Uturuncu

Uturuncu is a dormant volcano in the Sur Lípez Province of Bolivia. It is 6,008 metres (19,711 ft) high, has two summit peaks, and consists of a complex of lava domes and lava flows with a total volume estimated to be 50–85 km3. It bears traces of a former glaciation, even though it does not currently carry glaciers. Volcanic activity took place during the Pleistocene epoch and the last eruption was 250,000 years ago; since then Uturuncu has not erupted but active fumaroles occur in the summit region, between the two summits.

"Uturunku" redirects here. For the mountain in Peru, see Uturunku (Peru).

Uturuncu
Uturuncu is a cone in a desolate landscape, with an adjacent smaller non-conical mountain.
Uturuncu seen from the northwest
Highest point
Elevation6,008 metres (19,711 ft)
Parent peakAcamarachi
ListingList of mountains in Bolivia
Coordinates22°16′12″S 67°10′48″W[1]
Naming
English translationJaguar
Language of nameQuechua
Geography
A map of Bolivia; the volcano is in the southernmost corner.
A map of Bolivia; the volcano is in the southernmost corner.
Location of Uturunku in Bolivia
LocationSan Pablo de Lípez Municipality, Sur Lípez Province, Potosí Department, Bolivia
Parent rangeCordillera de Lípez
Geology
Age of rockPleistocene
Mountain typeStratovolcano
Volcanic fieldAltiplano–Puna volcanic complex
Last eruption250,000 years ago.
Climbing
First ascent1955 by Friedrich Adolf Ernest Ahlfeld

The volcano rises within the Altiplano–Puna volcanic complex, a larger province of large volcanoes and calderas which over the last few million years (mya) have emplaced about 10000 km3 of ignimbrites[lower-alpha 1] in sometimes very large eruptions. Underneath it lies the so-called Altiplano–Puna magmatic body, a large sill[lower-alpha 2] formed by partially molten rocks.

Starting in 1992, satellite observations have indicated a large area of regional uplift centered on Uturuncu, which has been interpreted as an indication of large-scale magma intrusion under the volcano. This might be a prelude to large-scale volcanic activity, including "supervolcanic" activity and caldera formation.

Geography and geomorphology

Uturuncu lies in the San Pablo de Lípez municipality of the Sur Lípez area of southern Bolivia,[4][5][6] southeast of the town of Quetena and just northeast of the Eduardo Avaroa Andean Fauna National Reserve in the Cordillera de Lípez.[1][7][8] The region is almost uninhabited and the volcano was little known until ongoing large-scale ground deformation was discovered in the early 21st century; since then scientific interest and activity has increased, including a reconnaissance mission carried out by scientists in 2003,[1][9] and numerous geophysical studies have been carried out on the volcano.[10] The volcano has been used to reconstruct the regional history of glaciation.[11] The term uturuncu means 'jaguar' in the Quechua language.[12] The volcano is visible from afar.[13] Today Uturuncu is a tourism target.[14]

It was first ascended in 1955 by Friedrich Adolf Ernest Ahlfeld (Germany), but like other volcanoes in the Puna region miners and native inhabitants may have ascended it earlier.[15] A former sulfur mine named "Uturuncu" is situated on the mountain, close to the summit,[16][17] and was considered to be one of the highest in the world.[13] It reportedly contained reserves of 50 million tons of ore, consisting mainly of sulfur with some realgar which is dispersed among tephra[lower-alpha 3] deposits and contains large amounts of arsenic.[19][20] A winding road that served the sulfur mine leads up the mountain, and roads pass along the northern, eastern and southwestern feet of Uturuncu.[21][22][7][8]

Structure

At an elevation of 6,008 metres (19,711 ft), Uturuncu is the highest mountain in southwestern Bolivia.[23][24] It dominates the regional geomorphology,[25] rising about 1,510–1,670 metres (4,950–5,480 ft) above the surrounding terrain and there is a good view of the surrounding mountains from the summit.[13][26][27] The volcano has two summit peaks,[26] one 5,930 metres (19,460 ft) and the other 6,008 metres (19,711 ft) high.[28] They are about 1 kilometre (0.62 mi) apart and separated by a saddle that is 5,700 metres (18,700 ft) high.[28][29] Uturuncu is a stratovolcano with remnants of a crater,[1][13] and consists of lava domes and lava flows erupted from a number of vents in the central part of the volcano.[30]

About 105 lava flows propagate outward from the central sector of the volcano,[30][31] reaching lengths of 15 kilometres (9.3 mi) and featuring levees, flow ridges and steep, blocky fronts over 10 metres (33 ft) thick.[24][30] The northernmost lava flow is known as Lomo Escapa and with a length of 9 kilometres (5.6 mi) it is also the largest lava flow at Uturuncu.[32][33] Five lava domes south, west and northwest of the summit form a northwest–southeast trending alignment that appears to be an older volcanic system;[34] the southern of these domes have volumes of about 1 km3 and the western dome bears traces of a large collapse.[33][35]

The broad edifice of the volcano covers an area of about 400 square kilometres (150 sq mi) and has a volume of 85 km3–50 km3.[24][36][37] It appears to consist entirely of lava flows and lava domes;[38] while the occurrence of pyroclastic flow deposits was reported at first,[30] later research has not found any evidence of explosive eruptions.[26] Aside from volcanic deposits there are also traces of glaciation that has smoothened the slopes of Uturuncu,[24] as well as Pleistocene and Holocene alluvium[lower-alpha 4] and colluvium.[lower-alpha 5][30]

