Aucanquilcha
Stratovolcano in Antofagasta Region, Chile
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Aucanquilcha is a large compound volcano in the Antofagasta Region of northern Chile, within the Central Volcanic Zone of the Andes. The volcano has the form of a ridge with a maximum height of 6176 m and formed between 1.04 and 0.23 million years ago; there is ongoing fumarolic activity. The volcano is part of a larger cluster of volcanoes, including lava domes and lava flows, which formed in several stages over 11 million years of activity with varying magma output. During the ice ages, Aucanquilcha was covered in an ice cap that left moraines and cirques.
| Aucanquilcha | |
|---|---|
| Aucaquilcha and Auncanquilcha[1] | |
View of Aucanquilcha volcano from the northwest | |
| Highest point | |
| Elevation | 6,176 m (20,262 ft)[2] |
| Prominence | 2,145 m (7,037 ft)[3] |
| Parent peak | Huascaran |
| Coordinates | 21°13′15″S 68°28′07″W |
| Naming | |
| Etymology | Quechua,[4] although the ending "-che"[a] might be influenced by the Diaguita language:[6] Auqa/aukka; "cruel"/"enemy", kichka/khiska; "spine"; "cruel spine"[7] |
| Pronunciation | OW-kahn-KEEL-chuh |
| Geography | |
  Aucanquilcha Location within Chile | |
| Location | Antofagasta |
| Parent range | Andes |
| Geology | |
| Rock age | Up to 11 Ma (Late Miocene) |
| Stratovolcano | |
| Rock type | Dacite |
| Volcanic zone | Central Volcanic Zone |
| Last eruption | 240,000 ± 50,000 years ago (Pleistocene)[8] |
The cluster has generated lava ranging in composition from andesite to dacite, with the main Aucanquilcha volcano having produced dacites exclusively. Systematic variations in temperature, crystal and biotite content have been recorded during the evolution of the cluster, reflecting changes in the crust from dispersed magma chambers to a centralized volcanic system.
The volcano has sulfur deposits in its summit area, which were mined in the past. One mine at an altitude of 5950 m was opened in 1913 and remained in use from 1950 to 1992, constituting at that time the world's highest mine. As part of this mining activity, a road and an aerial cableway were built on Aucanquilcha, which still stand today although they are partially unusable. In 1986, four men were reported to be living at an altitude of 5900 m, making them the highest permanent residents on Earth and drawing scientific attention.
Geography and geomorphology
Aucanquilcha is a compound volcano[9] in the El Loa Province[10] of Chile's Antofagasta Region.[11] Roads and railways,[10] including a branch line of the Antofagasta-Bolivia railway going to the Collahuasi mine,[12] pass near the volcano.[13] A road with numerous switchbacks[14] leads up to the Aucanquilcha mine; it was built in 1972 and is now impassable because of rock falls,[15] and might have made the mine on Aucanquilcha the highest point on Earth accessible by road.[13] The mountain was evaluated as a potential site for the European Southern Observatory[16] and its surroundings for the Submillimeter Array observatory.[17]
The main volcano is composed of an east–west 8 km long chain of at least six stratovolcanoes, some with well-preserved volcanic craters,[18][19] that rise 1.4 km above a platform of andesitic rocks.[20] The mountains are formed by about 37 km3[b] of lava domes and pyroclastic rocks,[19][20] making it one of the largest volcanoes of northern Chile.[22] Four peaks[c] exceed altitudes of 6000 m;[24] at the end of a ridge[25] is the highest peak, reaching 6176 m[d] above sea level. It is the summit of the Aucanquilcha volcano,[22] and one can see the Salar de Uyuni and other Andean volcanoes from there.[28] Lava flows extend mostly from the summit areas as far as 2–3 km from their vents; they are dark to grey in colour. It is likely that two small lava domes (Cerro Cumbre Negra and Summit 5867) on the northwest flank occupy flank vents.[29] To the north lies the 3.3 million years old andesite Cerro Tres Monos ridge; to the west lies the east-west Cerro Polan and La Luna ridge.[20]
Aucanquilcha collapsed to the northwest,[30] forming a 1 km3 debris avalanche[31] that descended 2100 m and ran for 17 km[23] to the northwest and north,[32] eventually covering an area of 59 km2[23] to form a tongue-shaped deposit.[33] The flow was channeled between Miño Volcano and Cerro Cumbre Negra (an eroded lava massif) towards the dry Rio Loa valley, favouring the preservation of the slide deposit.[34] The slide lacks the hummocky topography usually found on debris avalanches but has radial ridges and grooves and lateral levees;[31] its upper sector is buried by more recent volcanic rocks and moraines.[35] Another landslide occurred during the Redondo stage on the eastern side of the main volcano into the Salar de Carcote. It has the classic hummocky topography of landslides and covers a length of 17 km and a surface area of 35 km2, roughly half of the surface area of the Mount St Helens avalanche of 1980 and one-third of the surface area of the Ollagüe avalanche. A volume of 0.35 km3 is assumed based on a probable thickness of 10 m.[36][37]
