Lake Tauca

Lake Tauca is a former lake in the Altiplano of Bolivia. It is also known as Lake Pocoyu for its constituent lakes: Lake Poopó, Salar de Coipasa and Salar de Uyuni. The lake covered large parts of the southern Altiplano between the Eastern Cordillera and the Western Cordillera, covering an estimated 48,000 to 80,000 square kilometres (19,000 to 31,000 sq mi) of the basins of present-day Lake Poopó and the Salars of Uyuni, Coipasa and adjacent basins. Water levels varied, possibly reaching 3,800 metres (12,500 ft) in altitude. The lake was saline. The lake received water from Lake Titicaca, but whether this contributed most of Tauca's water or only a small amount is controversial; the quantity was sufficient to influence the local climate and depress the underlying terrain with its weight. Diatoms, plants and animals developed in the lake, sometimes forming reef knolls.

Lake Tauca
Lake Pocoyu
Satellite image of the Altiplano. The green, brown and white surfaces in the lower right quadrant of the image are Lake Poopó, Salar de Coipasa and Salar de Uyuni, respectively. The blue surface at centre top is Lake Titicaca
Lake Tauca is located in Bolivia
Lake Tauca
Lake Tauca
LocationAndes, South America
Coordinates20°S 68°W[1]
TypeFormer lake
Pleisto- Holocene glacial lake
72,600–7200 BP
Part ofAltiplano
Primary inflowsGlacial meltwater
Desaguadero River, Río Grande de Lipez, Lauca River
Primary outflowsPotentially Pilcomayo River
Basin countriesBolivia, Chile, Peru
Surface area48,000–80,000 km2 (19,000–31,000 sq mi)
Average depth100 m (330 ft)
Max. depth142 m (466 ft)
Water volume1,200–3,810 km3 (290–910 cu mi)
Salinity20–90 g/L (0.00072–0.00325 lb/cu in)
Surface elevation3,660–3,770 m (12,010–12,370 ft)
Max. temperature10 °C (50 °F)
Min. temperature2 °C (36 °F)

The duration of Lake Tauca's existence is uncertain. Research in 2011 indicated that the rise in lake levels began 18,500 BP, peaking 16,000 and 14,500 years ago. About 14,200 years ago, lake levels dropped before rising again until 11,500 years ago. Some researchers postulate that the last phase of Lake Tauca may have continued until 8,500 BP. The drying of the lake, which may have occurred because of the Bølling-Allerød climate oscillation, left the salt deposits of Salar de Uyuni.

Lake Tauca is one of several ancient lakes which formed in the Altiplano. Other known lakes are Lake Escara, Ouki, Salinas, Minchin, Inca Huasi and Sajsi, in addition to several water-level rises of Lake Titicaca. The identity of these lakes is controversial; Sajsi is often considered part of Lake Tauca, and the lake is frequently divided into an earlier (Ticaña) and a later (Coipasa) phase.

The formation of Lake Tauca depended on a reduction in air temperature over the Altiplano and an increase in precipitation, which may have been caused by shifts in the Intertropical Convergence Zone (ITCZ) and increased easterly winds. It was originally supposed that glacial melting might have filled Lake Tauca, but the quantity of water would not have been sufficient to fill the whole lake. The lake was accompanied by glacial advance, noticeable at Cerro Azanaques and Tunupa. Elsewhere in South America, water levels and glaciers also expanded during the Lake Tauca phase.

Description
World map, with the Altiplano in red
The Altiplano, in red
The Altiplano and extent of Lake Tauca, clearly visible in the topography of the central Andes

Overview

Lake Tauca existed on the Altiplano, a high plateau with an average altitude of 3,800 to 4,000 metres (12,500 to 13,100 ft),[2] covering an area of 196,000 square kilometres (76,000 sq mi)[3] or 1,000 by 200 kilometres (620 mi × 120 mi).[4] The highland is in the Andes, the world's longest mountain chain which was formed during the Tertiary with a primary phase of uplift in the Miocene. Its central area, which contains the Altiplano, is formed by the eastern and western chains:[2] the Eastern and Western Cordillera of Bolivia, which reach an altitude of 6,500 metres (21,300 ft).[4] The Eastern Cordillera creates a rain shadow over the Altiplano.[5] The climate of the Altiplano is usually dry when westerly winds prevail; during the austral summer, heating induces easterly winds which transport humidity from the Amazon.[6] A north-south gradient exists, with mean temperatures and precipitation decreasing from 15 °C (59 °F) and 700 millimetres (28 in) in the north, to 7 °C (45 °F) and 100 millimetres (3.9 in) in the southern Lípez area.[4] Although precipitation decreases from north to south, the evaporation rate throughout the Altiplano exceeds 1,500 millimetres per year (59 in/year).[7] Most precipitation is recorded between October and April.[8] Occasionally during winter (but also in summer), frontal disturbances result in snowfall.[9] Strong winds and high insolation are other aspects of the Altiplano climate.[10] Much of the water balance in the present-day Altiplano-Atacama area is maintained by groundwater flow.[11] The terrain of the Altiplano consists primarily of sediments deposited by lakes and rivers during the Miocene and Pleistocene.[12] A Paleozoic basement underlies Cretaceous and Tertiary sediments.[13] The Andean Central Volcanic Zone and the Altiplano–Puna volcanic complex are in the Cordillera Occidental.[14]

Lake Tauca was one of many lakes which formed around the world during glacial epochs; others include the Baltic Ice Lake in Europe and Lake Bonneville in North America. Today, the Altiplano contains Lake Titicaca, with a surface area of 8,800 square kilometres (3,400 sq mi), and several other lakes and salt pans.[15] The latter include the Salar de Uyuni, at an altitude of 3,653 metres (11,985 ft) with an area of 10,000 square kilometres (3,900 sq mi), and the Salar de Coipasa, covering 2,500 square kilometres (970 sq mi) at an altitude of 3,656 metres (11,995 ft).[16] Lake Titicaca and the southern salt flats are two separate water basins, connected by the Rio Desaguadero when Titicaca is high enough.[8] The theory that the Altiplano was formerly covered by lakes was first proposed by J. Minchin in 1882.[17] The formation of such lakes usually, but not always, coincided with lower temperatures.[18][19] No evidence has been found for lake expansions in the Altiplano region below an altitude of 3,500 metres (11,500 ft).[20]

Geography
The basin of Lake Poopó (upper right), Salar de Uyuni (white beneath centre) and Salar de Coipasa (white left of centre)

Larger than Lake Titicaca,[21] Tauca was over 600 kilometres (370 mi) long[22] and covered the area of the present-day Lake Poopo, Salar de Uyuni and Salar de Coipasa.[23] Lake Tauca was the largest paleolake in the Altiplano[3] in the last 120,000 years at least,[24] and comparable to present-day Lake Michigan.[25] Several different estimates for its surface area exist:

Surface
(1000 km²)		 Surface
(1000 sq mi)		Details Date of
estimate
43 17 1981[26]
80 31Possibly triggered by a large spillover from Lake Titicaca,[27] 13,000 years ago 1995[28]
33–60 13–23 2006[29]
50 19 2009[15]
52 20At a 3,775 m (12,385 ft) water level 2011[8]
48 19Around 12,000 BP, and extending towards the Lípez area 2012[30]
55 21 2013[3]
56.7 21.9 2013[31]
Estimates of lake levelsDate of
estimate
3,760 m (12,340 ft)2002,[32] 1995[33]
3,770 m (12,370 ft)2013[3]
3,780 m (12,400 ft)2001,[34] 2006[35]
3,790 m (12,430 ft)2013[31]
Almost 3,800 m (12,500 ft)2005[36]

Water depths reached 110–120 metres (360–390 ft).[37] Water levels were about 140 metres (460 ft) higher than Salar de Uyuni,[38] or 135 to 142 metres (443 to 466 ft).[39] According to research published in 2000, the lake level varied from 3,700 to 3,760 metres (12,140 to 12,340 ft).[40] Some disagreement about water levels at various sites may reflect differing isostatic rebound of the land covered by the lake.[26][41] The original 1978 research on the Tauca phase postulated its shoreline at 3,720 metres (12,200 ft).[42] Of the previous lake cycles in the area, only the Ouki cycle appears to have exceeded that altitude.[43]

A later phase in lake levels (known as the Ticaña phase) was lower, at 3,657 metres (11,998 ft);[33] the drop from Tauca was abrupt. The late phase of Lake Tauca, Coipasa, had a water level of 3,660 metres (12,010 ft)[44] or 3,700 metres (12,100 ft)[45] and covered an area of about 32,000 square kilometres (12,000 sq mi). Transitions between lake cycles occurred in about one thousand years.[37]

Lake Tauca was the largest lake on the Altiplano during the last 100,000[36]-130,000 years.[46] Although the preceding paleolake (Minchin) was probably shallower,[36][47] there is disagreement about the methods used to ascertain water depth.[48] Some consider Minchin the larger lake;[49] a 1985 paper estimated its size at 63,000 square kilometres (24,000 sq mi), compared with Tauca's 43,000 square kilometres (17,000 sq mi).[50] Confusion may have resulted from the incorrect attribution of Tauca's shorelines to Lake Minchin;[51] a shoreline at 3,760 metres (12,340 ft) formerly attributed to Lake Minchin was dated to the Tauca phase at 13,790 BP.[52] The theory that Tauca is the largest lake follows a deepening trend in the southern Altiplano paleolakes which contrasts with a decreasing trend in the level of Lake Titicaca during the Pleistocene. This pattern probably occurred because the threshold between the two basins progressively eroded, allowing water from Titicaca to flow into the southern Altiplano.[39] The lakes left erosional benches, fan deltas (where the lakes interacted with ice) and lake-sediment deposits,[53] and eroded into moraines.[54] The ridge that separates the Salar de Uyuni and Salar de Coipasa was a peninsula in the lake; San Agustín, San Cristóbal and Colcha formed islands.[55][56]

The lake and its predecessors (such as Lake Minchin) formed in the area currently occupied by salt flats such as the Salar de Uyuni, Salar de Coipasa,[2] Lake Poopó,[57] Salar de Empexa,[58] Salar de Laguani,[29] and Salar de Carcote—several tens of meters beneath the Tauca water level.[59] The present-day cities of Oruro and Uyuni are located in areas flooded by Lake Tauca.[60] Salar de Ascotán may[61][55] or may not have been part of Lake Tauca.[59] The submergence of a large part of the Altiplano under Lake Tauca reduced the production of dust there and its supply to Patagonia,[62] but "restocked" the sediments and thus increased dust supply once Lake Tauca dried up.[63][64] The terrain above 3,800 metres (12,500 ft) was affected by glaciation.[9] In the Coipasa basin, a major debris avalanche from the Tata Sabaya volcano rolled over terraces left by Lake Tauca.[65]

  • Salar de Ascotan
    Salar de Ascotan
  • Salar de Carcote
    Salar de Carcote
  • The course of the Lauca River
    The course of the Lauca River
  • Tata Sabaya with the landslide to the left
    Tata Sabaya with the landslide to the left
  • 3D geography of Salar de Uyuni, remainder of Lake Tauca
    3D geography of Salar de Uyuni, remainder of Lake Tauca

Hydrology
Altiplano drainage basin overlaid on present Peru, Bolivia, Chile and Argentina
Drainage basin of the Altiplano

At a water level of 3,720 metres (12,200 ft), the total volume of the lake has been estimated to be 1,200 cubic kilometres (290 cu mi)[66] to 3,810 cubic kilometres (910 cu mi) at a level of 3,760 metres (12,340 ft).[67] Such volumes could have been reached in centuries.[68] The quantity of water was sufficient to depress the underlying bedrock, which rebounded after the lake disappeared; this has resulted in altitude differences of 10 to 20 metres (33 to 66 ft).[41] Based on oxygen-18 data in lake carbonates, water temperatures ranged from 2 to 10 °C (36 to 50 °F)[69] or 7.5 ± 2.5 °C (45.5 ± 4.5 °F).[70] Tauca may have been subject to geothermal heating.[71]

The lake was deep and saline,[72] with salinity increasing from the Tauca to the Coipasa stages.[73] The salt content seems to have consisted of NaCl and Na2SO4.[28] Estimated salt concentrations:

Salt concentrationCommentSource
20 g/L (0.00072 lb/cu in)[40]
30 to 40 g/L (0.0011 to 0.0014 lb/cu in)The latter, earlier, estimate may be incorrect; many salinity values were obtained from deposits at the lake margins, which tend to be less saline[74][75]
60 to 90 g/L (0.0022 to 0.0033 lb/cu in)Later research[76]

Estimated salt concentrations (based on a lake level of 3,720 metres (12,200 ft), for sodium chloride, lithium and bromine):

MineralConcentrationSource
Sodium chloride73 g/L (0.0026 lb/cu in)[77]
Chlorine54 g/L (0.0020 lb/cu in)[78]
Sodium32 g/L (0.0012 lb/cu in)[78]
Sulfate8.5 g/L (0.00031 lb/cu in)[78]
Magnesium3 g/L (0.00011 lb/cu in)[78]
Potassium2.2 g/L (7.9×10−5 lb/cu in)[78]
Calcium1 g/L (3.6×10−5 lb/cu in)[78]
Boron60 mg/L (2.2×10−6 lb/cu in)[78]
Lithium10 mg/L (3.6×10−7 lb/cu in) or 80 mg/L (2.9×10−6 lb/cu in)[77] and [79]
Bromine1.6 ± 0.4 mg/L (5.8×10−8 ± 1.4×10−8 lb/cu in)[79]

Some of this salt penetrated aquifers beneath the lake, which still exist.[80] A significant excess NaCl concentration has been inferred for Lake Tauca, possibly stemming from salt domes whose contents moved from lake to lake.[81] Precipitation of calcium carbonate resulted in lake waters becoming progressively enriched in more soluble salts.[82]

Glacial meltwater may have contributed substantially to Lake Tauca's development.[75] Strontium isotope data indicates that water draining from Lake Titicaca through the Rio Desaguadero may have contributed between 70% and 83% of Lake Tauca's water, an increase of between 8 and 30 times the current outflow of Lake Titicaca via the Desaguadero.[83] A drop in the level of Lake Titicaca about 11,500 BP may have resulted in its outflow drying up, favouring the disappearance of Lake Tauca.[84] According to other research, the increased outflow of Lake Titicaca would have had to be unrealistically large to supply Lake Tauca with water if Titicaca was its principal source.[85] Other estimates assume that one-third of Tauca's water came from Lake Titicaca,[86] no more than 15% for any lake cycle,[31] or the much-lower four per cent (similar to today's five-per cent contribution from Titicaca to Lake Poopó). During the Coipasa cycle, Lake Poopó may have contributed about 13% of the water.[69] About 53% of Lake Tauca's water came from the Eastern Cordillera.[87] About 60,000 years ago, the Desaguadero probably began transporting water from Lake Titicaca to the Uyuni area and the southern paleolakes.[88] Tauca was fed by the Río Grande de Lipez on the south,[89] the Río Lauca on the northwest and the glaciers of the two cordilleras on the east and west.[42] The lake's total drainage basin has been estimated at about 200,000 square kilometres (77,000 sq mi).[90] If lake levels reached an altitude of 3,830 metres (12,570 ft),[91] the lake may have drained into the Pilcomayo River and from there through the Río de la Plata into the Atlantic Ocean.[92] Formerly an outlet may have formed at Salar de Ascotán, into the Pacific Ocean, before it was obstructed by lava flows.[93][94] A theory proposed by Campbell in 1985 that a former Altiplano-wide lake catastrophically drained into the Rio Beni during the Holocene[95] has not received much support.[96]

