Wikipedia

Cerro Guacha

Cerro Guacha is a Miocene caldera in southwestern Bolivia's Sur Lípez Province. Part of the volcanic system of the Andes, it is considered to be part of the Central Volcanic Zone (CVZ), one of the three volcanic arcs of the Andes, and its associated Altiplano-Puna volcanic complex (APVC). A number of volcanic calderas occur within the latter.

Cerro Guacha
Cerro Guacha is located in Bolivia
Cerro Guacha
Cerro Guacha
Highest point
Coordinates22°45′S 67°28′W / 22.750°S 67.467°W / -22.750; -67.467
Naming
Language of nameSpanish

Cerro Guacha and the other volcanoes of that region are formed from the subduction of the Nazca Plate beneath the South American Plate. Above the subduction zone, the crust is chemically modified and generates large volumes of melts that form the local caldera systems of the APVC. Guacha is constructed over a basement of sediments.

Two major ignimbrites, the 5.6-5.8 mya Guacha ignimbrite with a volume of 1,300 cubic kilometres (310 cu mi) and the 3.5-3.6 mya Tara ignimbrite with a volume of 800 cubic kilometres (190 cu mi) were erupted from Cerro Guacha. More recent activity occurred 1.7 mya and formed a smaller ignimbrite with a volume of 10 cubic kilometres (2.4 cu mi).

The larger caldera has dimensions of 60 by 40 kilometres (37 mi × 25 mi) with a rim altitude of 5,250 metres (17,220 ft). Extended volcanic activity has generated two nested calderas, a number of lava domes and lava flows and a central resurgent dome.

Geography and structure

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The caldera was discovered in 1978 thanks to Landsat imagery. It lies in Bolivia next to the Chilean frontier. The terrain is difficult to access being located at altitudes between 3,000–4,000 metres (9,800–13,100 ft). The caldera is named after Cerro Guacha, a feature named as such by local topographic maps.[1] Later research by the Geological Service of Bolivia indicated the presence of three welded tuffs.[2] Paleogene red beds and Ordovician sediments form the basement of the caldera.[3]

Cerro Guacha is part of the Altiplano-Puna volcanic complex, an area of extensive ignimbrite volcanism in the Central Andes between the Altiplano and the Atacama and associated with the Central Volcanic Zone of the Andes. Several large caldera complexes are found within this area, formed by crustal magma chambers generated by magmas derived from the melting of deep crustal layers. Present day activity is limited to geothermal phenomena in El Tatio, Sol de Manana and Guacha,[4] with recent activity encompassing the extrusion of Quaternary lava domes and flows. Deformation in the area occurs beneath Uturuncu volcano north of the Guacha centre.[5]

A westward-facing semicircular scarp (60 by 40 kilometres (37 mi × 25 mi)) contains subvertically banded Guacha ignimbrite layers rich in lithic clasts and is the presumable vent of the Guacha ignimbrite. The resulting caldera formed like a trapdoor and with a volume of 1,200 cubic kilometres (290 cu mi) is among the largest known. Volcanic structures are aligned along the eastern moat of this structure, which is filled by lacustrine deposits and welded ignimbrites. Another eastern collapse was generated by the Tara Ignimbrite eruption, with dimensions of 30 by 15 kilometres (18.6 mi × 9.3 mi).[2][6] The margins of the caldera-graben structure are about 5,250 metres (17,220 ft) high while the caldera floors are about 1,000 metres (3,300 ft) lower. Probably dacitic lava domes are found on the northern caldera rim, with the caldera floor possibly containing lava flows.[1]

The caldera contains a resurgent dome, the western part of it is formed by the Tara ignimbrite while the eastern is part of the Guacha ignimbrite. This dome was cut by the Tara collapse, exposing 700 metres (2,300 ft) of Guacha ignimbrites. The resurgent dome in the caldera rises about 1.1 kilometres (0.68 mi) above the caldera floor.[6] A second resurgence episode occurred inside the Tara caldera.[7] The caldera is filled up to 1 kilometre (0.62 mi) thick with ignimbrites. Three lava domes, roughly coeval with the Tara ignimbrite, are constructed on the northern side of the resurgent dome. The western dome is named Chajnantor and is the most silica-rich of the domes. Rio Guacha in the middle is more dacitic. The Puripica Chico lavas on the western side of the caldera are not associated with a collapse.[6] Dark coloured lava flows are found to the southwest of the caldera.[8]