Lakes and rivers

Several lakes surround Uturuncu. Mama Khumu lies on the eastern foot of Uturuncu and is bordered by steep slopes;[30][41][42] Laguna Celeste is located northeast of Uturuncu,[41][30] Chojllas southeast of the volcano and Loromayu to the south.[41] The first two receive their inflow from Uturuncu.[43] Beach terraces,[44] deposits of diatomaceous earth[lower-alpha 6] and former shorelines are visible around the lakes.[46][47] The Rio Grande de Lípez flows along the western foot of the volcano and receives tributaries which originate close to Uturuncu's northeastern foot;[41] it eventually flows into the Salar de Uyuni.[48] These watercourses are usually confined between steep bedrock walls and are characterized by gravelly beds, anastomosing channels[lower-alpha 7] and wetlands[47] that are used to keep llamas and sheep.[9]

Geology

Regional

The eastward subduction of the Nazca Plate beneath the South American Plate has generated three volcanic belts within the Andes,[50] including the Central Volcanic Zone,[1] which spans parts of Peru, Chile, Bolivia and Argentina and includes Uturuncu.[1][31] Aside from Uturuncu, it includes about 69 Holocene volcanoes in a high elevation region,[51] such as the potentially active volcanoes Irruputuncu, Olca-Paruma, Aucanquilcha, Ollagüe, Azufre, San Pedro, Putana, Sairecabur, Licancabur, Guayaques, Colachi and Acamarachi.[52]

Local

Uturuncu has formed about 100 kilometres (62 mi) east of the main volcanic front in the Western Cordillera, in a terrain formed by various volcanic and sedimentary rocks of Miocene to Quaternary age.[52] The region is characterized by the Altiplano high plateau, which reaches an elevation of 4,000 metres (13,000 ft) and is only exceeded by Tibet in dimension.[53][54]

The Vilama (8.41 mya old) and Guacha (5.65 mya old) ignimbrites underlie the volcano and crop out in the Quetena River valley.[55][56] The Vilama lavas (4 mya old) are found southwest of Uturuncu and are partly buried by the volcano.[26] The crust in the region is about 65 kilometres (40 mi) thick.[53]

Volcanic activity in the area occurred between 15 and 10 mya ago.[25] Cerro San Antonio,[41] a Miocene volcano with a westward-opening collapse scar, lies just north of Uturuncu.[30] It is heavily eroded and 3 mya old.[57] Other volcanoes from east counterclockwise to west are the Cerro Panizos caldera, Cerro Lípez, Suni K'ira and Quetena volcanoes as well as many more minor volcanic centres. Many of them formed along northwest–southeast trending lineaments such as the Lipez-Coranzuli and Pastos Grandes-Cojina lineament that passes through Uturuncu.[52][58]

Geologic history and Altiplano–Puna volcanic complex

The geological history of the region is complex.[59] After subduction commenced in the Jurassic,[60] 26 mya ago the breakup of the Farallon Plate into the Cocos Plate and the Nazca Plate was accompanied by an increased subduction rate and the onset of the Andean Orogeny. This subduction process at first involved a relatively flat descent of the Nazca Plate until 12 mya ago, after which it steepened. The Altiplano–Puna volcanic complex formed beginning 10 mya ago,[59] with a volcanic flare-up occurring during the Miocene.[61]

The complex covers an area between 50,000 square kilometres (19,000 sq mi) and 70,000 square kilometres (27,000 sq mi) of the Altiplano-Puna in Argentina, Bolivia and Chile and consists of a number of calderas, composite volcanoes and about 10000 km3 of ignimbrite.[50][59][62][63] Uturuncu lies at its centre but unlike it most surrounding volcanic systems have been characterized by explosive eruptions,[64][65] including several so-called "supereruptions" with Volcanic Explosivity Indexes of 8 at Cerro Guacha, La Pacana, Pastos Grandes and Vilama.[54] Over 50 volcanoes in the region are potentially active.[62]

Within the last two mya, the Laguna Colorada, Tatio and Puripica Chico ignimbrites were erupted in the surrounding terrain.[66] The Atana (4 mya old) and Pastos Grandes (3 mya old) ignimbrites are other large ignimbrites in the area while the San Antonio ignimbrite (10.33 ± 0.64 mya old) is more sparse.[67][68]

The Altiplano–Puna volcanic complex is underpinned at about 20 kilometres (12 mi) depth by a wide magmatic sill where rocks are partially molten, the Altiplano–Puna magmatic body.[63] Its existence has been established with various techniques;[64] it extends over an area of 50,000 square kilometres (19,000 sq mi) and has a volume of about 500000 km3 with a thickness variously estimated at 1–20 kilometres (0.62–12.43 mi);[31][50][55] about 20-30% of its volume is melt.[10] It has been referred to as the largest reservoir of magma in the continental crust of Earth.[69] The Altiplano–Puna magmatic body is the source of magmas for many of the volcanoes in the Altiplano–Puna volcanic complex.[70] Its magma is extremely water-rich, consisting of about 10% water by weight;[71] in addition, about 500000 km3 of brine[lower-alpha 8] are contained in the rocks underneath Uturuncu.[73]

Composition and magma genesis

Uturuncu has erupted dacite[1] (as well as andesite in the form of inclusions within the dacite). Rocks are vesicular[74] or porphyritic[lower-alpha 9] and contain phenocrysts[lower-alpha 10] of biotite, clinopyroxene, hornblende, ilmenite, magnetite, orthopyroxene, plagioclase and quartz[55][77] along with apatite, monazite and zircon within a rhyolite groundmass,[lower-alpha 11][79] and define a potassium-rich calc-alkaline suite.[80] Xenoliths[lower-alpha 12] consisting of gneiss, igneous rocks and norites have also been found;[24] the first two appear to be derived from country rocks while the third is a by-product of the magma generation process.[82][83] Additionally, the occurrence of cumulates, gabbros, hornfels, limestones and sandstones as xenolithic phases has been reported.[24]

