Earth:Mount Ruapehu

From HandWiki
Short description: Volcano in New Zealand

Mount Ruapehu
Tongariro Northern Circuit, New Zealand (5).JPG
Mt Ruapehu from Tongariro Northern Circuit, 2015
Highest point
Elevation2,797 m (9,177 ft) [1][2]
Prominence2,797 m (9,177 ft)
ListingUltra
New Zealand #19
Coordinates [ ⚑ ] : 39°17′S 175°34′E / 39.28°S 175.57°E / -39.28; 175.57 [1]
Naming
Native nameˈɾʉaˌpɛhʉ  (Māori) (Māori)
English translationpit of noise or exploding pit[3]
Geography
Mount Ruapehu is located in New Zealand
Mount Ruapehu
Mount Ruapehu
North Island, New Zealand
Geology
Age of rock~200,000 years[1]
Mountain typeStratovolcano
Volcanic arc/beltTaupō Volcanic Zone
Last eruption25 September 2007
Climbing
First ascent1879 by G. Beetham and J. P. Maxwell (non-indigenous)
Easiest routeHike

Mount Ruapehu (/ˈruːəˌpeɪhuː/; Māori: [ˈɾʉaˌpɛhʉ]) 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.

Ruapehu, the largest active volcano in New Zealand, has the highest point in the North Island and has three major peaks: Tahurangi (2,797 m), Te Heuheu (2,755 m) and Paretetaitonga (2,751 m). The deep, active crater is between the peaks and fills with water between major eruptions, being known as Crater Lake (Māori: Te Wai ā-moe). The name Ruapehu means "pit of noise" or "exploding pit" in Māori.[4]

Geography

Ruapehu is located in the centre of the North Island of New Zealand, 23 km (14 mi) northeast of Ohakune, New Zealand and 23 km (14 mi) southwest of the southern shore of Lake Taupō, within Tongariro National Park. Ruapehu is the largest and southernmost volcano in the national park, with an estimated volume of 110 km3.[5] The volcano is surrounded by a ring plain of volcanic material, made from lahar deposits, ash fall, and landslide debris.[6]

There are three access routes to Ruapehu, and each access route leads to one of the three skifields that are found on its slopes. State Highway 48 leads to Whakapapa Village at the base of the mountain, and from there an access road leads up the mountain to Iwikau Village at the base of the Whakapapa skifield on the northwestern bumpy hilly slopes. An access road from Ohakune leads to Turoa skifield on the southwestern slopes, and a four-wheel drive track leads from the Desert Road (State Highway 1) to the Tukino skifield on the eastern slopes.[7][8]

Ruapehu's active crater, dubbed Crater Lake (Te Wai ā-moe), is situated at the southern end of the Summit Plateau, and as the name suggests, is filled with a warm, acidic lake. The lake's outlet is at the head of the Whangaehu Valley, where the Whangaehu River arises. The Whangaehu River is notorious for destructive lahars caused by Ruapehu's eruptions. In historic times, eruptions have built tephra dams across the outlet on several occasions, most recently in 1945 and 1996. These dams failed in 1953 and 2007 respectively, causing an outburst of Crater Lake each time, which sent destructive lahars down the river. The 1953 lahar was the cause of the Tangiwai disaster, in which 151 people died. Even larger lahars occurred in 1862 and 1895.[9][10]

A total of 18 glaciers have been recognised on Ruapehu, of which six are named.[11] Two glaciers are found in the active crater: one on the north side of the crater under Paretetaitonga Peak and another one to the south, and these are New Zealand's only crater glaciers.[12] Most of the ice on Ruapehu is contained in only three of its glaciers: the Whangaehu, Summit Plateau, and Mangatoetoenui glaciers.[11] The Summit Plateau glacier is not a glacier in the true sense, but rather an ice field that fills an extinct volcanic crater, and the ice there reaches more than 130 m thick.[12] The Whangaehu glacier feeds the Whangaehu River, and the Mangatoetoenui glacier is one of the principal sources of the Waikato River, which arises as a series of streams on Ruapehu's eastern slopes.[12][13] On the western side of the mountain, many of the streams that arise there, such as the Whakapapa and Manganui o te Ao rivers, feed the Whanganui River.[14]

Mount Ruapehu, January 2002.

Ruapehu's glaciers are situated at the northern limit for the formation of permanent ice in New Zealand, and thus they are extremely sensitive to changes in climate. Surveys of the glaciers undertaken since 1955 have found that the glaciers have all been thinning and retreating, with the exception of the northern crater glacier, which thickened and lengthened after the 1953 outburst of Crater Lake lowered the lake water level.[12][15]

Climate

Ruapehu has a polar tundra climate (Köppen: ET) on the upper slopes, with average temperatures ranging from −4–15 °C in summer and −7–7 °C in winter, depending on elevation and cloudiness.[16][17] On the lower slopes, Ruapehu has a subpolar oceanic climate (Köppen: Cfc).[16]

The prevalent wind direction in the region is westerly or northwesterly, and gale force conditions (i.e. wind speeds higher than 33 kn (61 km/h)) are common on the mountain.[17] Rainfall is higher on the western flanks of Ruapehu than the eastern flanks due to the rain shadow effect. Whakapapa Village receives an average of 2,200 mm of rain per year, whereas the Rangipo Desert to the east of Ruapehu receives slightly more than 1,500 mm of rain annually.[18] Snow falls on average as low as 1,500 m elevation.[18] Script error: No such module "weather box".

Severe weather incidents

Weather conditions can be changeable over the day, and mountain visitors are advised to be prepared and carry basic survival equipment.[20] Severe weather has claimed several lives over the years, including a party of five NZ Army soldiers and one RNZN naval rating, caught in a week-long storm while undergoing winter survival training in 1990.[21] The same storm also trapped an experienced Japanese mountaineer when the weather unexpectedly closed in on him, but he built a snow cave and sheltered in it until he was rescued days later.[22]

Extreme weather conditions have caused visitors to be trapped on the mountain in the past. In 2003, about 350 visitors to Whakapapa skifield and 70 staff had to stay overnight in various lodges at Iwikau village (small village at the top of mountain road) after a snow storm made the road too dangerous to descend.[23] In 2008 extreme weather resulted in about 2000 visitors being evacuated from Whakapapa skifield, with cars being led down the mountain in groups of five. About 100 cars were left at the skifield overnight.[24][25]