Although earlier theories postulated that large lakes formed from glacial meltwater, increased precipitation or decreased evaporation (or both) are today considered necessary for lake formation;[97] a complete glacial melting would have had to occur in less than about a century to produce the required volume.[98] The water volume would be insufficient to explain Lake Tauca's high water levels; however, some smaller lakes in the southern Altiplano probably expanded from glacial meltwater alone.[99] The lake may have contributed to increased precipitation by influencing land breezes.[20] According to strontium isotope data, there may have been little water exchange between Tauca's Uyuni and Coipasa basins.[100] During the Coipasa lake cycle, the Coipasa-Uyuni and Poopó basins had a limited connection.[101] Minor water-level fluctuations occurred during the lake's existence.[28]

Based on a 60,000-square-kilometre (23,000 sq mi) surface area, the evaporation rate has been estimated at over 70,000,000,000 cubic metres per year (2.5×1012 cu ft/a)—comparable to the discharges of the Nile or Rhine.[102] Less than half of this evaporation returned to the lake as precipitation;[103] in the central sector of the lake[104] at Tunupa, this would have increased precipitation by 80%,[90] delaying the retreat of glaciers in the area.[105] Groundwater from Lake Tauca may have drained into the Quebrada Puripica, northeast of Laguna Miscanti.[106] Given the height of the sill between the two basins and evidence found at Poopó,[102] water may have drained from the Coipasa-Uyuni basin into Lake Poopó during the Coipasa cycle.[107]

Glacial debris and ice were probably present at the lake,[36] with fan deltas at Tunupa overlapping the Lake Tauca shore.[108] At Tunupa and Cerro Azanaques, glaciers reached their maximum size shortly before the lake level peaked and probably contributed to water levels when their retreat began.[109] Two minor glacial advances, over 12,000 BP and about 11,000 BP, appear to coincide with Lake Tauca.[110]

Lake Tauca left up to 5 metres (16 ft) thick sediments in the southern Altiplano,[111] and tufa deposits formed in the lake. The continental environment Pleistocene sediments were formed from lacustrine carbonate deposits. These rocks contain amphibole, clay minerals such as illite, kaolinite and smectite, feldspar, plagioclase, potassium feldspar, pyroxene and quartz. The composition of these rocks resembles that of the Altiplano soils.[112] The sedimentation rate in the Uyuni basin was about 1 millimetre per year (0.0012 in/Ms).[113]

Biology
Vegetation during the Last Glacial Maximum

Low concentrations of pollen are found in sediments left by Lake Tauca in the Salar de Uyuni.[114] Lake Minchin sediments contain more pollen (indicating that it may have had a more favourable climate),[115] but the lack of pollen may be the product of a deeper lake.[116] Polylepis may have thrived in favourable salinity and climatic conditions.[36] Increased Polylepis and Acaena pollen is observed towards the end of the Tauca episode.[117]

The lake was deep enough for the development of planktonic diatoms,[36] including the dominant Cyclotella choctawatcheeana.[38] Other diatoms noted in Lake Tauca are the benthic Denticula subtilis, the epiphytic Achnanthes brevipes, Cocconeis placentula and Rhopalodia gibberula, the planktonic Cyclotella striata and the tychoplanktonic Fragilaria atomus, Fragilaria construens and Fragilaria pinnata.[118] Epithemia has also been found.[119]

Sediments at the shoreline contain fossils of gastropods and ostracods;[120] Littoridina and Succineidae snails have been used to date the lake.[121] Other genera included Myriophyllum, Isoetes[36] (indicating the formation of littoral communities)[116] and Pediastrum.[36] Algae grew in the lake and produced reef knolls (bioherms) formed by carbonate rocks. These grew in several phases,[122] and some were initially considered stromatolites.[120] Some dome-shaped bioherms reach a size of 4 metres (13 ft), forming reef-like structures on terraces. They developed around objects jutting from the surface, such as rocks. Tube- and tuft-shaped structures also appear on these domes.[123] Not all such structures formed during the Tauca episode.[122] Similar structures have been found in the Ries crater in Germany, where Cladophorites species were responsible for their construction. Taxa identified at Lake Tauca include Chara species.[119] The water above the tufa deposits was probably less than 20 metres (66 ft) deep.[120] In some places (linked to Phormidium encrustatum and Rivularia species), limited stromatolitic development took place.[119]

Research history

Reports of lake deposits on the Altiplano go back to 1861.[124] A John B. Minchin in 1882 reported the existence of encrustations around Lake Poopo and the salars south of Coipasa. He postulated that a lake with a surface area of 120,000 square kilometres (46,000 sq mi) left these encrustations and that the nitrate deposits in the Atacama and Tarapaca were likewise formed by water draining for this lake. Some estimates of the size of this lake claimed that it reached from Lake Titicaca as far as 27° South. The name "Lake Minchin" was applied in 1906 by Steinmann, who applied it to the Uyuni basin, while naming the lake covering the Poopo and Coipasa basins "Lake Reck".[125] The name was applied in honour of John B. Minchin.[126] Later it was found that Lake Titicaca was not part of Lake Minchin and the theory was put forward that meltwater from glaciers had formed the lake. A different lake (Lake Ballivian) was also defined which encompassed Lake Titicaca.[127] The lake episodes "Escara" and "Tauca" were first defined in 1978.[128] The relationship between various deposits in the southern Altiplano and these around Lake Titicaca was unclear at the beginning of the research history.[129] Lakes were identified by the lake terraces, sediments, bioherms[130] and drill cores.[131]

Predecessor lakes
Main articles: Ouki, Salinas, Inca Huasi, and Sajsi

Before Lake Tauca, there were Ouki (120,000–98,000 years ago), Salinas (95,000–80,000 years ago), Inca Huasi (about 46,000 years ago), Sajsi (24,000–20,500 years ago) and Coipasa (13,000–11,000 years ago).[132] Inca Huasi and Minchin are sometimes considered the same lake phase,[133] and other researchers have suggested that Lake Minchin is a combination of several phases.[134][135] The Ouki cycle may be subdivided in the future, and a number of sometimes-contradictory names and dates exist for these paleolakes.[107]

Preceding lake: Escara

Escara was identified in the central Altiplano,[130] it may be the oldest Altiplano lake cycle.[136] Lake levels reached an altitude of 3,780 metres (12,400 ft);[137] perhaps reaching the size of Lake Tauca and Ouki.[138] At the town of Escara, 8 metres (26 ft) thick deposits have been left by the lake.[139]

Escara is dated to 191,000 years BP.[140] This date is of a tuff associated with lake deposits, the deposits themselves have not been dated.[141] The L5 sediment[131] and S10 layers in Salar de Uyuni have been linked to Escara.[142] Some tuffs found in Escara lake deposits have been dated to about 1.87 million years ago.[138] During the episode of Lake Escara, Lake Ballivian may have existed in the northern Altiplano[137] as a southward extension of Lake Titicaca;[82] Lake Escara would be thus identical to "lake pre-Minchin" which has left terraces 60–70 metres (200–230 ft) above the present-day elevation.[143]

Hypothetical pluvial and lake: Minchin

A humid period 46,000-36,000 years ago has been deemed "Lake Minchin"; it led to the formation of a large body of water on the Altiplano[144] where Lake Tauca would later develop.[145] The layer S4 in Salar de Uyuni drill cores has been linked to Lake Minchin.[142] During this time, a salt lake existed at Laguna Pozuelos,[146] while numerous lakes formed in northwestern Argentina after valleys were dammed by landslides,[147] several lake basins in the Lipez region[148] and many salt flats in the Altiplano filled with lakes, in which bioherms and stromatolites grew,[149] moisture increased in the Brazilian and Bolivian Amazon[150] and sediment accumulated in the Pativilca valley,[151] the Pisco River valley (forming the "Minchin Terrace")[152] and the Lomas de Lachay valleys.[153] Like Lake Tauca, Lake Minchin has been correlated to the last glacial maximum,[154] and regional glacial advance extending to the southern Altiplano/Puna has been correlated with the Minchin/Inca Huasi stage;[155][156] the Choqueyapu II glacier advance in the Bolivian Andes,[157] more debatably the Canalaya Phase in the Cordillera Apolobamba[158] and the formation of the N-III moraines at Choquelimpie may coincide with the Minchin pluvial.[159] Sedimentation rates in the main Altiplano lake were much less than during the Tauca pluvial.[113]

The name "Lake Minchin" has been used inconsistently to refer to either the palaeolake at Lake Poopo,[160] a lake existing 45,000 years ago, the highest lake in the Altiplano, or to sediment formations.[34] An alternative theory postulates that Lake Minchin was formed by several lakes, including Ouki and Inca Huasi,[134][133] and by unreliable radiocarbon dates.[161] Sometimes the term "Minchin" is also applied to the whole hydrological system Titicaca-Rio Desaguadero-Lake Poopo-Salar de Coipasa-Salar de Uyuni,[126] or to the highest ancient lake in the Altiplano (usually known as Lake Tauca).[162] There are also contradictions between lake level records in different parts of the system.[6] This confusion has led to calls to drop the usage of the name "Minchin".[34]

Chronology
Subdivision and glacial history of the latest Pleistocene and early Holocene Europe

The existence of Lake Tauca was preceded by a dry period, with minor lake events recorded in Salar de Uyuni in the Late Pleistocene at 28,200–30,800 and 31,800–33,400 BP.[145] This period was accompanied by the disappearance of ice from Nevado Sajama.[86] A dry period is also noted in Africa and other parts of South America around 18,000 BP, and the retreat of the Amazon rainforest may have produced the lake low-water mark.[163] The era may have been drier than the present.[164] The drying of Lake Minchin left a salt layer about 20 metres (66 ft) thick in the Salar de Uyuni, where gullies formed.[165] Some ooid sediments formed before the Lake Tauca phase.[166] Around 28,000 BP, lake levels rose in Lake Huinaymarca (Lake Titicaca's southern basin), preceding Lake Tauca by about two millennia.[167] During this period, lakes in the Uyuni basin were intermittent.[168] Previous lakes in the basin were generally small and shallow.[21]

The radiometric age of Lake Tauca ranges from 72,600 to 7200 BP.[169] The duration of the lake highstands may be overestimated due to radiation scatter.[170] Radiocarbon dates have been obtained on crusts containing calcite, gastropod shells, stromatolites and structures left behind by algae.[171] The Lake Tauca shorelines formed over more than century-long periods.[98]

The first research, by Servant and Fontes in 1978, indicated a lake age between 12,500 and 11,000 BP according to C-14 dating.[172] These were bracketed by dates between 12,360 ± 120 and 10,640 ± 280 BP for the highest deposits at Salar de Coipasa and Salar de Uyuni, and 10,020 ± 160 and 10,380 ± 180 BP for deposits which formed shortly before the lake dried.[173][26] The reliability of the dates was questioned in 1990,[95] and a later estimate was set at 13,000 to 10,000 BP.[174] In 1990, Rondeau proposed ages of 14,100 to 11,000 BP based on radiocarbon dating and 7,000 to 14,800 BP based on uranium-thorium dating.[175]

In 1993 it was suggested that Lake Tauca had an earlier phase, with water levels reaching 3,740 metres (12,270 ft), and a later phase reaching 3,720 metres (12,200 ft).[174] Research published in 1995 indicated that the lake was shallow for over a millennium before rising to (and stabilizing at) its maximum level. Water levels between 13,900 and 11,500 BP reached 3,720 metres (12,200 ft); 3,740 metres (12,270 ft) was reached between 12,475 and 11,540 BP, and 3,760 to 3,770 metres (12,340 to 12,370 ft) between 12,200 and 11,500 BP.[176]

Research in 1999 indicated an earlier start of the Tauca lake cycle, which was subdivided into three phases and several sub-phases. Around 15,438 ± 80 BP (the Tauca Ia phase), water levels in Salar de Uyuni were 4 metres (13 ft) higher than the current salt crust. Lake levels then rose to 27 metres (89 ft) above the salt flat, accompanied by freshwater input (Tauca Ib). Around 13,530 ± 50 BP (Tauca II), the lake reached an altitude of 3,693 metres (12,116 ft), [118] not exceeding 3,700 metres (12,100 ft).[177] At this time, strong gully erosion and alluvial fans probably formed in Bolivian valleys.[178] Between 13,000 and 12,000 BP, the lake reached its greatest depth—110 metres (360 ft)—of the Tauca III period. Dates of 15,070 BP and 15,330 BP were obtained for the highest shoreline, at 3,760 metres (12,340 ft).[177] After 12,000 BP, water levels decreased abruptly by 100 metres (330 ft).[179] An even-earlier start was proposed by 2001 research, based on sediments in the Uyuni basin, which determined that Lake Tauca began developing 26,100 BP.[145] A 2001 review indicated that most radiometric dates for Lake Tauca cluster between 16,000 and 12,000 BP, with lake levels peaking around 16,000 BP.[35] A drop in oxygen-18 concentration in the Nevado Sajama glaciers has been associated with increased precipitation around 14,300 years ago.[68] A 2005 book estimated the duration of the Lake Tauca phase at between 15,000 and 10,500 BP.[180]

Research in 2006 postulated that the Lake Tauca transgression began 17,850 BP and peaked at altitudes of 3,765 to 3,790 metres (12,352 to 12,434 ft) between 16,400 and 14,100 years ago.[181] Spillovers into neighbouring basins may have stabilized the lake levels at that point,[182] and the level subsequently dropped over a 300-year period.[181] The following Coipasa phase ended around 11,040 +120/-440 BP, but its chronology is uncertain.[182]

