Misti

Misti
Misti as viewed from Arequipa
Highest point
Elevation	5,822 m (19,101 ft)
Listing	Ultra
Coordinates	16°17′40″S 71°24′32″W
Geography
Misti Peru
Country	Peru
Region	Arequipa
Parent range	Andes
Geology
Mountain type	Stratovolcano
Volcanic arc/belt	Central Volcanic Zone

Misti is a dormant volcano in the Arequipa Department of southern Peru, approximately 17 kilometres (11 mi) northeast of the city of Arequipa, and one of the most dangerous volcanoes in the world. Part of the Central Volcanic Zone of the Andes, it rises 5,822 metres (19,101 ft) above sea level. The volcano's summit features two nested craters, an outer 835–950-metre (2,740–3,117 ft) wide crater and an inner 550-metre (1,800 ft) wide crater. The inner crater contains a volcanic plug or lava dome with active fumaroles. Below the summit, Misti has the shape of a mostly regular cone. The volcano formed during the Pleistocene in four different phases; intense explosive eruptions that produced mudflows, pyroclastic flows and tephra fallout took place.

The last securely dated eruption occurred during the Inka times between 1440 and 1470 AD; the impact of this eruption was so severe that the Inka carried out human sacrifices on the mountain. Reports of subsequent eruptions probably reflect increased fumarolic activity. Future eruptions could threaten the city of Arequipa - Peru's second-largest city - with mudflows, tephra fallout and pyroclastic flows. The volcano is especially a threat for people living in the northeastern suburbs of Arequipa and in the valleys on Misti's southern flank, as flows from the volcano can be channelled by these. Misti is monitored by the Peruvian geological service INGEMMET, which has published a volcano hazard map for Misti.

Geography and geomorphology

Misti rises about 3.5 kilometres (2.2 mi) above Arequipa, the second-largest city in Peru, and is the best known volcano of Peru. Politically, it is in Arequipa Department. The name is either Quechua or Spanish and means "mixed", "mestizo" or "white" and may refer to snow cover. The indigenous name is Putina. Other names for the volcano are Guagua-Putina, El Volcan, San Francisco and Volcan de Arequipa. Sometimes chroniclers confused it with other volcanoes like Ubinas and Huaynaputina. Misti appears on the seal of Arequipa.

Misti is part of the Andean Central Volcanic Zone (CVZ). The CVZ is one of the four volcanic belts of the Andes; the others are the Northern Volcanic Zone, the Southern Volcanic Zone and the Austral Volcanic Zone. The CVZ extends for 1,000 kilometres (620 mi) from southern Peru over Bolivia to northern Argentina and Chile. Volcanoes are numerous in the CVZ, but poorly known due to the low population density of much of the Central Andes. Several Peruvian volcanoes were active since the Spanish conquest: Andagua volcanic field, Huaynaputina, Sabancaya and Ubinas, and possibly Ticsani, Tutupaca and Yucamane. Other Peruvian volcanoes in the CVZ are Ampato, Casiri, Coropuna, Huambo volcanic field, Purupuruni and Sara Sara. Ubinas is the most active volcano in Peru, having erupted 24 times since 1550. The 1600 eruption of Huaynaputina claimed more than 1,000 casualties; recent eruptions of Sabancaya 1987-1998 and Ubinas 2006-2007 had severe impacts on the local populations.

The volcano is a young, symmetric cone with 30° degree slopes with a nested summit crater. The outer crater has a diameter of 950 metres (3,120 ft)-835 metres (2,740 ft) and is 120 metres (390 ft) deep. There is a gap in the southwestern rim, almost to the bottom of the crater; otherwise the inner crater walls are nearly vertical and consist of lapilli, lava and volcanic ash. The 550-metre (1,800 ft) wide and 200-metre (660 ft) deep inner crater is in the southeastern part of the outer crater. The inner crater cuts across metre-thick ash and scoria deposits and historical lava domes and is rimmed by scoria. In the crater is a 120-metre (390 ft) wide and 15-metre (49 ft) high volcanic plug/lava dome, covered with cracks, boulders and fumarolic sulfur deposits; it is fumarolically active. The highest point of the volcano is at 5,822 metres (19,101 ft) on the northwestern outer crater rim; an iron cross marks the highest point. Other summits of the Western Cordillera, including Ubinas and Pichu Pichu, can be seen from the summit.

During the wet season, snow can cover an area of 1–7 kilometres (0.62–4.35 mi) on the upper cone. Unlike neighbouring Chachani, Misti lacks any evidence of glacial or periglacial processes, probably due to its inner heat. There is no clear indication of past glaciation, either, except possibly on the western flank. A thin ice cover may not have left traces on the volcano, however.

The volcano is about 20 kilometres (12 mi) wide. Estimates of the edifice's volume range reach 150 cubic kilometres (36 cu mi), but more likely its volume is only 90 cubic kilometres (22 cu mi)-40 cubic kilometres (9.6 cu mi). It is notably asymmetric, with the western side more heavily eroded and featuring older rocks than the eastern side. The western rim of the outer crater is about 150 metres (490 ft) higher than the southern. Underneath the Misti cone is an older, eroded stratovolcano ("Misti 1"). The stratovolcano is made up of pyroclastic rocks and stubby lava flows, which form a 2.2-kilometre (1.4 mi) thick pile. On the northwestern foot, there is a rhyolitic landform named "Hijo de Misti". Misti is surrounded by a fan of volcanic debris, which covers an area of 200 square kilometres (77 sq mi) on Misti and extends 25 kilometres (16 mi) from the volcano. On the southern side, the volcano is cut by 20–80-metre (66–262 ft) deep ravines, while the northern side is flatter. Dune fields and volcanic ash deposits extend for 20 kilometres (12 mi) northeast of Misti; they are formed by wind-blown ash. The terrain between Arequipa and Misti is initially gently sloping, before reaching the steep flanks of the cone.

There are no obvious traces of a sector collapse on the volcano, except on its western foot and a narrow chute on the northwestern flank of Misti that reaches its summit. Two debris avalanche deposits lie on the southeastern and southwestern-southern side of Misti, extending 25 kilometres (16 mi) and 12 kilometres (7.5 mi) from the volcano. The first is made up by hummocks of mixed debris and covers an area of 100 square kilometres (39 sq mi); the second forms a flat-topped terrain with an area of about 40 square kilometres (15 sq mi) on both sides of the Rio Chili.

Hydrology and human geography

The perennial Rio Chili rounds the northern and western sides of Misti, where it has cut the 20-kilometre (12 mi) long and 150–2,600-metre (490–8,530 ft) deep Charcani Gorge. From southeast to southwest the Quebrada Carabaya, Quebrada Honda, Quebrada Grande, Quebrada Agua Salada, Quebrada Huarangual, Quebrada Chilca, Quebrada San Lazaro and Quebrada Pastores drain the edifice. They eventually join to the Rio Chili west and Rio Andamayo south of Misti; the Andamayo joins the Chili south of Arequipa. Quebrada San Lazaro and Quebrada Huarangual have formed alluvial fans at the foot of the volcano. The quebradas carry water during the wet season in November-December and March-April.

The old roads heading from Arequipa to Chivay and Juliaca run along the northern/western and southern/eastern foot of Misti, respectively. Inka roads from the Arequipa area passed by the volcano. There are numerous dams on the Rio Chili, including the Aguada Blanca Dam and reservoir north of the volcano, El Fraile and Hidroeléctrica Charcani I, II, III, IV, V and VI. These dams are hydroelectric power plants which supply electricity to Arequipa. The river is also the principal water resource for the city. Roads leaving the city cross the rivers on bridges.

