Payún Matrú

Payun Matru
Payún Matrú seen from space, black tongue-like lava flows and orange volcanic cones next to a white caldera
Payun Matru
Highest point
Elevation3,715 m (12,188 ft) [1]
Coordinates36°25′19″S 69°14′28″W / 36.422°S 69.241°W / -36.422; -69.241Coordinates: 36°25′19″S 69°14′28″W / 36.422°S 69.241°W / -36.422; -69.241[1]
Payun Matru is located in Argentina
Payun Matru
Payun Matru
Parent rangeAndes
Mountain typeShield volcano
Last eruption515 ± 50 years ago

Payun Matru is a shield volcano in Argentina, located in the Reserva Provincial La Payunia of the Malargüe Department, to the south of the Mendoza Province. It is situated in the back-arc region of the Andean Volcanic Belt, which formed through processes associated with the subduction of the Nazca Plate beneath the South American Plate. Together with other volcanic fields such as the Llancanelo volcanic field, Nevado volcanic field and Salado Basin volcanic field Payún Matrú forms the Payenia volcanic province. The volcano is part of the Reserva Provincial La Payunia and has been proposed to become a World Heritage Site.

Payún Matrú developed over sediments and volcanic rocks ranging from Mesoproterozoic to Tertiary age. It consists of a large shield volcano capped off by a 7–8 km (4.3–5.0 mi) caldera that formed during a large explosive eruption between 168,000 and 82,000 years ago, a 3,680–3,797 m (12,073–12,457 ft) high compound volcano named Payun or Payun Liso and two groups of scoria cones and lava flows due west and east from the main shield volcano, respectively. One of these lava flows, the Pleistocene Pampas Onduladas lava flow, reaches a length of 167–181 km (104–112 mi) and is the world's longest Quaternary lava flow.

Volcanic activity at Payún Matrú commenced during the Plio-Pleistocene and first generated the lava flow fields such as Pampas Onduladas, the Payún Matrú shield volcano and the Payun volcano. After the formation of the caldera volcanism continued both within the caldera in the form of lava domes and lava flows, and outside of it with the formation of scoria cones and lava flows east and especially west of Payún Matrú. Volcanic activity continued into the Holocene until about 515 years ago; oral tradition of local inhabitants contains references to past volcanic eruptions.


According to the local population, the term Payún or Paium means "bearded" and the term Matru means "goat".[2] The field is sometimes also known as Payenia.[3]

Geography and geomorphology


Payún Matrú lies in the Malargüe Department of the Mendoza Province, Argentina.[4] The area is inhospitable due to the lack of usable water and, at high elevations, of pastures and firewood;[2] nevertheless there are many paved roads in the area[5] such as National Route 40 which passes west of the volcanic field[6] and National Route 186 which runs around the northern and eastern parts of Payún Matrú.[7]

The volcano is located within the Reserva Provincial La Payunia.[8] Owing to the variety of volcanic landforms in the landscape, the Payunia volcanic province was included in the 2010 Tentative List of UNESCO World Heritage Sites[9] and a number of potential geosites have been identified at Payún Matrú itself.[10]

The volcanic field is part of the backarc area of the Southern Volcanic Zone, a 1,000 km (620 mi) long volcanic arc[11] and one of four volcanic belts in the Andes; the other three are the Northern Volcanic Zone, the Central Volcanic Zone and the Austral Volcanic Zone.[3] Among the volcanoes in the region is Laguna del Maule almost due west from Payún Matrú.[12]


Payún Matrú is a 15 km (9.3 mi) wide[13] shield volcano[1] whose foot coincides with the 1,750 m (5,740 ft) elevation line and which extends mainly east-west;[14] rising about 2 km (1.2 mi) above the surrounding terrain[15] it covers about 5,200 km2 (2,000 sq mi) of land with lavas[16] and has diverse volcanic landforms.[17] Ignimbrites cover and flatten its northern and eastern slopes, while in the west and south lava domes and coulées[a] predominate; these have often rough surfaces and are difficult to traverse. The lower slopes are more gentle and covered by Pleistocene-Holocene lava flows.[19] Wind erosion has created flutes, grooves and yardangs within the ignimbrites,[20] such as in the western sector where yardangs reach heights of 8 m (26 ft) and widths of 100 m (330 ft).[21] The total volume of this shield is about 240 km3 (58 cu mi).[22]

Labelled description of hills/mountains above a lake
View from within the caldera

In the summit region of the shield lies a 7–8 km (4.3–5.0 mi)[14][23] long and maximally 480 m (1,570 ft) deep[23] caldera surrounded by several peaks, which clockwise from north include the 3,650 m (11,980 ft) high Nariz/Punta del Payún, the Punta Media, the 3,450 m (11,320 ft) high Punta Sur and the approximately 3,700 m (12,100 ft) high Cerro Matru or Payen. In the field however Cerro Matru appears smaller than Nariz.[14] The caldera was once 8–9 km (5.0–5.6 mi) wide but erosion of its flanks and later volcanic activity have reduced its size[19] and hidden the rim below coulées, lava domes, lava flows[20] and pumice cones[13] that were emplaced after the caldera collapse.[24] The exception are the northern and southern walls which are almost vertical; remnants of old andesitic and trachyandesitic volcanism crop out there.[14] The caldera also contains a permanent lake known as "Laguna" that is fed by snowmelt and by occasional rainfall.[2]

The highest point of the volcanic field is the[17] 3,796 m (12,454 ft) high,[1] conical, eroded Payun stratovolcano.[17] It is also known as Payun Liso,[25] Payún and Payún Liso.[26] This volcano rises 1.8 km (1.1 mi)[17] from the southern side of Payún Matrú, 10 km (6.2 mi) away from the caldera.[26][27] It has a summit crater open to the north[17] and it has a volume of about 40 km3 (9.6 cu mi).[28]