Some geothermal activity occurs within the caldera.[9] Laudrum et al. suggested that the heat from Guacha and Pastos Grandes may be transferred to the El Tatio geothermal system to the west.[10]

Geology

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Guacha is part of a volcanic complex in the back-arc region of the Andes in Bolivia.[11] The Central Andes are underlaid by the Paleoproterozoic-Paleozoic Arequipa-Antofalla terrane.[7] The Central Andes started to form 70 mya. Previously, the area was formed from a Paleozoic marine basin with some early volcanics.[2]

Since the Jurassic, subduction has been occurring on the western margin of present-day South America, resulting in variable amounts of volcanic activity. A short interruption of volcanism, associated with a flattening of the subducting plate, occurred in the Oligocene 35-25 mya. Subsequently, renewed melt generation modified the overlying crust until major volcanism, associated with a "flare up" of ignimbritic volcanism occurred 10 mya. 100–250 kilometres (62–155 mi) beneath the local volcanic zone lies the Benioff zone of the subducting Nazca Plate. Recently a change in volcanic activity away from ignimbritic towards cone-forming volcanism has been observed.[5]

Local

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Guacha caldera is part of the Altiplano-Puna volcanic complex (APVC), an igneous province in the central Andes covering a surface area of 70,000 square kilometres (27,000 sq mi). Here on an average altitude of 4,000 metres (13,000 ft) between 10 and 1 mya roughly 10,000 cubic kilometres (2,400 cu mi) of ignimbrites were erupted. Gravitic research indicates the presence of a low density area centered beneath Guacha.[12] The magmatic body underpinning the APVC is centered beneath Guacha.[13] Guacha caldera is also closely linked to the neighbouring La Pacana caldera.[14]

The Guacha caldera forms a structure with the neighbouring Cerro Panizos, Coranzulí and Vilama calderas associated with a fault named the Lípez lineament. Activity along this lineament commenced with the Abra Granada volcanic complex 10 mya ago and dramatically increased more than a million years later. Volcanic activity is linked to this fault zone and to the thermal maturation of the underlying crust.[15] After 4 million years ago activity waned again in the Altiplano-Puna volcanic complex.[16]

Geologic record

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The Guacha system was constructed over a timespan of 2 million years with a total volume of 3,400 cubic kilometres (820 cu mi).[17] Eruptive activity occurred at regular intervals. Calculations indicate that the Guacha system was supplied by magmas at a rate of 0.007–0.018 cubic kilometres per year (5.3×10−5–0.000137 cu mi/Ms).[12]

Located at a high altitude in an area of long term arid climate has preserved old volcanic deposits over time.[4] Thus, unlike in other areas of the world such as the Himalayas where water erosion governs the landscape the morphology of the Altiplano-Puna volcanic complex is mostly tectonic in origin.[18]

Composition and magma properties

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The Guacha Ignimbrite is rhyodacite and rich in crystals. The Chajnantor lava dome contains sanidine while Rio Guacha of dacitic composition contains amphibole and pyroxene. The Tara ignimbrite has a composition intermediary to that of these two domes,[6] being andesitic-rhyolithic.[2] The Guacha Ignimbrite contains 62-65% SiO2, Puripicar 67-68% and the Tara Ignimbrite 63%. Plagioclase and quartz are found in all ignimbrites.[17]

Geological considerations indicate that the Guacha ignimbrite was stored at a depth of 5–9.2 kilometres (3.1–5.7 mi) and the Tara ignimbrite at a depth of 5.3–6.4 kilometres (3.3–4.0 mi). Zircon temperatures are 716 °C (1,321 °F), 784 °C (1,443 °F) and 705 °C (1,301 °F) for Guacha, Tara and Chajnantor respectively.[7]

Climate

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The climate of the Central Andes is characterized by extreme aridity. The eastern mountain chain of the Andes prevents moisture from the Amazon from reaching the Altiplano area. The area is also too far north for the precipitation associated with the Westerlies to reach Guacha. This arid climate may go back to the Mesozoic and was enhanced by geographical and orogenic changes during the Cenozoic.[19]

Oxygen isotope analysis indicates that the Guacha caldera ignimbrites have had little influence from meteoric waters. This is consistent with the climate of the Guacha region displaying long-term aridity for the last 10 mya as well as with the scarcity of pronounced geothermal systems in the APVC which are essentially limited to the El Tatio and Sol de Manana fields.[20]