Mixing processes involving hotter or more mafic magmas played a role in the genesis of Uturuncu rocks,[82] as did fractional crystallization[lower-alpha 13] processes and contamination with crustal rocks.[33][85] The origin of these magmas appears to relate to the Altiplano–Puna magmatic body, which generates melts through differentiation of basaltic magmas first to andesites and then to dacites before being transferred to the shallow crust below Uturuncu from where it was then erupted through buoyancy-dependent processes.[83][86][87] Magma composition has been stable over the history of the volcano.[88][89]

Glaciation

Modern Uturuncu features no glaciers;[6] however, perennial ice was reported in 1956,[48] remnants of snow in 1971,[90] the existence of sporadic snow fields in 1994,[5] and the summit area is occasionally ice-covered.[8] Evidence of past glaciation such as glacial striations, glacially eroded valleys,[37] both recessional and terminal moraines and roches moutonnées[lower-alpha 14] can be found on the northern, eastern and southern flanks of Uturuncu.[30][37][92][93] The past glaciation of Uturuncu was not extensive, owing to its steep flanks.[94] One valley on Uturuncu's southwestern flank has been subject to glaciology studies,[6] which identified a former glacier originating both from the summit and from an area about 0.5 kilometres (0.31 mi) south of the summit.[95][93]

This only weakly erosive glacier deposited five sets of moraines up to 5 metres (16 ft) high within the shallow valley; the lowest of these lies at 4,800–4,850 metres (15,750–15,910 ft) elevation and appears to be a product of an early last glacial maximum between 65,000 and 37,000 years ago, earlier than the global last glacial maximum. Afterwards, not much retreat occurred until 18,000 years ago.[93][96] During the Pleistocene, the snow line was about 0.7–1.5 kilometres (0.43–0.93 mi) lower than today.[97]

Conversely, the uppermost of these moraines is about 16,000–14,000 years old and correlates to a glacial advance in the Altiplano that has been linked to the maximum growth of the former Lake Tauca[98] north of Uturuncu and a wet and cold climate associated with Heinrich event 1.[95][99] At this same time 17,000–13,000 years ago, shorelines formed around the lakes that surround Uturuncu;[44][100] Lake Tauca may have been a source of moisture for Uturuncu.[101] After 14,000 years ago, the glacier receded at the same time as climate warmed during the Bolling–Allerod warming and the region became drier.[99]

Climate and vegetation

There is little information on local climatology, but mean annual precipitation is about 100–200 millimetres per year (3.9–7.9 in/year) or even less than that, most of it originating in the Amazon basin to the east and falling during December, January and February.[6][102] This low amount of precipitation is not adequate to sustain glaciers even though the summit of Uturuncu lies above the freezing level,[6] but it is enough to generate a seasonal snowcap on the mountain.[103] Annual temperatures in the region range between 0–5 °C (32–41 °F) and in 1963 the snowline was reported to exceed 5,900 metres (19,400 ft) elevation.[104][105]

The regional vegetation is relatively sparse at high elevations.[105] Polylepis trees are found on the lower slopes of the volcano;[106][107] the trees reach 4 metres (13 ft) in height and form forests.[108][27] They have been used as a source of tree ring climate records.[109]

Eruption history

Uturuncu was active during the Pleistocene.[1] A lower unit emplaced during the lower and middle Pleistocene (890,000–549,000 years ago[110]) makes up most of the peripheral sectors of the volcano, while an upper unit of middle to upper Pleistocene age (427,000–271,000 years ago[110]) forms its central sector[30] and is less extensive.[111] Several rocks have been dated through argon-argon dating and have yielded ages ranging from 1,050,000 ± 5,000 to 250,000 ± 5,000 years ago.[37] Dates of 271,000 ± 26,000 years ago have been obtained from the summit area,[30] 250,000 ± 5,000 for the youngest dated lava flow found just south-southeast of the summit and 544,000 years for the Lomo Escapa lava flow, while the aligned lava domes have been dated to be between 549,000 ± 3,000 and 1,041,000 ± 12,000 years old.[33][112] Overall, Uturuncu was active for about 800,000 years.[37]

Volcanic eruptions at Uturuncu were effusive[70] and involved the emission of voluminous lava flows (0.1–10 km3)[86] between pauses lasting between 50,000 and 180,000 years. The mean eruption rate was less than 60,000 cubic metres per year (2,100,000 cu ft/a)[113]-270,000 cubic metres per year (9,500,000 cu ft/a), much less than other rhyolitic volcanoes. There is no evidence of large ignimbrite eruptions nor of large flank collapses[24][114] but some lavas may have interacted with water or ice as they were erupted and were reportedly emplaced over moraines.[115][112]

Holocene and fumarolic activity

No large effusive eruptions have occurred since the 250,000 ± 5,000 eruption,[33] and Holocene or recent eruptions have not been reported.[111][116] At first, it was proposed that postglacial lavas existed,[110] but glaciation has affected the youngest lava flows.[24][25] The volcano is considered to be dormant.[6]

A snow-covered mountain slope is surmounted by steam clouds; mountainous landscape in the background
Fumaroles on Uturuncu