The volcano is part of a quasi-circular cluster of about 19–20 volcanoes[38][24] between the Rio Loa and the Chile–Bolivia border,[39] covering a surface area of 700 km2. Salt flats and alluvial deposits surround it to the east, north and south. On its southern side is the Cerro Chela volcano.[38][24] The cluster lies on a 70 km thick crust,[38] and arid conditions since the Miocene have preserved its structures.[39] Its volcanoes are arranged in north–south and northwestern alignments, which may indicate a rupture of the crust above shallow magma reservoirs.[40]
There are anecdotal reports of crater lakes on the mountain,[41] and lake El Toro on its southern foot.[42] Some of the source creeks and springs of the Rio Loa are on Aucanquilcha,[43][44] forming its headwaters when they converge in Lago Seco.[43][45] The Loa drains the western and northwestern sides of the volcano; the eastern side drains into the Salar de Ollagüe salt pan, the northeastern into the Salar de Laguani, and the southeastern into the Salar de Carcote. Most valleys[e] only intermittently transport water, if at all.[48]
Geology
Off the western coast of South America, the Nazca Plate subducts beneath the South America Plate at a rate of 7 °Cm/year.[49] As it descends, it releases fluids into the mantle that induce its melting and the onset of volcanism at the surface.[50] This volcanism of the Andean Volcanic Belt is distributed over four arcs,[51] including the Northern Volcanic Zone (NVZ), the Central Volcanic Zone (CVZ) and Southern Volcanic Zone (SVZ),[52] which are separated by gaps without volcanic activity.[53] Aucanquilcha is part of the CVZ,[20] which contains more than a thousand[53] volcanoes (including ignimbrites and compound volcanoes). During the past 28 million years, it has produced more than 3000 km3 of eruption products; the average rate of 0.11 km3/ka is one tenth of the global maximum rate of arc magma production.[20] Rocks are typically silicic or have intermediate compositions between silicic and mafic.[f][9] The arc has migrated eastward towards the high Andes from the Pacific Ocean coast since the Jurassic[20] and has been producing ignimbrites and stratovolcanoes since the Miocene.[24] The arc features an eastward offset at the latitude of Aucanquilcha.[29] Lascar is the most active volcano of the CVZ, having erupted more than thirty times since 1800;[51] other active volcanoes of the CVZ include Taapaca, Parinacota, Irruputuncu, Ollagüe, San Pedro, Socompa and Lastarria.[55]
The crust under the CVZ reaches high thicknesses exceeding 60–70 km, leading to widespread contamination of ascending magmas. The basement of the Central Andes consists of volcanic rocks and marine sediments from the Mesozoic, and volcanic and volcano-sedimentary rocks from the Cenozoic; they overlie metamorphic rocks and amphibolite of the lower crust.[38][20] The offset in the volcanic arc coincides with a boundary between two distinct crustal domains to the north and south[56] in the Arequipa-Antofalla terrane.[57] A fracture in the crust under Aucanquilcha might be responsible both for its elongated shape and the dominance of effusive eruptions (as it would facilitate degassing).[58] Seismic and electric tomography indicate the presence of a hot zone in the crust, which may be a developing batholith.[24]
The Aucanquilcha complex lies northwest of the Altiplano–Puna volcanic complex (APVC), a local large igneous province. The APVC is underpinned below at a depth of 20 km by a slow seismic velocity zone that has been linked to the presence of 15–25% of partial melts in the zone. The Aucanquilcha complex is much smaller volumetrically than the APVC ignimbrites, but the duration of activity and the location indicate that Aucanquilcha is a subcomponent of the APVC complex.[38] The volcano might be a surface manifestation of copper porphyry deposits and a batholith[40]-plutonic complex resembling the Tuolumne Intrusive Suite of the Sierra Nevada.[59]
Composition
