Licancabur (Spanish pronunciation: [likaŋkaˈbuɾ]) is a stratovolcano on the border between Bolivia and Chile, south of the Sairecabur volcano and west of Juriques. Part of the Andean Central Volcanic Zone, it has a prominent, 5,916-metre (19,409 ft)-high cone. A 400-metre (1,300 ft) summit crater containing Licancabur Lake, a crater lake which is among the highest lakes in the world, caps the volcano. Three stages of lava flow emanate from the volcano, which formed on Pleistocene ignimbrites.
|Elevation||5,916 m (19,409 ft) |
|Prominence||1,320 metres (4,330 ft)|
|Location||Chile / Bolivia|
|Age of rock||Holocene|
|First ascent||Inca, pre-Columbian|
Licancabur has been active during the Holocene, after the ice ages. Although no historic eruptions of the volcano are known, lava flows extending into Laguna Verde have been dated to 13,240 ± 100 BP. The volcano has primarily erupted andesite, with small amounts of dacite and basaltic andesite.
Its climate is cold, dry and very sunny, with high levels of ultraviolet radiation. Licancabur is not covered by glaciers, and vegetation such as cushion plants and shrubs are found lower on its slopes. Chinchillas were formerly hunted on the volcano.
Licancabur is considered a holy mountain by the Atacameno people, related to the Cerro Quimal hill in northern Chile. Archeological sites have been found on its slopes and in the summit crater, which was possibly a prehistoric watchtower.
Geography and geologyEdit
The Andean Volcanic Belt consists of three main volcanic zones: the Northern Volcanic Zone (from 2° N to 5° S), the Central Volcanic Zone (16° to 28° S) and the Southern Volcanic Zone (33° to 46° S). Active volcanism occurs where the Nazca Plate subducts beneath the South American Plate. The plates are separated by shallower subduction zones, with no present-day volcanism. These shallower zones have been attributed to the high speed of the plate collision, the young age of the subducting oceanic lithosphere and the curvature of the subducting plate. The most plausible theory is that variations in buoyancy of a subducting plate creates a flat subduction zone. The Cocos, Juan Fernandez and Nazca Ridges are associated with such volcanic gaps where they collide with the oceanic trench. The subduction of spreading ridges can also diminish volcanism, as observed in the Chile Rise further south. The buoyancy of these crustal structures may hinder subduction, reducing water supply to the mantle and inducing the formation of melts.
Not all volcanism in Chile is relative to subduction of the Nazca Plate; the Chile Ridge exhibits submarine volcanism, and volcanism in the Austral Volcanic Zone is triggered by the Antarctic Plate subducting beneath the South American Plate. One hundred ninety-eight South American volcanoes are on the Global Volcanism Program's Holocene volcano list.
Licancabur is part of the Central Volcanic Zone at the western edge of the Altiplano. Among the region's active volcanoes are Putana (erupted at the end of the 19th century), Llullaillaco (1868) and Lascar (1993).[a] Other stratovolcanoes are Tacora, Nevados de Payachata, Isluga, Tata Sabaya, Ollague, Tocorpuri, Sairecabur and Socompa. The Central Volcanic Zone has more than 1,100 volcanic centres—many older than the Pleistocene, since the area's prevailing arid climate prevented substantial erosion. During the Miocene, the area around Licancabur became the site of major ignimbrite-forming eruptions. Llano de Chajnantor (southeast of Licancabur) is the site of several observatories, including the Llano de Chajnantor Observatory.
The volcano is just south of Sairecabur, a group of volcanoes which rises to 5,800 metres (19,000 ft) and is an apparent source of recent volcanic activity. East of Licancabur is its companion volcano, Juriques. This 5,710-metre (18,730 ft)-high volcano has a large—1.5 kilometres (0.93 mi)—deep crater and is considered a parasitic cone. West-east alignments of volcanoes like Licancabur and Juriques are common in the region, due to tectonic influences. Araral, Cerro Cabana, Cerro Canapa, Cerros de Tocorpuri, Cerro Linzor, Inacaliri, Inca, Jardin, Putana, Volcan Tatio and Zapaleri are other volcanoes in the neighbourhood of Licancabur. Nineteen kilometres (12 miles) southeast, the volcanic chain continues with Tocol, the Purico Complex and the 6,723-metre (22,057 ft)-high Llullaillaco. Volcanoes in the Puna de Atacama formed during the Pliocene on Tertiary dacite, liparite and rhyolite ignimbrites. These rocks have a light colour, due to the rhyolite. Licancabur was formed over 1.35-million-year-old Purico, La Pacana and Chaxas ignimbrite. The Chaxas ignimbrite erupted 1.09 ± 0.56 million years ago.