Payún Matrú volcanic field

Aside from the caldera, the volcanic field features about 300 individual volcanic vents[16] with diverse morphologies[29] that are distributed in a western Los Volcanes group that reaches to the Rio Grande River and the eastern Guadaloso and El Rengo groups.[17] These fields are also known as West Payún Matrú or West Payén and East Payún Matrú or East Payén, respectively.[30] Two further volcanic units known as "Chapua" and "Puente" have been identified east of Payún Matrú.[1]

All of these groups include fissure vents,[1] lapilli cones,[17] scoria cones[29] and strombolian cones.[17] These edifices are up to 225 m (738 ft) high[31] and are associated with lava flows[17] and pyroclastic units;[6] the vents in the Los Volcanes group are spread through two separate belts.[26] Wind-driven ash transport has formed ash tails at individual vents.[32]

Older lava flows have pahoehoe surfaces with lava tubes and pressure ridges while Holocene lava flows are more commonly aa lava with blocky surfaces.[33][31] Some lava flows from the field have reached the Rio Grande River west of Payún Matrú, damming it; the river later cut through the lava flows and formed table-like landforms and canyons.[34] One of these is a slot canyon[26] known as La Pasarela,[35] where the structures of lava flows such as joints in the rocks and vesicles are clearly visible.[6] The entire volcanic field covers an area of over 12,000 km2 (4,600 sq mi)[26] and some of its flows have reached the Llancanelo Lake north of Payún Matrú and the Salado River in the east.[36] The estimated volumes of the entire Payún Matrú volcano are as large as 350 km3 (84 cu mi); the volcanic edifice was generated mostly through Strombolian and Hawaiian eruptions.[37]

Several cinder cones, some forming an alignment
Cinder cones on the La Carbonilla fault

The cones mostly are aligned along easterly or northeasterly lineaments[19] which are correlated to geological structures in the basement beneath the volcanic field[38] and appear to reflect the tectonic stresses underground.[39] Among these lineaments is the La Carbonilla fracture which runs in east-west direction and crops out in the eastern part of the field; in the central sector it is hidden by the caldera and in the western it is buried by lava flows.[40] The La Carbonilla fracture is a fault[39] that appears to have been an important influence on the development of the Payún Matrú volcanic complex in general.[41] Fissural ridges and elongated chains of vents and cones highlight the control that lineaments exercise on the volcanic eruptions.[42] In the summit area, pumice cones are aligned along the caldera rim.[43]

Among the volcanic cones in Payún Matrú are the Plio-Pleistocene Morados Grandes east and the cones around Pihuel volcano northeast of the volcanic field, respectively; the Guadalosos, La Mina and Montón de Cerros cones in the northern part of the volcanic field;[44] and the Holocene cones in the eastern and western part of the volcanic field. Among these the Los Morados, Morado Sur and Volcán Santa María cones in the eastern and northeastern part of the field are uneroded and are probably of recent age.[45] These volcanic cones are the source of conspicuous black lava flows in the western part of the volcanic field;[46] some lava flows are over 30 km (19 mi) long.[31]

  • Los Morados is a complex of scoria cones and vents of different ages[47] which during its emplacement underwent a sector collapse, intense Strombolian activity and a lava flow-induced rafting and re-healing of its slopes.[48]
  • On the southeast and east Los Morados is bordered by a lapilli plain, the Pampas Negras,[49] which was formed by fallout of Strombolian eruptions and is being reworked by wind with the formation of dunes.[31]
  • Morado Sur consists of two aligned volcanic cones that formed in the same eruption and are covered with reddish deposits;[50] it also features several vents and lava flows.[51]
  • Volcán Santa María is a volcanic cone with a small crater and also covered with red scoria and lava bombs.[52] It is 180 m (590 ft) high and is associated with an area called "El Sandial", where lava bombs have left traces such as impact craters and aerodynamically deformed rocks.[53]

Pampas Onduladas and other giant lava flows

Payún Matrú is the source of the longest Quaternary lava flow on Earth,[54][26] the Pampas Onduladas lava flow[55] in the eastern and northern sector of the volcanic field.[26] The flow originates on the eastern side of the volcanic field in the La Carbonilla fault[36] and eventually splits up into a shorter ("Llancanelo lava flow", 60–63 km (37–39 mi) long[56][57]) northwestern and the longer southeastern branch[56] which reaches all the way to an alluvial terrace of the Salado River[58] in the La Pampa Province.[36]

This compound lava flow moved over a gentle terrain[59] and is covered by lava rises and lava tumuli[33] especially in areas where the flow encountered obstacles in the topography.[60] There is some variation in its appearance between a wide, leveled initial proximal sector[57] and a more sinuous distal sector.[61] The unusually fast flowing lava[62] under the influence of its low viscosity and of a favourable topography[63] eventually accumulated to a volume of at least 7.2 km3 (1.7 cu mi), a surface area of about 739 km2 (285 sq mi) and depending on the measurement a length of 167–181 km (104–112 mi).[62] The process by which such long lava flows form has been explained as "inflation" whereby lava forms a crust that protects it from heat loss; the so protected lava flow eventually inflates from the entry of new magma, forming a system of overlapping and interconnected lava flow lobes. Such lava flows are known as "sheet flows".[56] Parts of the Pampas Onduladas lava flow have been buried by more recent lava flows.[24]

