| 词条 | Payún Matrú |
| 释义 |
| name = Payun Matru | photo =Payún Volcanic Field (8347075230).jpg | photo_caption = Payun Matru | map = Argentina | elevation_m = 3715 | elevation_ref = [1] | prominence = | location = Argentina | range = Andes | coordinates = {{coord|36.422|S|69.241|W|format=dms|type:mountain_region:AR|display=inline,title}} | coordinates_ref = [1] | topo = | type = Shield volcano | age = | last_eruption = 515 ± 50 years ago | first_ascent = | easiest_route = }}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 located 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 it forms the Payenia volcanic province. Payún Matrú is part of the Reserva Provincial La Payunia and has been proposed to become a World Heritage Site. Payún Matrú formed over sediments and volcanic rocks ranging from Mesoproterozoic to Tertiary age. It consists of a large shield volcano capped off by a {{convert|7|-|8|km}} caldera that formed during a large explosive eruption 168-82 thousands of years ago, by a compound volcano named Payun or Payun Liso that reaches a height of {{convert|3680|-|3797|m}} height and two groups of scoria cones and lava flows due west and east from the main shield volcano. One of these lava flows, the Pleistocene Pampas Onduladas lava flow, reaches a length of {{convert|167|-|181|km}} and is the world's longest Quaternary lava flow. Volcanic activity at Payún Matrú commenced during the Plio-Pleistocene and formed first 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. NameAccording to the local population, the term Payún or Paium means "bearded" and the term Matru means "goat".{{sfn|Díaz|F|1972|p=9}} The field is sometimes also known as Payenia.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=718}} Geography and geomorphologyRegionalPayún Matrú lies in the Malargüe Department of the Mendoza Province, Argentina.{{sfn|Blazek|Lourdes|2017|p=90}} The area is inhospitable due to the lack of usable water and at high elevations of pastures and firewood;{{sfn|Díaz|F|1972|p=9}} nevertheless there are many paved roads{{sfn|Díaz|F|1972|p=24}} such as National Route 40 which passes west of the volcanic field{{sfn|Risso|Németh|Martin|2006|p=486}} and National Route 186 which runs around the northern and eastern parts of Payún Matrú.{{sfn|Inbar|Risso|2001|p=331}} The volcano is located within the Reserva Provincial La Payunia.[3] 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{{sfn|Mikkan|2014|p=31}} and a number of potential geosites have been identified at Payún Matrú itself.{{sfn|Risso|Németh|Martin|2006|pp=485-487}} The volcanic field is part of the backarc area of the Southern Volcanic Zone, a {{convert|1000|km}} long volcanic arc{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=717}} and together with the Northern Volcanic Zone, the Central Volcanic Zone and the Austral Volcanic Zone one of four volcanic belts in the Andes.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=718}} Among these volcanoes is Laguna del Maule almost due west from Payún Matrú.{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=115}} LocalPayún Matrú is a {{convert|15|km}} wide{{sfn|Hernando|Petrinovic|D'Elia|Guzmán|2019|p=454}} shield volcano[1] whose foot is marked by the {{convert|1750|m}} elevation line and which extends mainly east-west;{{sfn|Díaz|F|1972|p=15}} rising about {{convert|2|km}} above the surrounding terrain{{sfn|Sato|Gonzalez|Llambias|Hernando|2012|p=160}} it covers about {{convert|5200|km2}} of land with lavas{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=91}} and has diverse volcanic landforms.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=719}} Ignimbrites cover and flatten its northern and eastern slopes, while in the west and south lava domes and coulees{{efn|name=Coulee|A coulee is a particular type of lava dome which has flowed sideward like a lava flow.[5]}} predominate; these have often rough surfaces and are difficult to cross. The lower slopes are more gentle and covered by Pleistocene-Holocene lava flows.{{sfn|Díaz|F|1972|p=16}} Wind erosion has created flutes, grooves and yardangs within the ignimbrites,{{sfn|Risso|Németh|Martin|2006|p=487}} such as in the western sector where yardangs reach heights of {{convert|8|m}} and widths of {{convert|100|m}}.