The geology of New Zealand is noted for its volcanic activity, earthquakes and geothermal areas because of its position on the boundary of the Australian Plate and Pacific Plates. New Zealand is part of Zealandia, a microcontinent nearly half the size of Australia that broke away from the Gondwanan supercontinent about 83 million years ago.[1] New Zealand's early separation from other landmasses and subsequent evolution have created a unique fossil record and modern ecology.
New Zealand's geology can be simplified into three phases. First the basement rocks of New Zealand formed. These rocks were once part of the super-continent of Gondwana, along with South America, Africa, Madagascar, India, Antarctica and Australia. The rocks that now form the mostly submerged continent of Zealandia were then nestled between Eastern Australia and Western Antarctica.[2] Secondly New Zealand drifted away from Gondwana and many sedimentary basins formed, which later became the sedimentary rocks covering the geological basement. The final phase is represented by the uplift of the Southern Alps and the eruptions of the Taupō Volcanic Zone.[3]
New Zealand's basement rocks range in age from mid-Cambrian in north-west Nelson to Cretaceous near Kaikōura. These rocks were formed in a marine environment before New Zealand separated from Gondwana. They are divided into the "Western Province", consisting mainly of greywacke, granite and gneiss, and an "Eastern Province", consisting mainly of greywacke and schist.[4] The provinces are further divided into terranes – large slices of crust with different geological histories that have been brought together by tectonic activity (subduction and strike-slip faulting) to form New Zealand.
The Western Province is older than the Eastern Province and outcrops along the west coast of the South Island from Nelson to Fiordland. The Western Province is divided into the Buller and Takaka terranes which formed in mid-Cambrian to Devonian time (510–400 Ma). This includes New Zealand's oldest rocks, trilobite-containing greywacke, which are found in the Cobb Valley in north-west Nelson.[5]
Large sections of the Western Province have been intruded by plutonic rocks or metamorphosed to gneiss. These plutonic basement rocks are subdivided into the Hohonu, Karamea, Median and Paparoabatholiths.[6] These rocks form the foundations beneath offshore Taranaki, and much of the West Coast, Buller, north-west Nelson, Fiordland and Stewart Island / Rakiura. Most of these plutonic rocks were formed in Devonian-Carboniferous time (380–335 Ma) and Jurassic-Cretaceous time (155–100 Ma). The Median Batholith represents a long-lived batholith dividing the Western and Eastern Provinces. Before Zealandia's separation from Gondwana it stretched from Queensland, through what is now New Zealand, into West Antarctica. It marks the site of a former subduction zone on the edge of Gondwana.
The Eastern Province underlies more of New Zealand than the Western Province, including the greywacke and schist of the Southern Alps and all of the basement rocks of the North Island. The Eastern Province contains seven main terranes, the Drumduan, Brook Street, Murihiku, Dun Mountain-Maitai, Caples, Torlesse Composite (Rakaia, Aspiring and Pahau terranes) and Waipapa Composite (Morrinsville and Hunua Terranes).[7] They are mostly composed of greywacke together with argillite, except for the Brook Street and Dun Mountain-Maitai Terranes which have significant igneous components (see Dun Mountain Ophiolite Belt). New Zealand's greywacke is mostly from the Caples, Torlesse Composite (Rakaia and Pahau) and Waipapa Composite (Morrinsville and Hunua) terranes formed in Carboniferous-Cretaceous time (330–120 Ma). Much of these rocks were deposited as submarine fans. They have different origins, as shown by different chemical compositions and different fossils. In general, the sedimentary basement terranes become younger from West to East across the country, as the newer terranes were scraped off the subducting paleo-Pacific Plate, and accreted to the boundary of Gondwana over hundreds of millions of years.
Many rocks in the Eastern Province have been metamorphosed into the Haast Schist, due to exposure to high pressures and temperatures. Rocks grade continuously from greywacke (e.g., in Canterbury) to high-grade schist (e.g., around the Caples-Torlesse boundary in Otago and Marlborough, and Torlesse rocks just to the East of the Alpine Fault). The Alpine Fault that corresponds to the line of the Southern Alps has separated the basement rocks that used to be adjacent by about 480km.