According to Cumin 1925, there were three small man-made structures of unknown origin in the crater. He noted that they were known since 1677. Inka ceremonial platforms on the summit were probably destroyed by human activities around 1900 AD. Professor S.I.Bailey from the Harvard College Observatory in 1893 installed the world's highest weather station on Misti. The station was one of several high-altitude stations built at the time, which aimed to investigate the high-elevation atmosphere; additionally, the Observatory performed research on the response of the human body to high altitudes and on the Solar eclipse of April 16, 1893. Another weather station, named "Mt. Blanc Station", was installed at the base of the volcano. Both were shut down in 1901 when the Observatory decided to only maintain a station in Arequipa. Physics observations were sporadically carried out on Misti during the 20th century. In 1906 a mule path went up to the summit.

Geology

Off the western coast of Peru, the Nazca Plate subducts under South America at a rate of 5–6 centimetres per year (2.0–2.4 in/year). The subduction is responsible for the volcanism of the CVZ, as the downgoing slab releases fluids that chemically modify the overlying mantle, causing it to produce melts. Most Peruvian volcanoes have produced potassium-rich andesitic magmas, derived from the mantle and further modified by fractional crystallization and assimiliation of material from the often thick crust.

Volcanic activity goes back to the Jurassic. Various volcanic arcs formed in Peru during the past 30 million years: The Tacaza Arc 30-15 million years ago, the Lower Barroso 9-4 million years ago, the Upper Barroso 3-1 million years ago and the Pleistocene-Holocene Frontal Arc during the past one million years. Two distinct episodes of uplift took place 24-13 and 9-4 million years ago, and were accompanied by the emplacement of numerous large ignimbrites.

During the Cretaceous-Paleogene, the Toquepala Group of volcanics was emplaced. The Tacaza Arc is correlated to the Huaylillas Formation, the Barroso Group to the Sencca Formation. The Nazca fracture zone on the Nazca Plate projects under Misti.

Local setting

Misti is part of the Cordillera Occidental of the Andes. It is the youngest of a group of three Plio-Pleistocene volcanoes; the others are dormant Chachani 15 kilometres (9.3 mi) northwest and extinct Pichu Pichu 20 kilometres (12 mi) southeast. This group lies at the margin of the Altiplano and may have developed on top of a northwest-trending fault. The fault was active during the Holocene, offsetting tephra deposits, and magma intruded along the fault plane.

The area lies at the southern foot of the Cordillera Occidental, next to the 600-square-kilometre (230 sq mi) tectonic depression of Arequipa where the city lies. The depression has dimensions of 30 by 15 kilometres (18.6 mi × 9.3 mi) and appears to be formed by fault activity. Other faults include the active Huanca normal fault and faults that influenced the formation of the Rio Chili canyon. The crust under the volcano reaches a thickness of 55 kilometres (34 mi).

The basement under Misti crops out in the Rio Chili gorge. It consists of Proterozoic rocks of the Arequipa Terrane, which are more than a billion years old, Jurassic sediments of the Socosani Formation and Yura Group, and the Cretaceous-Paleogene La Caldera batholith. The batholith forms the hills south of Arequipa. These formations are covered by rhyodacitic ignimbrites known as "sillars". They are between 13.8 and 2.4 million years old; the older are part of the Huaylillas Formation and the younger of the Barroso Arc. Individual ignimbrites crop out in the Rio Chili gorge and include the 300-metre (980 ft) thick "Río Chili" ignimbrite from 13.19 ± 0.09 million years ago, the 4.89 ± 0.02 million years old "La Joya" ignimbrite or "sillar", the 1.65 ± 0.04 million years old "Aeropuerto" or "Sencca" ignimbrite, and the 1.02 million years old "Yura Tuff" and Capillune Formation. The ignimbrites were erupted from multiple calderas, one of which is now buried under Chachani. The ignimbrites are covered by volcanic sedimentary rocks and debris from the sector collapse of Pichu Pichu.

Composition

Misti has erupted mainly andesite, while dacite and rhyolite are less common. There are reports of trachyandesite erupted during the Holocene eruptions. Rhyolites and dacites are associated with explosive eruptions. The volcanic rocks are subdivided into several classes: Pyroxene-amphibole andesites, amphibole andesites, amphibole dacites and amphibole rhyolites; mica has also been reported. The rocks define a potassium-rich calc-alkaline suite typical for Peruvian volcanoes.Phenocrysts include amphibole, augite, biotite, enstatite, plagioclase and titanomagnetite. Magma composition has varied over time and the most recent volcanic stage has produced slightly different magmas, but overall the composition of Misti magmas is highly homogeneous. The composition of Misti magmas and these of its neighbours Pichu Pichu and Chachani resembles adakite, an unusual kind of volcanic rock formed by the direct melting of a subducting plate. Some rocks erupted by the volcano show evidence of hydrothermal alteration.

The formation of the magmas of Misti is a complicated process, involving the arrival of new magma, assimilation of crustal material, and fractional crystallization. Initially mantle-derived melts pool in a reservoir at the base of the crust, where they assimilate crustal material and undergo fractional crystallization. Afterwards they ascend to a shallower reservoir, where they interact with Proterozoic gneisses. It is not clear whether Misti has a single magma chamber or multiple magma reservoirs at depth, although the rock composition implies that only one large magma system is present. The reservoir appears to be located at 6–15 kilometres (3.7–9.3 mi) depth and has a volume of several cubic kilometres. A second rhyolitic reservoir may have been activated during the 2 ka eruption. The magma system is periodically recharged, but such an influx of new magma does not trigger eruptions; instead multiple recharges are necessary to cause activity. Numerous mixing and decompression events can happen to each magma batch before it is erupted. A recharge of the magma chamber may have occurred at some point before 2000 AD. Assimilation of basement rocks gave rise to the rhyolitic magmas erupted 34,000-31,000 years ago. Crystal-poor magma can form in the magmatic system through numerous processes and gives rise to the rhyolites and the volcanic plug.The overall rate of magma supply is 0.63 cubic kilometres per kiloare (0.15 cu mi/ka), comparable to other stratovolcanoes in volcanic arcs, but with brief surges reaching about 2.1 cubic kilometres per kiloare (0.50 cu mi/ka).

Eruption history

Misti is a young volcano. It developed in four stages, numbered 1 through 4; a pre-Misti volcano may have formed the southwestern debris avalanche. On average, sub-Plinian eruptions take place all 4,000-2,000 years, while ash fallout occurs every 1,500-500 years and large ignimbrite-producing eruptions every 20,000-10,000 years. Outcrops showing the stratigraphy of Misti are found mainly in the ravines on the southern side and the Rio Chili gorge. Seismic tomography has identified solidified buried magma bodies from the early stages of volcanism.

Long andesitic lava flows and ignimbrites, which reach a thickness of more than 400 metres (1,300 ft), form the oldest edifice. They have an age of 833,000 years, but it is not clear if they should be considered part of "Misti 1" or of a pre-Misti volcano. After the south-southwestern collapse, the present stratovolcano began to grow 112,000 years ago. During the following 42,000 years lava flows and lava domes built an edifice with an elevation of 4,000–4,500 metres (13,100–14,800 ft), in the southern and eastern sectors of present-day Misti. During the subsequent 20,000 years, repeated collapses of lava domes deposited blocks, fallout deposits and scoria on the southern side of Misti and on Chachani to the northwest. The presence of cirques and evidence of hydromagmatic activity and mudflows imply that Misti was glaciated when the first last glacial maximum of the Central Andes occurred 43,000 years ago.