{{sfn|Inbar|Risso|2001|p=660}} The total volume of this shield is about {{convert|240|km3}}.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=727}} In the summit region of the shield lies a {{convert|7|km}}{{sfn|Díaz|F|1972|p=15}}//caldera">caldera surrounded by several peaks, which clockwise from north include the {{convert|3650|m}} high Nariz/Punta del Payún, the Punta Media, the {{convert|3450|m}} high Punta Sur and the approximately {{convert|3700|m}} high Cerro Matru or Payen. In the field however Cerro Matru looks smaller than Nariz.{{sfn|Díaz|F|1972|p=15}} The caldera was once {{convert|8|-|9|km}} wide but erosion of its flanks and later volcanic activity have reduced its size{{sfn|Díaz|F|1972|p=16}} and hidden the rim below coulees, lava domes, lava flows{{sfn|Risso|Németh|Martin|2006|p=487}} and pumice cones{{sfn|Hernando|Petrinovic|D'Elia|Guzmán|2019|p=454}} that were emplaced after the caldera collapse.{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=134}} The exception are the northern and southern walls which are almost vertical{{convert|60|km}} long) northwestern and the longer southeastern branch{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=132}} which reaches all the way to an alluvial terrace of the Salado River{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=138}} in the La Pampa Province.{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=133}} This compound lava flow moved over a gentle terrain{{sfn|Massironi|Pasquarè|Giacomini|Frigeri|2007|p=1}} and is covered by lava rises and lava tumuli{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=117}} especially in areas where the flow encountered obstacles in the topography.{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=120}} There is some variation in its appearance between a wide, leveled initial proximal sector{{sfn|Pasquarè|Bistacchi|Mottana|2005|p=130}} and a more sinouous distal sector.{{sfn|Pasquarè|Bistacchi|Mottana|2005|p=132}} The unusually fast flowing lava eventually accumulated to a volume of at least {{convert|7.2|km3}}, a surface area of about {{convert|739|km2}} and depending on the measurement a length of {{convert|167|-|181|km}}{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=125}} under the influence of a favourable topography and low viscosity of the lava.{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=128}} 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".{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=132}} Parts of the Pampas Onduladas lava flow have been buried by more recent lava flows.{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=134}} 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 {{convert|100|km}}{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=114}} and it has been compared to some long lava flows on Mars.{{sfn|Massironi|Pasquarè|Giacomini|Frigeri|2007|p=2}} 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,{{sfn|Pasquarè|Bistacchi|Mottana|2005|p=129}} and the La Carbonilla lava flow which like Los Carrizales propagated southeastward and is located just west from the latter.{{sfn|Németh|Risso|Nullo|Kereszturi|2011|p=104}} 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.{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=133}} Hydrography and non-volcanic landscapeApart 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.{{sfn|Díaz|F|1972|p=9}} Likewise, there are no permanent rivers in the field and most of the precipitation quickly seeps into the permeable or sandy ground.{{sfn|Díaz|F|1972|p=18}} The whole massif is surrounded by sandy plains, which are simply volcanic rocks covered by aeolian sediments; the plains also feature small closed basins{{sfn|Díaz|F|1972|p=17}} and such basins are also found in the lavic area.{{sfn|Díaz|F|1972|p=19}} GeologyWest of South America, the Nazca Plate and the Antarctic Plate subduct beneath the South America Plate{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=116}} at a rate of {{convert|80|-|66|mm/year|in/year}},{{sfn|Mazzarini|Fornaciai|Bistacchi|Pasquarè|2008|p=2}} giving rise to the Andean volcanic belt. The volcanic belt is not continuous and is interrupted by gaps where the subduction is shallower{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=116}} and the asthenosphere between the two plates missing.