The rocks from the main Aucanquilcha volcano are uniformly dacitic and show little evidence of composition changes over time,[60] while the Aucanquilcha complex produced both andesite and dacite. Andesites appear as lava flows while dacites form lava domes and dome complexes.[18] The rocks define a calc-alkaline suite[61] rich in potassium (content ranges from 1.5 to 4%[62]), typical for Central Andean volcanoes and subduction zone volcanoes in general.[39][20] Plagioclase is the dominant component of the magma. Clinopyroxene + orthopyroxene + amphibole (hornblende and pargasite) or amphibole + biotite + minor amounts of pyroxene are subordinate components. Anhydrite, apatite, ilmenite, magnetite and zircon can also be found.[60][63][64] Rocks have a porphyritic texture and the more recent (last 1 million years) rocks contain inclusions of mafic rocks.[65] Basaltic andesites typically are less than 10% crystals while dacites generally are more than 20% crystals. The Alconcha group lavas form two distinct families: Early lavas are crystal-poor and lack biotite, later rocks contain biotite and more crystals.[66] There is evidence of magma mixing and mingling,[60][38] and of multiple generations of crystals being extracted from the magma reservoir[67] especially during inactive periods.[68] The magmas form at 5–20 km depth.[69]
Various parts of the main volcano have been subjected to hydrothermal alteration[36] and alteration by fumarolic activity, especially the central parts of the complex[18] and the Azufrera stage edifice.[36] Hydrothermal alteration may be driven by the formation of a deep magma reservoir and resulting hydrothermal circulation in overlying rocks.[70] The summit area and the area between the Azufrera and Angulo complex feature talus deposits containing sulfur,[36] which formed at temperatures of 450 °C[71] in a now extinct fumarole.[72] Some of the sulfur may have been emplaced in liquid form.[73] The geologist Friedrich Ahlfeld in a 1947 publication reported ongoing formation of sulfur crystals in a cave on the summit.[74] Apart from sulfur, pyrite[75] and hypogene-derived copper sulfides[76] such as covellite and idaite occur on Aucanquilcha[77] in the sulfur deposits, cementing volcanic rocks.[78] The copper sulfides found in the area appear to have formed through postvolcanic epithermal mineralization above deep porphyry copper mineralization,[79] and before the sulfur deposits.[80]
Magma output and evolution
The Aucanquilcha complex had a fairly stable magma output between 12 and 6 million years ago, followed by an increase that peaked between 4 and 1 million years ago (with a possible hiatus between 2 and 1 million years ago).[81] The long-term magma output of Aucanquilcha is comparable to the magma output of other long-term active volcanoes in the central Andes such as Ollagüe and Llullaillaco. In all such cases, an early peak in magma output is followed by later lower-volume activity (0.1 to 0.2 km3/ka, followed by 0.01 to 0.02 km3/ka). Unzen in Japan and Mount Duff and Lassen Peak in California have similar eruption histories.[82] Such decreases may occur because of the lithostatic load imposed by the edifices on the magma chambers and the increased travel distance of the magma through the edifice.[83] The low output of Aucanquilcha relative to other volcanoes in the region might reflect the fact that it is located at the edge of the Altiplano-Puna volcanic complex,[84] and might explain why no major caldera-forming eruption ever took place.[85]
The repeated formation of magma chambers heated the crust under the volcano, warming the magmatic system.[86] This crustal feedback and increased deep crustal influx of mantle-derived basalts drove increased magma production,[40] and ephemeral shallow magma chambers formed which were supplied from the deeper reservoir.[87] Eruption rates and hydrothermal activity increased,[88] and crystal populations in the magmatic system shifted.[89] Four million years ago the magmatic system became centralized[90] and stable, allowing the continuous production of dacitic magmas.[91] Dacite built up under the volcano and formed a barrier to the ascent of denser magmas,[84] so that andesite was spatially segregated with the peripheral Miño Volcano while the more central volcanoes erupted dacites.[92] The Aucanquilcha volcanic complex has been interpreted as the surface component of a developing pluton.[65]
Crustal rocks were absorbed in the magma, especially the more evolved (dacitic) ones[93] and during declining stages.[94] Magma and included crystals being drawn from depths of 3 to 23 km during the main Aucanquilcha stage of volcanism,[38][95] with evidence of stronger crustal contributions or of a change of their composition.[93] Based on geothermometric data, the highest temperatures occurred during phases of high activity and lower temperatures are associated with low output periods.[86]