Between 50,000 and 40,000 years ago, the summit of Misti collapsed one or more times above 4,400 metres (14,400 ft) elevation, forming a 6-by-5-kilometre (3.7 mi × 3.1 mi) caldera. Intense pyroclastic eruptions yielded ignimbrites with volumes of 3–5 cubic kilometres (0.72–1.20 cu mi), which cover an area of 100 square kilometres (39 sq mi) on the southern side of Misti. This activity brought "Misti 2" to an end; subsequently lava domes built "Misti 3" to an elevation of 5,600 metres (18,400 ft), almost entirely erasing the caldera. Between 36,000 and 20,000 years ago collapses of lava domes produced numerous block-and-ash flows of dacitic to andesitic composition, which reach thicknesses of several tens of metres on the southern side of Misti. Several named from this time include the 34,000-33,000 year old "Fibroso I", and the "Sacarosa", "Sacaroso" or "Sacaroide" which took place 21,000 or 37,000 years ago. The "Sacarosa" eruption produced two layers of pumice from a 22-kilometre (14 mi) high eruption column. The total volume of tephra is about 0.5–1.5 cubic kilometres (0.12–0.36 cu mi), equivalent to a volcanic explosivity index of 4. The 15,000 years old "Autopista" is the best preserved: It consists of three layers mostly formed by pumice with smaller quantities of lithics. During its eruption about 0.16 cubic kilometres (0.038 cu mi) of volcanic ash fell west of the volcano. The "Autopista" eruption with a volcanic explosivity index of 4 produced about 0.6 cubic kilometres (0.14 cu mi) of tephra; a similar eruption today would cover parts of Arequipa with 10 centimetres (3.9 in) of pumice.

Between 24,000 and 12,000 years ago ice fields formed on Chachani and Misti during the last glacial maximum; tephra fell on ice and was reworked by meltwater. Two eruptions 13,700 and 11,300 years ago produced pyroclastic surges that extended 12 kilometres (7.5 mi) away from the volcano; a 2-kilometre (1.2 mi) wide caldera formed at an elevation of 5,400 metres (17,700 ft). Other deposits spanning the Pleistocene and Holocene are the "Fibroso II", "Blanco", "La Zebra", "Autopista", "Espuma gris", "Espuma iridiscente" and "Rosado".

Holocene

More than ten eruptions took place during the last 11,000 years, with only brief pauses in activity. They filled the younger caldera with scoria and lava flows, forming the "Misti 4" edifice with the nested summit craters. Tephra forms 5–6-metre (16–20 ft) thick deposits around the volcano, and pyroclastic surges reached distances of many kilometres >6,400 and 5,200 years ago. The 9,000 and 8,500 years old eruptions produced the "Sándwich" deposits. They extend for more than 15 kilometres (9.3 mi) on the southwestern flank of Misti, but they also resulted in ash fall over the Pacific Ocean and Lake Titicaca. Radiocarbon dating has identified eruptions 8,140, 6,390, 5,200, 4,750, 3,800 and 2,050 years ago. The Global Volcanism Program lists eruptions in 310 BCE ± 100, 2230 BCE ± 200, 3510 BCE ± 150, 4020 BCE ± 200, 5390 BCE ± 75 and 7190 BCE ± 150.

2 ka eruption and later activity

The last major explosive eruption - one or several events - took place about 2,000 years ago. The date is constrained to 2,060-1,920 years before present; ages of 2,300 BP are probably too old. The eruption produced about 0.4 cubic kilometres (0.096 cu mi) dense rock equivalents of rock and probably lasted a few hours. The eruption had a volcanic explosivity index of 4 or 5.

The eruption was probably triggered when fresh andesitic magma entered a pre-existent rhyolitic body. Magma rose through the edifice and expelled part of the hydrothermal system, causing initial phreatic eruptions. Tephra rained down around the edifice, with pumice falling in 25 kilometres (16 mi) distance. Owing to magma mixing, the pumice deposits have an appearance resembling chocolate and vanilla swirls. Eventually, the conduit fully cleared and a 29-kilometre (18 mi) high eruption column rose above the volcano. Pyroclastic flows emanated from the column and descended the southern flanks of the volcano, possibly through the gap in the crater rim. During the course of the eruption, collapses of the crater and conduit walls caused a temporary decline in the intensity of the column. The eruption column periodically collapsed and reformed, until the eruption ended with phreatomagmatic explosions.

Mudflows descended from the mountain. The water source for the mudflows is unclear, but the eruption took place during the neoglacial between 2,500 and 1,000 years ago. Thus Misti may have featured a snow or ice cap at the time of the eruption; its melting would have given rise to mudflows. Rainfall generated further mudflows after the eruption. The relative importance of pyroclastic flows and mudflows during the 2 ka eruption is contentious. The outer summit crater probably formed during this eruption. Tephra layers in the Sallalli and (in this case with less certainty) Mucurca peat bogs close to Sabancaya, and (tentatively) for an ice core in the Antarctic Plateau in Antarctica, are attributed to this eruption. This is the only Plinian eruption during the Holocene.

After the 2 ka eruption, activity was limited to small Vulcanian eruptions, mudflows and tephra fallout, including scoria and volcanic ash. Dating has yielded ages of 330, 340, 520, 620, 1035 and 1,300 years before present for several such events. Mudflows took place 1,035±45, 520±25, 340±40 and 330±60 years ago and left 5–15-metre (16–49 ft) thick deposits. Not all of these mudflows are associated with eruptions. Pyroclastic flows and ash falls were emplaced 1,290±100 and 620±50 years ago.

The last eruption took place in AD 1440-1470 and produced about 0.006 cubic kilometres (0.0014 cu mi) of ash. It was probably a prolonged eruption that lasted for months or years, depositing ash in the Laguna Salinas and possibly as far as Siple Dome and Law Dome in Antarctica. The eruption was severe enough that the wife of the Inka emperor Pachacutec came to Chiguata to provide assistance, where black ash had fallen. There is no evidence that a supposed Inka settlement was destroyed by this eruption. Along with other volcanic eruptions around that time and the beginning Spörer sunspot Minimum, the AD 1440-1470 eruption of Misti may have affected global climate conditions. In 1600, the volcano was covered by ash from the Huaynaputina.

Historical eruptions and seismicity

There is no clear evidence of historical eruptions, while the Global Volcanism Program reports a last eruption in 1985. Mudflows descended the southern valleys until the 17th century. Phreatic eruptions may have taken place in 1577, on the 2 May 1677, 9 July 1784, 28 July 1787 and 10 October 1787. Questionable eruptions are recorded in 1542, 1599, August 1826, August 1830, 1831, September 1869, March 1870. They probably constitute fumarolic activity and often took place after heavy precipitation; the water would have infiltrated the edifice and evaporated from the volcanic heat. Comparisons between 1967 photos of the volcanic plug and more recent images show no changes.

The volcano is seismically active, with long-period earthquakes, tremors, "tornillos" and volcano-tectonic earthquakes recorded. The hypocentres, the actual sites of the earthquakes, are found within the edifice of Misti and cluster on the northwest flank of the volcano. The seismic activity appears to be linked to Misti's hydrothemal system. Seismic swarms were recorded in August 2012, May 2014 and June 2014. No deformation of the volcanic edifice is evident in satellite images. Clouds rising from the mountain are sometimes mistaken for renewed activity.

Hazards

Misti is Peru's most dangerous volcano and one of the most dangerous in the world, owing to its proximity (17 kilometres (11 mi)) to Arequipa, where more than a million inhabitants live. The city is constructed on mudflow and pyroclastic flow deposits of the volcano and all valleys that drain Misti pass directly or indirectly through Arequipa. The city has expanded to 12 kilometres (7.5 mi) of the volcano, with new towns like Alto Selva Alegre, Mariano Melgar, Miraflores and Paucarpata and towns such as Chiguata within 11 kilometres (6.8 mi). About 8.6% of Peru's GDP depends on Arequipa and would be impacted by future eruption of Misti. At least 220,000 people live on the alluvial fans and in the ravines on the southern side of Misti, and are threatened by floods, mudflows and pyroclastic flows emanating from the volcano that can be channelled through the ravines.