{{sfn|Pomposiello|Favetto|Mackie|Booker|2014|p=813}} North of the Payún Matrú, flat slab subduction takes place; in the past flat slab subduction occurred farther south as well with noticeable influence on magma chemistry.{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=90}} In general, the mode of subduction in the region has been variable over time.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=717}} There is evidence of Precambrian{{sfn|Díaz|F|1972|p=81}} and Permian-Triassic volcanism (Choique Mahuida Formation){{sfn|Mazzarini|Fornaciai|Bistacchi|Pasquarè|2008|p=4}} 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 volcanic were emplaced.{{sfn|Díaz|F|1972|p=82}} This kind of calcalkaline volcanic activity is interpreted to be the consequence of flat slab subduction during the Miocene and Pliocene,{{sfn|Hernando|Petrinovic|D'Elia|Guzmán|2019|p=454}} and which took place between 20 and 5 million years ago.{{sfn|Pomposiello|Favetto|Mackie|Booker|2014|p=813}} Later during the Pliocene and Quaternary the slab steepened, and volcanism in the abovelying land increased probably as a consequence,{{sfn|Pomposiello|Favetto|Mackie|Booker|2014|p=814}} reaching a peak between 8 and 5 million years ago.{{sfn|Sato|Gonzalez|Llambias|Hernando|2012|p=160}} LocalThe basement underneath Payún Matrú is formed by Mesoproterozoic to Triassic rocks of the San Rafael Block, Mesozoic{{sfn|Hernando|Franzese|Llambías|Petrinovic|2014|p=123}} to Paleogene sediments of the Neuquén Basin and Miocene lava flows{{sfn|Hernando|Franzese|Llambías|Petrinovic|2014|p=124}} such as the Tertiary Patagonian basalts.{{sfn|Rossotti|Massironi|Boari|Bertotto|2008|p=133}} The Andean orogeny during the Miocene has folded and deformed the basement, forming basins and uplifted basement blocks.{{sfn|Hernando|Franzese|Llambías|Petrinovic|2014|p=124}} Oil has been drilled close to the volcanic field from sediments of Mesozoic age.{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=91}} It is part of the backarc volcanic province, {{convert|200|km}} east of the Andes{{sfn|Blazek|Lourdes|2017|p=90}} and {{convert|530|km}} east of the Peru-Chile Trench.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=717}} The volcanic activity still relates to the subduction of the Nazca Plate beneath the South America Plate, however;{{sfn|Blazek|Lourdes|2017|p=90}} one proposed mechanism is that a Miocene change in the subduction regimen led to the development of extensional tectonics{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=90}} and to the development of faults that form the pathways for magma ascent.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=719}} Other volcanic fields in the region are the Llancanelo volcanic field, the Nevado volcanic field and Salado Basin volcanic field, the first two farther north of Payún Matrú and the last farther south. These fields are subdivided on the basis of geochemical differences{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=116}} and consist of two stratovolcanoes Payún Matrú and Nevado and many monogenetic volcanoes.{{sfn|Inbar|Risso|2001|p=323}} The volcanic field is part of the larger Payunia volcanic province, which covers an area of about {{convert|36000|km2}}{{sfn|Blazek|Lourdes|2017|p=88}} and is also known as the Payenia{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=90}} or Andino-Cuyana volcanic province.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=718}} 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,{{sfn|Hernando|Petrinovic|Llambías|D'Elia|2016|p=151}}{{sfn|Hernando|Franzese|Llambías|Petrinovic|2014|p=122}} although historical eruptions have not been observed.{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=90}} Even farther south are the Chachahuen and Auca Mahuida volcanoes{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=718}} and the Tromen volcano farther west appears to relate to Payún Matrú as well.