A 2011 lake history study set the beginning of the lake-level rise at 18,500 years ago. Levels rose slowly to 3,670 metres (12,040 ft) 17,500 years ago, before accelerating to 3,760 metres (12,340 ft) by 16,000 years ago. Contradictions between lake depths determined by shorelines and diatom-fossil analysis led to two lake-level-rise chronologies: one reaching 3,700 metres (12,100 ft) 17,000 years ago and the other reaching 3,690 metres (12,110 ft) between 17,500 and 15,000 years ago. The lake level would have peaked from 16,000 to 14,500 years ago at 3,765 to 3,775 metres (12,352 to 12,385 ft) altitude. Shortly before 14,200 BP, the lake level would have begun its drop to 3,660 metres (12,010 ft) by 13,800 BP.[183] The Coipasa phase began before 13,300 BP and reached its peak at 3,700 metres (12,100 ft) 12,500 years ago. The Coipasa lake's regression was nearly complete around 11,500 years ago.[70] A 2013 reconstruction envisaged a lake level rise between 18,000 - 16,500 years ago, followed by a highstand between 16,500 - 15,500 and a decrease in lake levels between 14,500 - 13,500 years ago.[184]

Lake Tauca is sometimes subdivided into three phases (Lake Tauca proper, Ticaña and Coipasa), with the Tauca phase lasting from 19,100 to 15,600 BP.[130] The Coipasa phase, originally thought to have lasted from 11,400 and 10,400 BP, was corrected to 9,500 to 8,500 BP and later to 12,900 - 11,800 BP; it was preceded by a 400-year long lake level rise and was followed by a 1,600 years long decline.[185] During this phase, lake levels rose to 3,660 metres (12,010 ft) altitude[186] or 3,700 square kilometres (1,400 sq mi) with a surface area of 28,400 square kilometres (11,000 sq mi);[185] the depth of the lake reached 55 metres (180 ft).[24] According to a 1998 publication, Lake Tauca and the Coipasa phase lasted from 15,000 to 8,500 BP.[187] The Coipasa phase has also been identified in Lake Chungará.[188] The Coipasa phase was much less pronounced than the Tauca phase and shorter in duration,[189] and was concentrated on the Coipasa basin, presumably because it receives more water than the Uyuni basin.[73] An earlier lake phase, Sajsi (24,000–20,000 years ago), is sometimes considered part of Lake Tauca[133] with the Tauca and Coipasa cycles.[48] The Sajsi lake phase preceded the Tauca phase by one or two millennia[183] and water levels were about 100 metres (330 ft) lower than during the Tauca stage;[190] it coincided with the Last Glacial Maximum.[24]

The Ticaña phase was accompanied by a 100-metre (330 ft) drop in water level.[33] The Tauca and Coipasa phases are sometimes considered separate.[35] Lakes Tauca and Minchin have been considered the same lake system and called Lake Pocoyu, after the present-day lakes in the area.[191] "Minchin" is also used by some authors as a name for the system.[126]

Bare, dormant volcano
The Tunupa volcano was glaciated during the Tauca episode

The Chita tuff was deposited in Lake Tauca at 3,725 metres (12,221 ft) altitude approximately 15,650 years BP, when the lake may have been regressing.[138] Another tuff of uncertain age was deposited above Tauca-age sediments and tufas at the southeastern Salar de Coipasa.[192] Data from Tunupa indicate that lake levels stabilized between 17,000 and 16,000 years ago. A 50-metre (160 ft) lake-level drop occurred by 14,500 BP, with the lake drying between then and 13,800 years ago. Rising temperatures and a drop in precipitation were the likely triggers of lake and glacial retreat at the end of Heinrich event 1.[193] In contrast, data from the Uyuni-Coipasa basin indicate that water levels peaked 13,000 years ago.[28] The drying of Lake Tauca during the Ticaña lowstand[194] has been linked to the Bølling–Allerød climate period and increased wildfires on the Altiplano;[195] Lake Titicaca may have dropped beneath its outflow, cutting off the water supply to Lake Tauca.[196] Glacial retreat at the beginning of the Holocene may also have been a contributing factor.[75] As the lake receded, decreased evaporation (and cloud cover) would have enabled sunlight to increase the evaporation rate, further contributing to a decline in lake surface area.[197]

A pattern of lake cycles becoming longer than the preceding one has been noted.[39] Water from the lake may have contributed to increased oxygen-18 at Sajama around 14,300 years ago, possibly triggered by evaporation.[198] As the lake level dropped, Lake Poopó would have been disconnected first; the sill separating it from the rest of Lake Tauca is relatively shallow. Coipasa and Uyuni would have remained connected until later.[76] Water levels in Lake Titicaca's Lake Huinaimarca were low by 14,200 BP.[168] By the Antarctic Cold Reversal, Lake Tauca was dry.[199]

The end of the Tauca phase was followed by dry and cold conditions in the Puna, similar to the Younger Dryas, then by an early-Holocene humid period associated with decreased solar radiation. After 10,000 BP, another drought lasted from 8,500 BP to 3,600 BP,[187] and peaked from 7,200–6,700 BP.[200] The world's largest salt pan was left behind when Lake Tauca dried up,[30] with approximately 10 metres (33 ft) of material left at Salar de Uyuni.[201] Lake basins in the Altiplano which had filled during the Tauca phase were separated by lower lake levels.[202] Channels between the lakes testify to their former connections.[37]

Climate
Last Glacial Maximum sea water temperature map

There are few reconstructions of how the climate looked before and after the Lake Tauca highstand.[37] It has been estimated that summer precipitation would have increased by 315 ± 45 millimetres (12.4 ± 1.8 in) and temperature dropped 3 °C (5.4 °F) for Lake Tauca to form.[203] According to a 1985 estimate, increased precipitation of 200 millimetres per year (7.9 in/year) would be needed;[204] the estimate was subsequently revised to 300 millimetres per year (12 in/year).[51] With a 5 to 7 °C (9.0 to 12.6 °F) temperature decrease, a 20–75% increase in precipitation would be required to form the lake.[205] Research in 2013 indicated that the climate at the Tunupa volcano (in the centre of Lake Tauca) was about 6 to 7 °C (11 to 13 °F) colder than present, with rainfall estimated at 320 to 600 millimetres (13 to 24 in).[206] A 2018 estimate supported by 2020 research[207] envisages a temperature decrease of 2.9 ± 0.2 °C (5.22 ± 0.36 °F) and a mean precipitation 130% higher than today, about 900 ± 200 millimetres per year (35.4 ± 7.9 in/year);[208] this precipitation increase was concentrated on the eastern side of the catchment of Lake Tauca while the southernmost watershed was almost as dry as present-day.[104] In a coupled glacier-lake model, temperatures were conditionally estimated at 5.7 ± 1.1 °C (10.3 ± 2.0 °F) lower than today.[209] In the southern Altiplano, precipitation exceeded 500 millimetres (20 in) during this epoch.[210] In the central Altiplano, precipitation was 1.5 to three times higher than today.[211] In and around the Arid Diagonal, precipitation doubled from 300 millimetres per year (12 in/year) to 600 millimetres per year (24 in/year).[212] Around the lakes precipitation may have increased nine-fold.[213]

The formation of Lake Tauca coincides with Heinrich event 1[46] and has been explained with a southward shift of the Bolivian high[lower-alpha 1] that increased transport of easterly moisture into the Altiplano[215] and a strengthening of the South American Summer Monsoon due to a decrease in the cross-equatorial transport of heat.[216] Earlier highstands of Altiplano lakes may also correlate to earlier Heinrich events.[25] Increased cloud cover probably increased the effective precipitation by reducing evaporation rates.[109] In contrast, insolation rates do not appear to be linked to lake-level highstands in the Altiplano;[217] the lake expansion occurred when summer insolation was low[187] although recently an insolation maximum between 26,000 and 15,000 years ago has been correlated to the Tauca stage.[218] The humidity above the lake has been estimated at 60%, taking into account the oxygen-18 content of carbonates deposited by the lake.[69]

Coinciding with Lake Tauca, between 17,000 and 11,000 BP glaciers expanded in the Andes between 18° and 24° south latitude.[219] At Lake Titicaca, glacial tongues approached the shore.[220] The equilibrium line altitude of glaciers in the dry Andes decreased by 700 to 1,000 metres (2,300 to 3,300 ft).[221] Such glacial advances may have been preceded by the humid episodes which formed Lake Tauca.[110] Around 13,300 BP, maximum glacier size in southern Bolivia is associated with a highstand of Lake Tauca.[222] Glaciers did not expand everywhere, however, and there is little evidence for glacial expansion at El Tatio, Tocorpuri and parts of the Puna. Glacier expansions at Llano de Chajantor and surroundings may or may not have occurred.[223][212] Frequent incursions of polar air may have contributed to glacial expansion.[224] At Tunupa, a volcano located in the centre of Lake Tauca, maximum glacial extent lasted until the lake reached its highest level. Glacial shrinkage beginning 14,500 years ago probably occurred at the same time as a drop in lake levels, although dating ambiguity leaves room for debate. [3] The Cerro Azanaques moraines reached their greatest extent from 16,600 to 13,700 BP.[225] The existence of Lake Tauca coincides with the Late Glacial Maximum,[226] when temperatures in the central Altiplano were about 6.5 °C (11.7 °F) lower.[211] Part of the glacial advance may have been nurtured by moisture from Lake Tauca,[227][228] a conclusion supported by oxygen isotope data from the Sajama glaciers[229] and by paleoclimate reconstructions around the former Lake Tauca.[230] The Chacabaya glacial advance may be contemporaneous with Lake Tauca.[231] Just like the Lake Tauca highstand may have coincided with the first Heinrich event, the Younger Dryas may be associated with the Coipasa highstand[232][8] and the second Central Andean Pluvial Event although the Younger Dryas ended two millennia before the CAPE.[233] The second CAPE was caused either by changes in the South American monsoon or by changes in the atmospheric circulation over the Pacific Ocean, and its end has been attributed to a warming North Atlantic drawing the ITCZ northward.[234] Today, the average temperature at stations at an altitude of 3,770 metres (12,370 ft) is 9 °C (48 °F).[8]

Context

The formation and disappearance of Lake Tauca was a major hydrological event[46] that was accompanied by several millennia of wetter climate.[190] Its formation and the later Coipasa lake phase is associated with the Central Andean Pluvial Event (CAPE), which occurred from 18,000–14,000 to 13,800–9,700 BP. During this epoch, major environmental changes occurred in the Atacama as precipitation increased between 18° and 25° degrees south. In some areas, oases formed in the desert and human settlement began.[235] The Central Andean Pluvial Event has been subdivided into two phases, a first one which began either 17,500 or 15,900 years ago and ended 13,800 years ago and a second phase which began 12,700 years ago and ended either 9,700 or 8,500 years ago;[236] they were separated by a short dry period[237] that coincides with the Ticaña lowstand. The second phase of the Central Andean Pluvial Event has been subdivided further into a wetter earlier and a drier later subphase.[238] During the Coipasa lake cycle, precipitation may have focused on the southern Altiplano and been transported there from the Chaco; the main Tauca cycle may have been accompanied by precipitation from the northeast.[45] A glacial advance in the Turbio valley (a feeder of the Elqui River) between 17,000 and 12,000 years ago has been attributed to the Central Andean Pluvial Event.[239] Other indicators point to dry conditions/lack of glacier advances in central Chile and the central Puna during the highstand of Lake Tauca,[240][155] glaciers had already retreated from their maximum positions by the time it began[190] and the Central Andean Pluvial Event may not have been synchronous between the southern Altiplano and the southern[241] and northern Atacama.[242]

Increased precipitation during the Tauca phase was probably triggered by the southern movement of the ITCZ and the strengthening of the South America monsoon,[243] possibly caused by chilling in the northern hemisphere[244] and North Atlantic, along with higher water temperatures off Northeastern Brazil.[245] Combined with a southern shift of high pressure zones, increased moisture during late glacial times[246] would have flowed from the Amazon.[247] This change, which occurred from 17,400–12,400 years or 18,000–11,000 BP, is recorded in Bolivian Chaco and Brazilian cave records.[248] Some 20th century phases of higher water levels in Lake Titicaca have been correlated with episodes of increased snow cover on Northern Hemisphere continents; this may constitute an analogy to conditions during the Lake Tauca phase.[249] The Tauca phase may have been triggered by the southern shift of tropical atmospheric circulation[250] and a weakening of the Atlantic meridional overturning circulation that decreased northward heat transport.[245] An intensification and southward shift of the South Atlantic Convergence Zone[lower-alpha 2] may have contributed to the precipitation increase[252] but not all records agree.[253]

Another theory posits that vegetation changes and lake development would have decreased the albedo of the Altiplano, resulting in warming and moisture advection of moisture towards the Altiplano,[254] but such positive feedback mechanisms were considered questionable in a 1998 study.[255] Persistent La Niña climatic conditions may have contributed to the lake's filling[256][161] and also to the onset of the first CAPE.[237] Conversely, a global climatic warming and a northward shift of the monsoon occurred around 14,500 years ago,[193] and the northward shift of the ITCZ accompanied the Ticaña lowstand.[194] The ideal conditions for the development of paleolakes in the Altiplano do not appear to exist during maximum glaciation or warm interglacial periods.[157]

Some lake water highstands of Salar de Atacama are associated with Lake Tauca's main highstand phase

During the Tauca phase, Lake Titicaca grew in size; the pampas around Titicaca were left by that lake and the paleolake Minchin.[257] Lake Titicaca rose by about 5 metres (16 ft),[137] reaching a height of 3,815 metres (12,516 ft),[130] and its water became less saline.[72] Another shoreline, at 3,825 metres (12,549 ft) altitude, has been linked to a highstand of Lake Titicaca during the Tauca epoch.[258] The highstand, in 13,180 ± 130 BP, is contemporaneous with the Tauca III phase. Titicaca's water level then dropped during the Ticaña phase and probably rose again during the Coipasa.[186] The highstands left terraces at the southern and eastern shores of Lake Titicaca[lower-alpha 3],[259] which were later deformed by tectonic processes.[260]

Lake Titicaca probably overflowed on the south between 26,000 and 15,000 BP,[196] adding water to Lake Tauca.[261][262] Titicaca's outflow, the Rio Desaguadero, may have been eight times that of today.[83] Lake Titicaca was thought to have had a low water level during the Tauca phase before evidence of deeper water was found.[263] Higher lake levels have been found at the same time in other parts of the Altiplano and areas of the Atacama above 3,500 metres (11,500 ft).[264] This was not the first time Lake Titicaca rose; Pleistocene lake-level rises are known as Mataro, Cabana, Ballivian and Minchin.[265] The overflow from Lake Titicaca into the southern Altiplano was possible for the last 50,000 years; this might explain why there is little evidence of large lakes in the southern Altiplano in the time before 50,000 years ago.[262]