Individual threats from Misti include:

• There are few outcrops of tephra within Arequipa, which however probably reflects erosion and the dense urban environment. The 2 ka and 1440-1470 AD eruptions deposited tephra over what today is Arequipa. Tephra fallout can cause health problems, pollute water resources, cause roofs to collapse, bury fields, and cause road accidents and accidents during cleanup. Volcanic bombs can fall much closer to the volcano.
• Mudflows are mixtures of rocks and water. They are caused by rainfall or the melting of snow and ice; thus they can occur in the absence of volcanic activity. At Misti, they occur on average every century or two. Even small mudflows can reach the city and they bury and destroy everything in their path. Eruptions of Misti could generate mudflows on Chachani, thus threatening settlements that are on the other side of the Rio Chili.
• Pyroclastic flows are hot (300–800 °C (572–1,472 °F)) masses of gas and rocks that can descend the slopes at speeds of 200–400 kilometres per hour (56–111 m/s); they can flow over topographic obstacles and reach large distances from the volcanic vent. Pyroclastic flows and surges can reach 13 kilometres (8.1 mi) from the volcano, although denser flows are likely to stop before reaching the city.
• The steep slopes put Misti at risk of sector collapses. Debris avalanches from the collapse of volcanoes can reach large distances, larger than that between Arequipa and Misti. Debris flows, like mudflows, can destroy everything in their path. Such collapses could also dam the Rio Chili, producing mudflows and threaten neighbourhoods like Vallecito, Av. La Marina and Club Internacional. Even small landslides on the western side of the volcano could threaten the water supply of Arequipa.
• Other threats are: Toxic gases can accumulate in closed spaces to dangerous concentrations, or interact with precipitation to form acid rains. Lava flows are highly destructive, but their slow speed means that they do not constitute a major threat to life.

Heavy metals presumably from Misti and Chachani are found in water resources.

Monitoring and hazard management

In 2001, there was neither emergency planning nor land use planning around Misti; the 2002-2015 development plan mentioned volcanic hazards but did not envisage any specific measures. The last eruption of Misti had taken place shortly before the foundation of Arequipa, and thus there is no memory of the hazards of volcanic activity, unlike the hazards of earthquake. Before the eruption of Ubinas in 2006-2007, volcanic hazards drew little attention by the Peruvian state and there was little awareness in Arequipa. Beginning in 2005, INGEMMET began monitoring volcanoes in Peru; the first monitoring equipment was targeted at the Charcani V hot spring. Later the monitoring was extended to other hot springs and to fumaroles in the crater; the latter both visually from Arequipa and in the crater. Monitoring of seismic activity commenced in or before 2007. Beginning in 2008 geodesic measurement stations were installed on the northeastern and southern slopes of the volcano. In 2012, a new monitoring station for the volcano was inaugurated. In May 2009 and April 2010, two exercise evacuations of several suburbs of Arequipa were carried out. These efforts have yielded an increased awareness of the dangers posed by Misti, which is now being increasingly perceived as an active volcano. Efforts have been made to slow the growth of the northern suburbs of Arequipa, which are closest to Misti.

A volcano hazard map was developed in 2005 by numerous local and international organizations, and officially presented on the 17 January 2008. It defines three hazard categories: A red "high risk" zone, an orange "intermediate risk" zone and a yellow "low risk" zone. These are defined by the risk of debris flows, lava flows, mudflows, pyroclastic flows, and tephra fallout. The "high risk" zone encompasses the entire volcanic cone, its immediate surroundings and the valleys that emanate from it. Parts of Arequipa lie in the "high risk" zone. The "intermediate risk" zone surrounds the "high risk" zone, including the lower slopes of neighbouring mountains and most of the northeastern parts of Arequipa. The "low risk" zone in turn surrounds the "intermediate risk" zone and includes the rest of the city. Additional maps show areas at risk of tephra fallout and of being flooded by mudflows. These maps serve to mitigate volcano hazards and to inform local development. In November 2010, the municipality of Arequipa decreed that the hazard map would have to be considered in future city zoning decisions.

Scenarios

Three different scenarios of future eruptions have been evaluated. The first envisages a small eruption, similar to recent activity at Sabancaya or the 1440-1470 AD eruption of Misti. Ash fall would occur around the volcano, reaching 5 centimetres (2.0 in) in the urban area, shutting down the Arequipa Airport, and landslides could damage the dams on the Rio Chili, while mudflows would descend the southern slopes. The second scenario involves an eruption like the 2 ka eruption. Thicker ash falls (exceeding 10 centimetres (3.9 in)) could cause buildings to collapse, and pyroclastic flows down the steep slopes south of Misti would reach suburbs of Arequipa and Chiguata. Most risk assessments are based on these two scenarios.

The third scenario is a Plinian eruption like the "Fibroso" and "Sacaroso" events or the 1600 Huaynaputina eruption; pyroclastic flows would sweep all the flanks of Misti and past Arequipa, blocking the Rio Chili. Thick ash fall would occur over the entire region, including over the cities of El Alto, Peru, La Joya and agricultural areas. A Plinian eruption would require the evacuation of Arequipa. Other hazard scenarios are the emissions of short lava flows, the formation and collapse of lava domes and the collapse of part of the volcanic edifice.

Fumarolic and geothermal system

Fumaroles on Misti occur in three locations: On the volcanic plug, the northern/northeastern walls of the inner crater, and on the southeastern flank of the volcano. They emit noises, visible clouds of water vapour and the smell of hydrogen sulfide. The smell reaches the crater rim, and, at times, the gas becomes so concentrated that it causes irritations to the eyes, nose and throat. Fumarolic activity has been reported since the 1440-1470 eruption. In 1948-1949 and 1984-1985 it was intense enough that it could be seen from Arequipa. The fumarolic activity is visible in satellite images as a temperature anomaly of about 6 K (11 °F).

Water is the most important component of the fumarole gases, followed by carbon dioxide, sulfur dioxide, hydrogen sulfide and hydrogen. The gases are highly acidic, containing hydrogen chloride and hydrogen sulfide. Fumarole temperatures have varied through the years, generally they are between 125–310 °C (257–590 °F) with peaks of 430 °C (806 °F). The present-day (21st century) fumarole gases appear to derive directly from magma, with no interaction with a hydrothermal system. The fumaroles outside of the summit crater are colder, with temperatures of 50–80 °C (122–176 °F), and do not smell of sulfur.

Fumarolic vents are surrounded by concentric deposits of anhydrite close to the vent, gypsum at some distance, and sulfur in the colder vents. Other minerals are ammonium sulfate, hematite, ralstonite, soda alum and sodium chloride. Elemental compositions and isotope ratios indicate that the fumarole deposits are derived from the leaching of volcanic rocks and the water from precipitation. The chemistry of the deposits changed between 1967 and 2018, with decreasing zinc and increasing lead concentrations, concomitant to a warming of the fumarolic system. Sometimes the temperature of the fumaroles is high enough to melt the sulfur and the fumarolic gases can ignite.

Hot springs occur at the foot of the volcano. These include the Humaluso/Umaluso spring north and the Agua Salada, Bedoya/La Bedoya, Calle Cuzco, Charcani V, Chilina Norte, Chilina Sur, Jésus, Ojo de Milagro, Puente de Fierro, Sabandia, Tingo, Yumina and Zemanat south and southwest of Misti. The hottest of these is the Charcani V spring in the Rio Chili gorge; it is also the closest to the volcano, being only 6 kilometres (3.7 mi) from the crater. The Jésus and Umaluso springs produce gas bubbles. The springs are fed by a low-temperature geothermal system that mostly produces alkaline waters containing bicarbonate, chloride and sulfate. Their waters appear to originate through the mixing of freshwater, magmatic water and chloride-rich deep water. Many of these springs form artificial pools or have water intakes, and several are monitored by INGEMMET for changes in activity.