Together with the Þjórsá Lava in Iceland and the Toomba and Undara lava flows in Queensland, Australia, it is one of only a few Quaternary lava flows that reached a length of over 100 km (62 mi)[55] and it has been compared to some long lava flows on Mars.[64] Southwest from Pampas Onduladas lie the Los Carrizales lava flows, which have in part advanced to even larger distances than Pampas Onduladas but owing to a straighter course are considered to be shorter than the Pampas Onduladas lava flow,[65] and the La Carbonilla lava flow which like Los Carrizales propagated southeastward and is located just west from the latter.[49] Additional large lava flows are located in the western part of the field and resemble the Pampas Onduladas lava flow, such as the El Puente Formation close to the Rio Grande River of possibly recent age.[36] Long lava flows have also been produced by volcanic centres directly south of Payún Matrú,[66] including the 70–122 km (43–76 mi) long El Corcovo, Pampa de Luanco and Pampa de Ranquelcó flows.[67]

Hydrography and non-volcanic landscape

Apart from the lake in the caldera, the area of Payún Matrú is largely devoid of permanent water resources, with most water sites that draw in humans being either temporary so-called "toscales" or ephemeral.[2] Likewise, there are no permanent rivers in the field and most of the precipitation quickly seeps into the permeable or sandy ground.[68] The whole massif is surrounded by sandy plains, which are simply volcanic rocks covered by aeolian sediments; the plains also feature small closed basins[69] which are also found in the lavic area.[70]


West of South America, the Nazca Plate and the Antarctic Plate subduct beneath the South America Plate[40] at a rate of 66–80 mm/a (2.6–3.1 in/year),[71] giving rise to the Andean volcanic belt. The volcanic belt is not continuous and is interrupted by gaps where the subduction is shallower[40] and the asthenosphere between the two plates missing.[72] North of the Payún Matrú, flat slab subduction takes place; in the past flat slab subduction occurred farther south as well and had noticeable influence on magma chemistry.[73] In general, the mode of subduction in the region over time has been variable.[11]

There is evidence of Precambrian[74] and Permian-Triassic volcanism (Choique Mahuida Formation)[75] in the region, but a long hiatus separates them from the recent volcanic activity which started in the Pliocene. At that time, the basaltic El Cenizo Formation and the andesitic Cerro El Zaino volcanics were emplaced.[76] This kind of calcalkaline volcanic activity is interpreted to be the consequence of flat slab subduction during the Miocene and Pliocene,[13] and took place between 20 and 5 million years ago.[72] Later during the Pliocene and Quaternary the slab steepened, and probably as a consequence volcanism in the land above increased,[77] reaching a peak between 8 and 5 million years ago.[15]


The basement underneath Payún Matrú is formed by Mesoproterozoic to Triassic rocks of the San Rafael Block, Mesozoic[78] to Paleogene sediments of the Neuquén Basin and Miocene lava flows[25] such as the Tertiary Patagonian basalts.[36] The Andean orogeny during the Miocene has folded and deformed the basement, creating basins and uplifted basement blocks.[25] Oil has been drilled close to the volcanic field from sediments of Mesozoic age.[16]

Payún Matrú is part of the backarc volcanic province, 200 km (120 mi) east of the Andes[4] and 530 km (330 mi) east of the Peru-Chile Trench.[11] The volcanic activity still relates to the subduction of the Nazca Plate beneath the South America Plate, however;[4] one proposed mechanism is that a Miocene change in the subduction regimen led to the development of extensional tectonics[73] and of faults that form the pathways for magma ascent,[17] while other mechanisms envisage changes in mantle characteristics.[79]

Payún Matrú is part of a group of volcanoes, with a string of volcanoes just to its south
Geological context of the volcanoes

Other volcanic fields in the region are the Llancanelo volcanic field, the Nevado volcanic field and Salado Basin volcanic field, the first two lie north of Payún Matrú and the last south. These fields are subdivided on the basis of geochemical differences[40] and consist of two stratovolcanoes (Payún Matrú itself and Nevado) and many monogenetic volcanoes.[80] The volcanic field is part of the larger Payunia volcanic province, which covers an area of about 36,000 km2 (14,000 sq mi)[81] in the Provinces of La Pampa, Mendoza and Neuquén[82] and is also known as the Payenia[73] or Andino-Cuyana volcanic province.[3] Monogenetic volcanism of mainly basaltic composition has been active here for the last 3-2 million years accompanied by the formation of several polygenetic volcanoes,[83][84] generating over 800 monogenetic cones[82] although historical eruptions have not been observed.[73] Even farther south are the Chachahuen and Auca Mahuida volcanoes[3] and the Tromen volcano farther west appears to relate to Payún Matrú as well.[85]

Lava and magma composition

The volcanic field has erupted rocks with composition ranging from alkali basalts[16] over basalts, trachyandesite, basaltic trachyandesite, trachybasalt and trachyte to rhyolite. They define a calc-alkaline volcanic suite with some variation between the various volcanic centres; Los Volcanes is formed mainly by calc-alkaline magmas while Payun and Payun Matru are more potassium-rich and shoshonitic.[86] The volcanic rocks contain variable amounts of phenocrysts, including alkali feldspar, amphibole, apatite, biotite, clinopyroxene, olivine, plagioclase and sanidine, but not all phenocryst phases can be found in every rock formation.[87][88] Magma temperatures of 1,122–1,276 °C (2,052–2,329 °F) have been inferred.[89]

Volcanic rocks erupted at Payún Matrú resemble ocean island basalt volcanism, implying a deep origin of the magma although a shallow origin cannot be ruled out.[16] Magnetotelluric[b] observations indicate the presence of a "plume"-like structure that rises from 200–400 km (120–250 mi) depth close to the edge of the Nazca Plate slab to underneath Payún Matrú; it may indicate that magma erupted in the volcanic field originates at such depths which would explain the ocean island basalt-like composition.[91]