Lakes also formed (or expanded) in the Atacama at that time;[51] highstands in Lejía Lake began rising after 11,480 ± 70 BP, and in Salar Aguas Calientes high-water levels lasted until 8,430 ± 75 BP.[186] Highstands in Laguna Khota occurred around 12,500 and 11,000 BP.[266] The formation of a lake at Salar de Llamara[267] and some Salar de Atacama highstands are associated with Lake Tauca, the Minchin humid period and the Coipasa highstand.[268] Traces of the Tauca humid episode have been found at Salar Pedernales, past 26° south latitude.[269] Between 23,000 and 14,600 a lake formed at Laguna Pozuelos.[146] Lake Tauca's highstand correlates with river terraces in Peru's Pisco River;[270] terraces dated 24,000–16,000 BP in its tributary, the Quebrada Veladera;[133] enlarged drainage systems in the Quebrada Veladera;[271] a humid period at Lake Junin,[272] and new soil formation in the pampas south of the Quinto River in Argentina[273] and in the Ahorcado river valley in Peru.[274] During the second Central Andean Pluvial Event, soils also formed in a wetland of northern Chile.[275]

During the Tauca phase, water levels in Laguna Miscanti were higher than today;[276] shorelines formed from an event in Ch'iyar Quta[148] and Lake Tuyajto;[lower-alpha 4][277] saline lakes formed in the Lipez area,[175] and water levels rose in the Guayatayoc-Salinas Grandes basin,[278] in Laguna de Suches in Peru[279] and lakes at Uturuncu and Lazufre.[280] Some Atacama Altiplano lake levels increased by 30 to 50 metres (98 to 164 ft),[149] Lake levels rose in Laguna Mar Chiquita,[216] Laguna La Salada Grande in the Cordillera Oriental[281] and Salina de Bebedero in Argentina.[232]

Downward expansion of vegetation and increased discharge in the rivers draining to the Pacific Ocean has been correlated to the Tauca period.[232] Evidence exists at the Quebrada Mani archeological site for a higher water supply 16,400–13,700 years ago.[282] During the Tauca, greater flow occurred in rivers in the Atacama region[283] as well as a higher groundwater recharge;[lower-alpha 4][284] more precipitation fell in the Rio Salado valley;[285] flooding in the Río Paraguay-Parana basin[286] and the contribution from Andean rivers such as the Rio Salado and Rio Bermejo increased;[287] the excavation of the Lluta River Valley[lower-alpha 4],[288] Quebrada de Purmamarca[289] and the Colca Canyon may have been aided by an increased water supply,[290] river incision changed,[218] river terraces formed in the Lomas de Lachay,[153] erosion occurred along the Pilcomayo,[291] and an increase in Pacific plankton was probably linked to increased runoff (and an increased nutrient supply) from the Andes.[219] groundwater-fed wetlands developed in the Cordillera de la Costa,[lower-alpha 4][292] and valleys and large salt caves formed northwest of the Salar de Atacama.[lower-alpha 4][293]

Glaciers advanced in the Cordillera de Cochabamba.[243] An ice cap formed over the Los Frailes ignimbrite plateau; its demise after the end of the Lake Tauca period may have allowed magma to ascend and form the Nuevo Mundo volcano.[294] Moraine formed at Hualca Hualca[295] and Nevado de Chañi[296] where glaciers expanded;[281] the Choqueyapu II glacier in the Eastern Cordillera advanced; moraines formed from glacial advances in Argentina[5] (including the Sierra de Santa Victoria);[297] basal sliding glaciers formed at Sajama;[36] periglacial phenomena became more significant in northwestern Argentina from increased moisture supply;[298] glaciers and probably also rock glaciers grew at Sillajhuay;[299] snow cover in the Atacama Altiplano increased to about 10% above 4,000 metres (13,000 ft) elevation;[300] A glacial advance in central Chile around 15,000 years ago, also associated with increased precipitation and the Lake Tauca period, was probably triggered by tropical circulation changes.[301]

Landslide activity decreased in northwestern Argentina[302] but increased at Aricota, Locumba River, Peru;[303] alluvial fans were active in the Cordillera Oriental of Peru;[190] tufa deposition began[lower-alpha 4] in the Cuncaicha cave north of Coropuna;[304] the climate grew wetter over the southern Amazon[305] as evidenced in Brazilian cave deposits;[281] precipitation and forest cover in Pampa del Tamarugal increased[306] with an interruption ("Late Pleistocene Pampa del Tamarugal desiccation event") during the Ticaña lowstand;[194] the vegetation limit in the Atacama desert descended towards the coast; groundwater discharge in the Atacama increased;[307] wetlands developed[lower-alpha 4] at Salar de Punta Negra;[308] the "Pica glass" formed in the Atacama as a consequence of increased vegetation and the occurrence of wildfires in this vegetation[309] and plant pathogens such as rust fungi were more diverse than today.[310] Prosopis tamarugo grew at higher altitude thanks to a better water supply;[lower-alpha 4][311] and vegetation coverage increased in the Atacama Altiplano.[300] The well dated record of Lake Tauca has been used to correlate climatic events elsewhere in the region.[312]

Environmental consequences
The salt deposits of Salar de Uyuni were left by the lake

Paleoindian settlement in South America commenced during the Lake Tauca and Ticaña stages,[313] facilitated by the more favourable environment during the CAPE;[232] the Viscachani culture around Lake Titicaca was contemporaneous with Lake Tauca.[314] The earliest human dispersal in the region around Lake Tauca occurred towards the end of the Ticaña phase, with the Coipasa phase coinciding with the definitive establishment of humans in the region[315] and also their spread through northwestern Argentina, where conditions were favourable.[316] In the Atacama area, Tauca-age paleolakes had provided the environment for first settlers;[300] the end of the paleolake phase coinciding with Lake Tauca was accompanied by the end of the first phase of human settlement,[317] which had occurred during the Central Andean Pluvial Event; now humans left the desert.[318] Likewise in the Altiplano,[319] the wet period that was contemporaneous to Lake Tauca[235] allowed the settlement of Cerro Kaskio[319] and Cueva Bautista close by,[320] and the Central Andean Pluvial Event did the same in the Pampa del Tamarugal[321] and the southern Atacama valleys.[322] The initial peopling of the Salar de Atacama region was during the Lake Tauca[lower-alpha 4] time, but a sharp population drop took place after its drying.[238] Inca towers on the Altiplano have been built with rocks left by Lake Tauca.[323]

Some fossil water reserves in the dry Andes formed during the Tauca phase,[324] the groundwater in the northern Chilean Central Valley[325] and part of the groundwater under Pampa del Tamarugal for example date back to the Lake Tauca wet phase.[326] Lake Tauca may have supplied water to the Rio de la Plata region, sustaining life there during dry periods.[91]

The Lake Tauca and preceding cycles left evaporite deposits,[327] with sediment layers left by the lake in the Salar de Uyuni reaching a thickness of 6 metres (20 ft).[131] The salts are continually washed out and re-deposited by ephemeral rainfall, causing the salt surfaces of the Salars to become very flat and smooth.[82] The high aerosol content of the air in the Uyuni region has been attributed to fine sediments left by Lake Tauca.[22] Diatomaceous deposits containing clay or calc were left behind by the lake,[42] and ulexite deposits were formed by sediments in its deltas.[328]

The taxonomic similarity between fish species of the genus Orestias in Lauca National Park and Salar de Carcote has been attributed to these watersheds' being part of Lake Tauca;[61] in general the evolution of these fish was heavily influenced by the various lake cycles including these that preceded the Tauca cycle.[329] The drying of the ancient lakes would have fragmented amphibious habitats, generating separate populations.[330] Lake Tauca and its predecessors may have created a productive environment[55] that was populated by mammals like glyptodonts;[331] the Atacama Altiplano had far more life than today during the Tauca cycle, including now-extinct deer and horses.[332] On the other hand, the Altiplano lakes would have separated the animal and plant populations.[333]

Altiplanos and paleolakes in Latin America
Latin America Valley of Mexico Altiplano Cundiboyacense Altiplano Boliviano
M
M
C
C
B
B
Paleolake Lake Texcoco Lake Humboldt Lake Tauca
Human occupation (yr BP) 11,100 - Tocuila 12,460 - El Abra 3530 - Tiwanaku
Pre-Columbian civilisation Aztec Muisca Inca
Today Mexico Mexico City Colombia Bogotá, Tunja Peru Lake Titicaca
Bolivia Salar de Uyuni
Elevation 2,236 m (7,336 ft) 2,580 m (8,460 ft) 3,800 m (12,500 ft)
Area 9,738 km2 (3,760 sq mi) 25,000 km2 (9,700 sq mi) 175,773 km2 (67,866 sq mi)
References
[334][335][336]
[337][338][lower-alpha 5]
[339][340][341]

See also

Notes
  1. The Bolivian high is an anticyclone which steers moist air onto the Altiplano.[214]
  2. The South Atlantic Convergence Zone is a rainfall belt over central and southern Brazil during southern hemisphere summer.[251]
  3. The name "Lake Minchin" is often used for the largest lake on the Altiplano,[34] however the highstand at the end of the Pleistocene is called Tauca.[52]
  4. The associated Central Andean Pluvial Event coincided with the formation of Lake Tauca[235]
  5. Area Altiplano Cundiboyacense approximately 25,000 square kilometres (9,700 sq mi)