High soil temperatures on the cone, hot springs and fumaroles indicate that Misti contains a hydrothermal system. Electric potential measurements indicate that the system appears to be confined between faults or to the older caldera. The activity has not been stable over time; after the 2001 southern Peru earthquake flow at the Charcani V spring and the temperature of the crater emissions increased noticeably. Water temperatures decreased after the 2007 Peru earthquake. Over time old fumarolic vents shut down and new vents develop, but the configuration of the dome vents is stable over time. The fumarolic activity is correlated to earth tides.

Climate and vegetation

The region has a semi-arid climate with temperate temperatures; the annual mean temperature in Arequipa is 13.7 °C (56.7 °F). Temperatures decrease with elevation; in 1910 monthly mean temperatures at the summit ranged from −6 °C (21 °F) in January to −9.7 °C (14.5 °F) in May, June and August. Most precipitation falls during austral summer (December to March) and reaches 89.1 millimetres per year (3.51 in/year). On the summit, as of 1910 precipitation fell mostly as snow or hail. During the wet season, rainstorms and flash floods erode the volcanic debris deposits. The snow cover rapidly melts away during the dry season. The altitude belt between 3,200 metres (10,500 ft) and 3,800 metres (12,500 ft) is the wettest. Between 8,200 and 3,600 years before present, the climate was drier than today and wind erosion may have been enhanced. The dry period ended between 3,000 and 2,000 years ago.

The region west of the Andes, including the terrain at the foot of Misti, is mostly desert with cacti and dwarf shrubs as the principal vegetation forms. They are known as the "Misti zone". There is an altitudinal gradation: Between 2,200–2,900 metres (7,200–9,500 ft) vegetation is dominated by Franseria bushes, above 3,000 metres (9,800 ft) by Diplostephium tacorense. Other bushes occur mainly in creeks and valleys. At higher elevations, other genera such as Adesmia and Senecio idiopappus become more frequent, and at about 3,900 metres (12,800 ft) elevation Lepidophyllum quadrangulare becomes the dominant plant. Polylepis species form woodlands. Above 4,200 metres (13,800 ft) elevation, tola/ichu form grasslands. The upper slopes of Misti are barren. Azorella forms cushion-shaped plant growths on Misti. The Bolivian grass mouse and a plant species, Cantua volcanica, were discovered at Misti; the latter was named after its finding site. 358 plant, 37 mammal and 158 bird species have been recorded in the region, including alpacas, guanacos, llamas and vicuñas. Most of the volcano is within the Salinas y Aguada Blanca National Reserve, which extends northwest of Misti and which includes the volcano among its main attractions. Arequipa is in an oasis at the southern foot of Misti.

Surrounding area

A long history of eruptions from Misti and its neighboring volcanoes has caused the local soil to be extremely fertile, making the surrounding area one of the most agriculturally productive in Peru. Locals also make extensive use of a white volcanic rock called sillar, which is strong but easily workable. The city of Arequipa has a significant number of buildings constructed with sillar, resulting in the nickname la ciudad blanca ("the white city").

Religious importance and mummies

The mountain was considered the apu and "volcano of the city". It was venerated by the inhabitants of Arequipa, a common practice for inhabitants of the Andes. According to the late 16th-century chronist Cristóbal de Albornoz, Misti was one of the important mountains (waqa, a kind of deity or idol) of the Arequipa area of the Inka Empire, along with Ampato, Coropuna, Sara Sara and Solimana. This tradition probably originated with the previous inhabitants of the area and was taken over by the Inka when they conquered the region. The Inka gave them cups of gold and silver and settled people around Misti that would continue the mountain veneration. People used to alter the shape of the skulls of their infant children so that they resembled the volcano. Misti had the reputation of being aggressive, always demanding a sacrifice, and the mountain had to be exorcised in colonial times. After the Spanish conquest, the mountain was consecrated to St. Francis. According to the Jesuit College of Arequipa, "Indian sorcerers" thought that Huaynaputina had asked Misti for assistance in expelling the Spaniards; Misti however had turned down, saying it was already Christianized, so Huaynaputina had proceeded alone.

Eight or nine mummies were found on Misti by Johan Reinhard in 1998, inside the crater and below the summit. The mummies were of children, mostly boys around six years old. Unusually, the mummies were buried in shared tombs. Along with the mummies were figurines, ceramics and other objects; the high number of figurines found on Misti indicates that the site was important to the Inkas. These mummies were Inka human sacrifices, so-called capacochas, and the Misti capacocha is considered to be the most spectacular such sacrifice. However, the hostile conditions within the crater had seriously damaged the mummies. The sacrifices on Misti, and others on Chachani and Pichu Pichu, were probably motivated by the 1440-1470 eruption of Misti. According to the 16th century chronicler Martín de Murúa, the Inka Thupa Yapanki sacrificed llamas to calm a volcano Putina close to Arequipa (probably Misti), going as closely as possible to the summit. This description however most likely refers to the 1600 eruption of Huaynaputina, rather than of eruptions at Misti.

Climbing and recreation

Misti was first ascended by pre-Columbian people, which left archaeological evidence around the summit. Numerous ascents of the volcano were made already during the 18th and 19th centuries. The iron cross on the summit was placed in 1784 and was still there a century later. The climbers reported difficulties due to the loose ground, noxious gases and mountain sickness.

Tourist activities at Misti include running down scree slopes.

Gallery

• 
  Aerial picture of Ubinas with Misti in the back (2015).
• 
  Misti, as seen from Arequipa (2015).
• 
  This mosaic of two astronaut photographs taken from the ISS illustrates the proximity of Arequipa to Misti, just 17 km away (2009).
• 
  The crater of El Misti (2005).