The formation process of the magma erupted at Payún Matrú begins with partial melting of enriched mantle;[92] the resulting melts then undergo crystal fractionation,[93] assimilation of crustal material[94] and magma mixing in magma chambers.[95] The magmas eventually reach the surface through deep faults.[37] The edifice of Payún Matrú acts as an obstacle to magmas ascending to the surface; this is why only evolved[c] magmas are erupted in the caldera area of Payún Matrú while basic magmas reached the surface mainly outside of the main edifice.[97]

Obsidian from Payún Matrú has been found in archeological sites, although its use was not widespread in the region perhaps owing to its low quality, the difficulty of accessing the volcanic complex and that human activity in Payunia only began comparatively late in the Holocene and mostly from the margins of the region.[98] Further, Payun volcano is notable for large crystals of hematite pseudomorphs which originated in fumaroles.[99]

Climate, soils and vegetation

The climate at Payún Matrú is cold and dry[8] with strong westerly winds.[37] Annual temperature varies between 20–2 °C (68–36 °F)[100] while the average temperature in the wider region is about 15 °C (59 °F) and the average annual precipitation amounts to 200–300 mm/a (7.9–11.8 in/year).[100][101] Generally, the area of Payún Matrú is characterized by a continental climate with hot summers especially at lower elevations and cold winters especially at higher elevations.[70] The climate is dry owing to the rainshadow effect of the Andes which block moisture bearing winds from reaching Payún Matrú, and strong winds and the evaporation associated with them reinforce the dryness.[101] In the westerly part of the volcanic field most precipitation falls during winter under the influence of the Andes, while the eastern part has most precipitation occurring during summer.[102] The higher parts of Payún Matrú may have risen above the snowline during ice ages,[103] and periglacial landforms have been observed.[104] Palynology data from south of the region indicate that the climate has been stable since the Late Pleistocene.[37]

The vegetation in the volcanic field is mostly characterized by sparse bushes as well as herbaceous vegetation but few trees,[105] and is classified as xerophytic.[37] Soils are shallow and are mainly rocky to loess-like.[100] Representative plant genera are Opuntia cactus and Poa and Stipa grasses.[106] Payún Matrú is a refuge for a number of animals such as the armadillos, black-chested buzzard-eagle, condors, Darwin's rhea, guanaco, mara, Pampas fox or South American gray fox, puma and Southern viscacha.[101]

Eruption history

The volcano is formed of many stratigraphic formations that were emplaced partly consecutively partly concurrently
Stratigraphy of Payún Matrú

The geological history of the Payún Matrú volcanic field is poorly dated[40] but the field has been active since Pliocene at least.[17] The older volcanism appears to be located in the eastern part of the field where ages of 0.95 ± 0.5 to 0.6 ± 0.1 million years ago have been obtained by potassium-argon dating.[40] Lava flows have been subdivided into the older Puente Group and the younger Tromen Group formations,[31] which are of Pleistocene to Pleistocene-Holocene age, respectively;[107] a Chapua Formation of Plio-Pleistocene age has been defined as well.[108] The eastern volcanism is also known as the Pre-caldera basaltic unit; a western counterpart to it is probably buried beneath younger eruption products.[23]

The first volcanic activity occurred west and east of Payún Matrú and involved the emission of olivine basalt lava flows.[39] The long Pampas Onduladas lava flow was erupted 373,000 ± 10,000 years ago[109] and buried parts of the 400,000 ± 100,000 years old Los Carrizales lava field;[36] both have hawaiitic composition.[110] The Payun volcano formed around 265,000 ± 5,000 years ago within a timespan of about 2,000 - 20,000 years.[34] Its inferred eruption rate of 0.004 km3/ka (0.00096 cu mi/ka) is similar to typical volcanic arc eruption rates such as at Mount St. Helens.[28]

The main Payún Matrú massif formed in about 600,000 years, with the oldest trachytic rocks dated to 700,000 years ago. It is comprised by the lavic and ignimbritic Pre-caldera Trachyte unit[23] and consists of trachyandesitic to trachytic rocks, with trachyte being the most important component.[13] The massif may have formed a tall edifice like the Payun volcano before caldera collapse.[65]

The formation of the caldera coincides with the eruption of the Portezuelo Ignimbrite[40]/Portezuelo Formation[17] and took place between 168,000 ± 4,000 and 82,000 ± 2,000 years ago.[33] This ignimbrite formation where it is not buried by younger eruption products[111] covers an area of about 2,200 km2 (850 sq mi) on the northern and southern sides of Payún Matrú,[17] and its volume is estimated to be about 25–33 km3 (6.0–7.9 cu mi).[111] The event was probably precipitated by the entry of mafic magma in the magma chamber and its incomplete mixing with pre-existent magma chamber melts,[89] or by tectonic processes;[97] the resulting Plinian eruption generated an eruption column, which collapsed, producing the ignimbrites.[17] After the eruption, the summit of the volcano collapsed as well, forming the caldera; activity continued and emplaced lava domes[17] and lava flows in the caldera area. These post-caldera volcanic formations are subdivided into three separate lithofacies.[111]

Basaltic and trachyandesitic activity continued after the formation of the caldera.[1] Morphology indicates that the El Rengo and Los Volcanes volcanic cones appear to be of Holocene age, while the Guadaloso vents formed during the Plio-Pleistocene.[17] One age from the eastern side is 148,000 ± 9,000 years ago, it comes from northeast of the Payún Matrú caldera.[112]

Uneroded volcanic cones and dark basaltic lavas indicate that activity continued into the Holocene and oral tradition by local inhabitants indicate that recent volcanic activity occurred,[17] although no historical eruptions have been observed.[16] Future volcanic eruptions would be unlikely to constitute a hazard given the low population density of the area, although roads might be interrupted and lava dams might form in rivers.[113]

Various dating methods have yielded various ages for late Pleistocene-Holocene volcanic eruptions:

  • 44,000 ± 2,000 years ago, surface exposure dating.[114]
  • 43,000 - 41,000 ± 3,000 years ago, surface exposure dating, El Puente Formation. Basaltic lava flows of this formation reach ages of about 320,000 ± 5,000 years, implying a prolonged history of emplacement.[115]
  • 41,000 ± 1,000 years ago, underlying the Los Morados lava flow.[116]
  • 37,000 ± 3,000 years ago, surface exposure dating,[114] close to the Rio Grande River.[49]
  • 37,000 ± 1,000 years ago, La Planchada fallout deposit.[117]
  • 37,000 ± 2,000 years ago, northwestern side of the caldera.[118]
  • 28,000 ± 5,000 years ago, potassium-argon dating, lava flow[117] on the westerly side.[119]
  • 26,000 ± 5,000 years ago, potassium-argon dating, close to the Rio Grande.[119]
  • 26,000 ± 2,000 years ago, potassium-argon dating, not the same as the 26,000 ± 5,000 flow.[119]
  • 26,000 ± 1,000 years ago, potassium-argon dating, rhyolitic lava flow in the La Calle group.[117]
  • 20,000 ± 7,000 years ago, north of the Payún Matrú caldera.[112]
  • 16,000 ± 1,000 years ago, underlying the Los Morados lava flow.[116]
  • 15,200 ± 900 years ago,[120] potassium-argon dating, lava flow on the northwesterly[117]-westerly side.[119]
  • 9,000 years ago, potassium-argon dating.[114]
  • 7,000 ± 1,000 years ago, potassium-argon dating, Escorial del Matru within the caldera.[117]
  • <7,000 years ago, potassium-argon dating, trachyandesitic lava flow[117] in the western part of the field.[119]
  • 4,760 ± 450 years before present, thermoluminescence dating.[114]
  • 6,900 ± 650 years before present, thermoluminescence dating on the Guadalosos cones.[114]
  • 4,760 ± 450 years before present, thermoluminescence dating.[114]
  • 2,000 ± 2,000 years ago, surface exposure dating, young looking lava flow in the west.[121]
  • 1,470 years before present, thermoluminescence dating on Volcán Santa María[114] although a much older age of 496,000 ± 110,000 years ago has also been given.[53]
  • 515 ± 50 years[122] before present, thermoluminescence dating on Morado Sur cone.[114]

See also


  1. ^ A coulée is a particular type of lava dome which has flowed sideward like a lava flow.[18]
  2. ^ The magnetotelluric technique is a research technique, which exploits natural electromagnetic fields to obtain information on the electrical conductivity underground.[90]
  3. ^ Evolved magmas are magmas which due to a settling of crystals have lost part of their magnesium oxide.[96]