References
  1. Kohfeld, K.E.; Graham, R.M.; de Boer, A.M.; Sime, L.C.; Wolff, E.W.; Le Quéré, C.; Bopp, L. (May 2013). "Southern Hemisphere westerly wind changes during the Last Glacial Maximum: paleo-data synthesis". Quaternary Science Reviews. 68: 79. Bibcode:2013QSRv...68...76K. doi:10.1016/j.quascirev.2013.01.017.
  2. De la Riva, Ignacio; García-París, Mario; Parra-Olea, Gabriela (25 March 2010). "Systematics of Bolivian frogs of the genus (Anura, Ceratophryidae) based on mtDNA sequences". Systematics and Biodiversity. 8 (1): 58. doi:10.1080/14772000903526454. hdl:10261/51796. S2CID 85269358.
  3. Blard et al. 2013, p. 261.
  4. Rouchy et al. 1996, p. 974.
  5. Zech et al. 2008, p. 639.
  6. Chepstow-Lusty et al. 2005, p. 91.
  7. Argollo & Mourguiart 2000, p. 38.
  8. Blard et al. 2011, p. 3974.
  9. Servant & Fontes 1978, p. 10.
  10. Ballivian & Risacher 1981, p. 17.
  11. Yechieli, Uri Kafri, Yoseph (2010). "Current Continental Base-Levels Above Sea Level". Groundwater Base Level Changes and Adjoining Hydrological Systems. Berlin: Springer. p. 82. doi:10.1007/978-3-642-13944-4_9. ISBN 978-3-642-13944-4.{{cite book}}: CS1 maint: multiple names: authors list (link)
  12. Clayton & Clapperton 1997, p. 169.
  13. Risacher & Fritz 1991, p. 211.
  14. Placzek et al. 2009, p. 25.
  15. Gornitz, Vivien (2009). "Glacial Sediments". Encyclopedia of Paleoclimatology and Ancient Environments. Encyclopedia of Earth Sciences Series (Online-Ausg. ed.). Dordrecht, Netherlands: Springer. p. 380. doi:10.1007/978-1-4020-4411-3_95. ISBN 978-1-4020-4411-3.
  16. Risacher & Fritz 1991, p. 212.
  17. Clayton & Clapperton 1997, p. 170.
  18. Blodgett, Isacks & Lenters 1997, p. 20.
  19. Blodgett, Isacks & Lenters 1997, p. 21.
  20. Blodgett, Isacks & Lenters 1997, p. 23.
  21. Broecker & Putnam 2012, p. 20.
  22. Goudie, Andrew S.; Middleton, Nicholas J. (2006). Desert Dust in the Global System. Berlin, Heidelberg: Springer. pp. 76–77. doi:10.1007/3-540-32355-4. ISBN 978-3-540-32355-6.
  23. Nunnery et al. 2019, p. 883.
  24. Heine 2019, p. 253.
  25. Bradley, Raymond S.; Diaz, Henry F. (December 2021). "Late Quaternary Abrupt Climate Change in the Tropics and Sub‐Tropics: The Continental Signal of Tropical Hydroclimatic Events (THEs)". Reviews of Geophysics. 59 (4): 12. Bibcode:2021RvGeo..5900732B. doi:10.1029/2020RG000732. S2CID 240919206.
  26. Ballivian & Risacher 1981, p. 33.
  27. Sylvestre et al. 1995, p. 296.
  28. Sylvestre et al. 1995, p. 293.
  29. Placzek, Quade & Patchett 2006, p. 516.
  30. Blanco, Saúl; Álvarez-Blanco, Irene; Cejudo-Figueiras, Cristina; De Godos, Ignacio; Bécares, Eloy; Muñoz, Raúl; Guzman, Héctor O.; Vargas, Virginia A.; Soto, Roberto (23 October 2012). "New diatom taxa from high-altitude Andean saline lakes". Diatom Research. 28 (1): 14. doi:10.1080/0269249X.2012.734528. S2CID 85126005.
  31. Placzek, Quade & Patchett 2013, p. 103.
  32. Rossi, Matti J.; Kesseli, Risto; Liuha, Petri; Meneses, Jédu Sagàrnaga; Bustamante, Jonny (October 2002). "A preliminary archaeological and environmental study of pre-Columbian burial towers at Huachacalla, Bolivian Altiplano". Geoarchaeology. 17 (7): 637. doi:10.1002/gea.10032. S2CID 129547417.
  33. Sylvestre et al. 1995, p. 286.
  34. Placzek, Quade & Patchett 2006, p. 517.
  35. Fornari, Risacher & Féraud 2001, p. 271.
  36. Chepstow-Lusty et al. 2005, p. 96.
  37. Martin et al. 2020, p. 2.
  38. Fritz, Sherilyn C; Baker, Paul A; Lowenstein, Tim K; Seltzer, Geoffrey O; Rigsby, Catherine A; Dwyer, Gary S; Tapia, Pedro M; Arnold, Kimberly K; Ku, Teh-Lung; Luo, Shangde (January 2004). "Hydrologic variation during the last 170,000 years in the southern hemisphere tropics of South America". Quaternary Research. 61 (1): 102. Bibcode:2004QuRes..61...95F. doi:10.1016/j.yqres.2003.08.007. hdl:10161/6625. S2CID 45518308.
  39. Fornari, Risacher & Féraud 2001, p. 280.
  40. Dassargues 2000, p. 412.
  41. Clayton & Clapperton 1997, p. 174.
  42. Servant & Fontes 1978, p. 16.
  43. Placzek, Quade & Patchett 2013, p. 99.
  44. Sylvestre et al. 1995, p. 292.
  45. Placzek, Quade & Patchett 2011, p. 242.
  46. Martin et al. 2018, p. 1.
  47. Rouchy et al. 1996, p. 990.
  48. McPhillips et al. 2013, p. 2492.
  49. Bills, Bruce G.; de Silva, Shanaka L.; Currey, Donald R.; Emenger, Robert S.; Lillquist, Karl D.; Donnellan, Andrea; Worden, Bruce (15 February 1994). "Hydro-isostatic deflection and tectonic tilting in the central Andes: Initial results of a GPS survey of Lake Minchin shorelines". Geophysical Research Letters. 21 (4): 293–296. Bibcode:1994GeoRL..21..293B. CiteSeerX 10.1.1.528.1524. doi:10.1029/93GL03544.
  50. Hastenrath & Kutzbach 1985, p. 250.
  51. Clayton & Clapperton 1997, p. 180.
  52. Blodgett, Isacks & Lenters 1997, p. 2.
  53. Clayton & Clapperton 1997, p. 171.
  54. Schäbitz & Liebricht 1999, p. 123.
  55. Arellano 1984, p. 87.
  56. Ahlfeld 1956, p. 130.
  57. Perez-Fernandez, Cesar A.; Iriarte, Mercedes; Hinojosa-Delgadillo, Wilber; Veizaga-Salinas, Andrea; Cano, Raul J.; Rivera-Perez, Jessica; Toranzos, Gary A. (January 2016). "First insight into microbial diversity and ion concentration in the Uyuni salt flat, Bolivia". Caribbean Journal of Science. 49 (1): 58. doi:10.18475/cjos.v49i1.a6. S2CID 89236061.
  58. Ericksen, Vine & Raul Ballón 1978, p. 355.
  59. Collado, Gonzalo A.; Méndez, Marco A. (November 2013). "Microgeographic differentiation among closely related species of (Gastropoda: Planorbidae) from the Andean Altiplano". Zoological Journal of the Linnean Society. 169 (3): 649. doi:10.1111/zoj.12073.
  60. Arellano 1984, p. 90.
  61. Vila, I.; Morales, P.; Scott, S.; Poulin, E.; Véliz, D.; Harrod, C.; Méndez, M. A. (March 2013). "Phylogenetic and phylogeographic analysis of the genus (Teleostei: Cyprinodontidae) in the southern Chilean Altiplano: the relevance of ancient and recent divergence processes in speciation". Journal of Fish Biology. 82 (3): 927–43. doi:10.1111/jfb.12031. hdl:10533/135014. PMID 23464552. S2CID 12989178.
  62. Torre, Gabriela; Gaiero, Diego M; Cosentino, Nicolás Juan; Coppo, Renata; Oliveira-Sawakuchi, André (1 April 2020). "New insights on sources contributing dust to the loess record of the western edge of the Pampean Plain during the transition from the late MIS 2 to the early Holocene". The Holocene. 30 (4): 543. Bibcode:2020Holoc..30..537T. doi:10.1177/0959683619875187. ISSN 0959-6836. S2CID 203137981.
  63. Romero, Matías; Torre, Gabriela; Gaiero, Diego M. (10 April 2021). "Paleoenvironmental changes in southern South American dust sources during the last glacial/interglacial transition: Evidence from clay mineral assemblages of the pampean loess". Quaternary International. 580: 19. Bibcode:2021QuInt.580...11R. doi:10.1016/j.quaint.2020.12.044. ISSN 1040-6182. S2CID 233526238.
  64. Torre, Gabriela; Gaiero, Diego; Coppo, Renata; Cosentino, Nicolás J.; Goldstein, Steven L.; De Vleeschouwer, François; Roux, Gael Le; Bolge, Louise; Kiro, Yael; Sawakuchi, André Oliveira (1 September 2022). "Unraveling late Quaternary atmospheric circulation in the Southern Hemisphere through the provenance of Pampean loess" (PDF). Earth-Science Reviews. 232: 12. Bibcode:2022ESRv..23204143T. doi:10.1016/j.earscirev.2022.104143. S2CID 251479393.
  65. Francis, P. W.; Wells, G. L. (July 1988). "Landsat Thematic Mapper observations of debris avalanche deposits in the Central Andes". Bulletin of Volcanology. 50 (4): 265. Bibcode:1988BVol...50..258F. doi:10.1007/BF01047488. S2CID 128824938.
  66. Risacher & Fritz 2000, p. 382.
  67. Blodgett, Isacks & Lenters 1997, p. 11.
  68. Vimeux, Françoise (2009). "Similarities and Discrepancies Between Andean Ice Cores over the Last Deglaciation: Climate Implications". In Vimeux, Françoise; Sylvestre, Florence; Khodri, Myriam (eds.). Past Climate Variability in South America and Surrounding Regions. Developments in Paleoenvironmental Research. Vol. 14. [Dordrecht]: Springer. p. 251. doi:10.1007/978-90-481-2672-9_10. ISBN 978-90-481-2672-9.
  69. Placzek, Quade & Patchett 2011, p. 240.
  70. Blard et al. 2011, p. 3986.
  71. Blard et al. 2011, p. 3975.
  72. Sylvestre et al. 1995, p. 282.
  73. Nunnery et al. 2019, p. 889.
  74. Risacher & Fritz 1991, p. 223.
  75. Servant & Fontes 1978, p. 20.
  76. Risacher & Fritz 1991, p. 224.
  77. Risacher & Fritz 2000, p. 381.
  78. Ballivian & Risacher 1981, p. 132.
  79. Risacher & Fritz 2000, p. 378.
  80. Coudrain-Ribstein, Anne; Olive, Philippe; Quintanilla, Jorge; Sondag, Francis; Cahuaya, David (1995). "Salinity and isotopic dynamics of the groundwater resources on the Bolivian Altiplano" (PDF). Application of Tracers in Arid Zone Hydrology: 270. Archived (PDF) from the original on 22 November 2006. Retrieved 25 September 2016.
  81. Risacher & Fritz 2000, p. 374.
  82. Ericksen, Vine & Raul Ballón 1978, p. 356.
  83. Grove et al. 2003, p. 294.
  84. Cross et al. 2001, p. 7.
  85. Coudrain et al. 2002, p. 303.
  86. Baker et al. 2001, p. 700.
  87. Placzek, Quade & Patchett 2011, p. 239.
  88. Fritz, S.C.; Baker, P.A.; Tapia, P.; Spanbauer, T.; Westover, K. (February 2012). "Evolution of the Lake Titicaca basin and its diatom flora over the last ~370,000 years". Palaeogeography, Palaeoclimatology, Palaeoecology. 317–318: 101. Bibcode:2012PPP...317...93F. doi:10.1016/j.palaeo.2011.12.013.
  89. Risacher, François; Fritz, Bertrand; Alonso, Hugo (May 2006). "Non-conservative behavior of bromide in surface waters and brines of Central Andes: A release into the atmosphere?". Geochimica et Cosmochimica Acta. 70 (9): 2144. Bibcode:2006GeCoA..70.2143R. doi:10.1016/j.gca.2006.01.019.
  90. Blard et al. 2009, p. 3421.
  91. Sánchez-Saldías & Fariña 2014, p. 258.
  92. Sánchez-Saldías & Fariña 2014, p. 257.
  93. Ahlfeld 1956, p. 132.
  94. Ahlfeld, Federico (1946). "Geología de Bolivia". Revista del Museo de La Plata. 3 (19): 299. ISSN 2545-6377.
  95. Seltzer 1990, p. 147.
  96. Seltzer 1990, p. 149.
  97. Grove et al. 2003, p. 282.
  98. Hastenrath & Kutzbach 1985, p. 254.
  99. Blodgett, Isacks & Lenters 1997, p. 12.
  100. Grove et al. 2003, p. 290.
  101. Placzek, Quade & Patchett 2011, p. 243.
  102. Placzek, Quade & Patchett 2011, p. 241.
  103. Blard et al. 2011, p. 3987.
  104. Martin et al. 2018, p. 4.
  105. Palacios et al. 2020, p. 16.
  106. Grosjean, Martin; Núñez, Lautaro; Cartajena, Isabel; Messerli, Bruno (September 1997). "Mid-Holocene Climate and Culture Change in the Atacama Desert, Northern Chile". Quaternary Research. 48 (2): 242. Bibcode:1997QuRes..48..239G. doi:10.1006/qres.1997.1917. S2CID 128555380.
  107. Placzek, Quade & Patchett 2011, p. 233.
  108. Blard et al. 2009, p. 3417.
  109. Clayton & Clapperton 1997, p. 181.
  110. Hastenrath & Kutzbach 1985, p. 255.
  111. Schäbitz & Liebricht 1999, pp. 115–116.
  112. Placzek et al. 2006, p. 11.
  113. Tapia, Joseline; Audry, Stéphane; van Beek, Pieter (March 2020). "Natural and anthropogenic controls on particulate metal(loid) deposition in Bolivian highland sediments, Lake Uru Uru (Bolivia)". The Holocene. 30 (3): 437. Bibcode:2020Holoc..30..428T. doi:10.1177/0959683619887425. S2CID 213568450.
  114. Chepstow-Lusty et al. 2005, p. 93.
  115. Chepstow-Lusty et al. 2005, p. 95.
  116. Chepstow-Lusty et al. 2005, p. 97.
  117. Gosling et al. 2008, p. 48.
  118. Sylvestre et al. 1999, p. 59.
  119. Rouchy et al. 1996, p. 987.
  120. Blard et al. 2011, p. 3976.
  121. Placzek, Quade & Patchett 2006, p. 519.
  122. Rouchy et al. 1996, p. 989.
  123. Rouchy et al. 1996, p. 978.
  124. Moon 1939, p. 30.
  125. Moon 1939, p. 31.
  126. Sánchez-Saldías & Fariña 2014, p. 250.
  127. Moon 1939, p. 32.
  128. ROUCHY, JEAN MARIE; SERVANT, MICHEL; FOURNIER, MARC; CAUSSE, CHRISTIANE (December 1996). "Extensive carbonate algal bioherms in upper Pleistocene saline lakes of the central Altiplano of Bolivia". Sedimentology. 43 (6): 975. Bibcode:1996Sedim..43..973R. doi:10.1111/j.1365-3091.1996.tb01514.x.
  129. Bowman 1914, p. 178.
  130. Fornari, Risacher & Féraud 2001, p. 270.
  131. Fornari, Risacher & Féraud 2001, p. 279.
  132. Placzek, Quade & Patchett 2006, p. 520.
  133. McPhillips et al. 2013, p. 2490.
  134. Placzek, Quade & Patchett 2006, p. 528.
  135. Nunnery et al. 2019, p. 882.
  136. Placzek et al. 2009, p. 34.
  137. Dejoux & Iltis 1992, p. 9.
  138. Placzek et al. 2009, p. 32.
  139. Placzek et al. 2009, p. 30.
  140. Collado, Gonzalo A.; Vila, Irma; Méndez, Marco A. (November 2011). "Monophyly, candidate species and vicariance in Biomphalaria snails (Mollusca: Planorbidae) from the Southern Andean Altiplano". Zoologica Scripta. 40 (6): 620. doi:10.1111/j.1463-6409.2011.00491.x. hdl:10533/134786. S2CID 84024906.
  141. Placzek et al. 2009, p. 27.