Geology

<mapframe text="Map centered on Mount Ruapehu to show approximate selected surface volcanic deposits around it with andesitic deposits in shades of red. To the north this is continuous with volcanic deposits from Mount Tongariro and beyond this is Lake Rotoaira and the andesitic deposits of Pihanga. Rhyolitic ignimbrite surface deposits are various shades of violet from eruptions of the Taupō Volcano. Mixed (e.g. lahars) and sedimentary deposits are not coloured. Clicking on the map enlarges it, and enables panning and mouseover of volcanic deposits name/wikilink and ages before present for wider volcanic context. The key to the shading of other volcanics that are shown (active in last million years odd) with panning is dacite - purple, rhyolite - violet, basalt - brown, monogenetic basalts - dark brown, undifferentiated basalts of the Tangihua Complex in Northland Allochthon - light brown, arc basalts - deep orange brown, arc ring basalts -orange brown, basaltic andesite`- light red, and plutonic - gray. White shading has been used for postulated calderas (usually subsurface now)." zoom="9" align="left" longitude="175.566667" height="250" class="no-icon" latitude="-39.283333" width="250">{{Wikipedia:Map data/Northern North Island Volcanics}}</mapframe> Ruapehu is a composite andesitic stratovolcano located at the southern end of the Taupō Volcanic Zone and forming part of the Tongariro Volcanic Center.[5] Volcanism at Ruapehu is caused by the subduction of the Pacific Plate under the Australian Plate at the Hikurangi Trench to the east of the North Island. Ruapehu has erupted from multiple craters over its lifetime, however, only one crater is presently active, a deep crater at the southern end of the summit plateau which is filled with hot, acidic water, dubbed Crater Lake (Te Wai ā-moe).

Ruapehu sits on a basement of Mesozoic greywacke overlain by a thin layer of sediments of the Wanganui Basin, composed of sands, silts, shell beds, and limestone.[26] It has not been clearly established when Ruapehu first began erupting, only that eruptions began at least 250,000 years ago and possibly as early as 340,000 years ago.[27] Ruapehu has been built in four distinct stages of relatively intense eruptive activity followed by periods of relative quiet. Each of these four stages of activity has left behind distinct rock formations, named the Te Herenga Formation (erupted 250,000–180,000 years ago), the Wahianoa Formation (erupted 160,000–115,000 years ago), the Mangawhero Formation (erupted 55,000–15,000 years ago), and the Whakapapa Formation (erupted 15,000–2,000 years ago).[27] Each of these rock formations is composed of lava flows and tuff breccias, and studies of these formations has revealed how volcanic activity at Ruapehu has developed over time.[5][27] During the Te Herenga stage of activity, magma rose quickly through the crust during eruptions. However, by 160,000 years ago a complex network of magma dikes and sills had formed in the crust under the volcano, and lava erupted since that time shows signs of extensive mixing between different magma chambers prior to eruptions.[26]

A composite satellite image looking west across Ruapehu, with the older eroded volcano Hauhungatahi visible behind it, and the cone of Ngauruhoe visible to the right.

In modern times, volcanic activity has been centred on Crater Lake. There are two active vents under the lake, dubbed North Vent and Central Vent.[28] Activity is characterized by cyclic heating and cooling of the lake over periods of 6–12 months. Each heating cycle is marked by increased seismic activity under the crater and is accompanied by increased emission of volcanic gases, indicating that the vents under Crater Lake are open to gas escape.[29][30] Evidence suggests that an open-vent system such as this has been in place throughout Ruapehu's 250,000 year history. This prevents build-up of pressure and results in relatively small, frequent eruptions (every 20–30 years on average) at Ruapehu compared to other andesitic volcanoes around the world.[27][29]

Crater Lake is emptied by major eruptions, such as the ones in 1945 and 1995–1996, but refills after eruptions subside, fed by melting snow and vented steam.[30] In historic times, major eruptions have deposited a tephra dam across the lake's outlet, preventing lake overflow into the Whangaehu valley. The dam collapses after several years causing a large lahar down the valley. The tephra dam created by the 1945 eruptions collapsed on 24 December 1953, sending a lahar down the Whangaehu River and causing the Tangiwai disaster. 151 people died when the lahar swept away the Tangiwai railway bridge just before an express train crossed it. Another dam was deposited by the 1995–1996 eruptions, which collapsed on 18 March 2007. A warning system, the Eastern Ruapehu Lahar Alarm and Warning System (ERLAWS) system was installed on the mountain in 2000 to detect such a collapse and alert the relevant authorities. The ERLAWS system detected the 2007 lahar, and roads were closed and railway traffic stopped until the lahar had subsided.[31]

Early eruptive history

The earliest known volcanic activity in Tongariro National Park was approximately 933,000 ± 46,000 years ago at Hauhungatahi, northwest of Ruapehu.[32] Subsequently, andesitic clasts found 100 km southwest of Ruapehu, near Whanganui, demonstrate that volcanism was likely present in the Ruapehu area 340,000 years ago.[27] However, the oldest rocks on Ruapehu itself are approximately 250,000 years old.[27] Eruptions during this period are believed to have built a steep volcanic cone around a central crater, which would have been located somewhere near the present-day upper Pinnacle Ridge.[5] Cone-building eruptions ceased about 180,000 years ago, and the cone began to be eroded away by glacial action. Rock formations that date to this period are collectively named the Te Herenga Formation, and today these formations be seen at Pinnacle Ridge, Te Herenga Ridge, and Whakapapanui Valley, all on the northwestern slopes of Ruapehu.[5][27]

Approximately 160,000 years ago, cone-building eruptions began again, this time from a crater that is thought to have lain northwest of present-day Mitre Peak (Ringatoto)—southeast of the original Te Herenga vent.[5] Eruptions continued until approximately 115,000 years ago, and the lava erupted during this period is known as the Wahianoa Formation. This formation has also been heavily eroded by glacial activity, and it now forms the southeastern flanks of modern Ruapehu.[5][26] The formation consists of lava flows and tuff breccias.[33]

Beginning approximately 55,000 years ago, a third phase of cone-building eruptions began, creating the Mangawhero Formation. This formation was erupted onto the eroded Wahianoa Formation in two phases: the first occurring 55,000–45,000 years ago and the second 30,000–15,000 years ago.[27] Multiple summit craters were active during this period, all lying between Tahurangi and the northern summit plateau. Parasitic eruptions also occurred at Pukeonake, a scoria cone to the northwest of Ruapehu, and at several isolated craters near Ohakune. The Mangawhero Formation can be found over most of modern Ruapehu, and it forms most of the mountain's high peaks as well as the Turoa skifield.[5][33]

Holocene activity

<timeline> ImageSize = width:320 height:800 PlotArea = right:50 top:10 left:50 bottom:10 DateFormat = yyyy TimeAxis = orientation:vertical order:reverse Period = from:300 till:2050 AlignBars = early ScaleMajor = unit:year increment:100 start:300 Colors = 

 id:canvas value:rgb(1,1,0.85)