The Australia-New Zealand continental fragment of Gondwana split from the rest of Gondwana in the late Cretaceous time (95–90 Ma). Then around 83 Ma, Zealandia started to separate from Australia forming the Tasman Sea, initially separating from the south. By 75 Ma, Zealandia was essentially separate from Australia and Antarctica, although only shallow seas might have separated Zealandia and Australia in the north. Dinosaurs continued to live in New Zealand after it separated from Gondwana, as shown by sauropod footprints from 70 million years ago in Nelson.[8] this meant that dinosaurs had about 20 million years to evolve unique New Zealand species. During the Cretaceous extension large normal faults formed throughout New Zealand, the Hawks Crag Breccia formed next to scarps and it has become New Zealand's best uraniummineral deposit.[9]
Currently, New Zealand has no native snakes or land mammals (other than bats). Neither marsupials nor placental mammals evolved and reached Australia in time to be on New Zealand when it drifted away 85 million years ago. The evolution and dispersal of snakes is less certain, but there is no hard evidence of them being in Australia before the opening of the Tasman Sea.[10] The multituberculates, another type of mammal which is now extinct, may have been in time to cross the land bridge to New Zealand.[11]
The landmasses continued to separate until early Eocene times (53 Ma). The Tasman Sea, and part of Zealandia then locked together with Australia to form the Australian Plate (40 Ma), and a new plate boundary was created between the Australian Plate and Pacific Plate. Zealandia ended up at a pivot point between the Pacific and Australian Plates, with spreading in the south, and convergence in the north, where the Pacific Plate was subducted beneath the Australian Plate. A precursor to the Kermadec Arc was created. The convergent part of the plate boundary propagated through Zealandia from the north, eventually forming a proto-Alpine Fault in Miocene times (23 Ma). The various ridges and basins north of New Zealand relate to previous positions of the plate boundary.[12]
Sedimentary basins and allochthons (Cretaceous–Recent)
Sedimentary rocks from an uplifted basin. Cape Farewell, South Island.
Erosion and deposition has led to much of Zealandia now being covered in sedimentary rocks that formed in swamps and marine sedimentary basins. Much of New Zealand was low lying around Mid Eocene–Oligocene times (40–23 Ma). Swamps became widespread, forming coal. The land subsided further, and marine organisms produced limestone deposits. Limestone of Oligocene–Early Miocene age formed in many areas, including the King Country, known for the Waitomo Glowworm Cave. In the South Island, limestone is present in Buller, Nelson, and the West Coast, including the Pancake Rocks at Punakaiki in Oligocene–Early Miocene times (34–15 Ma). It is debated whether all of New Zealand was submerged at this time or if small islands remained as "arks" preserving fauna and flora.[13]
The Pancake Rocks at Punakaiki have irregular chasms and ridges, typical of limestone country.
An allochthon is land that formed elsewhere and slid on top of other land (in other words, the material of an enormous landslide). Much of the land of Northland and East Cape were created in this manner.[14] Around 25–22 Ma, Northland and East Cape were adjacent, with East Cape near Whangārei. Northland–East Cape was an undersea basin. Much of the land that now forms Northland–East Cape was higher land to the northeast (composed of rocks formed 90–25 Ma). The Pacific-Australian plate boundary was further to the northeast, with the Pacific Plate subducting under the Australian Plate. Layers of rocks were peeled off the higher land, from the top down, and slid southwest under the influence of gravity, to be stacked the right way up, but in reverse order. Most of the material to slide were sedimentary rocks, however, the last rocks to be slid across were slabs of oceanic crust (ophiolites), mainly basalt. Widespread volcanic activity also occurred (23–15 Ma), and is intermixed with the foreign rocks. Sedimentary basins formed on the allochthons while they were moving. East Cape was later separated from Northland and moved further south and east to its present position.
Volcanism is recorded in New Zealand throughout its whole geological history. Most volcanism in New Zealand, both modern and ancient, has been caused by the subduction of one tectonic plate under another; this causes melting in the mantle, the layer of the Earth below the crust. This produces a volcanic arc, composed of mainly basalt, andesite and rhyolite. Basaltic eruptions tend to be fairly placid, producing scoria cones and lava flows, such as the volcanic cones in the Auckland volcanic field, although Mount Tarawera's violent 1886 eruption was an exception. Andesitic eruptions tend to form steep stratovolcanoes, including mountains such as Ruapehu, Tongariro and Taranaki, islands such as Little Barrier, Whakaari / White and Raoul Islands, or submarine seamounts like Monowai Seamount. Rhyolitic eruptions with large amounts of water tend to cause violent eruptions, producing calderas, such as Lake Taupō and Lake Rotorua. New Zealand also has many volcanoes which are not clearly related to present plate subduction including the extinct Dunedin Volcano and Banks Peninsula, and the dormant Auckland volcanic field.