Eruptive history
Volcanic activity of the Aucanquilcha cluster commenced 11 million years ago.[9] From 6-5 million years ago, activity increased, and at the same time the magmas became more uniform in composition and strong hydrothermal alteration commenced. The Aucanquilcha cluster generated about 340±20 km3 of volcanic rock,[38] with each centre being active for a few hundred thousand years.[84] Over time, centres became less distributed and their magmas more uniform.[96] Activity waned 2-1 million years ago:[38][95] the Aucanquilcha volcano proper may be a waning stage of the overall cluster.[40] Both the timing[93] and the duration of volcanic activity of the Aucanquilcha cluster are comparable to that of the Altiplano–Puna volcanic complex.[97]
Aucanquilcha itself began erupting about 1 million years ago, producing mostly lava flows with little variation in eruption style[98] and with a prolonged decline after an initial phase of high output.[99] Eruptions occurred every 50,000-100,000 years, with breaks as long as 250,000 years.[100] The age of the lava flows ranges from heavily glaciated andesite flows underlying less-eroded ones to possibly postglacial lava flows that may be tens of thousands of years old.[18] The site of volcanic activity has migrated over time.[101]
Stages
Both the Aucanquilcha cluster and Aucanquilcha proper formed in four stages each:
- The Alconcha group, with seven volcanoes, is constructed from andesite and dacite and formed 11–8 million years ago. It consists of two northern composite cones, Alconcha and Volcan Tuco (also known as Cerro Garage, dated 10.96–10.51 million years), and five lava domes on the northeastern side of the cluster. Alconcha has a large breach on the southern side of its crater that is likely the product of a flank collapse[92] but the avalanche deposit may be buried beneath younger material. Lavas within the breach are dated 10.78–10.43 million years. The centres of Volcan Tuco and Alconcha are heavily eroded, and Alconcha's lavas and scoria lie on top of Tuco. The dacitic Ujina ignimbrite was erupted 9.4 million years from an unknown vent and has a volume of 2 km3. While the vent location is unknown, the composition of the ignimbrite, and its dating and distribution, indicate an association with this group. The domes are poorly researched, with the Coscalito dome dated 8.9–8.7 million years and Cerro Amincha 8.01.[102] The total volume of this group is 46 km3, indicating a flux rate of 0.013 km3/ka.[103]
- The Gordo group, which erupted 6–4 million years ago following a probable 2-million-year hiatus,[92] is located in the southern and western parts of the cluster. Cerro Gordo itself (5.49 million years) has a crater that is breached westwards, exposing about twelve radial dykes but with no trace of a debris avalanche. One of the larger centres of the cluster, Gordo is associated with a lava field on its western side that is dated 4.9 million years. Cerro Puquíos and Cerro Negro (5.81–5.28 million years) lie on the southern side of the cluster, and glacial cirques cutting their northeastern flanks reveal layers of scoria and lavas. Puquíos has an amphitheatre structure on its western side. Paco Paco (4.41–4.27 million years) is located north of most Gordo group volcanoes. It forms a 4 km wide stratocone with a lava-filled crater, and layers of scoria and agglutinated lavas dip from it. Volcan Pabellón (4.14–4.12 million years) sits southwest of the Puquíos-Negro ridge. The Las Bolitas lava field (5.23–5.13 million years) is associated with the Gordo group but the locations of its vents are unknown.[81] The total volume of this group is 55 km3, indicating a flux rate of 0.027 km3/ka.[103]
- The 3.6–2.3 million years Polan group[81] is the largest group in the cluster. It includes ten dispersed volcanoes, such as Tres Monos, La Luna, Cerro Polan, Chaihuiri, Miño Volcano and the lavas of the Aucanquilcha platform. Cerro Polan's (3.5–3 million years) eastern side is deeply dissected, and the exposed materials are heavily altered in the deeper sections. Lava fields to Polan's west and southwest (2.6 million years on one western field) are associated with it. La Luna (2.97–2.57) lies just east of Polan; these two mountains were probably one volcano in the past. La Luna has a lava dome surrounded by a glaciated but unaltered lava table. Cerro Tres Monos (3.4–2.78 million years) forms a northbound 14 km long ridge with at least six vents. Hydrothermal alteration has affected some lavas and pyroclastics from Tres Monos, and the western side has lateral and terminal moraines. The Aucanquilcha platform (3.6–2.7 million years) sits underneath the main Aucanquilcha volcano, and its lava mostly flowed north. Its southern side is a 4500 m table with one hill, Cerro Campana, dated to 3.3 million years. The platform presumably forms one third of the total volume of the Aucanquilcha cluster[104] and may have originated from a part of the ridge of the La Luna-Polan trend, now buried beneath Aucanquilcha. Chaihuiri (2.39 million years) is a lava dome with moraines and two short lava flows; it is the youngest Polan group volcano.[37] The total volume of this group is 154 km3, indicating a flux rate of 0.077 km3/ka.[103]