  142. Martínez, José M.; Escudero, Cristina; Rodríguez, Nuria; Rubin, Sergio; Amils, Ricardo (2021). "Subsurface and surface halophile communities of the chaotropic Salar de Uyuni". Environmental Microbiology. 23 (7): 3996. doi:10.1111/1462-2920.15411. hdl:10261/269288. ISSN 1462-2920. PMID 33511754. S2CID 231767839.
  143. Ahlfeld, Federico (1972). Geología de Bolivia (in Spanish). Editorial Los Amigos del Libro. p. 158.
  144. Heine 2019, p. 223.
  145. Baker et al. 2001, p. 699.
  146. McGLUE, MICHAEL M.; PALACIOS-FEST, MANUEL R.; CUSMINSKY, GABRIELA C.; CAMACHO, MARIA; IVORY, SARAH J.; KOWLER, ANDREW L.; CHAKRABORTY, SUVANKAR (1 June 2017). "Ostracode Biofacies and Shell Chemistry Reveal Quaternary Aquatic Transitions in the Pozuelos Basin (Argentina)". PALAIOS. 32 (6): 423. Bibcode:2017Palai..32..413M. doi:10.2110/palo.2016.089. ISSN 0883-1351. S2CID 133734484 – via ResearchGate.
  147. Bookhagen, Bodo; Haselton, Kirk; Trauth, Martin H (May 2001). "Hydrological modelling of a Pleistocene landslide-dammed lake in the Santa Maria Basin, NW Argentina". Palaeogeography, Palaeoclimatology, Palaeoecology. 169 (1–2): 113. Bibcode:2001PPP...169..113B. doi:10.1016/S0031-0182(01)00221-8.
  148. Servant-Vildary & Mello e Sousa 1993, p. 71.
  149. Huber, Bugmann & Reasoner 2005, p. 96.
  150. Sifeddine, Abdelfettah; Martin, Louis; Turcq, Bruno; Volkmer-Ribeiro, Cecilia; Soubiès, Francois; Cordeiro, Renato Campello; Suguio, Kenitiro (15 April 2001). "Variations of the Amazonian rainforest environment: a sedimentological record covering 30,000 years". Palaeogeography, Palaeoclimatology, Palaeoecology. 168 (3): 231. Bibcode:2001PPP...168..221S. doi:10.1016/S0031-0182(00)00256-X.
  151. Litty, Camille; Schlunegger, Fritz; Akçar, Naki; Delunel, Romain; Christl, Marcus; Vockenhuber, Christof (15 August 2018). "Chronology of alluvial terrace sediment accumulation and incision in the Pativilca Valley, western Peruvian Andes". Geomorphology. 315: 55. Bibcode:2018Geomo.315...45L. doi:10.1016/j.geomorph.2018.05.005. S2CID 134540130.
  152. Litty, Camille; Duller, Robert; Schlunegger, Fritz (15 June 2016). "Paleohydraulic reconstruction of a 40 ka-old terrace sequence implies that water discharge was larger than today: Paleohydraulic Reconstruction in the Pisco Valley, Peru". Earth Surface Processes and Landforms. 41 (7): 885. doi:10.1002/esp.3872. S2CID 67779046.
  153. Kalicki, Tomasz; Kalicki, Piotr (15 May 2020). "Fluvial activity in the Lomas de Lachay during the upper Pleistocene and Holocene". Geomorphology. 357: 11. Bibcode:2020Geomo.35707087K. doi:10.1016/j.geomorph.2020.107087. ISSN 0169-555X. S2CID 214164504.
  154. Schäbitz & Liebricht 1999, p. 122.
  155. Luna, Lisa V.; Bookhagen, Bodo; Niedermann, Samuel; Rugel, Georg; Scharf, Andreas; Merchel, Silke (October 2018). "Glacial chronology and production rate cross-calibration of five cosmogenic nuclide and mineral systems from the southern Central Andean Plateau". Earth and Planetary Science Letters. 500: 249. Bibcode:2018E&PSL.500..242L. doi:10.1016/j.epsl.2018.07.034. ISSN 0012-821X. S2CID 134780354.
  156. Clapperton, C.M. (1991). "Glacier fluctuations of the last glacial-interglacial cycle in the Andes of South America". Bamberger Geograpische Schriften. 11: 196.
  157. Clapperton et al. 1997, p. 58.
  158. Seltzer 1990, p. 142.
  159. Heine 2019, p. 270.
  160. Gerth, H. (1 August 1915). "Geologische und morphologische Beobachtungen in den Kordilleren Südperús". Geologische Rundschau (in German). 6 (3): 131. Bibcode:1915GeoRu...6..129G. doi:10.1007/BF01797474. ISSN 1432-1149. S2CID 129226182.
  161. Placzek, Quade & Patchett 2006, p. 531.
  162. Bills, Bruce G.; Borsa, Adrian A.; Comstock, Robert L. (March 2007). "MISR-based passive optical bathymetry from orbit with few-cm level of accuracy on the Salar de Uyuni, Bolivia". Remote Sensing of Environment. 107 (1–2): 243. Bibcode:2007RSEnv.107..240B. doi:10.1016/j.rse.2006.11.006.
  163. Servant & Fontes 1978, pp. 20–21.
  164. Messerli, Grosjean & Vuille 1997, p. 231.
  165. Servant & Fontes 1978, p. 15.
  166. Rouchy et al. 1996, p. 983.
  167. Gosling et al. 2008, p. 46.
  168. Gosling et al. 2008, p. 47.
  169. Fornari, Risacher & Féraud 2001, p. 272.
  170. Broecker & Putnam 2012, p. 19.
  171. Sylvestre et al. 1999, p. 54.
  172. Servant & Fontes 1978, p. 19.
  173. Servant & Fontes 1978, p. 17.
  174. Servant-Vildary & Mello e Sousa 1993, p. 70.
  175. Rouchy et al. 1996, p. 975.
  176. Clayton & Clapperton 1997, p. 175.
  177. Sylvestre et al. 1999, p. 60.
  178. Sylvestre et al. 1999, p. 63.
  179. Sylvestre et al. 1995, p. 294.
  180. Institut de recherche pour le développement (França); Universitat de Barcelona; Instituto Geológico y Minero de España (2005). Geodinámica Andina: Resúmenes Ampliados. IRD Editions. p. 61. ISBN 978-2-7099-1575-5.
  181. Placzek, Quade & Patchett 2006, pp. 524–525.
  182. Placzek, Quade & Patchett 2006, p. 527.
  183. Blard et al. 2011, p. 3984.
  184. Martin et al. 2020, pp. 2–3.
  185. Martin et al. 2020, p. 3.
  186. Sylvestre et al. 1999, p. 62.
  187. Kull & Grosjean 1998, p. 871.
  188. Sáez, Alberto; Godfrey, Linda V.; Herrera, Christian; Chong, Guillermo; Pueyo, Juan J. (August 2016). "Timing of wet episodes in Atacama Desert over the last 15 ka. The Groundwater Discharge Deposits (GWD) from Domeyko Range at 25°S". Quaternary Science Reviews. 145: 91. Bibcode:2016QSRv..145...82S. doi:10.1016/j.quascirev.2016.05.036. hdl:2445/99385.
  189. Abbott, M (December 2000). "Holocene hydrological reconstructions from stable isotopes and paleolimnology, Cordillera Real, Bolivia". Quaternary Science Reviews. 19 (17–18): 1816. Bibcode:2000QSRv...19.1801A. doi:10.1016/S0277-3791(00)00078-0.
  190. Frechen et al. 2018, p. 16.
  191. Argollo & Mourguiart 2000, p. 40.
  192. Placzek et al. 2009, p. 33.
  193. Blard et al. 2013, p. 272.
  194. Workman et al. 2020, p. 16.
  195. Williams, Joseph J.; Gosling, William D.; Brooks, Stephen J.; Coe, Angela L.; Xu, Sheng (December 2011). "Vegetation, climate and fire in the eastern Andes (Bolivia) during the last 18,000 years". Palaeogeography, Palaeoclimatology, Palaeoecology. 312 (1–2): 122. Bibcode:2011PPP...312..115W. doi:10.1016/j.palaeo.2011.10.001.
  196. Baker, P. A. (2001). "The History of South American Tropical Precipitation for the Past 25,000 Years". Science. 291 (5504): 640–3. Bibcode:2001Sci...291..640B. doi:10.1126/science.291.5504.640. ISSN 0036-8075. PMID 11158674. S2CID 112618.
  197. Bush, M. B.; Hanselman, J. A.; Gosling, W. D. (December 2010). "Nonlinear climate change and Andean feedbacks: an imminent turning point?". Global Change Biology. 16 (12): 3227. Bibcode:2010GCBio..16.3223B. doi:10.1111/j.1365-2486.2010.02203.x. S2CID 86021680.
  198. Quesada et al. 2015, p. 94.
  199. Palacios et al. 2020, p. 33.
  200. Hoguin, Rodolphe; Catá, María Paz; Solá, Patricia; Yacobaccio, Hugo D. (April 2012). "The spatial organization in Hornillos 2 rockshelter during the Middle Holocene (Jujuy Puna, Argentina)". Quaternary International. 256: 45–53. Bibcode:2012QuInt.256...45H. doi:10.1016/j.quaint.2011.08.026.
  201. Rouchy et al. 1996, p. 976.
  202. Baied, Carlos A.; Wheeler, Jane C. (May 1993). "Evolution of High Andean Puna Ecosystems: Environment, Climate, and Culture Change over the Last 12,000 Years in the Central Andes". Mountain Research and Development. 13 (2): 145–156. doi:10.2307/3673632. JSTOR 3673632. Retrieved 27 September 2016.
  203. Kull, Christoph; Grosjean, Martin (1 December 2000). "Late Pleistocene climate conditions in the north Chilean Andes drawn from a climate–glacier model". Journal of Glaciology. 46 (155): 622–632. Bibcode:2000JGlac..46..622K. doi:10.3189/172756500781832611.
  204. Hastenrath & Kutzbach 1985, p. 253.
  205. Rigsby et al. 2005, p. 672.
  206. Blard et al. 2009, p. 3422.
  207. Martin et al. 2020, p. 23.
  208. Martin et al. 2018, p. 3.
  209. Placzek, Quade & Patchett 2013, p. 104.
  210. Valero-Garcés, Blas; Delgado-Huertas, Antonio; Ratto, Norma; Navas, Ana; Edwards, Larry (2000). "Paleohydrology of Andean saline lakes from sedimentological and isotopic records, Northwestern Argentina". Journal of Paleolimnology. 24 (3): 344. Bibcode:2000JPall..24..343V. doi:10.1023/A:1008146122074. hdl:10261/100304. S2CID 129052389.
  211. Londoño, Ana Cristina; Forman, Steven L.; Eichler, Timothy; Pierson, James (August 2012). "Episodic eolian deposition in the past ca. 50,000 years in the Alto Ilo dune field, southern Peru". Palaeogeography, Palaeoclimatology, Palaeoecology. 346–347: 13. Bibcode:2012PPP...346...12L. doi:10.1016/j.palaeo.2012.05.008.
  212. Palacios et al. 2020, p. 27.
  213. Palacios et al. 2020, p. 29.
  214. Martin et al. 2020, p. 24.
  215. Martin et al. 2018, pp. 5–6.
  216. Cuña-Rodríguez et al. 2020, p. 10.
  217. Placzek, Quade & Patchett 2006, p. 530.
  218. D'Arcy et al. 2019, p. 39.
  219. Mohtadi, M.; Romero, O. E.; Hebbeln, D. (May 2004). "Changing marine productivity off northern Chile during the past 19 000 years: a multivariable approach". Journal of Quaternary Science. 19 (4): 355. Bibcode:2004JQS....19..347M. doi:10.1002/jqs.832. S2CID 140586233.
  220. Flenley, Mark B. Bush, John (2011). "Andean montane forests and climate change". Tropical Rainforest Responses to Climatic Change (2 ed.). Berlin: Springer. pp. 35–60. doi:10.1007/978-3-642-05383-2_2. ISBN 978-3-642-05383-2. S2CID 128502460.{{cite book}}: CS1 maint: multiple names: authors list (link)
  221. Bräuning, A. (13 October 2009). "Climate variability of the tropical Andes since the late Pleistocene". Advances in Geosciences. 22: 15. Bibcode:2009AdG....22...13B. doi:10.5194/adgeo-22-13-2009.
  222. Grosjean, M.; Messerli, B.; Veit, H.; Geyh, M.A.; Schreier, H. (1 July 1998). "A late-Holocene (,2600 BP) glacial advance in the south- central Andes (298S), northern Chile". The Holocene. 8 (4): 473–479. doi:10.1191/095968398677627864. S2CID 129593047.
  223. Gardeweg, Moyra Cristina; Delcorto, Luis; Selles, Daniel (December 2018). Depósitos glaciares de la alta cordillera de Iquique - Región de Tarapacá, Chile (PDF). 15th Chilean Geological Congress (in Spanish). p. 672. Retrieved 13 November 2022.
  224. Servant & Fontes 1978, p. 22.
  225. Smith, Lowell & Caffee 2009, p. 367.
  226. Vizy & Cook 2007, p. 5.
  227. Smith, Colby A.; Lowell, Thomas V.; Owen, Lewis A.; Caffee, Marc W. (January 2011). "Late Quaternary glacial chronology on Nevado Illimani, Bolivia, and the implications for paleoclimatic reconstructions across the Andes". Quaternary Research. 75 (1): 8. Bibcode:2011QuRes..75....1S. doi:10.1016/j.yqres.2010.07.001. S2CID 129861307.
  228. Ammann, Caspar; Jenny, Bettina; Kammer, Klaus; Messerli, Bruno (August 2001). "Late Quaternary Glacier response to humidity changes in the arid Andes of Chile (18–29°S)". Palaeogeography, Palaeoclimatology, Palaeoecology. 172 (3–4): 324. Bibcode:2001PPP...172..313A. doi:10.1016/S0031-0182(01)00306-6.
  229. Quesada et al. 2015, p. 103.
  230. Martin et al. 2020, p. 25.
  231. Seltzer 1990, p. 150.
  232. Quade, Jay; Dente, Elad; Cartwright, Alyson; Hudson, Adam; Jimenez-Rodriguez, Sebastian; McGee, David (September 2022). "Central Andean (28–34°S) flood record 0–25 ka from Salinas del Bebedero, Argentina". Quaternary Research. 109: 123. Bibcode:2022QuRes.109..102Q. doi:10.1017/qua.2022.1. S2CID 252384172.
  233. Latorre et al. 2019, pp. 72–73.
  234. Latorre et al. 2019, p. 73.
  235. Santoro, Calogero M.; Osorio, Daniela; Standen, Vivien G.; Ugalde, Paula C.; Herrera, Katherine; Gayó, Eugenia M.; Rothhammer, Francisco; Latorre, Claudio (2011). "Ocupaciones humanas tempranas y condiciones paleoambientales en el Desierto de Atacama durante la transición Pleistoceno-Holoceno". Boletín de Arqueología PUCP (in Spanish). 15: 5–6. ISSN 1029-2004. Retrieved 1 September 2016.
  236. Díaz, Francisca P.; Latorre, Claudio; Carrasco‐Puga, Gabriela; Wood, Jamie R.; Wilmshurst, Janet M.; Soto, Daniela C.; Cole, Theresa L.; Gutiérrez, Rodrigo A. (25 February 2019). "Multiscale climate change impacts on plant diversity in the Atacama Desert". Global Change Biology. 25 (5): 1734. Bibcode:2019GCBio..25.1733D. doi:10.1111/gcb.14583. PMID 30706600. S2CID 73431668.
  237. Gutiérrez et al. 2018, p. 2.
  238. Souza et al. 2021, p. 2.
  239. Riquelme, Rodrigo; Rojas, Constanza; Aguilar, Germán; Flores, Pablo (January 2011). "Late Pleistocene–early Holocene paraglacial and fluvial sediment history in the Turbio valley, semiarid Chilean Andes". Quaternary Research. 75 (1): 173. Bibcode:2011QuRes..75..166R. doi:10.1016/j.yqres.2010.10.001. S2CID 140202754.
  240. Kaiser, Jérôme; Schefuß, Enno; Lamy, Frank; Mohtadi, Mahyar; Hebbeln, Dierk (November 2008). "Glacial to Holocene changes in sea surface temperature and coastal vegetation in north central Chile: high versus low latitude forcing". Quaternary Science Reviews. 27 (21–22): 2070. Bibcode:2008QSRv...27.2064K. doi:10.1016/j.quascirev.2008.08.025.