See also

• List of volcanoes in Peru

References

Sources

• Agassiz, Alexander (December 1875). "Misti and its Cloud". Nature. 13 (319): 107–108. doi:10.1038/013107d0.
• Andrés, Nuria; Palacios, David; Úbeda, José; Alcalá, Jesús (2011). "Relationship between geothermal ground anomalies and the absence of glacial or periglacial features on El Misti volcano (southern Peru). Boletín De La Asociación De Geógrafos Españoles". Boletín de la Asociación de Geógrafos Españoles. 57: 465–469. ISSN 2605-3322.
• Atwell, William S. (2001). "Volcanism and Short-Term Climatic Change in East Asian and World History, c. 1200-1699". Journal of World History. 12 (1): 29–98. ISSN 1045-6007.
• Bailey, S. I. (1897). "Harvard Observatory in Peru". Scientific American. 76 (21): 329–331. ISSN 0036-8733.
• Bailey, S. I.; Pickering, E. C. (1906). "Peruvian meteorology, 1888-1890". Annals of Harvard College Observatory. 39. Bibcode:1906AnHar..39....1B.
• Bandelier, Adolph F. (1906). "Traditions of Precolumbian Earthquakes and Volcanic Eruptions in Western South America". American Anthropologist. 8 (1): 47–81. ISSN 0002-7294.
• Besom, Thomas (2009). Of Summits and Sacrifice: An Ethnohistoric Study of Inka Religious Practices. University of Texas Press. ISBN 978-0292725720 – via Academia.edu.
• Birnie, R. W.; Hall, J. H. (March 1974). "The geochemistry of El Misti volcano, Peru fumaroles". Bulletin Volcanologique. 38 (1): 1–15. doi:10.1007/BF02597797.
• Bouysse-Cassagne, Thérèse; Chacama, Juan R (00/2012). "PARTICIÓN COLONIAL DEL TERRITORIO, CULTOS FUNERARIOS Y MEMORIA ANCESTRAL EN CARANGAS Y PRECORDILLERA DE ARICA (SIGLOS XVI-XVII)". Chungará (Arica). 44 (4): 669–689. doi:10.4067/S0717-73562012000400009. ISSN 0717-7356. {{cite journal}}: Check date values in: |date= (help)
• Cabrera-Pérez, Iván; Centeno, Riky; Soubestre, Jean; D'Auria, Luca; Rivera, Marco; Machacca, Roger (June 2022). "Ambient noise tomography of Misti volcano, Peru". Journal of Volcanology and Geothermal Research. 426: 107538. doi:10.1016/j.jvolgeores.2022.107538.
• Cacya, L.; Mariño, J.; Rivera, M. (2006). Características de la erupción pliniana de ~15,000 años del volcán Misti: Depósito "Autopista". Congreso Peruano de Geología, 13 (in Spanish). Lima: Sociedad Geológica del Perú. pp. 657–660. hdl:20.500.12544/458.
• Cacya, L.; Mariño, J.; Rivera, M. (2007). "La erupción pliniana "Autopista" del volcán Misti (21,000-11,000 años AP)". Boletín de la Sociedad Geológica del Perú (in Spanish). 102: 25–42. hdl:20.500.12544/388.
• Cacya, L.; Mamani, M. (2009). "Variaciones geoquímicas de los depósitos del volcán Misti: control de la asimilación somera y profunda". Boletín de la Sociedad Geológica del Perú (in Spanish): 91–107.
• Calderón Vilca, José Javier (December 2019). Informe anual 2019: instalación y mantenimiento de la red telemétrica de los volcanes Sabancaya, Ubinas, Misti y Ticsani (Report) (in Spanish). Instituto Geológico, Minero y Metalúrgico - INGEMMET. hdl:20.500.12544/2581.
• Chamberlain, Alexander F. (22 November 1901). "Practical Ameliorations of English Grammar". Science. 14 (360): 814–815. doi:10.1126/science.14.360.814.b.
• Cobeñas, Gisela; Thouret, Jean-Claude; Bonadonna, Costanza; Boivin, Pierre (October 2012). "The c.2030yr BP Plinian eruption of El Misti volcano, Peru: Eruption dynamics and hazard implications". Journal of Volcanology and Geothermal Research. 241–242: 105–120. doi:10.1016/j.jvolgeores.2012.06.006.
• Cobeñas, Gisela; Thouret, Jean-Claude; Bonadonna, Costanza; Boivin, Pierre (April 2014). "Reply to comment on: "Cobeñas, G., Thouret, J.-C., Bonadonna, C., Boivin, P., 2012. The c.2030yr BP Plinian eruption of El Misti volcano, Peru: Eruption dynamics and hazard implications. Journal of Volcanology and Geothermal Research 241–242, 105–120." by Harpel et al., JVGR 2013". Journal of Volcanology and Geothermal Research. 275: 103–113. doi:10.1016/j.jvolgeores.2014.02.014.
• Cruz, Vicentina; Finizola, Anthony; Macedo Sánchez, Orlando Efraín; Sortino, Francesco (2001). Disruptions in the hydrothermal water geochemistry inside Misti volcano in coincidence with the 8.4 Mw earthquake of June 23rd, 2001, in southern Peru (Report).
• Cumin, Gustavo (31 December 1925). "Alcuni appunti sul vulcano Misti". Bollettino della Società Geografica Italiana: 401–404. ISSN 2974-5780.
• Cuno, J.; Harpel, C.; Rivera, M.; García, F. (2021). La erupción subpliniana del volcán Misti ocurrida hace 33,700 años que emplazó el depósito de caída de tefra “sacarosa”. Congreso Peruano de Geología, 19 (in Spanish). Lima: Sociedad Geológica del Perú. pp. 882–885.
• Delaite, G.; Thouret, J. C.; Sheridan, M.; Labazuy, P.; Stinton, A.; Souriot, T.; Van Westen, C. (2005). "Assessment of volcanic hazards of El Misti and in the city of Arequipa, Peru, based on GIS and simulations, with emphasis on lahars". Zeitschrift für Geomorphologie. 140: 209–231 – via Academia.edu.
• Dirección Desconcentrada de Cultura de Arequipa - Ministerio de Cultura (October 2015). Arequipa Patrimonio Cultural de la Humanidad. Relexiones a quince años de su declaratoria (Report) (in Spanish) – via Academia.edu.
• Escobar, G. (2023). "Análisis de las Caídas Piroclásticas "Sandwich" Originadas por Erupciones Plinianas del volcán Misti en el Pleistoceno Superior, para evaluar el Peligro Volcánico en la Ciudad de Arequipa". In Masías, P.; Ortega, M. (eds.). Libro de Resúmenes IX Foro Internacional de Peligros Volcánicos – IX FIPVO (in Spanish). Lima: Instituto Geológico Minero y Metalúrgico. pp. 105–110.
• Espirilla, Alfonso Torres; Gómez, Trinidad Betty Paredes de (2 September 2022). "Distribution and assessment of the environmental risk of heavy metals in Aguada Blanca reservoir, Peru". Revista Ambiente & Água. 17: e2838. doi:10.4136/ambi-agua.2838. ISSN 1980-993X.
• Fergusson, S. P. (1895). "THE METEOROGRAPH FOR THE HARVARD OBSERVATIORY ON EL MISTI, PERU". American Meteorological Journal. A Monthly Review of Meteorology and Allied Branches of Study (1884-1896). 12 (4).
• Finizola, Anthony; Lénat, Jean-François; Macedo, Orlando; Ramos, Domingo; Thouret, Jean-Claude; Sortino, Francesco (August 2004). "Fluid circulation and structural discontinuities inside Misti volcano (Peru) inferred from self-potential measurements". Journal of Volcanology and Geothermal Research. 135 (4): 343–360. doi:10.1016/j.jvolgeores.2004.03.009.
• Franco, R.D. Vargas; Thouret, J.-C.; Delaite, G.; van Westen, C.; Sheridan, M.F.; Siebe, C.; Mariño, J.; Souriot, T.; Stinton, A. (2010). Mapping and assessing volcanic and flood hazards and risks, with emphasis on lahars, in Arequipa, Peru. Geological Society of America. doi:10.1130/2010.2464(13). ISBN 978-0-8137-2464-5. Retrieved 21 November 2023 – via ResearchGate. {{cite book}}: |work= ignored (help)
• "El Misti". Global Volcanism Program. Smithsonian Institution. Retrieved 16 November 2023.
• Harpel, Christopher J.; de Silva, Shanaka; Salas, Guido (2011), "The 2 ka Eruption of Misti Volcano, Southern Peru—The Most Recent Plinian Eruption of Arequipa's Iconic Volcano", The 2 ka Eruption of Misti Volcano, Southern Peru—The Most Recent Plinian Eruption of Arequipa's Iconic Volcano, Geological Society of America, doi:10.1130/2011.2484, ISBN 978-0-8137-2484-3, retrieved 17 November 2023 – via CiteSeer
• Harvard College Observatory (1895). Annual Report of the Director of the Astronomical Observatory of Harvard College (Report) – via Google Books.
• Hatch, Frederick Henry (1886). Ueber die Gesteine der Vulcan-Gruppe von Arequipa... (in German). Alfr. Hölder – via Google Books.
• Hill, Arthur W. (May 1905). "Notes on a journey in Bolivia and Peru around lake Titicaca". Scottish Geographical Magazine. 21 (5): 249–259. doi:10.1080/00369220508733561.
• Holmer, Nils M. (1 December 1960). "Indian Place Names in South America and the Antilles. II" (PDF). Names. 8 (4): 197–219. doi:10.1179/nam.1960.8.4.197.
• Julien, Catherine (2011). "LAS HUACAS PACARISCAS DE AREQUIPA Y EL VOLCAN MISTI". HISTORIA (in Spanish). 10. Escuela Profesional de Historia Universidad Nacional de San Agustín, Arequipa-Perú: 105–132. ISSN 2220-3826 – via Academia.edu.
• Juvigné, Etienne; Thouret, Jean-Claude; Loutsch, Isabelle; Lamadon, Sébastien; Frechen, Manfred; Fontugne, Michel; Rivera, Marco; Dávila, Jasmine; Mariño, Jersy (1 June 2008). "Retombées volcaniques dans des tourbières et lacs autour du massif des Nevados Ampato et Sabancaya (Pérou méridional, Andes Centrales)". Quaternaire. Revue de l'Association française pour l'étude du Quaternaire (in French) (vol. 19/2): 157–173. doi:10.4000/quaternaire.3362. ISSN 1142-2904. {{cite journal}}: |issue= has extra text (help)
• Kemp, J. F. (16 March 1906). "An Interesting Discovery of Human Implements in an Abandoned River Channel in Southern Oregon". Science. 23 (585): 434–436. doi:10.1126/science.23.585.434.b.
• Kurbatov, A. V.; Zielinski, G. A.; Dunbar, N. W.; Mayewski, P. A.; Meyerson, E. A.; Sneed, S. B.; Taylor, K. C. (27 June 2006). "A 12,000 year record of explosive volcanism in the Siple Dome Ice Core, West Antarctica". Journal of Geophysical Research: Atmospheres. 111 (D12). doi:10.1029/2005jd006072.
• Lebti, Perrine Paquereau; Thouret, Jean-Claude; Wörner, Gerhard; Fornari, Michel (June 2006). "Neogene and Quaternary ignimbrites in the area of Arequipa, Southern Peru: Stratigraphical and petrological correlations". Journal of Volcanology and Geothermal Research. 154 (3–4): 251–275. doi:10.1016/j.jvolgeores.2006.02.014.
• Legros, F (April 2001). "Tephra stratigraphy of Misti volcano, Peru". Journal of South American Earth Sciences. 14 (1): 15–29. doi:10.1016/S0895-9811(00)00062-6.