{{sfn|Pomposiello|Favetto|Mackie|Booker|2014|p=822}} Lava and magma compositionThe volcanic field has erupted rocks with composition ranging from alkali basalts{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=91}} over basalts, rhyolite, trachyandesite, basaltic trachyandesite, trachybasalt and trachyte. 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 is more potassium-rich and shoshonitic.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=724}} The volcanic rocks contain variable amounts of phenocrysts, including alkali feldspar, amphibole, apatite, biotite, clinopyroxene, olivine, plagioclase and sanidine. Not all phenocryst phases can be found in every rock formation.{{sfn|Hernando|Petrinovic|Llambías|D'Elia|2016|p=154}}{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|pp=723-724}} Magma temperatures of {{convert|1122|-|1276|C}} have been inferred.{{sfn|Hernando|Petrinovic|Llambías|D'Elia|2016|p=167}} Volcanic rocks erupted at Payún Matrú show no evidence of volcanic arc volcanism{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=90}} and rather resemble ocean island basalt volcanism, implying a deep origin of the magma although a shallow origin cannot be ruled out.{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=91}} Magnetotelluric{{efn|The magnetotelluric technique is a research technique, which exploits natural electromagnetic fields to obtain information on the electrical conductivity underground.[9]}} observations indicate the presence of a "plume"-like structure that rises from {{convert|200|-|400|km}} 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.{{sfn|Burd|Booker|Pomposiello|Favetto|2008|p=93}} The formation process of the magma erupted at Payún Matrú begins with partial melting of enriched mantle;{{sfn|Spakman|González|Frei|Aragón|2014|p=211}} the resulting melts then undergo crystal fractionation,{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=728}} assimilation of crustal material{{sfn|Spakman|González|Frei|Aragón|2014|p=234}} and magma mixing in magma chambers.{{sfn|Hernando|Petrinovic|Llambías|D'Elia|2016|p=163}} The magmas eventually reach the surface through deep faults.{{sfn|Inbar|Risso|2001|p=325}} The edifice of Payún Matrú acts as an obstacle to magmas ascending to the surface; this is why only evolved{{efn|Evolved magmas are magmas which due to a settling of crystals have lost part of their magnesium oxide.}} magmas are erupted in the caldera area of Payún Matrú while basic magmas reached the surface mainly outside of the main edifice.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=729}} 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.[11] Further, Payun volcano is notable for large crystals of hematite pseudomorphs after magnetite, of volcanic fumarole origin.[12]Climate, soils and vegetationThe climate at Payún Matrú is cold and dry[3] with strong westerly winds.{{sfn|Inbar|Risso|2001|p=325}} Annual temperature varies between {{convert|2|-|20|C}}{{sfn|Inbar|Risso|2001|p=658}} while the average temperature in the wider region is about {{convert|15|C}} and the average annual precipitation amounts to {{convert|300|mm/year|in/year}}{{sfn|Mikkan|2014|p=34}}//continent">continental climate with hot summers especially at lower elevations and cold winters especially at higher elevations.{{sfn|Díaz|F|1972|p=19}} 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.{{sfn|Mikkan|2014|p=34}} 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.{{sfn|Díaz|F|1972|p=20}} The higher parts of Payún Matrú may have risen above the snowline during ice ages,{{sfn|Inbar|Risso|2001|p=659}} and periglacial landforms have been observed.{{sfn|Inbar|Risso|2001|p=326}} Palynology data from south of the region indicate that the climate has been stable since the Late Pleistocene.{{sfn|Inbar|Risso|2001|p=325}} The vegetation in the volcanic field is mostly characterized by sparse bushes as well as herbaceous vegetation but few trees,{{sfn|Díaz|F|1972|p=22}} and is classified as xerophytic.{{sfn|Inbar|Risso|2001|p=325}} Soils are shallow and are mainly rocky to loess-like.{{sfn|Inbar|Risso|2001|p=658}} Representative plant genera are Opuntia cactus and Poa and Stipa grasses.{{sfn|Risso|Nemeth|Nullo|2009|p=21}} 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.