Eruptive history

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Guacha has been the source of eruptions with volumes of more than 450 cubic kilometres (110 cu mi) dense rock equivalents. These eruptions in Guacha's case have a Volcanic explosivity index of 8. The close succession of multiple large scale eruptions indicates that plutons feeding such eruptions are assembled over millions of years.[6]

The Guacha ignimbrite (including the Lowe Tara Ignimbrite, Chajnantor Tuff, Pampa Guayaques Tuff and possibly the Bonanza Ignimbrite)[17] was first considered part of another ignimbrite named Atana Ignimbrite. It has a minimum volume of 1,300 cubic kilometres (310 cu mi) and covers a surface area of at least 5,800 square kilometres (2,200 sq mi). Several different dates have been determined on the basis of argon-argon dating, including 5.81±0.01 on biotite and 5.65±0.01 mya on sanidine, which is the preferred age. Various samples are separated by distances of up to 130 kilometres (81 mi), making this ignimbrite among the most widespread in the Andes. One stream spreads 60 kilometres (37 mi) northwards past Uturunku volcano along the Quetena valley[6] until Suni K'ira.[2] Some ash deposits in the northern Chilean Coast Range are linked to the Guacha eruption.[21] The Guacha ignimbrite was also known as Lower Tara at first.[2]

The later Tara ignimbrite (including the Upper Tara Ignimbrite, the Filo Delgado Ignimbrite and the Pampa Tortoral Tuff)[17] forms the western dome of the Guacha caldera and spreads mostly north and southeast, between Argentina, Bolivia and Chile. It has a minimum volume of 800 cubic kilometres (190 cu mi) and covers a surface area of at least 1,800 square kilometres (690 sq mi) in Chile and 2,300 square kilometres (890 sq mi) in Bolivia where it was at first not recognized.[6] Some outflows are more than 200 metres (660 ft) thick.[2] Several different dates have been determined on the basis of argon-argon dating, including 3.55±0.01 on biotite and 3.49±0.01 mya on sanidine, which is the preferred age. The Chajnantor lavas and the Rio Guacha dome in the caldera have been K-Ar dated at 3.67±0.13 and 3.61±0.02 mya respectively.[6] This ignimbrite ponded inside the Guacha caldera, and one particularly thick layer (>200 metres (660 ft)) is found beneath Zapaleri stratovolcano.[22] This ignimbrite was formerly known as Upper Tara.[2] Geological considerations indicate that this ignimbrite formed from pre-existent melts and an influx of andesitic magma.[7]

The Puripica Chico ignimbrite is known for having formed the Piedras de Dali hoodoos, named like that by tourists because of their surreal landscape. It has a volume of 10 cubic kilometres (2.4 cu mi) and it was apparently erupted at the hinge of the Guacha caldera. It has been argon-argon dated at 1.72±0.01 mya, making it the youngest Guacha caldera volcanite.[6]

The Puripicar ignimbrite has a volume of 1,500 cubic kilometres (360 cu mi) and is 4.2 mya old.[17] After research indicated that it was different from another ignimbrite named Atana,[23] it was originally linked to the Guacha caldera but Salisbury et al. in 2011 linked the Tara ignimbrite to Guacha instead.[2] Another ignimbrite associated with Guacha is the Guataquina Ignimbrite named after Paso de Guataquina. It covers an area of 2,300 square kilometres (890 sq mi) and has an approximate volume of 70 cubic kilometres (17 cu mi).[1] It was later interpreted to be a combination of the Guacha, Tara and non-Guacha Atana ignimbrites.[2]