Active fumaroles occur in two fields below the summit,[116] with a number of tiny vents located between the two summit peaks;[17] vapour emissions are visible from close distance.[117] The summit fumaroles have temperatures of less than 80 °C (176 °F).[116] Their gases contain large quantities of carbon dioxide, water and larger amounts of hydrogen sulfide than sulfur dioxide perhaps due to the latter being filtered out by a hydrothermal system.[17] The fumaroles have emplaced abundant sulfur,[116] and silification[lower-alpha 15] has been observed.[119] Relatively invariant temperature anomalies (hot spots) have been recorded by satellites on Uturuncu[117][120] between its two summit peaks;[29] these temperature anomalies of about 15 °C (27 °F) are among the largest fumarole fields visible to satellites.[121] The existence of intense fumarolic activity on the northwestern slope at 5,500 metres (18,000 ft) was already reported in 1956.[13]

A spring on the northwestern flank produces water with temperatures of 20 °C (68 °F) and may be identical to the Campamento Mina Uturuncu spring which in 1983 was reported to produce 21 °C (70 °F) warm water at a rate of 5–7 litres per second (0.18–0.25 cu ft/s).[119][122] The presence of a weak hydrothermal system is likely[123][124] at Uturuncu although probably at great depth, considering the low temperature and spread out nature of the fumarolic activity.[66] There may be a shallow magma chamber below the volcano at 1–3 kilometres (0.62–1.86 mi) below sea level.[65][125]

Recent unrest and threats

Interferometric synthetic-aperture radar imaging has discovered that a region of about 1,000 square kilometres (390 sq mi) around Uturuncu is uplifting.[25][126] The uplift may have begun around 1965 but was first detected in 1992.[127] Between 1992 and 2006, the uplift amounted to 1–2 centimetres per year (0.39–0.79 in/year) in an area 70 kilometres (43 mi) wide,[1] with seasonal variations.[128] There are longer-term changes in the uplift rate,[110] such as a temporary acceleration after a 1998 earthquake,[129] a gradual slowdown either continuing[128][130] after 2017[127] or followed by an acceleration to about 9 millimetres per year (0.35 in/year) in the few years before 2017,[128] or constant deformation between 2010 and 2018.[131] The overall volume change between 1992 and 2006 was about 1 cubic metre per second (35 cu ft/s), with a total volume change of about 0.4 km3;[129] such rates are typical for intrusions in the Altiplano–Puna volcanic complex and historical lava dome eruptions and might reflect a short-term rate.[114]

The deformation is centered on an area 5 kilometres (3.1 mi) west of the summit and is most likely of magmatic origin given the lack of a large hydrothermal system at the volcano and the depth of the deformation.[129][132] The form of the deforming structure is not well known but it lies presumably at a depth of 15–20 kilometres (9.3–12.4 mi) below sea level.[53]

The uplifting area is surrounded by a ring-shaped area of subsidence (sinking),[64] which is occurring at a rate of 2 millimetres per year (0.079 in/year); the total width of deforming terrain is about 170 kilometres (110 mi) although it is not clearly visible in all InSAR data.[53][133] This joint uplift-subsidence has been called a "sombrero pattern" and the subsidence may reflect either a sideward or an upward migration of magma.[134][65] A second, shallow subsidence area has been found south of Uturuncu, which may relate to changes in a hydrothermal system.[130]

The deformation is most likely caused by magma intruding into the crust[70] from the Altiplano–Puna magmatic body,[135] with the intrusion taking place at a level below that where magma accumulated prior to past eruptions of Uturuncu.[136] The more recent changes may instead be a consequence of the upward movement of fluids, rather than magmatic processes.[137] It has been described as an ascending diapir,[lower-alpha 16][62][139] a plate-shaped intrusion[140] or as a growing pluton[lower-alpha 17][142] although an alternative theory holds the ascent of volatiles along a magma column reaching to the Altiplano–Puna magmatic body as responsible for the surface deformation; in that case the uplift might reverse over time.[133]

Such surface uplift has been observed at other volcanic centres in the Central Volcanic Zone but on a global scale it is unusual both for its long duration and its spatial extent,[143][144] and in the case of Uturuncu demonstrates the continuing activity of the Altiplano–Puna magmatic body.[145] There is no evidence for a net uplift in the geomorphology of the region,[66] and findings in the terrain around Uturuncu indicate that this uplift certainly began less than 1,000 years ago and likely also less than 100 years ago.[146] The uplift might be either a temporary deformation of the volcano that eventually deflates over time, or the current uplift might only be in its beginning stage.[147] The term 'zombie volcano' has been coined to describe volcanoes like Uturuncu that have been inactive for a long time but are actively deforming.[148]

Seismicity

In addition, the volcano features persistent seismic activity with occasional bursts of higher activity;[80] about three or four earthquakes occur every day at the volcano, and seismic swarms lasting minutes to hours with up to 60 earthquakes occur several times per month. The intensities of the earthquakes reach magnitude ML3.7. Most of this seismic activity occurs below the summit of Uturuncu around sea level[149] and some earthquakes appear to relate to the northwest-southeast tectonic trend of the region although swarms occur in several areal clusters.[58][150] Earthquakes are missing from the depth range of the Altiplano-Puna magmatic body but occur below it, implying that it is underlaid by brittle, cold crust.[151] Whether there are long-term trends in seismic activity is difficult to estimate as the detection and reconnaissance techniques of seismic activity at Uturuncu have changed over time.[152] This amount of seismic activity is large when compared to neighbouring volcanoes[153] and the seismic activity may be a consequence of the deformation, as intruding magma pressurizes and destabilizes local faults,[154][155] as well as the ascent of fluids in faults and cracks.[151] Further triggering processes are large earthquakes such as the 2010 Maule earthquake,[124] which caused an intense seismic swarm in February 2010.[149]