Licancabur is a 5,916-metre (19,409 ft)-high symmetrical cone. The cone, rising 1,500 metres (4,900 ft) above the surrounding terrain, has a base diameter of 9 cubic kilometres (2.2 cu mi) and a total volume of 35 cubic kilometres (8.4 cu mi). The top of the mountain is a 400-metre (1,300 ft)-wide crater, and its slopes have an approximately 30° gradient. The volcano has erupted blocky lava flows, with thicknesses ranging from 50 to 10 metres (164 to 33 ft); younger lava flows are thinner. Young lava flows on the western sides of the volcano are 6 kilometres (3.7 mi) long; older flows extend 15 kilometres (9.3 mi). Some old lava flows reach Laguna Verde, and 12-kilometre (7.5 mi)-long pyroclastic flow deposits have been found. The volcano's eastern and western flanks look different, since it formed on a basement which dips towards the Salar de Atacama. West of Licancabur are deposits stemming from debris avalanche activity, including blocks 10 metres (33 ft) wide. The border between Bolivia and Chile, defined by the Treaty of Peace and Friendship (1904), crosses the volcano.
An elliptical lake was identified in the Licancabur crater 90 metres (300 ft) beneath the crater rim, with a length of 85 metres (280 ft) and a depth of 1.5–3.0 metres (5–10 ft). Fed by snowfall, it is one of the highest lakes in the world. Based on its relative lack of salt deposits, in 1955 researchers postulated that the lake spilled through a 9.1-metre (30 ft) notch in the crater's southwestern rim when the climate was wetter. Excess water now leaves through seepage, keeping salt levels low. There are other lakes (usually frozen) at similar altitudes in the Andes.
The slopes of Licancabur are unstable and prone to rock falls. Some of the instability may be due to earthquakes, snow, wind or geothermal effects (resulting in thermal stress), and it frustrated a 1920s attempt by a Chuquicamata engineer to climb the mountain.
Licancabur has erupted primarily andesite, but basaltic andesite and dacite have also been found. The rocks are dark and grey-coloured. Basaltic andesite was found in the older lavas, and dacite in the more-recent ones. Although the rocks have a seriate texture, the groundmass is hyalopilitic. Phenocrysts include amphibole, clinopyroxene, hornblende, orthopyroxene, plagioclase and titanomagnetite; olivine is found in andesite, and biotite in dacites. Plagioclase is the most common. The amount of phenocrysts in Licancabur's rocks is smaller than that in other Central Volcanic Zone volcanoes, such as Lascar.
Clots of crystals with diameters of 2–3 millimetres (0.079–0.118 in) or larger have also been found. They contain glass, microliths and phenocrysts, and have a composition similar to phenocrysts. The clots probably formed from the aggregation of phenocrysts and their subsequent growth; some phenocrysts in the rocks formed when the clots broke apart.
The temperature of Licancabur's pre-eruption magma determined the composition of the rocks; it ranges from 860 to 1,060 ± 20 °C (1,580 to 1,940 ± 36 °F) for andesite and 930 ± 20 °C (1,706 ± 36 °F). Isotope ratios are typical of Central Volcanic Zone volcanoes. There are differences in the elemental composition of andesites and dacites, with the latter resembling adakites more than the former. Antisana (in the Northern Volcanic Zone) and El Negrillar (in the Central Volcanic Zone) are two other centres which have erupted adakites or adakite-like lavas.
Based on its composition, it is assumed that the magma at Licancabur formed from the partial melting of the oceanic crust subducted at the Peru-Chile Trench after metamorphosis. This magma melted part of the mantle wedge above the subducting plate, mixing with the melt products. Further contamination by crustal Tonalite-Trondhjemite-Granodiorite-like rocks from the Archean, crystal fractionation and magma mixing further up in the crust then yielded the Licancabur magmas. The younger lavas may have formed from the mixing of dacite with the magmas forming the older lavas. Some inclusions in Licancabur rocks seem to be from wall rocks of the magma chamber.
Xenoliths containing gabbro are also found. Unlike neighbouring volcanoes, such as Saciel at Sairecabur (further north) and Tocol (further south), there appear to be no sulfur deposits on Licancabur.
Climate and ecosystemEdit
The region's climate has been dry since the Tertiary. The area around Licancabur is dominated by year-round high pressure caused by the South Pacific High, giving it a very sunny climate. Because of the lack of moisture, solar radiation energy is dissipated primarily by wind. In the Llano de Chajnantor area, wind generally reaches its maximum strength during the day. Its prevailing direction is from the west, except in summer when winds are more variable. Because of the area's tropical location (where the ozone layer is thinner) and high altitude, it receives a large amount of ultraviolet radiation. The world's highest level of ultraviolet radiation was reported from Licancabur, although the high irradiation might have caused measurement artifacts.
Air temperatures obtained at the lake range from 5 to −40 °C (41 to −40 °F). According to observers in 1955, temperatures at the Licancabur summit were always below freezing, sometimes falling below −18 °C (0 °F). At Llano de Chajnantor, southeast of Licancabur, weather records indicate that maximum temperatures range from −15 to 15 °C (5 to 59 °F).
Average precipitation on Licancabur is estimated at about 360 millimetres (14 in) per year, but snowfall probably exceeded 4,300 millimetres (14 ft) in 1955. Snow has been recorded at Llano de Chajnantor when easterly winds transport moisture from the Amazon to the area in summer. Licancabur has no persistent snowpack; snow deposited by storms usually disappears within a few days. In sheltered areas, however, it can persist for months. Licancabur's present snow line is estimated at 6,190 metres (20,310 ft).