  1. ^ a b c d e f g "Payún Matru". Global Volcanism Program. Smithsonian Institution. Retrieved 28 May 2019.
  2. ^ a b c d Díaz & F 1972, p. 9.
  3. ^ a b c d Germa et al. 2010, p. 718.
  4. ^ a b c Blazek & Lourdes 2017, p. 90.
  5. ^ Díaz & F 1972, p. 24.
  6. ^ a b c Risso, Németh & Martin 2006, p. 486.
  7. ^ Inbar & Risso 2001, p. 331.
  8. ^ a b Corbalán, Valeria; Debandi, Guillermo; Kubisch, Erika (1 October 2013). "Thermal ecology of two sympatric saxicolous lizards of the genus Phymaturus from the Payunia region (Argentina)". Journal of Thermal Biology. 38 (7): 385. doi:10.1016/j.jtherbio.2013.05.006. ISSN 0306-4565.
  9. ^ Mikkan 2014, p. 31.
  10. ^ Risso, Németh & Martin 2006, pp. 485–487.
  11. ^ a b c Germa et al. 2010, p. 717.
  12. ^ Espanon et al. 2014, p. 115.
  13. ^ a b c d Hernando et al. 2019, p. 454.
  14. ^ a b c d Díaz & F 1972, p. 15.
  15. ^ a b Sato et al. 2012, p. 160.
  16. ^ a b c d e f Burd et al. 2008, p. 91.
  17. ^ a b c d e f g h i j k l m n o p q Germa et al. 2010, p. 719.
  18. ^ Blake, S. (1990). Viscoplastic Models of Lava Domes. Lava Flows and Domes. IAVCEI Proceedings in Volcanology. 2. Springer, Berlin, Heidelberg. p. 93. doi:10.1007/978-3-642-74379-5_5. ISBN 978-3-642-74381-8.
  19. ^ a b c Díaz & F 1972, p. 16.
  20. ^ a b Risso, Németh & Martin 2006, p. 487.
  21. ^ Inbar & Risso 2001, p. 660.
  22. ^ Germa et al. 2010, p. 727.
  23. ^ a b c d Hernando et al. 2016, p. 152.
  24. ^ a b Rossotti et al. 2008, p. 134.
  25. ^ a b c Hernando et al. 2014, p. 124.
  26. ^ a b c d e f g Marchetti, Hynek & Cerling 2014, p. 67.
  27. ^ Germa et al. 2010, p. 720.
  28. ^ a b Germa et al. 2010, p. 725.
  29. ^ a b Mikkan 2017, p. 88.
  30. ^ Németh et al. 2011, p. 103.
  31. ^ a b c d e Németh et al. 2011, p. 105.
  32. ^ Inbar & Risso 2001, p. 662.
  33. ^ a b c Espanon et al. 2014, p. 117.
  34. ^ a b Germa et al. 2010, p. 721.
  35. ^ Risso, Nemeth & Nullo 2009, p. 25.
  36. ^ a b c d e f Rossotti et al. 2008, p. 133.
  37. ^ a b c d e Inbar & Risso 2001, p. 325.
  38. ^ Hernando et al. 2014, p. 132.
  39. ^ a b c Mazzarini et al. 2008, p. 5.
  40. ^ a b c d e f g Espanon et al. 2014, p. 116.
  41. ^ Rossotti et al. 2008, p. 145.
  42. ^ Hernando et al. 2014, p. 127.
  43. ^ Hernando et al. 2019, p. 461.
  44. ^ Blazek & Lourdes 2017, p. 99.
  45. ^ Blazek & Lourdes 2017, p. 100.
  46. ^ Mikkan 2017, p. 87.
  47. ^ Németh et al. 2011, p. 107.
  48. ^ Németh et al. 2011, pp. 114–115.
  49. ^ a b c Németh et al. 2011, p. 104.
  50. ^ Mikkan 2017, pp. 88–89.
  51. ^ Mikkan 2017, p. 99.
  52. ^ Risso, Nemeth & Nullo 2009, p. 18.
  53. ^ a b Risso, Németh & Martin 2006, p. 485.
  54. ^ Mikkan 2014, p. 43.
  55. ^ a b Espanon et al. 2014, p. 114.
  56. ^ a b c Rossotti et al. 2008, p. 132.
  57. ^ a b Pasquarè, Bistacchi & Mottana 2005, p. 130.
  58. ^ Rossotti et al. 2008, p. 138.
  59. ^ Massironi et al. 2007, p. 1.
  60. ^ Espanon et al. 2014, p. 120.
  61. ^ Pasquarè, Bistacchi & Mottana 2005, p. 132.
  62. ^ a b Espanon et al. 2014, p. 125.
  63. ^ Espanon et al. 2014, p. 128.
  64. ^ Massironi et al. 2007, p. 2.
  65. ^ a b Pasquarè, Bistacchi & Mottana 2005, p. 129.
  66. ^ Sumino et al. 2019, Fig 1.
  67. ^ Sumino et al. 2019, p. 4.
  68. ^ Díaz & F 1972, p. 18.
  69. ^ Díaz & F 1972, p. 17.
  70. ^ a b Díaz & F 1972, p. 19.
  71. ^ Mazzarini et al. 2008, p. 2.
  72. ^ a b Pomposiello et al. 2014, p. 813.