Tomographic studies

Magnetotelluric imaging of the volcano has found a number of high-conductivity anomalies below Uturuncu, including a wide, deep conductor that extends to the volcanic arc to the west and several shallower ones which ascend from the deep conductor[156] that appears to coincide with the Altiplano–Puna magmatic body. The shallow conductors appear to relate to local volcanoes such as the Laguna Colorada vent but also Uturuncu; the latter conductor lies at 2–6 kilometres (1.2–3.7 mi) depth, is less than 10 kilometres (6.2 mi) wide and may consist of molten rock with saline aqueous fluids.[139]

Seismic tomography has found a tooth-shaped anomaly that begins at 2 kilometres (1.2 mi) depth and continues to over 80 kilometres (50 mi) of depth.[157] Such structures have been found at other volcanoes and explained by the presence of magma. Seismic activity concentrates at the top of this anomaly.[158] Finally, tectonic stress patterns delineate a 40–80 kilometres (25–50 mi) wide ring surrounding the volcano that may be prone to fracturing; such a ring could constitute a future pathway for magma transport or the margin of a future caldera.[159]

Threats

Whether the ongoing unrest at Uturuncu is part of a benign process of the growth of a pluton or the prelude of a new eruption or even a caldera-forming eruption is as of 2008 an open question. A large caldera-forming eruption could have catastrophic, globe-spanning consequences as demonstrated by the 1815 eruption of Mount Tambora in Indonesia and the 1600 eruption of Huaynaputina in Peru;[61][114] this possibility has resulted in international media attention[160] and in popular culture; the volcano's threat is depicted in the 2016 film Salt and Fire.[161] Evidence does not unequivocally indicate that a future super-eruption such as past events in the region[159][162] is possible and there is no indication for a near-future eruption,[17] but there is potential for a smaller eruption.[159]

See also

Notes
  1. Ignimbrites are fluids consisting of gas and fragmented rocks that are expelled from volcanoes and form ignimbritic rocks when they solidify.[2]
  2. A sill is a sheet-shaped magma intrusion between layers of rock.[3]
  3. Fragmented volcanic rocks erupted by the vent.[18]
  4. Sediments deposited by water.[39]
  5. Sediments deposited by gravity.[40]
  6. Sediments formed by the skeletons of diatoms.[45]
  7. An anastomosing river has multiple channels through which water flows.[49]
  8. A liquid with a very high salt content.[72]
  9. Rocks containing numerous crystals embedded in more fine-grained rock.[75]
  10. Large crystals embedded into volcanic rocks.[76]
  11. Fine-grained rock that surrounds phenocrysts.[78]
  12. Rock fragments entrained in ascending magma from surrounding rocks.[81]
  13. Changes in magma composition caused by crystals settling out under their weight.[84]
  14. Rock formations that are smooth on one side and rough on the other, which form when glaciers moving over the formation erode the flat side but do not smooth the other side.[91]
  15. Silification is the replacement of rock by silicon dioxide.[118]
  16. A diapir is a rock formation, which owing to having a lower density than surrounding rock ascends through the latter.[138]
  17. Intruded volcanic rock.[141]