• Macedo, O.; Centeno, R. (2010). Análisis de la actividad sísmica del volcán Misti para el período 2007-2008. XV Congreso Peruano de Geología, Resúmenes Extendidos (in Spanish). Sociedad Geológica del Perú. pp. 1124–1127.
• Macedo Franco, Luisa Diomira (2006). Plan piloto de educación, difusión y sensibilización frente a los peligros volcánicos del Misti (Report) (in Spanish). hdl:20.500.12544/3943.
• Macedo Franco, Luisa Diomira; Amache Cutipa, Roxana; Alfaro Gómez, Michael Johann; Pareja, Henry; Vásquez, José (2010). Primer simulacro de evacuación por erupción volcánica del Misti, Arequipa - Perú. XV Congreso Peruano de Geología (in Spanish). Cusco: Sociedad Geológica del Perú. pp. 1119–1123. hdl:20.500.12544/3006.
• Macedo Franco, Luisa Diomira; Vela Valdez, Jessica Carolina (September 2014). Límites de expansión urbana hacia los volcanes Misti y Chachani (Report) (in Spanish). Instituto Geológico, Minero y Metalúrgico - INGEMMET. hdl:20.500.12544/1741.
• Macedo Sánchez, Orlando; Masías Alvarez, Pablo Jorge; Palacios Estremera, David; Machacca Puma, Roger; Centeno Quico, Riky Gustavo; Úbeda Palenque, José; Arenas, Ronald (2012). Aparente influencia de la marea terrestre en la actividad hidrotermal del volcán Misti observada en datos de temperatura. XVI Congreso Peruano de Geología (in Spanish). Lima: Sociedad Geológica del Perú. hdl:20.500.12544/3022.
• Mariño, J.; Macedo, L.; Rivera, M.; Cacya, L. (2008). La ciudad de Arequipa y los peligros volcánicos asociados al volcán Misti, Perú (Report). Proyecto Multinacional Andino: Geociencias para las Comunidades Andinas. Experiencias andinas en mitigación de riesgos geológicos. Publicación Geológica Multinacional (in Spanish). Santiago: Servicio Nacional de Geología y Minería. pp. 71–75.
• Mariño, J.; Rivera, M.; Thouret, J.C.; Macedo, L. (2016). Geología y mapa de peligros del volcán Misti (Report). Serie C: Geodinámica e Ingeniería Geológica, 60. INGEMMET. p. 170.
• Mariño Salazar, Jersy; Rivera Porras, Marco Antonio; Cacya Dueñas, Lourdes (2008). Geología y evaluación de peligros volcánicos del Volcán Misti – Arequipa (Report) (in Spanish). Instituto Geológico, Minero y Metalúrgico. Dirección de Geología Ambiental y Riesgos. hdl:20.500.12544/3945.
• Masías Alvarez, Pablo Jorge (December 2007). Vigilancia geoquímica de aguas y fumarolas del volcán Misti (Arequipa), periodo 2007 (Report) (in Spanish). Instituto Geológico, Minero y Metalúrgico - INGEMMET. hdl:20.500.12544/2450.
• Masías Alvarez, Pablo Jorge (2008). Monitoreo geoquímico de los volcanes Misti (Arequipa) y Ubinas (Moquegua) periodo 2005-2008 (Report) (in Spanish). Instituto Geológico, Minero y Metalúrgico - INGEMMET. hdl:20.500.12544/2456.
• Masías, P.; Cruz, V. (2008). Estudio geoquímico de las fuentes de aguas termales alrededor del volcán Misti, Arequipa, Perú. Congreso Peruano de Geología, 14, Congreso Latinoamericano de Geología (in Spanish). Lima, Peru: Sociedad Geológica del Perú.
• Masías Alvarez, Pablo Jorge; Antayhua Vera, Yanet; Espinoza Oscanoa, Domingo; Ramos Palomino, Domingo A. (November 2009). Monitoreo del volcán Misti, periodo: 2005 a octubre de 2009 (Report) (in Spanish). Instituto Geológico Minero y Metalúrgico. Dirección de Geología Ambiental y Riesgo Geológico. hdl:20.500.12544/2461.
• Moussallam, Yves; Peters, Nial; Masias, Pablo; Apaza, Fredy; Barnie, Talfan; Ian Schipper, C.; Curtis, Aaron; Tamburello, Giancarlo; Aiuppa, Alessandro; Bani, Philipson; Giudice, Gaetano; Pieri, David; Davies, Ashley Gerard; Oppenheimer, Clive (June 2017). "Magmatic gas percolation through the old lava dome of El Misti volcano". Bulletin of Volcanology. 79 (6). doi:10.1007/s00445-017-1129-5.
• Oldfield, Thomas (1901). "XXI.—New mammals from Peru and Bolivia, with a list of those recorded from the Inambari River, Upper Madre de Dios". The Annals and magazine of natural history; zoology, botany, and geology. 7: 178–190. doi:10.1080/00222930108678454.
• Pallares, Carlos; Fabre, Denis; Thouret, Jean-Claude; Bacconnet, Claude; Charca-Chura, Juan Antonio; Martelli, Kim; Talon, Aurélie; Yanqui-Murillo, Calixtro (June 2015). "Geological and geotechnical characteristics of recent lahar deposits from El Misti volcano in the city area of Arequipa, South Peru". Geotechnical and Geological Engineering. 33 (3): 641–660. doi:10.1007/s10706-015-9848-x.
• Polk, Mary H.; Young, Kenneth R.; Crews-Meyer, Kelley A. (December 2005). "Biodiversity conservation implications of landscape change in an urbanizing desert of Southwestern Peru". Urban Ecosystems. 8 (3–4): 313–334. doi:10.1007/s11252-005-4864-x.
• Porter, Mark; Prather, Alan (2008). "Cantua dendritica (Polemoniaceae), a New Species from Peru, and Two New Cantua Names". Aliso. 25 (1): 31–35. doi:10.5642/aliso.20082501.03.
• Pritchard, M. E.; Simons, M. (February 2004). "An InSAR‐based survey of volcanic deformation in the central Andes". Geochemistry, Geophysics, Geosystems. 5 (2). doi:10.1029/2003gc000610.
• Rauh, Werner (1958). Beitrag zur Kenntnis der peruanischen Kakteenvegetation. Berlin, Heidelberg: Springer Berlin Heidelberg. doi:10.1007/978-3-662-30467-9. ISBN 978-3-540-02337-1.
• Reinhard, Johan; Ceruti, Maria Constanza (December 2006). "Sacred Mountains, Ceremonial Sites and Human Sacrifice among the Incas". Archeoastronomy; XIX. University of Texas Press: 1–43.
• Ren, Jiawen; Li, Chuanjin; Hou, Shugui; Xiao, Cunde; Qin, Dahe; Li, Yuansheng; Ding, Minghu (16 June 2010). "A 2680 year volcanic record from the DT‐401 East Antarctic ice core". Journal of Geophysical Research: Atmospheres. 115 (D11). doi:10.1029/2009jd012892.
• "Reports on Climates". Nature. 84 (2134): 377–377. September 1910. doi:10.1038/084377a0.
• Rivera, Marco; Martin, Hervé; Le Pennec, Jean-Luc; Thouret, Jean-Claude; Gourgaud, Alain; Gerbe, Marie-Christine (January 2017). "Petro-geochemical constraints on the source and evolution of magmas at El Misti volcano (Peru)". Lithos. 268–271: 240–259. doi:10.1016/j.lithos.2016.11.009.
• Rivera Porras, Marco Antonio (2008). Petrología y geoquímica de rocas de los volcanes Misti y Ubinas (Report) (in Spanish). Instituto Geológico, Minero y Metalúrgico - INGEMMET. hdl:20.500.12544/2290.
• Rivera Porras, Marco Antonio (December 2009). Estudio de productos emitidos por el volcán Misti durante los últimos 10,000 años (Report) (in Spanish). Instituto Geológico, Minero y Metalúrgico - INGEMMET. hdl:20.500.12544/1972.
• Rivera Porras, Marco Antonio; Martin, Hervé; Gourgaud, Alain; Le Pennec, Jean-Luc; Gerbe, Marie Christine; Thouret, Jean-Claude (2010). Rol de la contaminación crustal en el magmatismo de los Andes del sur peruano: ejemplo del volcán Misti. XV Congreso Peruano de Geología (in Spanish). Cusco: Sociedad Geológica del Perú. pp. 1144–1147. hdl:20.500.12544/3008.
• Ruprecht, Philipp; Wörner, Gerhard (September 2007). "Variable regimes in magma systems documented in plagioclase zoning patterns: El Misti stratovolcano and Andahua monogenetic cones". Journal of Volcanology and Geothermal Research. 165 (3–4): 142–162. doi:10.1016/j.jvolgeores.2007.06.002.
• Schijman, Edgardo (November 2005). "Artificial cranial deformation in newborns in the pre-Columbian Andes". Child's Nervous System. 21 (11): 945–950. doi:10.1007/s00381-004-1127-8.
• Sekido, Yataro; Elliot, Harry, eds. (1985). Early History of Cosmic Ray Studies: Personal Reminiscences with Old Photographs. Astrophysics and Space Science Library. Vol. 118. Dordrecht: Springer Netherlands. doi:10.1007/978-94-009-5434-2. ISBN 978-94-010-8899-2.
• "Reserva Nacional de Salinas y Aguada Blanca". gob.pe (in Spanish). SERNANP. 1 January 2019. Retrieved 20 November 2023.
• Sigurdsson, Haraldur; Houghton, B. F.; McNutt, Stephen R.; Rymer, Hazel; Stix, John (2015). The encyclopedia of volcanoes (2 ed.). Amsterdam Boston: Elsevier/AP, Academic Press is an imprint of Elsevier. ISBN 978-0-12-385938-9.
• Socha, Dagmara M.; Reinhard, Johan; Perea, Ruddy Chávez (March 2021). "Inca Human Sacrifices on Misti Volcano (Peru)". Latin American Antiquity. 32 (1): 138–153. doi:10.1017/laq.2020.78. ISSN 1045-6635.
• Süring, Reinhard (1895). Wissenschaftliche Ballonfahrten (in German). H. Paetel – via Google Books.
• Thouret, Jean-Claude; Finizola, Anthony; Fornari, Michel; Legeley-Padovani, Annick; Suni, Jaime; Frechen, Manfred (December 2001). "Geology of El Misti volcano near the city of Arequipa, Peru". Geological Society of America Bulletin. 113 (12): 1593–1610. doi:10.1130/0016-7606(2001)113<1593:GOEMVN>2.0.CO;2.
• Thouret, J. C.; Juvigné, E.; Mariño, J.; Moscol, M.; Legeley-Padovani, A.; Loutsch, I.; Dávila, J.; Rivera, M. (2002). Late Pleistocene and Holocene Tephro-Stratigraphy and Chronology in Southern Perú (Report) – via Academia.edu.
• Tort, Anthony; Finizola, Anthony (March 2005). "The buried caldera of Misti volcano, Peru, revealed by combining a self-potential survey with elliptic Fourier function analysis of topography". Journal of Volcanology and Geothermal Research. 141 (3–4): 283–297. doi:10.1016/j.jvolgeores.2004.11.005.
• Ward, Robert DeC. (1901). "Notes on Climatology". Bulletin of the American Geographical Society. 33 (1): 47–51. ISSN 0190-5929.
• Vlastelic, Ivan; Apaza, Fredy; Masias, Pablo; Rivera, Marco; Piro, Jean-Luc; Gannoun, Abdelmouhcine (February 2022). "Probing the hidden magmatic evolution of El Misti volcano (Peru) with the Pb isotope composition of fumaroles". Bulletin of Volcanology. 84 (2). doi:10.1007/s00445-021-01521-9.
• Zielinski, Gregory A. (2006). Collaborative Research: A 700-Year Tephrochronology of the Law Dome Ice Core, East Antarctica (Report). Vol. 199. University of Maine Office of Research Administration: Grant Reports.