Extinct volcanoes
The South Island has no currently active volcanoes. However, in the late Cretaceous (100–65 Ma), there was widespread volcanic activity in Marlborough, West Coast, Canterbury and Otago which contributes to landforms such as Mount Somers. In Eocene times (40 Ma), there was volcanic field activity near present day Oamaru. The most well known Miocene volcanic centres are the intra-plate Dunedin Volcano and Banks Peninsulas. The Dunedin Volcano which later eroded to form Otago Peninsula near Dunedin was built up by a series of mainly basaltic intra-plate volcanic eruptions in Miocene times (16–10 Ma).[15] Banks Peninsula near Christchurch was built from two mainly basaltic intra-plate volcanoes in Miocene times (12–6 Ma and 9.5–7.5 Ma), corresponding to the Lyttelton / Whakaraupo and Akaroa Harbours. Southland's Solander Islands / Hautere were active as recently as 150,000 years old.[16] There are also minor volcanics from a similar time period throughout Canterbury, Otago and also on the Chatham Islands.
Intra-plate basaltic volcanic eruptions also occurred in the North Island, near the Bay of Islands in Northland, in the Late Miocene (10 Ma), and again more recently (0.5 Ma). The South Auckland volcanic field was active in Pleistocene times (1.5–0.5 Ma). The Auckland volcanic field started erupting around 250,000 years ago. It includes around 50 distinct eruptions, with most of the prominent cones formed in the last 30,000 years, and the most recent eruption, which formed Rangitoto Island, around 600 years ago. The field is currently dormant and further eruptions are expected. Over time the volcanic field has slowly been drifting northwards.[17]
Volcanism in the North Island has been dominated by a series of volcanic arcs which have evolved into the still active Taupō Volcanic Zone. Over time, volcanic activity has moved south and east, as the plate boundary moved eastward. This started in Miocene times (23 Ma) when a volcanic arc became active to the west of Northland, and gradually moved South down to New Plymouth, where Taranaki is still active. It produced mainly andesitic strato-volcanoes. The Northland volcanoes include the volcanoes that produced the Waipoua Plateau (site of the Waipoua Forest) and the Kaipara Volcano. The Waitakere Volcano (22–16 Ma) has mainly been eroded, but conglomerate from the volcano forms the Waitākere Ranges, and produced most of the material that makes up the Waitemata sandstones and mudstones.[18]Lahars produced the coarser Parnell Grit. Notable visible volcanoes in the Waikato include Karioi and Pirongia (2.5 Ma). The volcanoes off the West coast of the North Island, together with Taranaki and the Tongariro Volcanic Centre, are responsible for the black iron sand on many of the beaches between Taranaki and Auckland.
After this, activity shifted further East to the Taupō Volcanic Zone, which runs from the Tongariro Volcanic Centre (Ruapehu and Tongariro), through Taupō, Rotorua, and out to sea to form the Kermadec Ridge.[19] Activity was initiated around 2 Ma, and continues to this day. The Tongariro Volcanic Centre is composed of andesitic volcanoes, while the areas around Taupō and Rotorua are largely rhyolitic with minor basalt. Early eruptions between Taupō and Rotorua around 1.25 Ma, and 1 Ma, were large enough to produce an ignimbrite sheet that reached Auckland, Napier, and Gisborne. This includes vast pumice deposits generated from eruptions in the Taupō Volcanic Zone occur throughout the central North Island, Bay of Plenty, Waikato, King Country and Manawatū-Whanganui regions. Every so often, there are swarms of earthquakes within an area of the Taupō Volcanic Zone, which last for years. These earthquake swarms indicate that some movement of magma is occurring below the surface. While they have not resulted in an eruption in recent times, there is always the potential for a new volcano to be created, or a dormant volcano to come to life.