References
  1. Sparks et al. 2008, p. 728.
  2. "Ignimbrite". Dictionary of Geotourism ([2020] ed.). Springer. 2020. p. 273. doi:10.1007/978-981-13-2538-0_1142. ISBN 978-981-13-2538-0. S2CID 242929983. Archived from the original on 20 May 2021. Retrieved 10 June 2021.
  3. "Sill". Dictionary of Geotourism. Springer. 2020. pp. 566–567. doi:10.1007/978-981-13-2538-0_2251. ISBN 978-981-13-2537-3. S2CID 242284510. Archived from the original on 10 June 2021. Retrieved 10 June 2021.
  4. Municipio San Pablo de Lípez 2021, p. 4.
  5. Schäbitz & Liebricht 1999, p. 109.
  6. Blard et al. 2014, p. 210.
  7. Servicio Nacional de Áreas Protegidas 2019, Mapa: Área protegida.
  8. Wilken 2017, p. 68.
  9. Ahlfeld 1956, p. 129.
  10. Hudson et al. 2022, p. 1.
  11. Alcalá-Reygosa 2017, p. 661.
  12. Read, William A. (1952). "Indian Terms in Vázquez' Compendio". International Journal of American Linguistics. 18 (2): 82. doi:10.1086/464153. ISSN 0020-7071. JSTOR 1263293. S2CID 145156070.
  13. Ahlfeld 1956, p. 131.
  14. Municipio San Pablo de Lípez 2021, p. 55.
  15. Echevarría, Evelio (1963). "Part II. Chile and Argentina". American Alpine Journal. A Survey of Andean Ascents. Archived from the original on 9 August 2021. Retrieved 9 August 2021.
  16. U.S. Geological Survey & Servicio Geologico de Bolivia 1983, p. 122.
  17. Pritchard et al. 2018, p. 976.
  18. Bowes, D. R. (1989). "Tephra". Petrology. Encyclopedia of Earth Science. Boston, MA. pp. 554–557. doi:10.1007/0-387-30845-8_238. ISBN 978-0-387-30845-6. Archived from the original on 4 June 2018. Retrieved 20 July 2021.{{cite book}}: CS1 maint: location missing publisher (link)
  19. Gustavson Associates (1992). Compendio de geología económica de Bolivia (Report). Ministeria de Minería y Metalurgia – via Google Books.
  20. U.S. Geological Survey & Servicio Geologico de Bolivia 1983, p. 256.
  21. 1999 American Alpine Journal. The Mountaineers Books. p. 323. ISBN 978-1-933056-46-3.
  22. "Stop 6: Volcán Uturuncu". Volcano World. Oregon State University. Archived from the original on 17 December 2019. Retrieved 22 November 2019.
  23. "Uturuncu". Global Volcanism Program. Smithsonian Institution. Retrieved 22 November 2019.
  24. Sparks et al. 2008, p. 737.
  25. Walter & Motagh 2014, p. 464.
  26. Muir et al. 2015, p. 60.
  27. Servicio Nacional de Áreas Protegidas 2019, Atractivos turísticos.
  28. Wilken 2017, p. 69.
  29. Pritchard et al. 2018, p. 972.
  30. Sparks et al. 2008, p. 731.
  31. McFarlin et al. 2018, p. 50.
  32. Muir et al. 2015, p. 61.
  33. Muir et al. 2015, p. 71.
  34. Muir et al. 2015, pp. 60–61.
  35. Muir et al. 2015, p. 70.
  36. Muir et al. 2015, p. 76.
  37. Muir et al. 2015, p. 65.
  38. Muir et al. 2014, p. 3.
  39. "Alluvium". Encyclopedia of Soil Science. Encyclopedia of Earth Sciences Series. Springer. 2008. p. 39. doi:10.1007/978-1-4020-3995-9_30. ISBN 978-1-4020-3994-2. Archived from the original on 10 June 2021. Retrieved 10 June 2021.
  40. "Colluvium". Encyclopedic Dictionary of Archaeology. Springer. 2021. p. 304. doi:10.1007/978-3-030-58292-0_30757. ISBN 978-3-030-58291-3. S2CID 240799800. Archived from the original on 10 June 2021. Retrieved 10 June 2021.
  41. Perkins et al. 2016, p. 1081.
  42. Perkins et al. 2016, p. 1082.
  43. U.S. Geological Survey & Servicio Geologico de Bolivia 1983, p. 201.
  44. Perkins et al. 2016, p. 1086.
  45. Capinera, John L. (2008). "Diatomaceous Earth". Encyclopedia of Entomology. Springer. pp. 1215–1217. doi:10.1007/978-1-4020-6359-6_913. ISBN 978-1-4020-6242-1. Archived from the original on 2 June 2018. Retrieved 10 June 2021.
  46. Ahlfeld 1956, p. 135.
  47. Perkins et al. 2016, p. 1084.
  48. Ahlfeld 1956, p. 128.
  49. Yu, Xinghe; Li, Shengli; Li, Shunli (2018). "Fluvial Depositional System". Clastic Hydrocarbon Reservoir Sedimentology. Advances in Oil and Gas Exploration & Production. Springer. pp. 353–415. doi:10.1007/978-3-319-70335-0_9. ISBN 978-3-319-70335-0. Archived from the original on 24 November 2021. Retrieved 12 June 2021.
  50. Muir et al. 2015, p. 59.
  51. Henderson & Pritchard 2013, p. 1358.
  52. Sparks et al. 2008, p. 729.
  53. Comeau, Unsworth & Cordell 2016, p. 1391.
  54. Salisbury et al. 2011, p. 822.
  55. Muir et al. 2014, p. 750.
  56. Salisbury et al. 2011, p. 832.
  57. Perkins et al. 2016, p. 1090.
  58. Jay et al. 2012, p. 829.
  59. Sparks et al. 2008, p. 730.
  60. Muir et al. 2014, p. 749.
  61. Kukarina et al. 2017, p. 1855.
  62. Lau, Tymofyeyeva & Fialko 2018, p. 43.
  63. Jay et al. 2012, p. 818.
  64. Comeau et al. 2015, p. 243.
  65. Maher & Kendall 2018, p. 39.
  66. Pritchard et al. 2018, p. 958.
  67. Comeau, Unsworth & Cordell 2016, p. 1394.
  68. Kern et al. 2016, p. 1058.
  69. Maher & Kendall 2018, p. 38.
  70. Muir et al. 2014, p. 2.
  71. Morand, Brandeis & Tait 2021, p. 2.
  72. "Brine". Dictionary of Geotourism. Springer. 2020. p. 51. doi:10.1007/978-981-13-2538-0_200. ISBN 978-981-13-2538-0. S2CID 241883097.