BackgroundColors = canvas:canvas PlotData = 

 width:15 color:black
 bar:test from:300 till:332 # Pre Taupo

PlotData = 

 width:15 color:white
 bar:test from:332 till:1200 # Pre Maori

PlotData = 

 width:15 color:yellow
 bar:test from:1200 till:1840 # Pre accurate

PlotData = 

 width:15 color:orange
 bar:test from:1840 till:2050 # Accurate

PlotData = 

 at:305 shift:(10,0) text: Eruption 
 at:332 shift:(130,0) textcolor:red text:( km  )
 at:332 shift:(150,5) textcolor:red fontsize:XS text:3
 at:305 shift:(100,0) textcolor:red text:Eruptive volume
 at:304 shift:(200,0) textcolor:red text:Tephra Layers 
 at:332 shift:(205,0) textcolor:red text: 6 5 4 3 2 1
 at:1995 shift:(10,-5) text: 1995-96 (T32, Tf19)
 at:1995 shift:(120,-5) textcolor:red fontsize:S text:0.004
 bar:test at:1995 mark:(line,red)
 at:1945 shift:(10,-5) text: 1945 (T31)
 at:1945 shift:(120,-5) textcolor:red fontsize:S text:0.00214
 bar:test at:1945 mark:(line,red)
 at:1835 shift:(10,-5) text: 1835 (T30, Tf18)
 at:1835 shift:(120,-5) textcolor:red fontsize:S text:0.00725
 bar:test at:1835 mark:(line,red)
 at:1788 shift:(10,-5) text: 1788  (T29, Tf17)
 at:1788  shift:(120,-5) textcolor:red fontsize:S text:0.0118
 bar:test at:1788  mark:(line,red)
 at:1747 shift:(10,-6) text: 1747 (T28, Tf16)
 at:1747 shift:(120,-6) textcolor:red fontsize:S text:0.00691
 bar:test at:1747 mark:(line,red)
 at:1735 shift:(10,-2) text: 1735 (T27, Tf15)
 at:1735 shift:(120,-2) textcolor:red fontsize:S text:0.00788
 bar:test at:1735 mark:(line,red)
 at:1655 shift:(10,-5) text: 1655 (T26)
 at:1655 shift:(120,-5) textcolor:red fontsize:S text:0.000576
 bar:test at:1655 mark:(line,red)
 at:1626 shift:(10,-5) text: 1626 (T25)
 at:1626 shift:(120,-5) textcolor:red fontsize:S text:0.004
 bar:test at:1625 mark:(line,red)
 at:1559 shift:(10,-10) text: 1559 (T24, Tf14)
 at:1559 shift:(120,-10) textcolor:red fontsize:S text:0.011
 bar:test at:1559 mark:(line,red)
 at:1540 shift:(10,-10) text: 1540 (T23, Tf13)
 at:1540 shift:(120,-10) textcolor:red fontsize:S text:0.000985
 bar:test at:1540 mark:(line,red)
 at:1526 shift:(10,-7) fontsize:S text: 1526 (T22, Tf12)
 at:1526 shift:(120,-7) textcolor:red fontsize:S text:0.00288
 bar:test at:1526 mark:(line,red)
 at:1514 shift:(10,-4) fontsize:S  text: 1514 (T21, Tf11) 
 at:1514 shift:(120,-4) textcolor:red fontsize:S text:0.00301
 bar:test at:1514 mark:(line,red)
 at:1493 shift:(10,-5) fontsize:S  text: 1493 (T20, Tf10)
 at:1493 shift:(120,-5) textcolor:red fontsize:S text:0.0133
 bar:test at:1493 mark:(line,red)
 at:1464 shift:(10,-8) fontsize:S text: 1464 (T19, Tf9)
 at:1464 shift:(120,-8) textcolor:red fontsize:S text:0.00591
 bar:test at:1464 mark:(line,red)
 at:1443 shift:(10,-8) fontsize:S text: 1443 (T18)
 at:1443 shift:(120,-8) textcolor:red fontsize:S text:0.000313
 bar:test at:1443 mark:(line,red)
 at:1431 shift:(10,-5) fontsize:S  text: 1431 (T17, Tf8)
 at:1431 shift:(120,-5) textcolor:red fontsize:S text:0.018
 bar:test at:1431 mark:(line,red)
 at:1420 shift:(10,-2) fontsize:S  text: 1420 (T16, Tf7)
 at:1420 shift:(120,-2) textcolor:red fontsize:S text:0.00218
 bar:test at:1420 mark:(line,red)
 at:1418 shift:(10,5) fontsize:S text: 1418 (T15)
 at:1418 shift:(120,5) textcolor:red fontsize:S text:0.0141
 bar:test at:1418 mark:(line,red)  
 at:1393 shift:(10,4) text: 1393 (T14)
 at:1393 shift:(120,4) textcolor:red fontsize:S text:0.000855
 bar:test at:1393 mark:(line,red)  
 at:1346 shift:(10,-5) text: 1346 (T13, Tf5)
 at:1346 shift:(120,-5) textcolor:red fontsize:S text:0.0507  
 bar:test at:1346 mark:(line,red)  
 at:1319 shift:(10,-5) text: 1319 (T12)
 at:1319 shift:(120,-5) textcolor:red fontsize:S text:0.000223
 bar:test at:1319 mark:(line,red) 
 at:1196 shift:(10,-5) text: 1196 (T11, Tf4)
 at:1196 shift:(120,-5) textcolor:red fontsize:S text:0.0181
 bar:test at:1196 mark:(line,red)
 at:1158 shift:(10,-5) text: 1158 (T10)
 at:1158 shift:(120,2) textcolor:red fontsize:S text:0.00194
 bar:test at:1158 mark:(line,red)
 at:1064 shift:(10,-5) text: 1064 (T9)
 at:1064 shift:(120,-5) textcolor:red fontsize:S text:0.00019
 bar:test at:1064 mark:(line,red) 
 at:1005 shift:(10,-5) text: 1005 (T8, Tf3)
 at:1005 shift:(120,-5) textcolor:red fontsize:S text:0.00143
 bar:test at:1005 mark:(line,red)
 at:613 shift:(10,-5) text: 613 (T7) 
 at:613 shift:(120,-5) textcolor:red fontsize:S text:0.00358
 bar:test at:613 mark:(line,red)
 at:588 shift:(10,-5) text: 588 (T6)
 at:588 shift:(120,-5) textcolor:red fontsize:S text:0.00145
 bar:test at:588 mark:(line,red)  
 at:534 shift:(10,-5) text: 534 (T5, Tf2)
 at:534 shift:(120,-5) textcolor:red fontsize:S text:0.00251
 bar:test at:534 mark:(line,red)  
 at:456 shift:(10,-5) text: 456 (T4)
 at:456 shift:(120,-5) textcolor:red fontsize:S text: 0.00379
 bar:test at:456 mark:(line,red)
 at:379 shift:(10,-10) text: 379 (T3)
 at:379 shift:(120,-10) textcolor:red fontsize:S text:0.000172
 bar:test at:379 mark:(line,red)
 at:370 shift:(10,-4) text: 370 (T2, Tf1)
 at:370 shift:(120,-4) textcolor:red fontsize:S text:0.00932
 bar:test at:370 mark:(line,red)
 at:366 shift:(10,5) text: 366 (T1)
 at:366 shift:(120,5) textcolor:red fontsize:S text:0.000215
 bar:test at:366 mark:(line,red) 
 at:1230 shift:(10,-5) textcolor:black text: Māori in NZ 
 bar:test at:1200 mark:(line,black) 
 at:1860 shift:(10,-5) textcolor:black text: European colonisation
 bar:test at:1840 mark:(line,black)