The Tongariro Volcanic Centre developed over the last 275,000 years and contains the active andesitic volcanic cones of Ruapehu, Tongariro, and Ngauruhoe (really a side cone of Tongariro). Ruapehu erupts about once a decade, and while the eruptions cause havoc for skiers, plane flights and hydroelectric dams, the eruptions are relatively minor. However, the sudden collapse of the crater wall caused major problems when it generated a lahar in 1953, that destroyed a rail bridge, and caused 151 deaths at Tangiwai. The last significant eruption was 1995–96. Ngauruhoe last erupted 1973–75. Taranaki is a perfectly formed andesitic strato-volcano, that last erupted in 1755.
Lake Taupō, the largest lake in the North Island, is a volcanic caldera, responsible for rhyolitic eruptions about once every 1,000 years.[20] The largest eruption in the last 65,000 years was the cataclysmic Oruanui Eruption 26,500 years ago, producing 530 cubic kilometres of magma. The most recent eruption, around 233 AD was also a major event, the biggest eruption worldwide in the last 5,000 years. The eruption caused a pyroclastic flow that devastated the land from Waiouru to Rotorua in 10 minutes.
The Ōkataina Volcanic Centre, to the East of Rotorua, is also responsible for major cataclysmic rhyolitic eruptions. The last eruption, of Tarawera and Lake Rotomahana in 1886, was a relatively minor eruption, which was thought to have destroyed the famous Pink and White Terraces, and covered much of the surrounding countryside in ash, killing over 100 people. In 2017 researchers rediscovered the locations of the Pink and White Terraces using a forgotten survey from 1859.[21][22] Many lakes around Rotorua are calderas from rhyolitic eruptions. For example, Lake Rotorua erupted around 13,500 years ago.
A line of undersea volcanoes extends out along the Kermadec Ridge. Whakaari / White Island, in the Bay of Plenty, represents the southern end of this chain and is a very active andesitic volcano, erupting with great frequency. It has the potential to cause a tsunami in the Bay of Plenty, as does the dormant Mayor Island / Tūhua volcano.
New Zealand is currently astride the convergent boundary between the Pacific and Australian Plates. Over time, the relative motion of the plates has altered and the current configuration is geologically recent. Currently the Pacific Plate is subducted beneath the Australian Plate from around Tonga in the north, through the Tonga Trench, Kermadec Trench, and Hikurangi Trough to the east of the North Island of New Zealand, down to Cook Strait. Through most of the South Island, the plates slide past each other (Alpine Fault), with slight obduction of the Pacific Plate over the Australian Plate, forming Southern Alps. From Fiordland south, the Australian Plate subducts under the Pacific Plate forming the Puysegur Trench.[24] This configuration has led to volcanism and extension in the North Island forming the Taupō Volcanic Zone and uplift in the South Island forming the Southern Alps.
The Pacific Plate is colliding with the Australian Plate at a rate of about 40mm/yr.[25] The East coast of the North Island is being compressed and lifted by this collision, producing the North Island and Marlborough Fault Systems. The East Coast of the North Island is also rotating clockwise, relative to Northland, Auckland and Taranaki, stretching the Bay of Plenty, and producing the Hauraki Rift (Hauraki Plains and Hauraki Gulf) and Taupō Volcanic Zone. The East Coast of the South Island is sliding obliquely towards the Alpine Fault, relative to Westland, causing the Southern Alps to rise about 10mm/yr (although they are also worn down at a similar rate).[26] The Hauraki Plains, Hamilton, Bay of Plenty, Marlborough Sounds, and Christchurch are sinking. The Marlborough Sounds are known for their sunken mountain ranges. As Wellington rises, and Marlborough sinks, Cook Strait is being shifted further south.[27]
Great stress is built up in the Earth's crust due to the constant movement of the tectonic plates. This stress is released by earthquakes, which can occur on the plate boundary or on any of thousands of smaller faults throughout New Zealand. Because the Pacific Plate is subducting under the eastern side of the North Island, there are frequent deep earthquakes east of a line from the Bay of Plenty to Nelson (the approximate edge of the subducted plate), with the earthquakes being deeper to the west, and shallower to the east. Because the Australian Plate is subducting under the Pacific Plate in Fiordland, there are frequent deep earthquakes near Fiordland, with the earthquakes being deeper to the east and shallower near the west.