Bibliography

• Reinhard, Johan (2005). The Ice Maiden: Inca Mummies, Mountain Gods, and Sacred Sites in the Andes. Washington, D.C.: National Geographic Society. ISBN 0-7922-6838-5.

External links

• CHARBONNIER, SYLVAIN; THOURET, JEAN-CLAUDE; GUEUGNEAU, VALENTIN; CONSTANTINESCU, ROBERT (2020). "New Insights Into the 2070calyrBP Pyroclastic Currents at El Misti Volcano (Peru) From Field Investigations, Satellite Imagery and Probabilistic Modeling". Frontiers in Earth Science. 8. doi:10.3389/feart.2020.557788/full. ISSN 2296-6463.{{cite journal}}: CS1 maint: unflagged free DOI (link)
• Bailey, S. I.; Shapley, H. (1923). "Peruvian meteorology : observations made at the auxiliary stations, 1896-1900". Annals of the Astronomical Observatory of Harvard College. 86. Cambridge, Mass: The Observatory: 119–194. Bibcode:1923AnHar..86..119B.
• "El Misti Volcano and Arequipa, Peru". Earth Observatory. NASA. 2009-11-02. Retrieved 2016-06-03.
• "El Misti Volcano and the City of Arequipa, Peru". Earth Observatory. NASA. 2001-12-31. Retrieved 2016-06-03.