LineData = 

 at:366 frompos:310 tillpos:320 color:red width:2
 at:370 frompos:310 tillpos:320 color:red width:2
 at:379 frompos:310 tillpos:320 color:red width:2
 at:456 frompos:290 tillpos:320 color:red width:2
 at:534 frompos:310 tillpos:320 color:red width:2
 at:588 frompos:310 tillpos:320 color:red width:2
 at:613 frompos:310 tillpos:320 color:red width:2
 at:1005 frompos:310 tillpos:320 color:red width:2
 at:1064 frompos:310 tillpos:320 color:red width:2
 at:1158 frompos:310 tillpos:320 color:red width:2
 at:1196 frompos:290 tillpos:320 color:red width:2
 at:1319 frompos:310 tillpos:320 color:red width:2
 at:1346 frompos:260 tillpos:320 color:red width:2
 at:1393 frompos:310 tillpos:320 color:red width:2
 at:1418 frompos:270 tillpos:320 color:red width:2
 at:1420 frompos:310 tillpos:320 color:red width:2
 at:1431 frompos:260 tillpos:320 color:red width:2
 at:1443 frompos:310 tillpos:320 color:red width:2
 at:1464 frompos:270 tillpos:320 color:red width:2
 at:1493 frompos:260 tillpos:320 color:red width:2
 at:1514 frompos:300 tillpos:320 color:red width:2
 at:1526 frompos:300 tillpos:320 color:red width:2
 at:1540 frompos:310 tillpos:320 color:red width:2
 at:1559 frompos:290 tillpos:320 color:red width:2
 at:1626 frompos:300 tillpos:320 color:red width:2
 at:1655 frompos:310 tillpos:320 color:red width:2
 at:1735 frompos:300 tillpos:320 color:red width:2
 at:1747 frompos:300 tillpos:320 color:red width:2
 at:1788 frompos:290 tillpos:320 color:red width:2
 at:1835 frompos:300 tillpos:320 color:red width:2
 at:1945 frompos:290 tillpos:320 color:red width:2
 at:1995 frompos:300 tillpos:320 color:red width:2
</timeline>

Medium size tephra eruptions of Ruapehu since the 232 CE
Taupo eruption[34][35][36][37]

Lava flows that have been erupted from Ruapehu since the last glacial maximum are called the Whakapapa Formation. These flows all erupted between 15,000 and 2,000 years ago from a number of different craters on the summit of Ruapehu as well as from craters on the northern and southern flanks of the mountain.[5][26]

Approximately 10,000 years ago, a series of major eruptions occurred, not just on Ruapehu, but also at the Tama Lakes between Ruapehu and Tongariro volcanoes. This period of intense eruptions is called the Pahoka-Mangamate event and is thought to have lasted between 200 and 400 years.[38] On Ruapehu, lava was erupted from Saddle Cone—a flank crater on the northern slopes—and from another crater on the southern slopes. This southern crater erupted three times, and lava flows from this crater travelled nearly 14 km to the south.[5][26]

There is evidence that a sector collapse on the northwestern slopes about 9,400 years ago formed the amphitheatre that now comprises the Whakapapa skifield and left an extensive avalanche deposit on the northwestern ring plain that can still be seen today.[26] Since then eruptions have been an order of magnitude lower in intensity and volume.[39] Accordingly, most of the 150 km3 (36 cu mi) cone and 150 km3 (36 cu mi) ring-plain is older than 10,000 years.[32] Eruptions between 10,000 and 2,500 years ago generated lava flows that all flowed into the Whakapapa amphitheatre and created the slopes of the modern skifield.[26]

For the past 2,000 years, activity at Ruapehu has been largely focused through a crater lake at the summit.[27] Eruptive activity has typically consisted of relatively small but explosive phreatomagmatic eruptions occurring every few decades and lasting several months each.[27][26] The eruptive record is only well understood from tephra deposits before 1950 for 1718 years from the Taupō Hatepe eruption in 232 CE. Over this period there are 30 assigned tephra units by composition studies to Ruapehu and in the 370 years before 1950 the mean time between these months of eruptive period was 40 years.[34][40]

In recorded history, these eruptions have occurred about 50 years apart, in 1895 (lahar),[41] 1945 and 1995–1996.[4] Minor phreatic or hydrothermal eruptions occur every few years on average, with notable minor eruptions occurring in 1969, 1975, and 2007.[30][42] More than 600 eruptive events of various sizes have been documented since 1830.[43]

1945 eruptions and 1953 lahar

Ruapehu entered an eruptive phase in March 1945 after several weeks of volcanic tremors. The first indication of an eruption was reported on 8 March, with ashfall seen on the eastern slopes.[44] A lava dome was observed in Crater Lake on 19 March but was destroyed in a series of explosive eruptions over the following week. A second, larger lava dome appeared in May, which continued to grow over the following months and had emptied Crater Lake of water by July.[44]

Eruptions increased from August through November. A particularly powerful eruption in the early hours of 21 August was heard in Hawkes Bay and the Tararua District, loud enough to awaken people from sleep and cause alarm.[44] Eruptions began declining in December and had ended by January.

The eruptions dispersed ash across most of the North Island, and eruption columns could be seen from as far afield as Palmerston North, Whanganui, and Hawkes Bay. Ash caused disruption to several North Island communities, entering houses, causing eye and throat irritation, and damaging paintwork on cars. Crop damage was reported in Ohakune, and the water supply at Taumarunui was disrupted.[44][45]

After eruptions subsided in late December, Crater Lake slowly began refilling, with a "boiling lake" already filling the bottom of the crater by mid-January.[44] A tephra dam had formed at the lake's normal outlet during the eruptions, which eventually collapsed on 24 December 1953 causing a lahar that led to the Tangiwai disaster with the loss of 151 lives when the Tangiwai railway bridge across the Whangaehu River collapsed while the lahar was in full flood, just before an express train crossed it.