- The main Aucanquilcha volcano is the youngest volcano in the cluster[9] and formed in four stages:
- Between 1.04 and 0.92 million years during the Azufrera stage, the bulk of the volcano formed.[29] A vent at 6116 m altitude fed most of this edifice; a second vent on the northern flank at the 5887 m summit generated three lava flows, two shorter ones and a long one to the northwest. One lava flow toward the southwest is unusually long, at 6 km. The Azufrera stage lavas are blocky dacites with large clasts and flow fronts up to 20 m high. These flows are moderately altered and have oxidation rinds. There is little evidence of explosive activity, but it may have been obscured by glacial erosion.[36] The total volume is 21.1 km3, indicating a flux rate of 0.16 km3/ka.[60] This volcano was probably an isolated cone, but the existence of a previous stage cannot be excluded.[105]
- The second stage, named Rodado, lasted from 0.95 to 0.85 million years. It formed on the eastern slopes of the Azufrera volcano, with one vent at the 6073 m summit. Rodado stage lavas are blocky, platy and usually thicker than Azufrera stage lavas. Some of the summit vent lavas are among the most vesicular of this stage. They are also less weathered (oxidation rinds are c. 1 °Cm thick) and less subject to solfataric alteration. The Cerro Chinchillas lavas are the oldest of this stage; erupted from an unknown vent, they lack amphiboles.[36] The total volume is 9.1 km3, indicating a flux rate of 0.09 km3/ka.[60] A flank collapse, possibly triggered by a large earthquake, occurred during this stage.[105]
- The third stage is the Cumbre Negra stage, named after the westernmost summit and principal vent of this stage, Cerro Cumbre Negra (5670 m). The timing of its activity is less defined than the previous two stages; it may have occurred between 1–0.47 million years, but most likely 0.6–0.5 million years based on potassium–argon dating. Four lava flows derived from the main vent, all less than one kilometre long and 40–60 m thicker than previous stages. They all have hydration rinds but no native sulfur deposits. This stage generated Aucanquilcha's only pyroclastic flow[g] during a lava dome collapse.[36] The total volume of this stage is 0.7 km3, indicating a flux rate of 0.005 km3/ka.[60]
- The youngest stage, known as Angulo, lasted from 0.66 to 0.2–0.23 million years. It took place between the Azufrera and Rodado stage edifices,[36] on a 1 km long ridge that includes Aucanquilcha's highest summit and which became the source of most of the Angulo lava flows. One crater on the northeast side of the ridge fed lavas to the north. Other than that, most flows extend southwards 4 to 9 km from the vent, and with the exception of a due south flow 50 m thick they are thin, with thicknesses of 15–20 m. One of the oldest flows has been compared in length to the 50% longer Chao Dacite flow but is much thinner. The flows from this stage are weakly weathered and partially overlie glacial deposits. The total volume is 5.8 km3, indicating a flux rate of 0.015 km3/ka.[60]
Last activity, fumaroles and hazards
The last dated eruption occurred 450,000±70,000 years ago.[106] Some scoria cones of basaltic composition, including Poruñita and Luna de Tierra, formed between Aucanquilcha and Ollagüe after Aucanquilcha's last activity.[96] There is no clear evidence of Holocene activity,[107] except possibly for lava flows overlying moraines,[105][22] and there are no known historical eruptions[108] or ongoing ground deformation.[109] There are active fumaroles[22] or hot ground,[75] most conspicuous in the trenches dug during sulfur mining operations.[100][h] The emitted gases have temperatures of 60–85 °C;[112] others describe them as "low temperature".[111]
The Chilean geology agency SERNAGEOMIN considers Aucanquilcha a low hazard volcano, ranking it 71st[i] out of 87 volcanoes as of 2023[update].[115] As of 2021[update] Aucanquilcha was not monitored.[116] Avalanches from the ice and snow,[19] lava flow emissions and minor explosive activity, confined to the edifice of the volcano, are the most important risks from renewed activity,[100] and a hazard map has been published.[42] There are signs that warn of volcanic danger in the area.[117]