{{sfn|Mikkan|2014|p=34}} Eruption historyThe geological history of the Payún Matrú volcanic field is poorly dated{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=116}} but the field has been active since Pliocene at least.{{sfn|Germa|Quidelleur|Gillot|Tchilinguirian|2010|p=719}} 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 measured by potassium-argon dating.{{sfn|Espanon|Chivas|Phillips|Matchan|2014|p=116}} Lava flows have been subdivided into the older Puente Group and the younger Tromen Group formations,{{sfn|Németh|Risso|Nullo|Kereszturi|2011|p=105}} which are of Pleistocene to Pleistocene-Holocene age, respectivelywesterly side.{{sfn|Marchetti|Hynek|Cerling|2014|p=69}}
See also
Notes{{notelist}}References1. ^1 {{cite book|last1=Blake|first1=S.|title=Viscoplastic Models of Lava Domes|journal=Lava Flows and Domes|volume=2|date=1990|page=93|doi=10.1007/978-3-642-74379-5_5|publisher=Springer, Berlin, Heidelberg|language=en|series=IAVCEI Proceedings in Volcanology|isbn=978-3-642-74381-8}} [1][2][3][4][5][6][7][8]2. ^1 {{Cite book|title=Electromagnetic methods in applied geophysics. Vol. 2, Applications, Parts A and B|date=1991|publisher=Society of Exploration Geophysicists|others=Nabighian, Misac N., Society of Exploration Geophysicists.|isbn=9781560802686|location=Tulsa, Okla. (8801 South Yale St., Tulsa OK 74137-3175)|oclc=778681058|chapter=The Magnetotelluric Method}} 3. ^1 Payun volcano at Mindat.org 4. ^1 2 {{cite journal |last1=Corbalán |first1=Valeria |last2=Debandi |first2=Guillermo |last3=Kubisch |first3=Erika |title=Thermal ecology of two sympatric saxicolous lizards of the genus Phymaturus from the Payunia region (Argentina) |journal=Journal of Thermal Biology |date=1 October 2013 |volume=38 |issue=7 |page=385 |doi=10.1016/j.jtherbio.2013.05.006 |issn=0306-4565}} 5. ^1 {{Citation|last=Perucca|first=Laura P.|date=2009-01-01|work=Developments in Earth Surface Processes|volume=13|page=293|editor-last=Latrubesse|editor-first=Edgardo M.|series=Natural Hazards and Human-Exacerbated Disasters in Latin America|publisher=Elsevier|last2=Moreiras|first2=Stella M.|doi=10.1016/S0928-2025(08)10014-1|title=Natural Hazards and Human-Exacerbated Disasters in Latin America|isbn=9780444531179}} 6. ^1 2 3 4 5 6 7 {{cite gvp|vn=357066|name=Payún Matru}} 7. ^1 {{cite journal |last1=Giesso |first1=M. |last2=Durán |first2=V. |last3=Neme |first3=G. |last4=Glascock |first4=M. D. |last5=Cortegoso |first5=V. |last6=Gil |first6=A. |last7=Sanhueza |first7=L. |title=A Study of Obsidian Source Usage in the Central Andes of Argentina and Chile |journal=Archaeometry |date=2011 |volume=53 |issue=1 |page=16 |doi=10.1111/j.1475-4754.2010.00555.x |language=en |issn=1475-4754}} 8. ^1 {{Cite journal|last=Schimmelpfennig|first=Irene|last2=Benedetti|first2=Lucilla|last3=Garreta|first3=Vincent|last4=Pik|first4=Raphaël|last5=Blard|first5=Pierre-Henri|last6=Burnard|first6=Pete|last7=Bourlès|first7=Didier|last8=Finkel|first8=Robert|last9=Ammon|first9=Katja|date=2011-05-15|title=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)|journal=Geochimica et Cosmochimica Acta|volume=75|issue=10|page=2619|doi=10.1016/j.gca.2011.02.013|issn=0016-7037}} }} Sources{{refbegin}}
|first6=Gabriel|last7=Orozco Bernal|first7=Luz|date=1 January 2008|title=Electrical conductivity beneath the Payún Matrú Volcanic Field in the Andean back-arc of Argentina near 36.5°S: Insights into the magma source|journal=Proceedings of the 7th International Symposium on Andean Geodynamics|url=https://www.researchgate.net/publication/240615312|via=ResearchGate|language=en|access-date=2019-01-20|ref=harv}}
first5=Andrea|last6=Federico|first6=Costanzo|date=1 June 2007|url=https://www.researchgate.net/publication/233855189_The_Payun-Matru_lava_field_a_source_of_analogues_for_Martian_long_lava_flows|format=PDF|title=The Payun-Matru lava field: a source of analogues for Martian long lava flows|website=ResearchGate|language=en|access-date=2019-01-20|ref=harv}}
External links
7 : Volcanoes of Mendoza Province|Andean Volcanic Belt|Polygenetic shield volcanoes|Subduction volcanoes|Mountains of Argentina|Quaternary volcanoes|Quaternary South America |
| 随便看 |
|
开放百科全书收录14589846条英语、德语、日语等多语种百科知识，基本涵盖了大多数领域的百科知识，是一部内容自由、开放的电子版国际百科全书。