1969 and 1975 eruptions

Ruapehu saw a period of heightened activity between 1966 and 1982, with multiple small eruptions occurring in Crater Lake and two larger eruptions in 1969 and 1975, which ejected rocks across the summit region and produced significant lahars.[43]

The eruption in 1969 occurred in the early hours of 22 June. It was a moderate phreatic eruption, which blasted rocks up to 1 km northwest of the crater and sent lahars down several valleys. The Whakapapa skifield was left covered in mud. This was the largest eruption since 1945.[46]

A larger phreatic eruption occurred at 3:59 a.m. on 24 April 1975, blasting rocks up to 1.6 km northwest of the crater, against the wind, and depositing ash more than 100 km to the southeast. Nine minutes of seismic activity preceded the eruption, but crater dilation had been measured two weeks earlier. Nearly half of the water in Crater Lake was erupted into the air, which subsequently rained down onto the summit, generating lahars down several river valleys. Lahars which travelled down the Whakapapa and Manganui o te Ao rivers entered the Whanganui River and poisoned it, which affected much of the aquatic life downstream.[42][47] Additionally, the lahars damaged ski installations on the Whakapapa ski field, several bridges and hydroelectric tunnel intakes, but no loss of life occurred.[42][48]

Three days later, on the morning of 27 April, Ruapehu erupted again. A series of five eruptions occurred between 7:10 a.m. and 10:18 a.m., sending surges of mud, rocks, and ash northwards across the summit plateau and producing eruption columns up to 500 m high.[42]

The 1975 eruptions deepened Crater Lake from 55 to 60 m to more than 90 m.[42]

1995–1996 eruptions

Earthquake swarms to the west of Ruapehu between November 1994 and September 1995 marked the beginning of renewed heightened activity at the volcano. Bursts of earthquake activity immediately preceded rapid rises in the temperature of Crater Lake, with the surface temperature reaching 51.4 °C in January 1995—one of the highest temperatures recorded in 30 years and about 10 °C higher than its usual peak temperature.[49][50] A minor eruption occurred on 26 April, which sent waves against the walls of the crater and damaged some monitoring equipment there. A second eruption on 29 June destroyed the equipment and produced a lahar. Chemical analysis showed that magma was interacting with water under the lake.[43][49]

The first significant eruption took place at 8:05 a.m. on 18 September 1995, raining tephra onto the summit region and sending lahars down the mountain. On 23 September, an even larger eruption blasted rocks up to 1.5 km from the crater, sent lahars down three valleys, and generated an eruption column 12 km high.[50] Phreatomagmatic eruptions occurred through the rest of the month and throughout October, with some eruptions continuing for hours at a time. Ash fell up to 250 km downwind. Explosive eruptions on 11 October emptied Crater Lake of water.[43][36]

Crater Lake and Tahurangi, the highest peak (top right) in 2016. The 1996 tephra dam is the bluish dark area at lake edge directly below Tahurangi.

Following this, activity died off until 15 June 1996 when renewed seismic activity was recorded. This was followed by eruptions on 17 and 18 June which once again emptied the partially refilled Crater Lake of water. Strombolian eruptions occurred on 27 June and throughout July and August, producing eruption columns more than 10 km high and shooting rocks 1.4 km from the crater.[43][36]

These eruptions produced more than 7 million tonnes of ash, which contaminated water supplies, destroyed crops, and lead to the deaths of livestock.[51] Ash in the Tongariro River also damaged the intake turbines at the Rangipo power station,[52] and ash clouds caused airport closures as far away as Auckland and Wellington.[53] The eruptions also caused closures to the three ski fields on the mountain, costing the region an estimated $100 million in lost revenue.[53]

After the 1996 eruption it was recognised that a catastrophic lahar could again occur when Crater Lake burst the volcanic ash dam blocking the lake outlet as it did in 1953. In 2000, the Eastern Ruapehu Lahar Alarm and Warning System (ERLAWS) system was installed on the mountain to detect such a collapse and alert the relevant authorities. The lake gradually filled with snowmelt and had reached the level of the hard rock rim by January 2005. The lahar finally occurred on 18 March 2007 (see below).

2006 and 2007 activity

Ruapehu erupted at 10:24 p.m. on 4 October 2006. The small eruption was marked by a magnitude 2.9 volcanic earthquake and sent waves 4–5 m (16 ft) tall crashing into the wall of the crater. No ash was erupted into the atmosphere, and the eruption is presumed to have occurred entirely underwater.[54]

Fresh lahar channels scar Ruapehu's eastern slopes, 2007.

At 11:22 a.m. 18 March 2007, the tephra dam which had been holding back Crater Lake burst, sending a lahar down the mountain. An estimated 1.9–3.8 million cubic metres of mud, rock, and water travelled down the Whangaehu river.[31] ERLAWS activated, sending an alarm to pagers at 11:25 a.m. and automatically activating warning lights and barrier arms to close roads and stop trains. There was no serious damage and no injuries. A toilet block at the Tangiwai memorial was destroyed, but the memorial had already been closed due to the lahar threat.[31] One family was trapped for around 24 hours after the lahar swept away the access route to their home.[55]

At 8:16 p.m. on 25 September 2007, volcanic tremor was detected underneath Ruapehu, which was followed at 8:26 p.m. by an explosive surtseyan eruption.[30] The explosive phase of the eruption lasted for less than a minute and blasted ash, mud, and rocks northward, reaching to about 2 km from Crater Lake.[30][56] Two climbers were caught in the eruption at Dome Shelter, an alpine hut approximately 600 m from the crater, when the hut was struck by the surge.[30] The climbers nearly drowned before the hut floor gave way and the water drained into the basement seismometer vault. One of them, a 22-year-old primary school teacher, had a leg pinned and crushed by a boulder as the water subsided. A rescue operation was mounted after his companion, who was unable to free him, went down the mountain for help.[30][57]

The eruption initiated lahars down the Whangaehu valley and the Whakapapa skifield.[58] ERLAWS detected the lahars in the Whangaehu valley.[31][59] A snow groomer on the Whakapapa skifield narrowly avoided being caught in the lahar there.[30]

Current activity and future hazards

Only one eruptive event has been recorded at Ruapehu since the 2007 eruption—a minor event on 13 July 2009 when a small volcanic earthquake beneath Crater Lake caused the lake water level to rise 15 cm and triggered a snow slurry lahar in the upper Whangaehu valley.[43][60] Since then, Crater Lake has continued its regular cycle of heating and increased gas emissions, although with periods of sustained high temperatures that occurred in 2011, 2016 and 2019.[60][61][62]

Eruptions at Ruapehu are expected to continue much as they have for the past 2,000 years, with frequent minor eruptions and more significant events every 20–30 years, although the possibility of larger events like the Pahoka-Mangamate event cannot be ruled out.[27] The previous activity trend until 10,000 years ago was about 7.5 km3 (1.8 cu mi) erupted each 10,000 years.[32] Minor eruptions, such as the one in 2007, especially if they are hydrothermal, can occur at any time without warning. However, in historic times, major eruptions such as the ones in 1995–96 have only occurred within periods of enhanced activity.[43][32]

The main recent volcanic hazard at Ruapehu is from lahars. Two major lahar paths run through the Whakapapa skifield, and in recent times, lahars have travelled through the ski field in 1969, 1975, 1995, and 2007.[30][10] An eruption warning system operates in the ski field to warn skiers in the event of another eruption.[63] Lahars also represent a significant hazard to surrounding river valleys, particularly the Whangaehu River, which is crossed by national highways, the North Island Main Trunk railway line, and electricity transmission lines.[10] Large, destructive lahars have been observed in the Whangaehu River in 1862, 1895, 1953, 1975, and 2007.[10][9]

GNS Science continuously monitors Ruapehu using a network of seismographs, GPS stations, microphones and webcams. Chemical analysis of the water in Crater Lake is regularly undertaken along with airborne gas measurements.[64] Live data can be viewed on the GeoNet website.