  73. Hovland, Martin; Rueslåtten, Håkon; Johnsen, Hans Konrad (1 April 2018). "Large salt accumulations as a consequence of hydrothermal processes associated with 'Wilson cycles': A review, Part 2: Application of a new salt-forming model on selected cases". Marine and Petroleum Geology. 92: 129. Bibcode:2018MarPG..92..128H. doi:10.1016/j.marpetgeo.2018.02.015. ISSN 0264-8172.
  74. Sparks et al. 2008, p. 732.
  75. "Porphyritic". Dictionary Geotechnical Engineering/Wörterbuch GeoTechnik. Springer. 2014. p. 1027. doi:10.1007/978-3-642-41714-6_163019. ISBN 978-3-642-41714-6. Archived from the original on 12 June 2021. Retrieved 12 June 2021.
  76. "Phenocryst". Dictionary of Gems and Gemology. Springer. 2009. p. 661. doi:10.1007/978-3-540-72816-0_16699. ISBN 978-3-540-72816-0. Archived from the original on 9 June 2018. Retrieved 12 June 2021.
  77. Sparks et al. 2008, p. 752.
  78. "Groundmass". Dictionary of Gems and Gemology. Springer. 2009. p. 405. doi:10.1007/978-3-540-72816-0_10097. ISBN 978-3-540-72816-0. S2CID 241964748. Archived from the original on 12 June 2021. Retrieved 12 June 2021.
  79. Muir et al. 2014, p. 5.
  80. Sparks et al. 2008, p. 749.
  81. "Xenolith". Dictionary of Geotourism. Springer. 2020. p. 695. doi:10.1007/978-981-13-2538-0_2806. ISBN 978-981-13-2538-0. S2CID 240947814. Archived from the original on 24 November 2021. Retrieved 12 June 2021.
  82. Sparks et al. 2008, p. 760.
  83. Sparks et al. 2008, p. 763.
  84. "Gravity differentiation". Dictionary Geotechnical Engineering/Wörterbuch GeoTechnik. Springer. 2014. p. 628. doi:10.1007/978-3-642-41714-6_71993. ISBN 978-3-642-41714-6. Archived from the original on 20 May 2021. Retrieved 12 June 2021.
  85. Muir et al. 2014, p. 20.
  86. Sparks et al. 2008, p. 764.
  87. Muir et al. 2015, p. 80.
  88. Muir et al. 2014, p. 16.
  89. Muir et al. 2015, p. 74.
  90. Hastenrath, Stefan (1 January 1971). "On Snow Line Depression and Atmospheric Circulation in the Tropical Americas during the Pleistocene*". South African Geographical Journal. 53 (1): 56. doi:10.1080/03736245.1971.10559484. ISSN 0373-6245. Archived from the original on 20 October 2021. Retrieved 23 February 2021.
  91. Fairbridge, Rhodes W. (1997). "Roche moutonnée". Geomorphology. Encyclopedia of Earth Science. Springer. pp. 963–964. doi:10.1007/3-540-31060-6_316. ISBN 978-3-540-31060-0. Archived from the original on 12 June 2021. Retrieved 12 June 2021.
  92. Schäbitz & Liebricht 1999, p. 113.
  93. Blard et al. 2014, p. 211.
  94. Graf, K. (1991). "Ein Modell zur eiszeitlichen und heutigen Vergletscherung in der bolivianischen Westkordillere". Bamberger Geographische Schriften (in German). 11: 145. OCLC 165471239.
  95. Martin, Léo C. P.; Blard, Pierre-Henri; Lavé, Jérôme; Condom, Thomas; Prémaillon, Mélody; Jomelli, Vincent; Brunstein, Daniel; Lupker, Maarten; Charreau, Julien; Mariotti, Véronique; Tibari, Bouchaïb; Team, Aster; Davy, Emmanuel (1 August 2018). "Lake Tauca highstand (Heinrich Stadial 1a) driven by a southward shift of the Bolivian High". Science Advances. 4 (8): 2. Bibcode:2018SciA....4.2514M. doi:10.1126/sciadv.aar2514. ISSN 2375-2548. PMC 6114991. PMID 30167458.
  96. Alcalá-Reygosa 2017, p. 652.
  97. Veettil, Bijeesh K.; Kamp, Ulrich (2 December 2017). "Remote sensing of glaciers in the tropical Andes: a review". International Journal of Remote Sensing. 38 (23): 7106. Bibcode:2017IJRS...38.7101V. doi:10.1080/01431161.2017.1371868. S2CID 134344365.
  98. Blard et al. 2014, p. 216.
  99. Blard et al. 2014, p. 219.
  100. Perkins et al. 2016, p. 1088.
  101. Ward, Dylan J.; Cesta, Jason M.; Galewsky, Joseph; Sagredo, Esteban (15 November 2015). "Late Pleistocene glaciations of the arid subtropical Andes and new results from the Chajnantor Plateau, northern Chile". Quaternary Science Reviews. 128: 110. Bibcode:2015QSRv..128...98W. doi:10.1016/j.quascirev.2015.09.022. ISSN 0277-3791.
  102. Henderson & Pritchard 2017, p. 1843.
  103. Hargitai, Henrik I.; Gulick, Virginia C.; Glines, Natalie H. (November 2018). "Paleolakes of Northeast Hellas: Precipitation, Groundwater-Fed, and Fluvial Lakes in the Navua–Hadriacus–Ausonia Region, Mars". Astrobiology. 18 (11): 1435–1459. Bibcode:2018AsBio..18.1435H. doi:10.1089/ast.2018.1816. PMID 30289279. S2CID 52922692. Archived (PDF) from the original on 24 November 2021. Retrieved 4 July 2021 – via ResearchGate.
  104. Kessler, Albrecht (1963). "Über Klima und Wasserhaushalt des Altiplano (Bolivien, Peru) während des Hochstandes der letzten Vereisung (Klimate and Hydrology of the Altiplano Bolivia, Perú) during the Climax of the Last Glaciation". Erdkunde. 17 (3/4): 168. doi:10.3112/erdkunde.1963.03.03. ISSN 0014-0015. JSTOR 25637015. Archived from the original on 24 November 2021. Retrieved 23 February 2021.
  105. Servicio Nacional de Áreas Protegidas 2019, Biodiversidad.