  73. ^ a b c d Burd et al. 2008, p. 90.
  74. ^ Díaz & F 1972, p. 81.
  75. ^ Mazzarini et al. 2008, p. 4.
  76. ^ Díaz & F 1972, p. 82.
  77. ^ Pomposiello et al. 2014, p. 814.
  78. ^ Hernando et al. 2014, p. 123.
  79. ^ Sumino et al. 2019, p. 7.
  80. ^ Inbar & Risso 2001, p. 323.
  81. ^ Blazek & Lourdes 2017, p. 88.
  82. ^ a b Sumino et al. 2019, p. 6.
  83. ^ Hernando et al. 2016, p. 151.
  84. ^ Hernando et al. 2014, p. 122.
  85. ^ Pomposiello et al. 2014, p. 822.
  86. ^ Germa et al. 2010, p. 724.
  87. ^ Hernando et al. 2016, p. 154.
  88. ^ Germa et al. 2010, pp. 723–724.
  89. ^ a b Hernando et al. 2016, p. 167.
  90. ^ "The Magnetotelluric Method". Electromagnetic methods in applied geophysics. Vol. 2, Applications, Parts A and B. Nabighian, Misac N., Society of Exploration Geophysicists. Tulsa, Okla. (8801 South Yale St., Tulsa OK 74137-3175): Society of Exploration Geophysicists. 1991. ISBN 9781560802686. OCLC 778681058.CS1 maint: others (link) CS1 maint: location (link)
  91. ^ Burd et al. 2008, p. 93.
  92. ^ Spakman et al. 2014, p. 211.
  93. ^ Germa et al. 2010, p. 728.
  94. ^ Spakman et al. 2014, p. 234.
  95. ^ Hernando et al. 2016, p. 163.
  96. ^ Allaby, Michael (2013). A Dictionary of Geology and Earth Sciences. OUP Oxford. p. 208. ISBN 9780199653065.
  97. ^ a b Germa et al. 2010, p. 729.
  98. ^ Giesso, M.; Durán, V.; Neme, G.; Glascock, M. D.; Cortegoso, V.; Gil, A.; Sanhueza, L. (2011). "A Study of Obsidian Source Usage in the Central Andes of Argentina and Chile". Archaeometry. 53 (1): 16. doi:10.1111/j.1475-4754.2010.00555.x. ISSN 1475-4754.
  99. ^ "Payún volcano, Altiplano de Payún Matru, Malargüe Department, Mendoza Province, Argentina". Retrieved 28 May 2019.
  100. ^ a b c Inbar & Risso 2001, p. 658.
  101. ^ a b c Mikkan 2014, p. 34.
  102. ^ Díaz & F 1972, p. 20.
  103. ^ Inbar & Risso 2001, p. 659.
  104. ^ Inbar & Risso 2001, p. 326.
  105. ^ Díaz & F 1972, p. 22.
  106. ^ Risso, Nemeth & Nullo 2009, p. 21.
  107. ^ Inbar & Risso 2001, pp. 324–325.
  108. ^ Inbar & Risso 2001, p. 324.
  109. ^ Espanon et al. 2014, p. 126.
  110. ^ Rossotti et al. 2008, p. 141.
  111. ^ a b c Hernando et al. 2016, p. 153.
  112. ^ a b Spakman et al. 2014, p. 212.
  113. ^ Perucca, Laura P.; Moreiras, Stella M. (1 January 2009), Latrubesse, Edgardo M. (ed.), "Natural Hazards and Human-Exacerbated Disasters in Latin America", Developments in Earth Surface Processes, Natural Hazards and Human-Exacerbated Disasters in Latin America, Elsevier, 13, p. 293, doi:10.1016/S0928-2025(08)10014-1, ISBN 9780444531179
  114. ^ a b c d e f g h Blazek & Lourdes 2017, p. 102.
  115. ^ Marchetti, Hynek & Cerling 2014, p. 73.
  116. ^ a b Mikkan 2017, p. 89.
  117. ^ a b c d e f Germa et al. 2010, p. 723.
  118. ^ Sato et al. 2012, p. 166.
  119. ^ a b c d e Marchetti, Hynek & Cerling 2014, p. 69.
  120. ^ Schimmelpfennig, Irene; Benedetti, Lucilla; Garreta, Vincent; Pik, Raphaël; Blard, Pierre-Henri; Burnard, Pete; Bourlès, Didier; Finkel, Robert; Ammon, Katja (15 May 2011). "Calibration of cosmogenic 36Cl production rates from Ca and K spallation in lava flows from Mt. Etna (38°N, Italy) and Payun Matru (36°S, Argentina)". Geochimica et Cosmochimica Acta. 75 (10): 2619. doi:10.1016/j.gca.2011.02.013. ISSN 0016-7037.
  121. ^ Marchetti, Hynek & Cerling 2014, p. 69,73.
  122. ^ Mikkan 2017, p. 90.