Climate and vegetation
Temperatures at the summit are usually below freezing,[118][j] but owing to the thin atmosphere at this altitude[120] insolation is among the highest on Earth's surface[16] and can cause sunburns.[121] Mean annual precipitation at Aucanquilcha is unknown, but it did not exceed 100 mm per year at Ollagüe in 1963.[122] It occurs mostly during summer as the so-called Bolivian winter.[123] Aridity has prevailed here since the Miocene[39] but with short-term fluctuations, a more humid period between 14,000 and 9,500 years ago and a drier period between 9,000 and 4,000 years ago for example.[53] The summit region is windy[124] and can experience snowstorms,[125] and seasonal snow cover can reach a substantial thickness.[126]
Three distinct vegetation belts occur in the region. While the aridity prevents plant growth below 3100 m altitude, a sparse cover of Acantholippia punensis exists above this. Between 3750–3300 m vegetation is denser, featuring Baccharis boliviensi and Fabiana densa. A more diverse plant community is found between 4100 m and 3750 m, consisting of bushes and grasses. Species there include Azorella compacta, Festuca chrysophylla, Pycnophyllum and Stipa venusta. The occurrence of Polylepis has been reported. The exact vegetation structure depends on the availability of water.[127][123] Vegetation cover ends at about 4900 m.[128] Mice have been found around 4500 m;[129] regional mice populations are known to reach extreme altitudes.[130]
Glaciation
There is some snow and ice on the mountains,[131] as well as rock glaciers between 5200–5500 m[132] and permafrost down to 4385 m altitude.[133] With the exception of one 1999 report[134] sources agree that there are no active glaciers on Aucanquilcha[135][136] as the climate is too dry for glacier development despite the low temperature.[137]
During glacials a 45 km2 ice cap covered the volcano,[131] leaving cirques,[138] glacial striations[24] and extensive moraines[22] on both on the main volcano,[k] and its subsidiaries.[45] The exact altitude of the ice edge ranged between 4500–5200 m[l][24][139] with lower altitudes reached on the eastern and southeastern side.[140] At least two distinct glacier stages took place.[45] The development of glaciers in the region was probably a consequence of a wetter climate.[141]
Human activity and mining
A mine at 5950 m altitude on Aucanquilcha[142] is famous for being the highest mine in the world[m].[144][145] It produced sulfur ore with an ore grade of 30%[146] emplaced by fumaroles[147] in the area of hydrothermally altered rocks around the summit.[108] The mine was opened in 1913 by Julian B. Carrasco, who subsequently established the Compañía Minera y Azufrera Carrasco S.A in 1933,[148] in Ollagüe, moving to Amincha in 1950.[149] In 1942, the mine produced about 180 tons of ore per day,[150] in 1953 annual production was 12,000 tons[151] and in 1974 an annual production of 33,000 tons was reported.[152] The sulfur was transported down first with llamas, later by trucks[153] and eventually through an aerial cableway system from Quilcha/Quilca/El Ángulo to Amincha station[154][155][156] (3900 m)[15] where the sulfur was refined.[157] There are anecdotal reports of a railway.[158] The sulfur was then transported to Chuquicamata to be converted into sulfuric acid[159] or to Antofagasta to be shipped;[156] the Antofagasta-Bolivia railway was essential for the sulfur mining in the Ollagüe area.[160] In 1977 other sulfur mines were present to the west between Cerro Polan and Cerro Gordo and south of the main Aucanquilcha massif,[48] and another camp (Polan) is marked on modern maps west-southwest of Aucanquilcha.[42] Neighbouring volcanoes were also mined.[12]
In 1935, mining took place throughout the year[161] but typical workhours were only about 8 hours per day owing to the conditions.[162] Owing to the extreme conditions, sulfur from the mines in the Ollagüe area was only rarely competitive on global markets.[160] After an initial crisis in the 1950s,[163] sulfur mining began to decline in the Ollagüe region during the 1970s;[164] during the 1980s[165]–1990s the worker camps were abandoned.[149] Amincha was closed in 1992[165] or 1993,[166] and the last reported mining activity on the mountain was in 1993[167] or 1994.[20] The cessation of sulfur production in Chile during the 1990s was due to imported sulfur being cheaper and of higher quality.[168] The mines and adjacent infrastructure were investigated beginning in 2015 as part of the Alto Cielo Archaeological Project[169] and there has been research on the living conditions[170] and ethnic relations between Bolivian and Chilean workers in the region.[171]