See also

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References

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  1. ^ a b c Francis, P.W.; Baker, M.C.W. (August 1978). "Sources of two large ignimbrites in the central andes: Some landsat evidence". Journal of Volcanology and Geothermal Research. 4 (1–2): 81–87. Bibcode:1978JVGR....4...81F. doi:10.1016/0377-0273(78)90029-X.
  2. ^ a b c d e f g h i j Iriarte, Rodrigo (2012). "The Cerro Guacha caldera complex : an upper Miocene-Pliocene polycyclic volcano-tectonic structure in the Altiplano Puna Volcanic Complex of the Central Andes of Bolivia". OSU Libraries. Oregon State University. Retrieved 27 September 2015.
  3. ^ Mobarec, Roberto C.; Heuschmidt, B. (1994). "Evolucion Tectonica Y Differenciacion Magmatica De La Caldera De Guacha, Sudoeste De Bolivia" (PDF). biblioserver.sernageomin.cl (in Spanish). Concepcion: 7o Congreso Geologico Chileno. Archived from the original (PDF) on 27 November 2015. Retrieved 26 November 2015.
  4. ^ a b de Silva, S. L. (1989). "Altiplano-Puna volcanic complex of the central Andes". Geology. 17 (12): 1102. Bibcode:1989Geo....17.1102D. doi:10.1130/0091-7613(1989)017<1102:APVCOT>2.3.CO;2.
  5. ^ a b De Silva, S.; Zandt, G.; Trumbull, R.; Viramonte, J. G.; Salas, G.; Jimenez, N. (1 January 2006). "Large ignimbrite eruptions and volcano-tectonic depressions in the Central Andes: a thermomechanical perspective". Geological Society, London, Special Publications. 269 (1): 47–63. Bibcode:2006GSLSP.269...47D. doi:10.1144/GSL.SP.2006.269.01.04. S2CID 129924955. Retrieved 27 November 2015.
  6. ^ a b c d e f g h i Salisbury, M. J.; Jicha, B. R.; de Silva, S. L.; Singer, B. S.; Jimenez, N. C.; Ort, M. H. (21 December 2010). "40Ar/39Ar chronostratigraphy of Altiplano-Puna volcanic complex ignimbrites reveals the development of a major magmatic province" (PDF). Geological Society of America Bulletin. 123 (5–6): 821–840. doi:10.1130/B30280.1. Retrieved 26 September 2015.
  7. ^ a b c d Grocke, Stephanie (2014). "Magma dynamics and evolution in continental arcs : insights from the Central Andes". OSU Libraries. Oregon State University. Retrieved 28 September 2015.
  8. ^ Baker, M.C.W. (December 1981). "The nature and distribution of upper cenozoic ignimbrite centres in the Central Andes". Journal of Volcanology and Geothermal Research. 11 (2–4): 293–315. Bibcode:1981JVGR...11..293B. doi:10.1016/0377-0273(81)90028-7.
  9. ^ Mattioli, Michele; Renzulli, Alberto; Menna, Michele; Holm, Paul M. (November 2006). "Rapid ascent and contamination of magmas through the thick crust of the CVZ (Andes, Ollagüe region): Evidence from a nearly aphyric high-K andesite with skeletal olivines". Journal of Volcanology and Geothermal Research. 158 (1–2): 87–105. Bibcode:2006JVGR..158...87M. doi:10.1016/j.jvolgeores.2006.04.019.
  10. ^ Landrum, J.T.; Bennett, P.C.; Engel, A.S.; Alsina, M.A.; Pastén, P.A.; Milliken, K. (April 2009). "Partitioning geochemistry of arsenic and antimony, El Tatio Geyser Field, Chile". Applied Geochemistry. 24 (4): 664–676. Bibcode:2009ApGC...24..664L. doi:10.1016/j.apgeochem.2008.12.024. hdl:10533/142624.
  11. ^ Jiménez, Néstor; López-Velásquez, Shirley; Santiváñez, Reynaldo (October 2009). "Evolución tectonomagmática de los Andes bolivianos". Revista de la Asociación Geológica Argentina (in Spanish). 65 (1). ISSN 1851-8249. Retrieved 26 September 2015.
  12. ^ a b de Silva, Shanaka L.; Gosnold, William D. (November 2007). "Episodic construction of batholiths: Insights from the spatiotemporal development of an ignimbrite flare-up". Journal of Volcanology and Geothermal Research. 167 (1–4): 320–335. Bibcode:2007JVGR..167..320D. doi:10.1016/j.jvolgeores.2007.07.015.