Ski fields

Turoa ski field.

Ruapehu has two commercial ski fields, Whakapapa on the northern side and Turoa on the southern slope. They are the two largest ski fields in New Zealand, with Whakapapa the larger. The club Tukino field is on the east of the mountain and is open to the public. The season is generally from June to October but depends on snow and weather conditions.

Both ski fields are accessible by car and chairlifts, with beginners' to advanced skiing slopes. Whakapapa has five chair lifts with limited accommodation and refreshments available at Top o' the Bruce (the car park at the top of Bruce Road) and at the entry to Whakapapa, and elsewhere on the mountain. Alpine huts are provided for trampers and climbers. These are mainly owned by private clubs.

In popular culture

Some scenes of the fictional Mordor and Mount Doom in Peter Jackson's The Lord of the Rings film trilogy were filmed on the slopes of Mount Ruapehu.[65]

See also

  • List of mountains of New Zealand by height
  • List of volcanic eruptions by death toll
  • List of volcanoes in New Zealand
  • Volcanism of New Zealand

References

  1. ↑ 1.0 1.1 1.2 "Ruapehu". Smithsonian Institution. https://volcano.si.edu/volcano.cfm?vn=241100. 
  2. ↑ "Topographic map of Mount Ruapehu". https://opentopomap.org/#marker=14/-39.28/175.57. 
  3. ↑ "Volcano Fact Sheet: Ruapehu Volcano". GNS Science. http://www.gns.cri.nz/content/download/6186/33930/file/VolcanoFactSheets%20Ruapehu.pdf. 
  4. ↑ 4.0 4.1 "Ruapehu". https://www.gns.cri.nz/Home/Learning/Science-Topics/Volcanoes/New-Zealand-Volcanoes/Ruapehu. 
  5. ↑ 5.0 5.1 5.2 5.3 5.4 5.5 5.6 5.7 5.8 5.9 Hackett, W. R. (1985). Geology and Petrology of Ruapehu Volcano and Related Vents (Ph.D.). Victoria University of Wellington.
  6. ↑ "Ruapehu / New Zealand Volcanoes / Volcanoes / Science Topics / Learning / Home - GNS Science". https://www.gns.cri.nz/Home/Learning/Science-Topics/Volcanoes/New-Zealand-Volcanoes/Ruapehu. 
  7. ↑ "How to get to Tukino - Tukino Skifield - Mt Ruapehu, NZ" (in en-NZ). https://www.tukino.org/how-to-get-to-tukino-ski-field. 
  8. ↑ "Getting there" (in en-nz). https://www.doc.govt.nz/parks-and-recreation/places-to-go/central-north-island/places/tongariro-national-park/things-to-do/tracks/round-the-mountain-track/getting-there/. 
  9. ↑ 9.0 9.1 Purves, A. M. (1990). Landscape Ecology of the Rangipo Desert (Ph.D.). Massey University.
  10. ↑ 10.0 10.1 10.2 10.3 Keys, Harry J.R. (2007). "Lahars of Ruapehu Volcano, New Zealand: risk mitigation". Annals of Glaciology 45 (1): 155–162. doi:10.3189/172756407782282390. Bibcode: 2007AnGla..45..155K. 
  11. ↑ 11.0 11.1 Chinn, T. J. (2001). "Distribution of the Glacial Water Resources of New Zealand". Journal of Hydrology (New Zealand) 40 (2): 139–187. https://www.jstor.org/stable/43922047. Retrieved 2 February 2021. 
  12. ↑ 12.0 12.1 12.2 12.3 Keys, H. (1988). "1988 Survery of the Glaciers on Mt Ruapehu, Tongariro National Park - A Baseline for Detecting Threats of Climate Change". Department of Conservation Science and Research Internal Report 24 (Unpublished). https://www.doc.govt.nz/globalassets/documents/science-and-technical/srir24.pdf. Retrieved 2 February 2021. 
  13. ↑ Miles, Sue (1984). The River : the story of the Waikato. Auckland, N.Z.: Heinemann. ISBN 978-0-86863-418-0. 
  14. ↑ Land Information New Zealand (2020). NZ Topo50 (Topographic map). 1:50,000. Land Information New Zealand.
  15. ↑ Odell, N. E. (1955). "Mount Ruapehu, New Zealand: Observations on its Crater Lake and Glaciers". Journal of Glaciology 2 (18): 601–605. doi:10.3189/002214355793702181. Bibcode: 1955JGlac...2..601O. 
  16. ↑ 16.0 16.1 Beck, Hylke E.; Zimmermann, Niklaus E.; McVicar, Tim R.; Vergopolan, Noemi; Berg, Alexis; Wood, Eric F. (18 December 2018). "Present and future Köppen-Geiger climate classification maps at 1-km resolution". Scientific Data 5 (1): 180214. doi:10.1038/sdata.2018.214. PMID 30375988. Bibcode: 2018NatSD...580214B. 
  17. ↑ 17.0 17.1 Thompson, C. S. (1984). "The weather and climate of the Tongariro region". New Zealand Meteorological Service Miscellaneous Publication 115(14). 
  18. ↑ 18.0 18.1 "Tongariro weather" (in en-nz). https://www.doc.govt.nz/parks-and-recreation/places-to-go/central-north-island/places/tongariro-national-park/about-tongariro-national-park/tongariro-weather/. 
  19. ↑ "Climate-data.org – Climate Data for Cities Worldwide". openstreetmap.org. https://en.climate-data.org/oceania/new-zealand/manawatu-wanganui/iwikau-60511/. 
  20. ↑ "Round the Mountain Track" (in en-nz). https://www.doc.govt.nz/parks-and-recreation/places-to-go/central-north-island/places/tongariro-national-park/things-to-do/tracks/round-the-mountain-track/#Weather. 
  21. ↑ "Special Honours List 1999". New Zealand Government. 23 October 1999. http://www.dpmc.govt.nz/honours/lists/list.asp?id=18. 
  22. ↑ "Japanese survives five days in blizzard". United Press International. 16 August 1990. https://www.upi.com/Archives/1990/08/16/Japanese-survives-five-days-in-blizzard/9501057097620/. 
  23. ↑ Charman, Paul (6 June 2014). "Outdoors: Preparing the snow". The New Zealand Herald. http://www.nzherald.co.nz/sport/news/article.cfm?c_id=4&objectid=11268723. 