Shallow earthquakes are more widespread, occurring almost everywhere throughout New Zealand (especially the Bay of Plenty, East Cape to Marlborough, and Alpine Fault). However, Northland, Waikato, and Otago are relatively stable. Canterbury had been without a major earthquake in recorded history until the Mw 7.1 Canterbury earthquake on 4 September 2010. The volcanic activity in the central North island also creates many shallow earthquakes.
Global palaeotemperature graphs (compressed scale) note the warmer Eocene and Miocene in green and the Ice Age in blue.
Since Zealandia separated from Gondwana (80 mya) in the Cretaceous the climate has typically been far warmer than today. However, since the Quaternary glaciation (2.9 mya) Zealandia has experienced climate either cooler or only slightly warmer than today.
In the Cretaceous, New Zealand was positioned at 80 degrees south at the boundary between Antarctica and Australia. But it was covered in trees as the climate of 90 million years ago was much warmer and wetter than today.[28] During the warm Eocene Period vast swamps covered New Zealand which became coal seams in Southland and Waikato. In the Miocene there are paleontological records of warm lakes in Central Otago with palm trees and small land mammals.[29]
Over the past 30,000 years three major climate events are recorded in New Zealand, the last glacial maximum's coldest period from 28 to 18,000 years ago, a transitional period from 18 to 11,000 years ago and the Holocene Inter Glacial which has been occurring for the past 11,000 years.[30] Throughout the last glacial maximum, global sea levels were about 130 metres (430 feet) lower than present levels. When this happened the North Island, South Island, and Stewart Island were joined.[31] Temperatures dropped by about 4–5°C. Much of the Southern Alps and Fiordland were glaciated, but the rest of New Zealand was largely ice-free. The land north of Hamilton was forested, but much of the rest of New Zealand was covered in grass or shrubs, due to the cold and dry climate.[32][33] This lack of vegetation cover lead to greater wind erosion and the deposition of loess (windblown dust).[30] The study of New Zealand's paleoclimate has settled some of the debate regarding links between the Little Ice Age (LIA) in the Northern Hemisphere and the climate in New Zealand at the same time. The key facts to emerge are that New Zealand did experience a noticeable cooler climate, but at a slightly later date than in the Northern Hemisphere.[34]
Geological hazards
Earthquake damage in Christchurch (2011).
New Zealand suffers from many natural hazards, including earthquakes and tsunamis, volcanic and hydrothermal eruptions and landslides.
The largest earthquake in New Zealand was an M8.2 event in the Wairarapa, in 1855,[35] and the most deaths (261) occurred in a M7.8 earthquake in Hawkes Bay in 1931. Widespread property damage was caused by the 2010 Canterbury earthquake, which measured 7.1; The M6.3 aftershock of 22 February 2011 (2011 Canterbury earthquake) resulted in 185 fatalities. Most recently, the M7.8 Kaikōura earthquake struck just after midnight on 14 November 2016, killing two people in the remote Kaikōura area northeast of Christchurch. Numerous aftershocks of M5.0 or greater are spread over a large area between Wellington and Culverden.
New Zealand is at risk from tsunamis that are generated from both local and international faults. The eastern coast of New Zealand is most at risk as the Pacific Ocean is more tectonically active than the Tasman Sea. Locally the faults along the North Island's east coast provide the greatest risk. Minor tsunamis have occurred in New Zealand from earthquakes in Chile, Alaska and Japan.
There are many potentially dangerous volcanoes in the Taupō Volcanic Zone. The most severe volcanic eruption since the arrival of Europeans is the Tarawera eruption in 1886. A lahar from Mount Ruapehu destroyed a bridge and derailed a train in December 1953, killing 151 people. Even a minor eruption at Ruapehu could cause the loss of electricity for Auckland, due to ash on the power lines, and in the Waikato River (stopping the generation of hydroelectric power).