There are still ruins of the cableway,[172] a relic network of roads leading up to 5900 m[20] as well as ruins of the Amincha and El Ángulo stations.[173] Apart from mining activity, an Inca mountain sanctuary with offerings of llamas has been reported to exist on Aucanquilcha.[174] Such Inca findings are common on mountaintops of the region.[126] Other archaeological sites are found around the volcano,[175] including the Inca road Qhapaq Ñan,[176] and there might have been copper mining at Miño.[177]
The inhabitants of Ollagüe viewed Aucanquilcha as the devil's mountain[178] and nicknamed it "El Rebelde".[144] Its masculine nature (reflecting the hard work of mining) was contrasted to the female, more ambiguous, interpretation of Ollagüe volcano.[179] Anecdotal reports indicate that mine workers presented offerings to the mountain to secure a high mine yield.[180] According to a local folktale, when the Spaniards attempted to rename the mountain to San José, it resisted as it had been named by the goddess Pachamama and occasionally threw sulfur and killed miners on the mountain.[181]
Altitude and habitation
Just below the mine[108] was (formerly)[n] the highest permanently inhabited place on Earth[30] in the form of a galvanized iron hut.[184] In 1986, several caretakers lived there, including Justo Copa who had been living there for two years;[o][186][184] they were the highest[p] human inhabitants on Earth.[188]
With increasing altitude, atmospheric pressure decreases and with it the availability of oxygen for breathing, eventually leading to altitude sickness.[189] Aucanquilcha has been used for studies on the effects of high altitude on human behaviour[190] and medical parameters. They indicated that the Aymara miners were fully acclimatized to the altitude, with less hyperventilation and higher hemoglobin than acclimatized people from lower areas,[191][192] and are more tolerant of the high altitude than the researchers who studied them in 1942,[193] although some European workers also managed to tolerate the environment.[126] Their families are born and raised at lower altitudes,[q][188] although they could handle the high altitude conditions as well.[194] Only a small fraction of the mineworkers could live on Aucanquilcha for longer timespans,[195] leading to a frequent turnover in personnel[196] and frequent sickness and mortality.[197]
See also
Notes
- Which in the Aymara language has a causative function.[5]
- During the Cumbre Negra stage, a pyroclastic flow occurred on the northwestern side of the volcano. It covered 34 km2 on a run of 10 km2 and now has a volume of 0.3 km3. It was at first identified as a debris avalanche, but the lack of hummocky topography and the presence of large juvenile blocks identify it as a pyroclastic flow.[36] The process through which it formed has been compared to the eruptions of Indonesia's Mount Merapi.[36] One block in the flow and the lava dome from which the flow originated have been dated at 0.6 million years.[37]
- The western Azufrera edifice was heavily glaciated in the past. At least three moraine stages have been mapped on that edifice, and on its southern side is found a modest cirque with glacially polished lavas on the floor. The Rodado stage edifice has several moraine stages on its southern slopes. Another small cirque with a moraine has been found in the northeastern side of the Cerro Cumbre Negra summit next to an Azufrera stage lava flow.[36] A small moraine lies on the south side of the Angulo edifice; some lavas from that edifice overlie glacial deposits.[60]
- The runner-up might have been the Ganesh Himal mine in the Himalayas.[143]
- Sites at comparable elevation include Indian Army outposts in the Himalayas;[182] some outposts at the Siachen Glacier might be at an even higher altitude.[183]
- An expedition in 1935, part of the International High Altitude Expedition,[187] found that 150 miners lived at an altitude of 5,300 metres (17,500 ft) in Quilcha[161] and reached the higher mine on foot. The expedition found that an even higher abandoned village at 5639 m existed, but miners refused to live there. The conclusion taken from the expedition was that 5334 m was the highest habitable altitude[187] but later investigations recognized that the caretakers lived at higher altitudes.[184]
- The highest known town with families is La Rinconada in Peru.[184]