  241. Núñez, Lautaro; Loyola, Rodrigo; Cartajena, Isabel; López, Patricio; Santander, Boris; Maldonado, Antonio; de Souza, Patricio; Carrasco, Carlos (February 2018). "Miscanti-1: Human occupation during the arid Mid-Holocene event in the high-altitude lakes of the Atacama Desert, South America". Quaternary Science Reviews. 181: 109. Bibcode:2018QSRv..181..109N. doi:10.1016/j.quascirev.2017.12.010. ISSN 0277-3791.
  242. Workman et al. 2020, p. 15.
  243. May, Jan-Hendrik; Zech, Jana; Zech, Roland; Preusser, Frank; Argollo, Jaime; Kubik, Peter W.; Veit, Heinz (July 2011). "Reconstruction of a complex late Quaternary glacial landscape in the Cordillera de Cochabamba (Bolivia) based on a morphostratigraphic and multiple dating approach". Quaternary Research. 76 (1): 115. Bibcode:2011QuRes..76..106M. doi:10.1016/j.yqres.2011.05.003. S2CID 129771332.
  244. Zech, Jana; Zech, Roland; May, Jan-Hendrik; Kubik, Peter W.; Veit, Heinz (July 2010). "Lateglacial and early Holocene glaciation in the tropical Andes caused by La Niña-like conditions". Palaeogeography, Palaeoclimatology, Palaeoecology. 293 (1–2): 252. Bibcode:2010PPP...293..248Z. doi:10.1016/j.palaeo.2010.05.026.
  245. D'Arcy et al. 2019, p. 40.
  246. Kull, C.; Imhof, S.; Grosjean, M.; Zech, R.; Veit, H. (January 2008). "Late Pleistocene glaciation in the Central Andes: Temperature versus humidity control — A case study from the eastern Bolivian Andes (17°S) and regional synthesis". Global and Planetary Change. 60 (1–2): 160. Bibcode:2008GPC....60..148K. doi:10.1016/j.gloplacha.2007.03.011.
  247. Grove et al. 2003, p. 292.
  248. May, Jan-Hendrik; Zech, Roland; Veit, Heinz (June 2008). "Late Quaternary paleosol–sediment-sequences and landscape evolution along the Andean piedmont, Bolivian Chaco". Geomorphology. 98 (1–2): 48. Bibcode:2008Geomo..98...34M. doi:10.1016/j.geomorph.2007.02.025.
  249. Heine 2019, p. 216.
  250. Grosjean, Martin (May 1994). "Paleohydrology of the Laguna Lejía (north Chilean Altiplano) and climatic implications for late-glacial times". Palaeogeography, Palaeoclimatology, Palaeoecology. 109 (1): 95. Bibcode:1994PPP...109...89G. doi:10.1016/0031-0182(94)90119-8.
  251. Wong et al. 2021, p. 1.
  252. Wong et al. 2021, p. 6.
  253. Wong et al. 2021, p. 7.
  254. Kull & Grosjean 1998, p. 872.
  255. Kull & Grosjean 1998, p. 878.
  256. Cohen, T.J.; Nanson, G.C.; Jansen, J.D.; Jones, B.G.; Jacobs, Z.; Larsen, J.R.; May, J.-H.; Treble, P.; Price, D.M.; Smith, A.M. (October 2012). "Late Quaternary mega-lakes fed by the northern and southern river systems of central Australia: Varying moisture sources and increased continental aridity". Palaeogeography, Palaeoclimatology, Palaeoecology. 356–357: 105–106. Bibcode:2012PPP...356...89C. doi:10.1016/j.palaeo.2011.06.023.
  257. John Wayne Janusek (12 May 2008). Ancient Tiwanaku. Cambridge University Press. p. 48. ISBN 978-0-521-81635-9.
  258. Blodgett, Isacks & Lenters 1997, p. 3.
  259. Quino Lima, Israel; Ramos Ramos, Oswaldo; Ormachea Muñoz, Mauricio; Quintanilla Aguirre, Jorge; Duwig, Celine; Maity, Jyoti Prakash; Sracek, Ondra; Bhattacharya, Prosun (June 2020). "Spatial dependency of arsenic, antimony, boron and other trace elements in the shallow groundwater systems of the Lower Katari Basin, Bolivian Altiplano". Science of the Total Environment. 719: 4. Bibcode:2020ScTEn.719m7505Q. doi:10.1016/j.scitotenv.2020.137505. PMID 32120110. S2CID 211832412.
  260. Vella, Marc-Antoine; Loget, Nicolas (1 November 2021). "Geomorphological map of the Tiwanaku River watershed in Bolivia: Implications for past and present human occupation" (PDF). CATENA. 206: 3. Bibcode:2021Caten.20605508V. doi:10.1016/j.catena.2021.105508.
  261. Vizy & Cook 2007, p. 1.
  262. Heine 2019, p. 217.
  263. Hillyer, Rachel; Valencia, Bryan G.; Bush, Mark B.; Silman, Miles R.; Steinitz-Kannan, Miriam (January 2009). "A 24,700-yr paleolimnological history from the Peruvian Andes". Quaternary Research. 71 (1): 78. Bibcode:2009QuRes..71...71H. doi:10.1016/j.yqres.2008.06.006. S2CID 32856578.
  264. Grosjean, Martin; Núñez, A. Lautaro (July 1994). "Lateglacial, early and middle holocene environments, human occupation, and resource use in the Atacama (Northern Chile)". Geoarchaeology. 9 (4): 274. doi:10.1002/gea.3340090402.
  265. E. Gierlowski-Kordesch; K. Kelts (23 November 2006). Global Geological Record of Lake Basins. Cambridge University Press. p. 405. ISBN 978-0-521-03168-4.
  266. Blodgett, Isacks & Lenters 1997, p. 4.
  267. Quezada, Andrés; Varas, Laura; Vásquez, Paulina; Sepúlveda, Fernando; Cifuentes, José Luis (December 2018). Evidencias de un paleolago durante el Pleistoceno Tardío en el salar de Llamara, Desierto de Atacama, Región de Tarapacá, Chile (PDF). 15th Chilean Geological Congress (in Spanish). p. 1342. Retrieved 13 November 2022.
  268. Bobst, Andrew L; Lowenstein, Tim K; Jordan, Teresa E; Godfrey, Linda V; Ku, Teh-Lung; Luo, Shangde (September 2001). "A 106ka paleoclimate record from drill core of the Salar de Atacama, northern Chile". Palaeogeography, Palaeoclimatology, Palaeoecology. 173 (1–2): 21–42. Bibcode:2001PPP...173...21B. doi:10.1016/S0031-0182(01)00308-X.
  269. Messerli, Grosjean & Vuille 1997, p. 232.
  270. Norton, K. P.; Schlunegger, F.; Litty, C. (2 February 2016). "On the potential for regolith control of fluvial terrace formation in semi-arid escarpments" (PDF). Earth Surface Dynamics. 4 (1): 148. Bibcode:2016ESuD....4..147N. doi:10.5194/esurf-4-147-2016. Retrieved 1 September 2016.
  271. McPhillips et al. 2013, p. 2497.
  272. Smith, Jacqueline A.; Mark, Bryan G.; Rodbell, Donald T. (September 2008). "The timing and magnitude of mountain glaciation in the tropical Andes". Journal of Quaternary Science. 23 (6–7): 630. Bibcode:2008JQS....23..609S. doi:10.1002/jqs.1224. S2CID 58905345.
  273. Tripaldi, Alfonsina; Forman, Steven L. (May 2016). "Eolian depositional phases during the past 50 ka and inferred climate variability for the Pampean Sand Sea, western Pampas, Argentina". Quaternary Science Reviews. 139: 91. Bibcode:2016QSRv..139...77T. doi:10.1016/j.quascirev.2016.03.007.
  274. Benavente, Carlos; Palomino, Anderson; Wimpenny, Sam; García, Briant; Rosell, Lorena; Aguirre, Enoch; Macharé, José; Rodriguez Padilla, Alba M.; Hall, Sarah R. (July 2022). "Paleoseismic evidence of the 1715 C.E earthquake on the Purgatorio Fault in Southern Peru: Implications for seismic hazard in subduction zones". Tectonophysics. 834: 8. Bibcode:2022Tectp.83429355B. doi:10.1016/j.tecto.2022.229355. S2CID 248279365.
  275. Pol-Holz, Ricardo De; Queffelec, Alain; Ibañez, Lucia; González, Juan S.; Sepulveda, Marcela; Gayo, Eugenia M.; Sitzia, Luca (2019). "A perched, high-elevation wetland complex in the Atacama Desert (northern Chile) and its implications for past human settlement" (PDF). Quaternary Research. 92 (1): 33–52. Bibcode:2019QuRes..92...33S. doi:10.1017/qua.2018.144. ISSN 0033-5894. S2CID 133749937.
  276. Núñez, Lautaro A.; Grosjean, Martín; Cartajena, Isabel F. (1999). "Un ecorefugio oportunístico en la puna de Atacama durante eventos áridos del Holoceno Medio". Estudios Atacameños. Arqueología y Antropología Surandinas (in Spanish). 17: 134. ISSN 0718-1043. Archived from the original on 2 December 2016. Retrieved 1 September 2016.
  277. Urrutia, Javier; Herrera, Christian; Custodio, Emilio; Jódar, Jorge; Medina, Agustín (20 December 2019). "Groundwater recharge and hydrodynamics of complex volcanic aquifers with a shallow saline lake: Laguna Tuyajto, Andean Cordillera of northern Chile". Science of the Total Environment. 697: 3. Bibcode:2019ScTEn.697m4116U. doi:10.1016/j.scitotenv.2019.134116. ISSN 0048-9697. PMID 32380610. S2CID 202876663.
  278. Lopez Steinmetz, Romina L.; Galli, Claudia I. (30 January 2015). "Cambio hidrológico asociado al Último Maximo Glacial-Altitermal durante la transición Pleistoceno-Holoceno en el borde oriental de Puna Norte". Andean Geology. 42 (1). doi:10.5027/andgeoV42n1-a01. Archived from the original on 3 November 2014. Retrieved 24 September 2016.
  279. Vining, Benjamin R; Steinman, Byron A; Abbott, Mark B; Woods, Arielle (28 November 2018). "Paleoclimatic and archaeological evidence from Lake Suches for highland Andean refugia during the arid middle-Holocene". The Holocene. 29 (2): 328–344. doi:10.1177/0959683618810405. ISSN 0959-6836.
  280. Perkins, Jonathan P.; Finnegan, Noah J.; Henderson, Scott T.; Rittenour, Tammy M. (August 2016). "Topographic constraints on magma accumulation below the actively uplifting Uturuncu and Lazufre volcanic centers in the Central Andes". Geosphere. 12 (4): 1078–1096. Bibcode:2016Geosp..12.1078P. doi:10.1130/GES01278.1.
  281. Guerra, Lucía; Martini, Mateo A.; Vogel, Hendrik; Piovano, Eduardo L.; Hajdas, Irka; Astini, Ricardo; De Haller, Antoine; Moscariello, Andrea; Loizeau, Jean‐Luc; Ariztegui, Daniel (October 2022). "Microstratigraphy and palaeoenvironmental implications of a Late Quaternary high‐altitude lacustrine record in the subtropical Andes". Sedimentology. 69 (6): 2608. doi:10.1111/sed.13004. hdl:20.500.11850/572803. ISSN 0037-0746. S2CID 248628487.
  282. Santoro, Calogero M.; Latorre, Claudio; Standen, Vivien G.; Salas, Carolina; Osorio, Daniela; Jackson, Donald; Gayó, Eugenia M. (2011). "Ocupación Humana Pleistocénica en el Desierto de Atacama: Primeros Resultados de la Aplicación de Un Modelo Predictivo De Investigación Interdisciplinaria" [Pleistocene Human Occupation in the Atacama Desert: First Results from the Application of an Interdisciplinary Predictive Research Model] (PDF). Chungara (in Spanish). 43 (1): 361. Retrieved 1 September 2016.
  283. Nester, P. L.; Gayo, E.; Latorre, C.; Jordan, T. E.; Blanco, N. (3 December 2007). "Perennial stream discharge in the hyperarid Atacama Desert of northern Chile during the latest Pleistocene". Proceedings of the National Academy of Sciences. 104 (50): 19724–19729. Bibcode:2007PNAS..10419724N. doi:10.1073/pnas.0705373104. PMC 2148365. PMID 18056645.
  284. Herrera, Christian; Gamboa, Carolina; Custodio, Emilio; Jordan, Teresa; Godfrey, Linda; Jódar, Jorge; Luque, José A.; Vargas, Jimmy; Sáez, Alberto (May 2018). "Groundwater origin and recharge in the hyperarid Cordillera de la Costa, Atacama Desert, northern Chile". Science of the Total Environment. 624: 114–132. Bibcode:2018ScTEn.624..114H. doi:10.1016/j.scitotenv.2017.12.134. hdl:2445/118767. ISSN 0048-9697. PMID 29248702.
  285. Latorre, Claudio; Betancourt, Julio L.; Arroyo, Mary T.K. (May 2006). "Late Quaternary vegetation and climate history of a perennial river canyon in the Río Salado basin (22°S) of Northern Chile". Quaternary Research. 65 (3): 463. Bibcode:2006QuRes..65..450L. doi:10.1016/j.yqres.2006.02.002. hdl:10533/178091. S2CID 129119233.
  286. Kruck, Wolfgang; Helms, Fabian; Geyh, Mebus A.; Suriano, José M.; Marengo, Hugo G.; Pereyra, Fernando (6 June 2011). "Late Pleistocene-Holocene History of Chaco-Pampa Sediments in Argentina and Paraguay". E&G Quaternary Science Journal. 60 (1): 199. doi:10.3285/eg.60.1.13.
  287. Höppner, Natalie; Chiessi, Cristiano M.; Lucassen, Friedrich; Zavala, Karina; Becchio, Raúl A.; Kasemann, Simone A. (1 May 2021). "Modern isotopic signatures of Plata River sediments and changes in sediment supply to the western subtropical South Atlantic during the last 30 kyr". Quaternary Science Reviews. 259: 9. Bibcode:2021QSRv..25906910H. doi:10.1016/j.quascirev.2021.106910. ISSN 0277-3791. S2CID 233564140.
  288. Madella, Andrea; Delunel, Romain; Oncken, Onno; Szidat, Sönke; Schlunegger, Fritz (27 July 2017). "Transient uplift of a long-term quiescent coast inferred from raised fan delta sediments". Lithosphere. 9 (5): 800. Bibcode:2017Lsphe...9..796M. doi:10.1130/L659.1. ISSN 1941-8264.
  289. May, Jan-Hendrik; Soler, Ramiro Daniel (21 January 2011). "Late Quaternary morphodynamics in the Quebrada de Purmamarca, NW Argentina". E&G Quaternary Science Journal. 59 (1/2): 32. doi:10.3285/eg.59.1-2.02. ISSN 0424-7116.
  290. Alcalá-Reygosa, Palacios & Zamorano Orozco 2016, p. 1167.
  291. Becel, David (2004). Modélisation numérique de l'érosion et de la sédimentation le long de la rivière Pilcomayo (Bolivie) : Un exemple de l'évolution d'une rivière dans un contexte tectoniquement actif sous l'effet des fluctuations climatiques quaternaires. Géologie Appliquée (PhD thesis) (in French). Grenoble I: Université Joseph-Fourier. p. 161. Archived from the original on 26 December 2016. Retrieved 25 September 2016.
  292. Paul, Jacob F.; González L., Gabriel; Urrutia M., Javier; Gamboa P., Carolina; Colucci, Stephen J.; Godfrey, Linda V.; Herrera L., Christian; Jordan, Teresa E. (2019). "Características isotópicas e implicaciones paleoclimáticas del evento de precipitación extrema de marzo de 2015 en el norte de Chile". Andean Geology. 46 (1): 1–31. doi:10.5027/andgeov46n1-3087. ISSN 0718-7106.