Many parts of New Zealand are susceptible to landslides, particularly due to deforestation and the high earthquake risk. Much of the North Island is steep, and composed of soft mudstone known as papa,[36] that easily generates landslides.[37]
New Zealand main geological resources are coal, gold, oil, and natural gas.[38][39]Coal has been mined in Northland, the Waikato, Taranaki, Nelson and Westland, Canterbury, Otago, and Southland. The West Coast contains some of New Zealand's best bituminous coal. The largest coal deposits occur in Southland. Gold has been mined in the Coromandel and Kaimai Ranges (especially the Martha Mine at Waihi), Westland, Central Otago, and Eastern Otago (especially Macraes Mine), and on the west coast of the South Island. The only area in New Zealand with significant known oil and gas deposits is the Taranaki area, but many other offshore areas have the potential for deposits.[40]Iron sand is also plentiful on the west coast from Taranaki to Auckland.[41]Jade (Pounamu in Māori) from South Island ophiolites continues to be extracted, mostly from alluvium, and worked for sale. Groundwater reservoirs are extracted throughout the country, but are particularly valuable in the dryer eastern regions of both the North and South Islands. Some of these reservoirs also can be used in low temperature heating and for agricultural frost protection, as well as being a pottable resource.[42]
The detailed study of New Zealand's geology began with Julius von Haast and Ferdinand von Hochstetter who created numerous regional geological maps of the country during resource exploration in the mid-late 1800s.[43] In 1865 James Hector was appointed to found the Geological Survey of New Zealand. Patrick Marshall coined the terms andesite line and ignimbrite in the early 1900s while working in the Taupō Volcanic Zone. Harold Wellman discovered the Alpine Fault and its 480km offset in 1941. Even though Wellman proved that large blocks of land could move considerable distances, the New Zealand geological survey was largely a late adopter of plate tectonics.[44]
Charles Cotton became an international authority on geomorphology using New Zealand active tectonics and variable climate to create universally applicably rules.[45] His major works becoming standard text books in New Zealand and overseas.[46]Charles Fleming established the Wanganui Basin as a classic site for studying past sea levels and climates. In 1975 the palaeontologistJoan Wiffen discovered the first dinosaur fossils in New Zealand.
The Geological Survey of New Zealand now known as GNS Science has done extensive mapping through New Zealand at 1:250,000 and 1:50:000 scales. The most modern map series are the "QMAPs" at 1:250,000.[47] New Zealand's geological research is published by GNS Science, in the New Zealand Journal of Geology and Geophysics, and internationally. A Map showing the distribution of earthquakes in New Zealand can be obtained from Te Ara: The Encyclopedia of New Zealand.[48] Current earthquake and volcanic activity can be obtained from the GeoNet website.[49] The universities of Auckland, Canterbury, Massey, Otago, Victoria and Waikato are activity engaged in geological research in New Zealand, Antarctica, the wider South Pacific and elsewhere.
Mount Ruapehu is an active stratovolcano at the southern end of the Taupō Volcanic Zone and North Island volcanic plateau in New Zealand. It is 23 km (14 mi) northeast of Ohakune and 23 km (14 mi) southwest of the southern shore of Lake Taupō, within the Tongariro National Park. The North Island's major ski resorts and only glaciers are on its slopes.
The Taupō Volcanic Zone (TVZ) is a volcanic area in the North Island of New Zealand. It has been active for at least the past two million years and is still highly active.
Mount Ngauruhoe is a volcanic cone in New Zealand. It is the youngest vent in the Tongariro stratovolcano complex on the Central Plateau of the North Island and first erupted about 2,500 years ago. Although often regarded as a separate mountain, geologically, it is a secondary cone of Mount Tongariro.
The natural history of New Zealand began when the landmass Zealandia broke away from the supercontinent Gondwana in the Cretaceous period. Before this time, Zealandia shared its past with Australia and Antarctica. Since this separation, the New Zealand landscape has evolved in physical isolation, although much of its current biota has more recent connections with species on other landmasses. The exclusively natural history of the country ended in about 1300 AD, when humans first settled, and the country's environmental history began. The period from 1300 AD to today coincides with the extinction of many of New Zealand's unique species that had evolved there.
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.
Zealandia, also known as Te Riu-a-Māui (Māori) or Tasmantis, is an almost entirely submerged mass of continental crust in Oceania that subsided after breaking away from Gondwana 83–79 million years ago. It has been described variously as a submerged continent, continental fragment, and microcontinent. The name and concept for Zealandia was proposed by Bruce Luyendyk in 1995, and satellite imagery shows it to be almost the size of Australia. A 2021 study suggests Zealandia is over a billion years old, about twice as old as geologists previously thought.