  106. Solíz, Claudia; Villalba, Ricardo; Argollo, Jaime; Morales, Mariano S.; Christie, Duncan A.; Moya, Jorge; Pacajes, Jeanette (15 October 2009). "Spatio-temporal variations in Polylepis tarapacana radial growth across the Bolivian Altiplano during the 20th century". Palaeogeography, Palaeoclimatology, Palaeoecology. 281 (3): 298. Bibcode:2009PPP...281..296S. doi:10.1016/j.palaeo.2008.07.025. ISSN 0031-0182.
  107. Servicio Nacional de Áreas Protegidas 2019, Vegetación y Flora.
  108. Aguilar, Sergio Gabriel Colque; Villca, Edwin Edgar Iquize (29 April 2020). "Sensibilidad del hongo (Leptosphaeria polylepidis) de la Keñua (Polylepis tarapacana) a la aplicación de fungicidas orgánicos y químicos en laboratorio". Apthapi (in Spanish). 6 (1): 1853. ISSN 2519-9382. Archived from the original on 24 November 2021. Retrieved 3 December 2020.
  109. Morales, M. S.; Carilla, J.; Grau, H. R.; Villalba, R. (15 September 2015). "Multi-century lake area changes in the Southern Altiplano: a tree-ring-based reconstruction". Climate of the Past. 11 (9): 1141. Bibcode:2015CliPa..11.1139M. doi:10.5194/cp-11-1139-2015. ISSN 1814-9324. Archived from the original on 3 March 2021. Retrieved 23 February 2021.
  110. Sparks et al. 2008, p. 740.
  111. Jay et al. 2012, p. 817.
  112. Muir et al. 2015, p. 62.
  113. Muir et al. 2015, p. 78.
  114. Sparks et al. 2008, p. 765.
  115. Kussmaul, S.; Hörmann, P. K.; Ploskonka, E.; Subieta, T. (1 April 1977). "Volcanism and structure of southwestern Bolivia". Journal of Volcanology and Geothermal Research. 2 (1): 87. Bibcode:1977JVGR....2...73K. doi:10.1016/0377-0273(77)90016-6. ISSN 0377-0273.
  116. Kukarina et al. 2017, p. 1856.
  117. Jay et al. 2013, p. 169.
  118. Belov, N. V. (1 November 1974). "The resonance mechanism of silification". Journal of Structural Chemistry. 15 (6): 987. doi:10.1007/BF00747613. ISSN 1573-8779. S2CID 96401225. Archived from the original on 12 June 2021. Retrieved 12 June 2021.
  119. McNutt, S. R.; Pritchard, M. E. (2003). "Seismic and Geodetic Unrest at Uturuncu Volcano, Bolivia". AGU Fall Meeting Abstracts. 2003: V51J–0405. Bibcode:2003AGUFM.V51J0405M.
  120. Jay et al. 2013, p. 164.
  121. Pritchard et al. 2018, p. 971.
  122. U.S. Geological Survey & Servicio Geologico de Bolivia 1983, p. 267.
  123. Maher & Kendall 2018, p. 47.
  124. Jay et al. 2012, p. 835.
  125. Comeau, Unsworth & Cordell 2016, p. 1409.
  126. Perkins et al. 2016, p. 1078.
  127. Morand, Brandeis & Tait 2021, p. 1.
  128. Henderson & Pritchard 2017, p. 1834.
  129. Sparks et al. 2008, p. 745.
  130. Lau, Tymofyeyeva & Fialko 2018, p. 45.
  131. Gottsmann, Eiden & Pritchard 2022, p. 3.
  132. Sparks et al. 2008, p. 743.
  133. Lau, Tymofyeyeva & Fialko 2018, p. 46.
  134. Perkins et al. 2016, p. 1080.
  135. Henderson & Pritchard 2013, p. 1359.
  136. Muir et al. 2014, p. 765.
  137. Gottsmann, Eiden & Pritchard 2022, p. 9.
  138. Ernst, Richard E. (2015). "Diapir (Mantle)". Encyclopedia of Planetary Landforms. Springer. pp. 581–585. doi:10.1007/978-1-4614-3134-3_127. ISBN 978-1-4614-3134-3. Archived from the original on 11 June 2018. Retrieved 12 June 2021.
  139. Comeau et al. 2015, p. 245.
  140. Morand, Brandeis & Tait 2021, p. 11.
  141. "Pluton". Dictionary Geotechnical Engineering/Wörterbuch GeoTechnik. Springer. 2014. p. 1018. doi:10.1007/978-3-642-41714-6_162618. ISBN 978-3-642-41714-6. Archived from the original on 12 June 2021. Retrieved 12 June 2021.
  142. Biggs, Juliet; Pritchard, Matthew E. (1 February 2017). "Global Volcano Monitoring: What Does It Mean When Volcanoes Deform?". Elements. 13 (1): 20. doi:10.2113/gselements.13.1.17. hdl:1983/93198190-f2f7-41cf-b380-afebd52bd60a. ISSN 1811-5209. S2CID 73697354. Archived from the original on 24 November 2021. Retrieved 24 February 2020.
  143. Henderson & Pritchard 2013, p. 1363.
  144. Pritchard et al. 2018, p. 955.
  145. Kern et al. 2016, p. 1057.
  146. Perkins et al. 2016, p. 1089.
  147. Perkins et al. 2016, p. 1095.
  148. Pritchard et al. 2018, p. 969.
  149. Jay et al. 2012, p. 820.
  150. Jay et al. 2012, p. 821.
  151. Hudson et al. 2022, p. 11.
  152. Jay et al. 2012, p. 824.
  153. McFarlin et al. 2018, p. 52.
  154. Jay et al. 2012, p. 830.
  155. Henderson & Pritchard 2013, p. 1366.
  156. Comeau et al. 2015, p. 244.
  157. Kukarina et al. 2017, p. 1860.
  158. Kukarina et al. 2017, p. 1861.
  159. Kukarina et al. 2017, p. 1864.
  160. Friedman-Rudovsky, Jean (13 February 2012). "Growth Spurt at a Bolivian Volcano Is Fertile Ground for Study". The New York Times. Archived from the original on 1 October 2015. Retrieved 27 August 2015.
  161. Dowler, Kenneth (2022). Corporate wrongdoing on film : the 'public be damned'. Abingdon, Oxon. pp. 79–80. ISBN 9780367757526.{{cite book}}: CS1 maint: location missing publisher (link)
  162. Salisbury et al. 2011, p. 835.

Sources
This article is issued from Wikipedia. The text is licensed under Creative Commons - Attribution - Sharealike. Additional terms may apply for the media files.