  • Blazek, González; Lourdes, Verónica (1 June 2017). "Evolución morfológica y morfométrica de los conos volcánicos monogenéticos de los campos volcánicos de Payún Matrú, Llancanelo y Cuenca del Río Salado". Boletín de Estudios Geográficos (in Spanish) (107). ISSN 0374-6186.
  • Burd, Aurora; Booker, John; Pomposiello, Cristina; Favetto, Alicia; Larsen, Jimmy; Giordanengo, Gabriel; Orozco Bernal, Luz (1 January 2008). "Electrical conductivity beneath the Payún Matrú Volcanic Field in the Andean back-arc of Argentina near 36.5°S: Insights into the magma source". Proceedings of the 7th International Symposium on Andean Geodynamics. Retrieved 20 January 2019 – via ResearchGate.
  • Díaz, González; F, Emilio (1972). "Descripción Geológica de la Hoja 30 d, Payún-Matrú" (in Spanish). Servicio Nacional Minero Geológico. Retrieved 20 January 2019.
  • Espanon, Venera R.; Chivas, Allan R.; Phillips, David; Matchan, Erin L.; Dosseto, Anthony (1 December 2014). "Geochronological, morphometric and geochemical constraints on the Pampas Onduladas long basaltic flow (Payún Matrú Volcanic Field, Mendoza, Argentina)". Journal of Volcanology and Geothermal Research. 289: 114–129. Bibcode:2014JVGR..289..114E. doi:10.1016/j.jvolgeores.2014.10.018. ISSN 0377-0273.
  • Germa, A.; Quidelleur, X.; Gillot, P. Y.; Tchilinguirian, P. (1 April 2010). "Volcanic evolution of the back-arc Pleistocene Payun Matru volcanic field (Argentina)". Journal of South American Earth Sciences. 29 (3): 717–730. Bibcode:2010JSAES..29..717G. doi:10.1016/j.jsames.2010.01.002. ISSN 0895-9811.
  • Hernando, I. R.; Franzese, J. R.; Llambías, E. J.; Petrinovic, I. A. (21 May 2014). "Vent distribution in the Quaternary Payún Matrú Volcanic Field, western Argentina: Its relation to tectonics and crustal structures". Tectonophysics. 622: 122–134. Bibcode:2014Tectp.622..122H. doi:10.1016/j.tecto.2014.03.003. ISSN 0040-1951.
  • Hernando, Irene Raquel; Petrinovic, Ivan Alejandro; Llambías, Eduardo Jorge; D'Elia, Leandro; González, Pablo Diego; Aragón, Eugenio (1 February 2016). "The role of magma mixing and mafic recharge in the evolution of a back-arc quaternary caldera: The case of Payún Matrú, Western Argentina". Journal of Volcanology and Geothermal Research. 311: 150–169. Bibcode:2016JVGR..311..150H. doi:10.1016/j.jvolgeores.2016.01.008. ISSN 0377-0273.
  • Hernando, I. R.; Petrinovic, I. A.; D'Elia, L.; Guzmán, S.; Páez, G. N. (1 March 2019). "Post-caldera pumice cones of the Payún Matrú caldera, Payenia, Argentina: Morphology and deposits characteristics". Journal of South American Earth Sciences. 90: 453–462. doi:10.1016/j.jsames.2018.12.017. ISSN 0895-9811.
  • Inbar, M.; Risso, C. (1 January 2001). "A morphological and morphometric analysis of a high density cinder cone volcanic field - Payun Matru, south-central Andes, Argentina". Zeitschrift für Geomorphologie: 321–343.
  • Inbar, Moshe; Risso, Corina (2001). "Holocene yardangs in volcanic terrains in the southern Andes, Argentina". Earth Surface Processes and Landforms. 26 (6): 657–666. Bibcode:2001ESPL...26..657I. doi:10.1002/esp.207. ISSN 1096-9837.
  • Marchetti, David W.; Hynek, Scott A.; Cerling, Thure E. (1 February 2014). "Cosmogenic 3He exposure ages of basalt flows in the northwestern Payún Matru volcanic field, Mendoza Province, Argentina". Quaternary Geochronology. Tracking the pace of Quaternary landscape change with cosmogenic nuclides. 19: 67–75. doi:10.1016/j.quageo.2012.10.004. ISSN 1871-1014.
  • Massironi, M; Pasquarè, G; Giacomini, Lorenza; Frigeri, Alessandro; Bistacchi, Andrea; Federico, Costanzo (1 June 2007). The Payun-Matru lava field: a source of analogues for Martian long lava flows (PDF). Exploring Mars and its Earth Analogues. ResearchGate. Retrieved 20 January 2019.
  • Mazzarini, F.; Fornaciai, A.; Bistacchi, A.; Pasquarè, F. A. (2008). "Fissural volcanism, polygenetic volcanic fields, and crustal thickness in the Payen Volcanic Complex on the central Andes foreland (Mendoza, Argentina)". Geochemistry, Geophysics, Geosystems. 9 (9): n/a. Bibcode:2008GGG.....9.9002M. doi:10.1029/2008GC002037. ISSN 1525-2027.
  • Mikkan, Raúl (2014). "Payunia, campos volcánicos Llancanelo y Payún Matrú: Patrimonio mundial". Tiempo y Espacio (in Spanish) (33): 31–47. ISSN 0719-0867.
  • Mikkan, Raúl (22 June 2017). "Morfología compleja y dinámica de los conos monogenéticos Los Morados Sur en el campo volcánico Payún Matrú, Malargüe, Mendoza". Boletín de Estudios Geográficos (in Spanish) (108). ISSN 0374-6186.
  • Németh, Karoly; Risso, Corina; Nullo, Francisco; Kereszturi, Gabor (2011). "The role of collapsing and cone rafting on eruption style changes and final cone morphology: Los Morados scoria cone, Mendoza, Argentina". Open Geosciences. 3 (2): 102–118. Bibcode:2011CEJG....3..102N. doi:10.2478/s13533-011-0008-4. ISSN 2391-5447.
  • Pasquarè, Giorgio; Bistacchi, Andrea; Mottana, Annibale (1 September 2005). "Gigantic individual lava flows in the Andean foothills near Malargüe (Mendoza, Argentina)". Rendiconti Lincei. 16 (3): 127–135. doi:10.1007/BF02904761. ISSN 1720-0776.
  • Pomposiello, M. C.; Favetto, A.; Mackie, R.; Booker, J. R.; Burd, A. I. (1 August 2014). "Three-dimensional electrical conductivity in the mantle beneath the Payún Matrú Volcanic Field in the Andean backarc of Argentina near 36.5°S: evidence for decapitation of a mantle plume by resurgent upper mantle shear during slab steepening". Geophysical Journal International. 198 (2): 812–827. Bibcode:2014GeoJI.198..812B. doi:10.1093/gji/ggu145. ISSN 0956-540X.
  • Risso, Corina; Németh, Karoly; Martin, Ulrike (1 September 2006). "Geotopvorschläge für pliozäne bis rezente Vulkanfelder in Mendoza, Argentinien" [Proposed geosites on Pliocene to Recent pyroclastic cone fields in Mendoza, Argentina]. Zeitschrift der Deutschen Gesellschaft für Geowissenschaften. 157 (3): 477–490. doi:10.1127/1860-1804/2006/0157-0477.
  • Risso, Corina; Nemeth, Karoly; Nullo, Francisco (14 April 2009). Field Guide to Payún Matru and Llancanelo volcanic fields, Malargüe - Mendoza (PDF). 3rd International Maar Conference. ResearchGate. Retrieved 20 January 2019.
  • Rossotti, Andrea; Massironi, Matteo; Boari, Elena; Bertotto, Gustavo Walter; Francalanci, Lorella; Bistacchi, Andrea; Pasquarè, Giorgio (2008). "Very long pahoehoe inflated basaltic lava flows in the Payenia volcanic province (Mendoza and la Pampa, Argentina)". Revista de la Asociación Geológica Argentina. 63 (1): 131–149. ISSN 0004-4822.
  • Sato, Kei; Gonzalez, Pablo D.; Llambias, Eduardo J.; Hernando, Irene R. (5 January 2012). "Volcanic stratigraphy and evidence of magma mixing in the Quaternary Payun Matru volcano, andean backarc in western Argentina". Andean Geology. 39 (1): 158–179. doi:10.5027/andgeoV39N1-a08. ISSN 0718-7106.
  • Spakman, W.; González, P. D.; Frei, R.; Aragón, E.; Hernando, I. R. (1 January 2014). "Constraints on the Origin and Evolution of Magmas in the Payún Matrú Volcanic Field, Quaternary Andean Back-arc of Western Argentina". Journal of Petrology. 55 (1): 209–239. Bibcode:2014JPet...55..209H. doi:10.1093/petrology/egt066. ISSN 0022-3530.
  • Sumino, Hirochika; Orihashi, Yuji; Ponce, Alexis Daniel; Bertotto, Gustavo Walter; Bernardi, Mauro Ignacio (30 January 2019). "Volcanology and inflation structures of an extensive basaltic lava flow in the Payenia Volcanic Province, extra-Andean back arc of Argentina". Andean Geology. 46 (2): 279–299. doi:10.5027/andgeoV46n2-3180. ISSN 0718-7106.

External links

  • Payún Matru Volcanic Field, Argentina : Image of the Day at NASA's Earth Observatory
  • Hernando, Irene Raquel (2012). Evolución volcánica y petrológica del volcán Payún Matrú, retroarco andino del sudeste de Mendoza (Thesis) (in Spanish). p. 358.
  • Llambías, Eduardo Jorge (1964). Geología y petrografía del volcán Payun Matru (Tesis Doctoral). Facultad de Ciencias Exactas y Naturales. Universidad de Buenos Aires.
  • Manton, Ryan (2012-01-01). The History and Evolution of Payún Matrú Caldera, Mendoza Province, Argentina. Faculty of Science, Medicine & Health - Honours Theses (Thesis).
  • Photos of minerals from Payún Matrú