  13. ^ Troise, Claudia; de Natale, Giuseppe; Kilburn, Christopher R. J. (2006). Mechanisms of activity and unrest at large calderas. London: Geological Society. p. 54. ISBN 9781862392113. Retrieved 26 November 2015.
  14. ^ De Silva, S.; Zandt, G.; Trumbull, R.; Viramonte, J. G.; Salas, G.; Jimenez, N. (1 January 2006). "Large ignimbrite eruptions and volcano-tectonic depressions in the Central Andes: a thermomechanical perspective". Geological Society, London, Special Publications. 269 (1): 47–63. Bibcode:2006GSLSP.269...47D. doi:10.1144/GSL.SP.2006.269.01.04. S2CID 129924955. Retrieved 26 September 2015.
  15. ^ Caffe, P.J.; Soler, M.M.; Coira, B.L.; Onoe, A.T.; Cordani, U.G. (June 2008). "The Granada ignimbrite: A compound pyroclastic unit and its relationship with Upper Miocene caldera volcanism in the northern Puna". Journal of South American Earth Sciences. 25 (4): 464–484. Bibcode:2008JSAES..25..464C. doi:10.1016/j.jsames.2007.10.004.
  16. ^ Schmitt, A.; de Silva, S.; Trumbull, R.; Emmermann, R. (March 2001). "Magma evolution in the Purico ignimbrite complex, northern Chile: evidence for zoning of a dacitic magma by injection of rhyolitic melts following mafic recharge". Contributions to Mineralogy and Petrology. 140 (6): 680–700. Bibcode:2001CoMP..140..680S. doi:10.1007/s004100000214. S2CID 129724498.
  17. ^ a b c d e Kay, Suzanne Mahlburg; Coira, Beatriz L.; Caffe, Pablo J.; Chen, Chang-Hwa (December 2010). "Regional chemical diversity, crustal and mantle sources and evolution of central Andean Puna plateau ignimbrites". Journal of Volcanology and Geothermal Research. 198 (1–2): 81–111. Bibcode:2010JVGR..198...81K. doi:10.1016/j.jvolgeores.2010.08.013.
  18. ^ Allmendinger, Richard W.; Jordan, Teresa E.; Kay, Suzanne M.; Isacks, Bryan L. (May 1997). "The Evolution of the Altiplano-Puna Plateau of the Central Andes". Annual Review of Earth and Planetary Sciences. 25 (1): 139–174. Bibcode:1997AREPS..25..139A. CiteSeerX 10.1.1.469.3590. doi:10.1146/annurev.earth.25.1.139.
  19. ^ Strecker, M.R.; Alonso, R.N.; Bookhagen, B.; Carrapa, B.; Hilley, G.E.; Sobel, E.R.; Trauth, M.H. (May 2007). "Tectonics and Climate of the Southern Central Andes". Annual Review of Earth and Planetary Sciences. 35 (1): 747–787. Bibcode:2007AREPS..35..747S. doi:10.1146/annurev.earth.35.031306.140158.
  20. ^ Folkes, Chris B.; de Silva, Shanaka L.; Bindeman, Ilya N.; Cas, Raymond A.F. (July 2013). "Tectonic and climate history influence the geochemistry of large-volume silicic magmas: New δ18O data from the Central Andes with comparison to N America and Kamchatka". Journal of Volcanology and Geothermal Research. 262: 90–103. Bibcode:2013JVGR..262...90F. doi:10.1016/j.jvolgeores.2013.05.014.
  21. ^ Breitkreuz, Christoph; de Silva, Shanaka L.; Wilke, Hans G.; Pfänder, Jörg A.; Renno, Axel D. (January 2014). "Neogene to Quaternary ash deposits in the Coastal Cordillera in northern Chile: Distal ashes from supereruptions in the Central Andes". Journal of Volcanology and Geothermal Research. 269: 68–82. Bibcode:2014JVGR..269...68B. doi:10.1016/j.jvolgeores.2013.11.001.
  22. ^ Ort, Michael H.; de Silva, Shanaka L.; Jiménez C., Néstor; Jicha, Brian R.; Singer, Bradley S. (January 2013). "Correlation of ignimbrites using characteristic remanent magnetization and anisotropy of magnetic susceptibility, Central Andes, Bolivia". Geochemistry, Geophysics, Geosystems. 14 (1): 141–157. Bibcode:2013GGG....14..141O. doi:10.1029/2012GC004276.
  23. ^ de Silva, S.L.; Francis, P.W. (May 1989). "Correlation of large ignimbrites — Two case studies from the Central Andes of northern Chile". Journal of Volcanology and Geothermal Research. 37 (2): 133–149. Bibcode:1989JVGR...37..133D. doi:10.1016/0377-0273(89)90066-8.
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