The Auckland Region of New Zealand is built on a basement of greywacke rocks that form many of the islands in the Hauraki Gulf, the Hunua Ranges, and land south of Port Waikato. The Waitākere Ranges in the west are the remains of a large andesitic volcano, and Great Barrier Island was formed by the northern end of the Coromandel Volcanic Zone. The Auckland isthmus and North Shore are composed of Waitemata sandstone and mudstone, and portions of the Northland Allochthon extend as far south as Albany. Little Barrier Island was formed by a relatively isolated andesitic volcano, active around 1 to 3 million years ago.
The Waikato and King Country regions of New Zealand are built upon a basement of greywacke rocks, which form many of the hills. Much of the land to the west of the Waikato River and in the King Country to the south has been covered by limestone and sandstone, forming bluffs and a karst landscape. The volcanic cones of Karioi and Pirongia dominate the landscape near Raglan and Kawhia Harbours. To the east, the land has been covered with ignimbrite deposits from the Taupō Volcanic Zone. Large amounts of pumice from the Taupō Volcanic Zone have been deposited in the Waikato Basin and Hauraki Plains.
Lake Taupō, in the centre of New Zealand's North Island, fills the caldera of the Taupō Volcano, a large rhyolitic supervolcano. This huge volcano has produced two of the world's most powerful eruptions in geologically recent times.
The Taranaki Region of New Zealand is built upon the Median Batholith in the West, and Greywacke Rocks in the East. However, no rocks older than Miocene times are visible at the surface. The dominant feature of the Taranaki Region is the andesitic stratovolcano of Mount Taranaki, which is only about 130,000 years old. The dissected hill country to the East of the Taranaki Peninsula, and West of the Central Volcanic Plateau is composed of soft Miocene to Pleistocene sandstone and mudstone. The coastal lowlands around Wanganui to the South have well-developed Quaternary marine terraces, and coastal sand dunes.
The Wellington Region of New Zealand has a foundation of Torlesse Greywacke rocks, that make up the Tararua and Rimutaka Ranges, that go from Wellington in the south to the Manawatū Gorge, where they are renamed as the Ruahine Ranges, and continue further north-northeast, towards East Cape. To the west of the Tararua Ranges are the Manawatū coastal plains. To the east of the Ruahine Ranges is the Wairarapa-Masterton Basin, then the Eastern Uplands that border the eastern coast of the North Island from Cape Palliser to Napier.
The Raukumara Region of New Zealand corresponds to the East Cape of the North Island, and associated mountain ranges.
Canterbury in New Zealand is the portion of the South Island to the east of the Southern Alps / Kā Tiritiri o te Moana, from the Waiau Uwha River in the north, to the Waitaki River in the south.
New Zealand's Northland Region is built upon a basement consisting mainly of greywacke rocks, which are exposed on the eastern side of the peninsula. In-place Eocene coal measures crop out at Kamo, near Whangārei, and Oligocene limestone crops out at Hikurangi, near Whangārei.
The Kapenga Caldera in New Zealand’s Taupō Volcanic Zone lies in a low land area immediately south of Lake Rotorua through the Hemo Gap in the Rotorua Caldera rim. At some time more than 60,000 years ago Lake Rotorua drained through the Hemo Gap and some of the Kapenga Caldera floor was likely occupied by a lake, that has been called Kapenga.
The relatively small Rotomā Caldera is in the Taupō Volcanic Zone in the North Island of New Zealand.
The Taupō Rift is the seismically active rift valley containing the Taupō Volcanic Zone, central North Island of New Zealand.
The Taupō Fault Belt contains many almost parallel active faults, and is located in the Taupō Rift of the central North Island of New Zealand geographically between Lake Taupō and the lakes of Rotorua, Tarawera, Rotomahana and Rerewhakaaitu. The potential active fault density is very high, with only 0.1 to 1 km separating the north-east to south-west orientated normal fault strands on detailed mapping of part of the belt. The Waikato River bisects the western region of the belt.
Much of the volcanic activity in the northern portions of the North Island of New Zealand is recent in geological terms and has taken place over the last 30 million years. This is primarily due to the North Island'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. The activity has included some of the world's largest eruptions in geologically recent times and has resulted in much of the surface formations of the North Island being volcanic as shown in the map.
