying Hawaii, it does not seem to have stayed still, but instead is migrating northward at a faster pace than the surrounding Indo-Australian Plate. Its motion has been explained as the tip of a propagating crack produced by the twisting of the North Island's crust.^[29][25]

The extinct Coromandel Volcanic Zone (CVZ) was a volcanic arc stretching from Great Barrier Island in the north, through the Coromandel Peninsula, to Tauranga and the southern Kaimai Ranges in the south. Activity began in the north around 18 million years ago, and was primarily andesitic until around 9–10 million years ago, when it changed to a bimodal basaltic/rhyolitic pattern. Eruptive centres gradually migrated southward,^[31] where they transitioned into early activity in the Taupō Volcanic Zone. Later activity in the CVZ and its interface with the Taupō Volcanic Zone is obscured by subsequent events and is not fully understood, but continued in the south until perhaps 1.5 million years ago in the Tauranga Volcanic Centre.^[32] Together with the extinct undersea Colville Ridge, the CVZ formed a precursor to the modern Taupō Volcanic Zone and Kermadec Ridge.^[33]

Mayor Island / Tūhua is a peralkaline shield volcano with a caldera partly formed in a large eruption some 7000 years ago. It has exhibited many eruptive styles, and its last eruption may have occurred only 500–1000 years ago.^[34] The island's Maori name, Tuhua, refers to the obsidian they found on the island and prized for its sharp cutting edge.

About 350 kilometres long by 50 kilometres wide, the Taupō Volcanic Zone (TVZ) is the world's most productive area of recent silicic volcanic activity,^[35] with the highest concentration of young rhyolitic volcanoes.^[36] Mount Ruapehu marks its southwestern end, and it continues up through Ngauruhoe, Tongariro, Lake Taupō, the Whakamaru, Mangakino, Maroa, Reporoa, and Rotorua calderas, the Okataina Volcanic Complex (including Mount Tarawera) and 85 kilometres beyond Whakaari / White Island to the submarine Whakatāne Seamount. The TVZ also contains numerous smaller volcanoes, along with geysers and geothermal areas. Volcanic eruptions began here around two million years ago, with silicic eruptions starting around 1.55 million years ago, as activity shifted southeast from the Coromandel Volcanic Zone.^[32]

Volcanism in the Taranaki region has migrated southeastward during the last two million years. Beginning in the Sugar Loaf Islands, near New Plymouth, activity then shifted to Kaitake (580,000 years ago) and Pouakai (230,000 years ago) before creating the large stratovolcano called Mount Taranaki, (former name Mount Egmont), which last erupted in 1854, and its satellite vent, Fanthams Peak.^[37] This southeastward migration is the continuation of the 25 million year activity of the Northland-Mohakatino Volcanic Belt that extends mainly under the present Tasman Sea from the west of Northland down to Mount Taranaki.^[23]

The higher portions of the Chatham Islands are formed from volcanic rock that is up to 81 million years old, although lava flows on the northern shore of Chatham Island date back only about five million years.^[38]

Banks Peninsula comprises the eroded remnants of two large stratovolcanoes, Lyttelton, which formed first, and Akaroa. These formed by intraplate volcanism through continental crust approximately eleven to eight million years ago (Miocene). The peninsula formed as offshore islands, with the volcanoes reaching to about 1,500 m above sea level. Two dominant craters were eroded, then flooded, to form the Lyttelton and Akaroa Harbours. The portion of crater rim lying between Lyttelton Harbour and Christchurch city forms the Port Hills.