  24. ↑ "Northland cops it as storm sweeps island". Fairfax New Zealand. 26 July 2008. http://www.stuff.co.nz/4631448a11.html. 
  25. ↑ "July 2008 North Island Weather Bomb ( 2008-07-26 )". https://hwe.niwa.co.nz/event/July_2008_North_Island_Weather_Bomb. 
  26. ↑ 26.0 26.1 26.2 26.3 26.4 26.5 26.6 26.7 Price, R. C.; Gamble, J. A.; Smith, I. E. M.; Maas, R.; Waight, T.; Stewart, R. B.; Woodhead, J. (October 2012). "The Anatomy of an Andesite Volcano: a Time–Stratigraphic Study of Andesite Petrogenesis and Crustal Evolution at Ruapehu Volcano, New Zealand". Journal of Petrology 53 (10): 2139–2189. doi:10.1093/petrology/egs050. Bibcode: 2012JPet...53.2139P. 
  27. ↑ 27.00 27.01 27.02 27.03 27.04 27.05 27.06 27.07 27.08 27.09 27.10 Gamble, John A.; Price, Richard C.; Smith, Ian E.M.; McIntosh, William C.; Dunbar, Nelia W. (February 2003). "40Ar/39Ar geochronology of magmatic activity, magma flux and hazards at Ruapehu volcano, Taupo Volcanic Zone, New Zealand". Journal of Volcanology and Geothermal Research 120 (3–4): 271–287. doi:10.1016/S0377-0273(02)00407-9. Bibcode: 2003JVGR..120..271G. 
  28. ↑ "GeoNet Volcanic Alert Bulletin RUA – 2020/08" (in en). https://www.geonet.org.nz/vabs/4cVdxClElNOctJS9LaQXty. 
  29. ↑ 29.0 29.1 Werner, C.; Christenson, B.W.; Hagerty, M.; Britten, K. (June 2006). "Variability of volcanic gas emissions during a crater lake heating cycle at Ruapehu Volcano, New Zealand". Journal of Volcanology and Geothermal Research 154 (3–4): 291–302. doi:10.1016/j.jvolgeores.2006.03.017. Bibcode: 2006JVGR..154..291W. 
  30. ↑ 30.0 30.1 30.2 30.3 30.4 30.5 30.6 30.7 30.8 Kilgour, G.; V. Manville; Pasqua, F. Della; A. Graettinger; Hodgson, K.A.; Jolly, G.E. (March 2010). "The 25 September 2007 eruption of Mount Ruapehu, New Zealand: Directed ballistics, surtseyan jets, and ice-slurry lahars". Journal of Volcanology and Geothermal Research 191 (1–2): 1–14. doi:10.1016/j.jvolgeores.2009.10.015. Bibcode: 2010JVGR..191....1K. 
  31. ↑ 31.0 31.1 31.2 31.3 Keys, H.; Green, P. (August 2008). "Ruapehu Lahar New Zealand 18 March 2007: Lessons for Hazard Assessment and Risk Mitigation 1995-2007". Journal of Disaster Research 3 (4): 284–296. doi:10.20965/jdr.2008.p0284. 
  32. ↑ 32.0 32.1 32.2 32.3 Leonard, Graham S.; Cole, Rosie P.; Christenson, Bruce W.; Conway, Chris E.; Cronin, Shane J.; Gamble, John A.; Hurst, Tony; Kennedy, Ben M. et al. (2021-05-02). "Ruapehu and Tongariro stratovolcanoes: a review of current understanding" (in en). New Zealand Journal of Geology and Geophysics 64 (2–3): 389–420. doi:10.1080/00288306.2021.1909080. https://www.tandfonline.com/doi/full/10.1080/00288306.2021.1909080. Retrieved 5 June 2022. 
  33. ↑ 33.0 33.1 Waight, T. E.; Price, R. C.; Stewart, R. B.; Smith, I. E. M.; Gamble, J. (December 1999). "Stratigraphy and geochemistry of the Turoa area, with implications for andesite petrogenesis at Mt Ruapehu, Taupo Volcanic Zone, New Zealand". New Zealand Journal of Geology and Geophysics 42 (4): 513–532. doi:10.1080/00288306.1999.9514858. 
  34. ↑ 34.0 34.1 Voloschina, Marija (2000). Eruption dynamics and frequency-magnitude relationships of explosive eruptions at Mt. Ruapehu, New Zealand over the past 1800 years : a thesis presented in partial fulfilment of the requirements for the degree of Doctor of Philosophy in Earth Science at Massey University, Palmerston North, New Zealand (Thesis). Retrieved 2023-04-16.
  35. ↑ Bonadonna, C.; Houghton, B.F. (2005). "Total grain-size distribution and volume of tephra-fall deposits". Bulletin of Volcanology 67: 441–456. doi:10.1007/s00445-004-0386-2. 
  36. ↑ 36.0 36.1 36.2 Nakagawa, M.; Wada, K.; Thordarson, T.; Wood, C. P.; Gamble, J. A. (11 July 1999). "Petrologic investigations of the 1995 and 1996 eruptions of Ruapehu volcano, New Zealand: formation of discrete and small magma pockets and their intermittent discharge". Bulletin of Volcanology 61 (1–2): 15–31. doi:10.1007/s004450050259. Bibcode: 1999BVol...61...15N. 
  37. ↑ C, S. L.; Neall, V. E.; Palmer, A. S.; Stewart, R. B. (1997). "The volcanic history of Ruapehu during the past 2 millenia based on the record of Tufa Trig tephras". Bulletin of Volcanology 59: 136-146. doi:10.1007/s004450050181. 
  38. ↑ Nairn, Ian A; Kobayashi, Tetsuo; Nakagawa, Mitsuhiro (November 1998). "The ~10 ka multiple vent pyroclastic eruption sequence at Tongariro Volcanic Centre, Taupo Volcanic Zone, New Zealand". Journal of Volcanology and Geothermal Research 86 (1–4): 19–44. doi:10.1016/S0377-0273(98)00085-7. 
  39. ↑ Pardo, Natalia; Cronin, Shane J.; Palmer, Alan S.; Németh, Karoly (2011-10-27). "Reconstructing the largest explosive eruptions of Mt. Ruapehu, New Zealand: lithostratigraphic tools to understand subplinian–plinian eruptions at andesitic volcanoes". Bulletin of Volcanology 74 (3): 617–640. doi:10.1007/s00445-011-0555-z. 
  40. ↑ Voloschina, Marija; Lube, Gert; Procter, Jonathan; Moebis, Anja; Timm, Christian (2020). "Lithosedimentological and tephrostratigraphical characterisation of small-volume, low-intensity eruptions: The 1800 years Tufa Trig Formation, Mt. Ruapehu (New Zealand)". Journal of Volcanology and Geothermal Research 402. doi:10.1016/j.jvolgeores.2020.106987. ISSN 0377-0273. https://www.sciencedirect.com/science/article/pii/S0377027320301475. 