Pariwhero / Red Rocks is a geological formation located in a scientific reserve on the south coast of Wellington, New Zealand. The site has been classified as nationally significant, and of high educational and scientific importance. The reserve provides examples of a wide range of rock formations and geological processes that are representative of the earliest stages in the formation of New Zealand.
↑ Scanlon, John D.; Lee, Michael S.Y.; Archer, Michael (2003). "Mid-Tertiary elapid snakes (Squamata, Colubroidea) from Riversleigh, northern Australia: early steps in a continent-wide adaptive radiation". Geobios. 36 (5): 573–601. Bibcode:2003Geobi..36..573S. doi:10.1016/S0016-6995(03)00056-1. ISSN0016-6995.
↑ Molloy, Catherine; Shane, Phil; Augustinus, Paul (2009). "Eruption recurrence rates in a basaltic volcanic field based on tephra layers in maar sediments: Implications for hazards in the Auckland volcanic field". Geological Society of America Bulletin. 121 (11–12): 1666–1677. Bibcode:2009GSAB..121.1666M. doi:10.1130/B26447.1. ISSN0016-7606.
↑ Hayward, Bruce W. (1979). "Eruptive history of the early to mid miocene Waitakere volcanic arc, and palaeogeography of the Waitemata Basin, Northern New Zealand". Journal of the Royal Society of New Zealand. 9 (3): 297–320. Bibcode:1979JRSNZ...9..297H. doi:10.1080/03036758.1979.10419410. ISSN0303-6758.
↑ Bunn, Rex; Nolden, Sascha (7 June 2017). "Forensic cartography with Hochstetter's 1859 Pink and White Terraces survey: Te Otukapuarangi and Te Tarata". Journal of the Royal Society of New Zealand. 48: 39–56. doi:10.1080/03036758.2017.1329748. ISSN0303-6758. S2CID134907436.
↑ Little, Timothy A.; Cox, Simon; Vry, Julie K.; Batt, Geoffrey (2005). "Variations in exhumation level and uplift rate along the obliqu-slip Alpine fault, central Southern Alps, New Zealand". Geological Society of America Bulletin. 117 (5): 707. Bibcode:2005GSAB..117..707L. doi:10.1130/B25500.1. ISSN0016-7606.
1 2 Alloway, Brent V.; Lowe, David J.; Barrell, David J. A.; Newnham, Rewi M.; Almond, Peter C.; Augustinus, Paul C.; Bertler, Nancy A. N.; Carter, Lionel; Litchfield, Nicola J.; McGlone, Matt S.; Shulmeister, Jamie; Vandergoes, Marcus J.; Williams, Paul W. (2007). "Towards a climate event stratigraphy for New Zealand over the past 30 000 years (NZ-INTIMATE project)". Journal of Quaternary Science. 22 (1): 9–35. Bibcode:2007JQS....22....9A. doi:10.1002/jqs.1079. ISSN0267-8179. S2CID130794280.
↑ Williams, Paul W.; McGlone, Matt; Neil, Helen; Zhao, Jian-Xin (2015). "A review of New Zealand palaeoclimate from the Last Interglacial to the global Last Glacial Maximum". Quaternary Science Reviews. 110: 92–106. doi:10.1016/j.quascirev.2014.12.017. ISSN0277-3791.
Graham, Ian J. et al.;A continent on the move: New Zealand geoscience into the 21st century – The Geological Society of New Zealand in association with GNS Science, 2008. ISBN978-1-877480-00-3
Campbell, Hamish; Hutching, Gerard; In Search of Ancient New Zealand, Penguin Books in association with GNS Science, 2007, ISBN978-0-14-302088-2
Lava and Strata: A guide to the volcanoes and rock formations of Auckland – Homer, Lloyd; Moore, Phil & Kermode, Les; Landscape Publications and the Institute of Geological and Nuclear Sciences, 2000. ISBN0-908800-02-9.
Vanishing volcanoes: a guide to the landforms and rock formations of Coromandel Peninsula – Homer, Lloyd; Moore, Phil; Landscape Publications and the Institute of Geological and Nuclear Sciences, 1992. ISBN0-908800-01-0.
Reading the rocks: a guide to geological features of the Wairarapa Coast – Homer, Lloyd; Moore, Phil & Kermode, Les; Landscape Publications and the Institute of Geological and Nuclear Sciences, 1989. ISBN0-908800-00-2
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