Vegetation at lower altitudes is typical of a high tropical desert climate. Three biozones have been described in the region: an Andean zone from 3,850 to 4,200 metres (12,630 to 13,780 ft), with cushion plants and tussock grass; a Puna zone from 3,100 to 3,800 metres (10,200 to 12,500 ft), and a pre-Puna zone from 2,700 to 3,100 metres (8,900 to 10,200 ft) with thorny shrubs. In oases and river valleys of the depression between the pre-Cordillera and the Andes, shrubs such as Atriplex grow; however, the surrounding Atacama Desert is mainly devoid of plant life.
Meltwater from snow supports more life, at higher altitudes, on Licancabur than on similar mountains. Grasses, tola bushes, butterflies, flies and lizards are found as high as 4,900 metres (16,000 ft). Life further down the mountain could be supported by the fertilizing effect of dust from volcanic rocks. Polylepis incana might have been more prevalent at Licancabur during wetter times, and is now more common in Bolivia. Chinchillas were found as high as 4,900 metres (16,000 ft) in 1955. The upper parts of the mountain had been avoided by hunters, and after some high-altitude attempts during the 1920s chinchilla hunting disappeared from the area. Licancabur is part of the Eduardo Avaroa Andean Fauna National Reserve.
Licancabur formed in three units, all of which have lava flows; the last one also includes pyroclastic deposits. The bulk of the cone was formed by the second unit. The second unit's eruption was preceded by the injection of basic magma into the magma chamber. The oldest flows crop out on the western and northern sides of the volcano and are partially covered by more-recent flows from Licancabur and flows from Sairecabur. Flows from both appear to be pre-glacial. The older lavas have compositions similar to shoshonite and old Sairecabur lavas, and tend to be more basic than recent lavas. Weak explosive activity left pyroclastic deposits on the volcano. Licancabur formed primarily after the late glacial period, between 12,000 and 10,000 years ago. Flank lava flows are its youngest feature. The neighbouring Juriques dates to the Pleistocene.
Licancabur's lava flows were not affected by glaciation, and some have levees and ridges. Lava flows reaching Laguna Verde have been radiocarbon dated to 13,240 ± 100 BP, and the volcano has not erupted during recorded history. Its crater lake may remain liquid due to geothermal heating.
Despite being lower than many neighbouring mountains, Licancabur stands out from other volcanoes in the region and is well-known. The Atacameno people worshiped it, and other high mountains are still considered sacred. Licancabur was considered divine, and attempts to climb it were discouraged and sometimes met by force; climbing it supposedly brought misfortune. It is said that Licancabur would punish people who climbed it, and the volcano is the mate of Quimal in the Cordillera Domeyko; at the solstices, the mountains overshadow one another. According to local myth, this copulation fertilizes the earth. Licancabur is considered "male" and a mountain of fire, in contrast to San Pedro (considered a mountain of water). The 1953 Antofagasta earthquake was considered divine retribution for an attempt to climb the mountain that year. According to legend, a golden object (most commonly a guanaco) was offered as tribute in the summit crater; human sacrifices have been reported on the volcano.
In 1953, climbers found three buildings open on one side on Licancabur. They were built in the pirca style, where stones are fitted together without mortar. A woodpile was found between two of the buildings, which were described as two dwellings and a fireplace. Wood was also scattered around its crater. With the summit's panoramic view, which includes Calama and pass routes from Argentina, Licancabur may have been a watchtower for the Atacamenos. Its watchtower function may have been coordinated with fortresses in the area such as Lasana, Turi and a settlement identified in 1955 at Quebrada de Chaxas (northwest of the volcano). The settlement at Licancabur had a central courtyard, surrounded by buildings, and ceramics found there resemble these of Pukará de Quitor and Toconao Oriente. A tambo reportedly existed at the volcano.
Other archeological findings on Andean mountains were made on Acamarachi and Pular (where ceremonial platforms were found), Cerro Colorado, Juriques, Llullaillaco, Miniques and Quimal. Sites had pirca structures and firewood, and some may have been part of a signaling system. Many were in use during the Inca civilization, and on Quimal artifacts and reports of use during the Spanish Empire have been found. Aconcagua, Coropuna, Chachani, El Plomo, El Toro, Llullaillaco, Mercedario and Picchu Picchu are other mountains with Inca sanctuaries.
The area around Licancabur was first settled by the Atacameno people, presumably because of the water in local canyons. The Incas, under Yawar Waqaq, were followed by the Spanish during the early 16th century in the region; both were looking for yareta and chinchillas.
Unlike neighbouring mountains, Licancabur is difficult to climb; its upper part slopes steeply, and the ground is loose and prone to landslides. Rumours about a "staircase", later probably obliterated by landslides and rockfalls, were reported in 1955. In 1953, a road climbed to 4,300 metres (14,000 ft). The first recorded ascent of the volcano was in 1884 by Severo Titicocha, who was accompanied by Juan Santelices (a delegate of the Chilean government) in an 1886 ascent.
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