  293. De Waele, Jo; Picotti, Vincenzo; Martina, Mario L. V.; Brook, George; Yang, Linhai; Forti, Paolo (1 December 2020). "Holocene evolution of halite caves in the Cordillera de la Sal (Central Atacama, Chile) in different climate conditions". Geomorphology. 370: 7–8. Bibcode:2020Geomo.37007398D. doi:10.1016/j.geomorph.2020.107398. hdl:11585/770259. ISSN 0169-555X. S2CID 224866010.
  294. Jimenez, Nestor (2019). "Eruption of the Nuevo Mundo dacitic domes in the Los Frailes volcanic region (Eastern Bolivian Altiplano) triggered by glacier unloading at the end of the LGM". Geophysical Research Abstracts. 21: 15849. Bibcode:2019EGUGA..2115849J.
  295. Alcalá-Reygosa, Palacios & Zamorano Orozco 2016, p. 1166.
  296. Cuña-Rodríguez et al. 2020, p. 11.
  297. Zech, Jana; Zech, Roland; Kubik, Peter W.; Veit, Heinz (December 2009). "Glacier and climate reconstruction at Tres Lagunas, NW Argentina, based on 10Be surface exposure dating and lake sediment analyses". Palaeogeography, Palaeoclimatology, Palaeoecology. 284 (3–4): 180–190. Bibcode:2009PPP...284..180Z. doi:10.1016/j.palaeo.2009.09.023.
  298. Seagren, Erin G.; Schoenbohm, Lindsay M.; Owen, Lewis A.; Figueiredo, Paula M.; Hammer, Sarah J.; Rimando, Jeremy M.; Wang, Yang; Bohon, Wendy (1 December 2020). "Lithology, topography, and spatial variability of vegetation moderate fluvial erosion in the south-central Andes". Earth and Planetary Science Letters. 551: 2. Bibcode:2020E&PSL.55116555S. doi:10.1016/j.epsl.2020.116555. ISSN 0012-821X. S2CID 225022310.
  299. Gardeweg, Moyra P.; Delcorto, Luis A. (October 2015). "Glaciares de roca en la Alta Cordillera de Iquique – Región de Tarapacá, Chile" (PDF). biblioteca.sernageomin (in Spanish). La Serena: 14th Chilean Geological Congress. p. 726. Retrieved 22 June 2018.
  300. Grosjean, Martin; Veit, Heinz (2005), Huber, Uli M.; Bugmann, Harald K. M.; Reasoner, Mel A. (eds.), "Water Resources in the Arid Mountains of the Atacama Desert (Northern Chile): Past Climate Changes and Modern Conflicts", Global Change and Mountain Regions: An Overview of Current Knowledge, Advances in Global Change Research, Dordrecht: Springer Netherlands, p. 97, doi:10.1007/1-4020-3508-x_10, ISBN 978-1-4020-3508-1, retrieved 9 December 2020
  301. Riquelme, R.; Aguilar, G.; Rojas, C.; Lohse, P. (November 2009). "Cronología 10 Be y 14 C del último avance glacial en Chile semiárido (29–30° S) y factor es que controlan los cambios climáticos del Pleistoceno tardío-Holoceno" (PDF). SERNAGEOMIN (in Spanish). Santiago: 12th Chilean Geological Congress. p. 3. Archived (PDF) from the original on 26 December 2016. Retrieved 1 September 2016.
  302. Trauth, Martin H; Alonso, Ricardo A; Haselton, Kirk R; Hermanns, Reginald L; Strecker, Manfred R (June 2000). "Climate change and mass movements in the NW Argentine Andes". Earth and Planetary Science Letters. 179 (2): 252. Bibcode:2000E&PSL.179..243T. doi:10.1016/S0012-821X(00)00127-8.
  303. Delgado, Fabrizio; Zerathe, Swann; Audin, Laurence; Schwartz, Stéphane; Benavente, Carlos; Carcaillet, Julien; Bourlès, Didier L.; Team, Aster (1 February 2020). "Giant landslide triggerings and paleoprecipitations in the Central Western Andes: The aricota rockslide dam (South Peru)". Geomorphology. 350: 13. Bibcode:2020Geomo.35006932D. doi:10.1016/j.geomorph.2019.106932. hdl:20.500.12544/2477. ISSN 0169-555X. S2CID 210268287.
  304. Meinekat, Sarah Ann; Miller, Christopher E.; Rademaker, Kurt (14 November 2021). "A site formation model for Cuncaicha rock shelter: Depositional and postdepositional processes at the high‐altitude keysite in the Peruvian Andes". Geoarchaeology. 37 (2): 20. doi:10.1002/gea.21889. S2CID 244146814.
  305. Sylvestre et al. 1999, pp. 64–65.
  306. Gayo, E.M.; Latorre, C.; Jordan, T.E. (November 2009). "Fantasmas de bosques y agua fó sil en la Pampa del Tamarugal, norte de Chile" (PDF). SERNAGEOMIN (in Spanish). Santiago: 12th Chilean Geological Congress. p. 3. Archived (PDF) from the original on 29 December 2016. Retrieved 21 September 2016.
  307. Santoro, Calogero M. (2009). "Propuesta metodológica interdisciplinaria para poblamientos humanos Pleistoceno tardío/Holoceno temprano, precordillera de Arica, Desierto de Atacama Norte" (PDF). Andes (Salta). Antropología e Historia (in Spanish). Pontificia Universidad Católica de Chile (7): 22.
  308. Souza et al. 2021, p. 4.
  309. Roperch, Pierrick; Gattacceca, Jérôme; Valenzuela, Millarca; Devouard, Bertrand; Lorand, Jean-Pierre; Arriagada, Cesar; Rochette, Pierre; Latorre, Claudio; Beck, Pierre (July 2017). "Surface vitrification caused by natural fires in Late Pleistocene wetlands of the Atacama Desert". Earth and Planetary Science Letters. 469: 23. Bibcode:2017E&PSL.469...15R. doi:10.1016/j.epsl.2017.04.009. ISSN 0012-821X. S2CID 55581133.
  310. Gutiérrez et al. 2018, p. 1.
  311. Chávez, R.O.; Clevers, J.G.P.W.; Decuyper, M.; de Bruin, S.; Herold, M. (January 2016). "50 years of water extraction in the Pampa del Tamarugal basin: Can Prosopis tamarugo trees survive in the hyper-arid Atacama Desert (Northern Chile)?". Journal of Arid Environments. 124: 301. Bibcode:2016JArEn.124..292C. doi:10.1016/j.jaridenv.2015.09.007. ISSN 0140-1963.
  312. Frechen et al. 2018, p. 2.
  313. Workman et al. 2020, p. 17.
  314. Dejoux & Iltis 1992, p. 477.
  315. Yacobaccio, Hugo D.; Morales, Marcelo R.; Hoguin, Rodolphe (October 2016). "Habitats of ancient hunter-gatherers in the Puna: Resilience and discontinuities during the Holocene". Journal of Anthropological Archaeology. 46: 2. doi:10.1016/j.jaa.2016.08.004.
  316. Morales, Marcelo R.; Bustos, Sabrina; Oxman, Brenda I.; Pirola, Malena; Tchilinguirian, Pablo; Orgeira, Ma. Julia; Yacobaccio, Hugo D. (April 2018). "Exploring habitat diversity of mid-holocene hunter-gatherers in the South-Central Andes: Multi-proxy analysis of Cruces Core 1 (TC1), Dry Puna of Jujuy, Argentina". Journal of Archaeological Science: Reports. 18: 710. Bibcode:2018JArSR..18..708M. doi:10.1016/j.jasrep.2017.07.010.
  317. Geyh, Mebus A.; Grosjean, Martin; Núñez, Lautaro; Schotterer, Ulrich (September 1999). "Radiocarbon Reservoir Effect and the Timing of the Late-Glacial/Early Holocene Humid Phase in the Atacama Desert (Northern Chile)". Quaternary Research. 52 (2): 151. Bibcode:1999QuRes..52..143G. doi:10.1006/qres.1999.2060. S2CID 128775185.
  318. Marquet, Pablo A.; Santoro, Calogero M.; Latorre, Claudio; Standen, Vivien G.; Abades, Sebastián R.; Rivadeneira, Marcelo M.; Arriaza, Bernardo; Hochberg, Michael E. (11 September 2012). "Emergence of social complexity among coastal hunter-gatherers in the Atacama Desert of northern Chile". Proceedings of the National Academy of Sciences. 109 (37): 14754–14760. doi:10.1073/pnas.1116724109. ISSN 0027-8424. PMC 3443180. PMID 22891345.
  319. Capriles, J. M.; Tripcevich, N.; Nielsen, A. E.; Glascock, M. D.; Albarracin-Jordan, J.; Santoro, C. M. (22 April 2018). "Late Pleistocene Lithic Procurement and Geochemical Characterization of the Cerro Kaskio Obsidian Source in South-western Bolivia". Archaeometry. 60 (5): 5. doi:10.1111/arcm.12363. hdl:11336/98239. S2CID 56047259.
  320. Capriles, José M.; Albarracin-Jordan, Juan; Lombardo, Umberto; Osorio, Daniela; Maley, Blaine; Goldstein, Steven T.; Herrera, Katherine A.; Glascock, Michael D.; Domic, Alejandra I.; Veit, Heinz; Santoro, Calogero M. (April 2016). "High-altitude adaptation and late Pleistocene foraging in the Bolivian Andes". Journal of Archaeological Science: Reports. 6: 472. Bibcode:2016JArSR...6..463C. doi:10.1016/j.jasrep.2016.03.006. ISSN 2352-409X.
  321. Santoro, Calogero M.; Gayo, Eugenia M.; Capriles, José M.; Rivadeneira, Marcelo M.; Herrera, Katherine A.; Mandakovic, Valentina; Rallo, Mónica; Rech, Jason A.; Cases, Bárbara; Briones, Luis; Olguín, Laura; Valenzuela, Daniela; Borrero, Luis A.; Ugalde, Paula C.; Rothhammer, Francisco; Latorre, Claudio; Szpak, Paul (March 2019). "From the Pacific to the Tropical Forests: Networks of Social Interaction in the Atacama Desert, Late in the Pleistocene". Chungará (Arica). 51 (1): 5–25. doi:10.4067/S0717-73562019005000602. ISSN 0717-7356.
  322. López, Patricio; Carrasco, Carlos; Loyola, Rodrigo; Flores-Aqueveque, Valentina; Maldonado, Antonio; Santana-Sagredo, Francisca; Méndez, Víctor; Díaz, Pablo; Varas, Daniel; Soto, Angélica (3 July 2022). "Huentelauquén coastal groups in the Andean highlands? An assessment of human occupations of the Early Holocene in Salar de Pedernales, Chile (26°S, 3356 masl)". PaleoAmerica. 8 (3): 258. doi:10.1080/20555563.2022.2057833. ISSN 2055-5563. S2CID 248465742.
  323. Hayashida, Frances M; Troncoso, Andrés; Salazar, Diego, eds. (2022). Rethinking the Inka : community, landscape, and empire in the Southern Andes (1 ed.). Austin: University of Texas Press. p. 224. doi:10.7560/323854. ISBN 978-1-4773-2386-1. S2CID 240085331.
  324. Messerli, Grosjean & Vuille 1997, p. 229.
  325. Houston, John; Iglesias, Arturo Jensen; Cunich, Gonzalo Arévalo (24 October 2017). "Constitución de derechos de aprovechamiento sobre aguas subterráneas almacenadas". Revista de Derecho Administrativo Económico (in Spanish) (5): 124. doi:10.7764/redae.5.4. ISSN 0719-5591.
  326. Houston, John; Iglesias, Arturo Jensen; Cunich, Gonzalo Arévalo (2001). "Constitución de derechos de aprovechamiento sobre aguas subterráneas almacenadas". Revista de Derecho Administrativo Económico (in Spanish) (5): 124. doi:10.7764/redae.5.4. ISSN 0719-5591.
  327. Banks, David; Markland, Howard; Smith, Paul V.; Mendez, Carlos; Rodriguez, Javier; Huerta, Alonso; Sæther, Ola M. (November 2004). "Distribution, salinity and pH dependence of elements in surface waters of the catchment areas of the Salars of Coipasa and Uyuni, Bolivian Altiplano". Journal of Geochemical Exploration. 84 (3): 146. Bibcode:2004JCExp..84..141B. doi:10.1016/j.gexplo.2004.07.001.
  328. Ballivian & Risacher 1981, p. 1273.
  329. Löffler, Heinz (1984). "The Importance of Mountains for Animal Distribution, Species Speciation, and Faunistic Evolution (With Special Attention to Inland Waters)". Mountain Research and Development. 4 (4): 299–304. doi:10.2307/3673232. JSTOR 3673232.
  330. Sánchez, Andrés Valenzuela; Soto-Azat, Claudio (March 2012). Conservación de Anfibios de Chile (in Spanish). Universidad Andres Bello. pp. 94–95. ISBN 978-956-7247-70-7. Retrieved 24 September 2016.
  331. Cuadrelli, Francisco; Zurita, Alfredo E.; Toriño, Pablo; Miño-Boilini, Ángel R.; Perea, Daniel; Luna, Carlos A.; Gillette, David D.; Medina, Omar (16 September 2020). "A new species of glyptodontine (Mammalia, Xenarthra, Glyptodontidae) from the Quaternary of the Eastern Cordillera, Bolivia: phylogeny and palaeobiogeography". Journal of Systematic Palaeontology. 18 (18): 1560. doi:10.1080/14772019.2020.1784300. ISSN 1477-2019. S2CID 221064742.
  332. Huber, Bugmann & Reasoner 2005, p. 97.
  333. Schull, William J. (1990). The Aymara : Strategies in Human Adaptation to a Rigorous Environment. Studies in Human Biology. Vol. 2. Dordrecht: Springer Netherlands. p. 27. doi:10.1007/978-94-009-2141-2. ISBN 978-94-010-7463-6.
  334. Acosta Ochoa, Guillermo (2007). Las ocupaciones precerámicas de la Cuenca de México - del poblamiento a las primeras sociedades agrícolas (PDF). Universidad Nacional Autónoma de Mexico. p. 9. Retrieved 19 January 2017.
  335. Bradbury, John P (1971). "Paleolimnology of Lake Texcoco, Mexico - evidence from diatoms". Limnology and Oceanography. 16 (2): 181. Bibcode:1971LimOc..16..180B. CiteSeerX 10.1.1.598.4873. doi:10.4319/lo.1971.16.2.0180.
  336. Rodríguez Tapia, Lilia; Morales Novelo, Jorge A. (2012). Integración de un sistema de cuentas económicas e hídricas en la Cuenca del Valle de México (PDF). Universidad Autónoma Metropolitana. p. 2. Retrieved 19 January 2017.
  337. Aceituno Bocanegra, Francisco Javier; Rojas Mora, Sneider (2012). "Del Paleoindio al Formativo: 10.000 años para la historia de la tecnología lítica en Colombia - From the Paleoindian to the Formative Stage: 10,000 years for the history of lithic technology in Colombia" (PDF). Boletín de Antropología, Universidad de Antioquia. 28 (43): 127. ISSN 0120-2510. Retrieved 19 January 2017.
  338. Pérez Preciado, Alfonso (2000). La estructura ecológica principal de la Sabana de Bogotá. Sociedad Geográfica de Colombia. p. 6.
  339. Ponce Sanginés, Carlos (1972). Tiwanaku: Espacio, tiempo y cultura. Academia Nacional de Ciencias de Bolivia. p. 90.
  340. "Datos Generales de Bolivia" (in Spanish). Archived from the original on 29 October 2016.
  341. Junta Directiva, undécima reunión anual: resoluciones y documentos. Inter-American Institute of Agricultural Sciences, Board of Directors. 1972. p. 71. Retrieved 19 January 2017.

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