  41. ↑ Blot, Claude (1979). "Deep earthquakes that were precursors of the eruption of Ruapehu, New Zealand on 22 June 1969". New Zealand Journal of Geology and Geophysics 22 (3): 413-414. doi:10.1080/00288306.1979.10424110. 
  42. ↑ 42.0 42.1 42.2 42.3 42.4 Nairn, I. A.; Wood, C. P.; Hewson, C. A. Y. (March 1979). "Phreatic eruptions of Ruapehu: April 1975". New Zealand Journal of Geology and Geophysics 22 (2): 155–170. doi:10.1080/00288306.1979.10424215. 
  43. ↑ 43.0 43.1 43.2 43.3 43.4 43.5 43.6 Scott, B. J. (2013). A revised catalogue of Ruapehu volcano eruptive activity: 1830-2012. GNS Science report (2013/45). 
  44. ↑ 44.0 44.1 44.2 44.3 44.4 Johnston, D. M. (1997). A Chronology of the 1945 eruption of Ruapehu volcano, New Zealand. Institute of Geological and Nuclear Sciences science report (97/2). 
  45. ↑ "Ruapehu 1861 - 1945". https://teara.govt.nz/en/historic-volcanic-activity/page-4. 
  46. ↑ Healy, J.; Lloyd, E. F.; Rishworth, D. E. H.; Wood, C. P.; Glover, R. B.; Dibble, R. R. (1978). "The eruption of Ruapehu New Zealand on 22 June 1969". DSIR Bulletin 224: 79. 
  47. ↑ Paterson, B. R.; Page, C. E.; Cudby, E. J. (1976). "The effects of lahars from the 1975 April Mt. Ruapehu eruption and the threat of future eruptions on Tongariro power development". New Zealand Geological Survey, Engineering Geology Section. 
  48. ↑ Montgomery, R.; Keys, H. (1993). Volcanic hazard management in Tongariro National Park. Department of Conservation. ISBN 0-478-01523-2. 
  49. ↑ 49.0 49.1 Hurst, A.W; McGinty, P.J (May 1999). "Earthquake swarms to the west of Mt Ruapehu preceding its 1995 eruption". Journal of Volcanology and Geothermal Research 90 (1–2): 19–28. doi:10.1016/S0377-0273(99)00019-0. Bibcode: 1999JVGR...90...19H. 
  50. ↑ 50.0 50.1 "Changes made since Ruapehu's eruptions / Media Releases and News / News and Events / Home - GNS Science". https://www.gns.cri.nz/Home/News-and-Events/Media-Releases-and-News/Changes-made-since-Ruapehu-s-eruptions. 
  51. ↑ "Remembering Ruapehu - ten years on" (in en-NZ). The New Zealand Herald. https://www.nzherald.co.nz/technology/remembering-ruapehu-ten-years-on/EZ7CRNK6SX344A5TNABCMPTW7A/. 
  52. ↑ "Mount Ruapehu erupts". https://www.waikatoregion.govt.nz/Services/Regional-services/Regional-hazards-and-emergency-management/Volcanic-activity/Mount-Ruapehu-erupts/. 
  53. ↑ 53.0 53.1 Taonga, New Zealand Ministry for Culture and Heritage Te Manatu. "Ruapehu since 1945" (in en). https://teara.govt.nz/en/historic-volcanic-activity/page-6. 
  54. ↑ Mordret, A.; Jolly, A.D.; Duputel, Z.; Fournier, N. (March 2010). "Monitoring of phreatic eruptions using Interferometry on Retrieved Cross-Correlation Function from Ambient Seismic Noise: Results from Mt. Ruapehu, New Zealand". Journal of Volcanology and Geothermal Research 191 (1–2): 46–59. doi:10.1016/j.jvolgeores.2010.01.010. Bibcode: 2010JVGR..191...46M. 
  55. ↑ "Photos: Lahar could have been much worse". The New Zealand Herald. NZPA. 18 March 2007. http://www.nzherald.co.nz/section/story.cfm?c_id=1&objectid=10429432. 
  56. ↑ Jolly, A.D.; Sherburn, S.; Jousset, P.; Kilgour, G. (March 2010). "Eruption source processes derived from seismic and acoustic observations of the 25 September 2007 Ruapehu eruption—North Island, New Zealand". Journal of Volcanology and Geothermal Research 191 (1–2): 33–45. doi:10.1016/j.jvolgeores.2010.01.009. Bibcode: 2010JVGR..191...33J. 
  57. ↑ Mussen, D (22 January 2016). "Mt Ruapehu eruption survivor William Pike inspires a generation of Kiwi 'Pike-lets'". https://www.stuff.co.nz/national/education/76103430/mt-ruapehu-eruption-survivor-william-pike-inspires-a-generation-of-kiwi-pike-lets. 
  58. ↑ "GeoNet Volcanic Alert Bulletin RUA-2007/03" (in en). https://www.geonet.org.nz/vabs/2KAPkCsfpm2ka6Sc4E0u62. 
  59. ↑ "GeoNet Volcanic Alert Bulletin RUA-2007/02" (in en). https://www.geonet.org.nz/vabs/6A6Ty6YEvYMEMugma6ikYW. 
  60. ↑ 60.0 60.1 Wunderman, R. (2011). "Report on Ruapehu (New Zealand)". Bulletin of the Global Volcanism Network 36 (7). doi:10.5479/si.GVP.BGVN201107-241100. 
  61. ↑ "Scientists monitoring Ruapehu as crater lake heats up" (in en-NZ). The New Zealand Herald. 10 April 2019. https://www.nzherald.co.nz/nz/news/article.cfm?c_id=1&objectid=12221130. 
  62. ↑ Agnes Mazot (10 April 2019). "Te Wai ā-moe, Mt Ruapehu: Increases in lake temperature and seismic activity". https://www.geonet.org.nz/vabs/4kjCTeqLSLY8mwsONDFDlq. 
  63. ↑ "Volcanic risk in Tongariro National Park" (in en-nz). https://www.doc.govt.nz/volcanicrisk. 
  64. ↑ "Monitoring volcanic unrest / Ruapehu / New Zealand Volcanoes / Volcanoes / Science Topics / Learning / Home - GNS Science". https://www.gns.cri.nz/Home/Learning/Science-Topics/Volcanoes/New-Zealand-Volcanoes/Ruapehu/Monitoring-volcanic-unrest. 
  65. ↑ Sibley, Brian (2002). The Making of the Movie Trilogy The Lord of the Rings. Houghton Mifflin. 

External links



Retrieved from "https://handwiki.org/wiki/index.php?title=Earth:Mount_Ruapehu&oldid=3295600"