Small sub-alkaline basalt to basaltic andesite Surtseyan volcanoes on the submerged continental shelf formed what was historically termed the Waiareka-Deborah volcanic group and now called the Waiareka-Deborah volcanic field in the area around Oamaru around 35 to 30 million years ago.^[39][40] A monogenetic volcanic field of more alkaline composition eruptives, with stronger surface features, as they are younger, extends north of Dunedin overlapping the southern Waiareka-Deborah volcanic field, and these volcanoes have now been characterised to be part of the Dunedin volcanic group.^[41]

The Alpine Dyke Swarm of volcanic intusion took place about 25 million years ago and is located near Lake Wānaka in the Southern Alps.^[42]

The Dunedin Volcano formed during the Miocene, beginning with basaltic eruptions on the Otago Peninsula, is the largest volcano in the large Dunedin volcanic group.^[41] Large central-vent structures formed, and then large domes, with seawater interacting explosively with erupting submarine magma.^[43]

The Solander Islands, a small chain of uninhabited islets close to the western end of the Foveaux Strait, are the emergent portions of a large extinct andesitic volcano that last erupted around 50,000 to 150,000 years ago.^[44] Caused by the subduction of the Australian Plate beneath the Pacific Plate, it is the only volcano associated with this subduction zone that protrudes above the sea.^[45][46]

The majority of New Zealand's widely separated subantarctic islands are primarily volcanic in origin, including Auckland Island, Campbell Island / Motu Ihupuku, and Antipodes Island.^[38] These are mainly Miocene intraplate volcanoes with ages decreasing towards the northeast, although Antipodes Island may have been active during the last 20,000 years.

Older remnants of volcanism are also found in several places around New Zealand. These were generally formed either when New Zealand still formed part of the Gondwana supercontinent, or while Zealandia was rifting away from the rest of Gondwana, although some have been emplaced in their current setting more recently. (New Zealand is the main part of the submerged microcontinent of Zealandia that currently emerges above the sea.)

A band of granitic intrusions covering over 10,000 km², the Median Batholith, stretches from Stewart Island / Rakiura through Fiordland, and again through the West Coast and Nelson after interruption by the Alpine Fault. This was produced between 375 and 105 million years ago in the course of subduction-related volcanism in a long mountain range along the Gondwanan coast somewhat like today's Andes. Two more batholiths, the Karamea-Paparoa and Hohonu Batholiths, are also found on the West Coast.

Basaltic lava flows, dikes, and tuff from fissure eruptions between 100 million and 66 million years ago, during Zealandia's separation from Gondwana, are found in Marlborough, the West Coast and offshore further west. Ultramafic intrusions are found in Marlborough and north Canterbury, including at the summit of Tapuae-o-Uenuku, the country's highest mountain outside the Southern Alps.^[47] The Mount Somers volcanics that erupted from 100 to 80 million years ago extend to Banks Peninsula but are mostly buried there by more recent volcanism.

Rhyolitic ignimbrite^[48] and tuff deposits found in Otago at Shag Point / Matakaea and in the Kakanui Mountains that were originally dated in the range 107 to 101 million years ago^[49] are now both dated to 112 ± 0.2 million years ago and so likely come from a large singe event.^[50]

The Hikurangi Plateau is an oceanic plateau on the Pacific Plate that attached to the Chatham Ridge after being partially subducted under it, and is now subducting under the North Island. It likely formed in one of the world's largest volcanic outpourings, the greater Ontong Java event.

Ophiolites, volcanic deposits from the ocean floor, have been incorporated into the continental basement of New Zealand in the Dun Mountain Ophiolite Belt, found at both ends of the South Island, and in Northland.

• North Island surface volcanism (for more geology details)
• South Island surface volcanism (for more geology details)
• Geothermal areas in New Zealand
• List of disasters in New Zealand by death toll
• List of earthquakes in New Zealand
• List of volcanoes in Antarctica (for volcanoes in New Zealand's Ross Dependency)
• List of volcanoes in New Zealand

• Dench, Alison; Essential Dates: A Timeline of New Zealand History, Auckland: Random House, 2005 ISBN 1-86941-689-9

• Geonet: NZ's geological hazard monitoring system
• GNS Science: NZ Government research site
• Earthquake Commission

Panorama across Lake Taupō, a large caldera lake.