Cerro Panizos

From Wikipedia, the free encyclopedia
Cerro Panizos
An image of the Cerro Panizos ignimbrite shield
The lava domes in the centre of the image form the Panizos centre
Geography
Parent rangeCordillera de Lípez
Geology
Volcanic arc/beltAltiplano-Puna volcanic complex
Last eruption6.1 mya

Coordinates: 22°15′S 66°45′W / 22.250°S 66.750°W / -22.250; -66.750[1] Panizos is a Late Miocene caldera in the Potosí Department of Bolivia and the Jujuy Province of Argentina. It is part of the Altiplano-Puna volcanic complex of the Central Volcanic Zone in the Andes. 50 volcanoes active in recent times are found in the Central Volcanic Zone, and several major caldera complexes are situated in the area. The caldera is located in a logistically difficult area of the Andes.

Panizos and the majority of these volcanoes are formed by the subduction of the oceanic Nazca Plate under the continental South American continental lithosphere. The caldera is located east of the main arc and is supplied chiefly by dacite magmas. Beneath Panizos lie Tertiary ignimbrites and a Paleozoic sedimentary basement.

The huge Panizos ignimbrite erupted by Cerro Panizos has a minimum volume of 950 cubic kilometres (230 cu mi). It erupted during an event 6.71 ± 0.04 mya and was preceded by another ignimbrite 7.9 mya ago. The last activity is a lava flow 6.1 mya ago.

The caldera is hidden beneath a shield with a diameter of 40 kilometres (25 mi) and some of its central summits are over 5,000 metres (16,000 ft) high. It has been referred to as an "ignimbrite shield".

Geography and structure[]

The centre is located on the border between Argentina and Bolivia.[2] It is a shield constructed from ignimbrites.[3] Research in this region of the Andes is made difficult by physical and logistics issues.[4] Cerro Guacha and La Pacana are among the few systems that were the subject of research.[5] The Panizos ignimbrite is well exposed with little modification.[6]

Cerro Panizos is part of the Central Volcanic Zone (CVZ) of the Andes, a belt of recent volcanism that runs from southern Peru into Chile and Argentina. 50 volcanoes in the belt have been identified as active in recent times. A major ignimbrite province called the Altiplano-Puna volcanic complex is associated with the area between 21° and 24° degrees southern latitude since 23 million years ago. Cerro Guacha, La Pacana and Pastos Grandes are calderas within this province which covers a surface of 50,000 cubic kilometres (12,000 cu mi), with geothermal manifestations in El Tatio and Sol de Manana being the latest manifestations of volcanism in the area.[4][7]

A group of lava domes with a diameter of 10–15 kilometres (6.2–9.3 mi) of dacitic composition forms the centre of the complex, with the domes having formed either during one single eruption or several. These domes form a ring structure with thin lava cover in its centre, which may be the rim of a collapse caldera formed in the later stages of the main Panizos eruption and filled by later eruption stages,[1] as suggested by the outward dip of the lower unit of the Panizos Ignimbrite. This caldera has a diameter of 15 kilometres (9.3 mi).[6] The centre is surrounded a shield with a diameter of 40 kilometres (25 mi). It is constructed from ignimbrites with a slope of 1–3°. Three lava platforms with the names Cerro Chinchinjaran, Cerro Tucunquis and Cerro Anta Quevas are present. The first and the last are part of a dacitic flowfield that includes a 10 kilometres (6.2 mi) long lava flow on its northern sector with some resemblance to pahoehoe lava. A pre-caldera lava structure in the south of the complex is known as Cerro Limitayoc, but it erupted lavas even after the Panizos ignimbrite was erupted. A depression is located just south of the lava dome group and may be a downsag caldera, likewise infilled by activity.[1] The Panizos complex covers an area of 7,000 square kilometres (2,700 sq mi) and has a total volume of 2,520 cubic kilometres (600 cu mi).[8] The structure of the Panizos complex has been called an "ignimbrite shield".[9] The central summits Limitayoc, Panizos, La Ramada and Vicuñahuasi are over 5,000 metres (16,000 ft) high.[10]

Geology[]

The volcanism in the area is triggered by the subduction of the Nazca plate beneath the South America plate; magmas formed from the subduction process trigger the melting of the crust.[4] The large calderas are located east of the main volcanic arc of the Central Volcanic Zone,[11] Panizos being 150 kilometres (93 mi) east of the main arc.[10] Volcanism in the area is heavily dominated by calderic silicic volcanics with volumes of 6,000 cubic kilometres (1,400 cu mi) contrasting to less than 1,000 cubic kilometres (240 cu mi) andesites.[7]

The volcano is part of the so-called Tin belt, a territory in the Andes where large tin mineral deposits are found in granitic and extrusive rocks,[2] formed from sulfidation reactions involving the numerous volcanoes in the area.[12] Magmas in the territory are derived from crystal fractionation and were heavily modified by interactions with the crust that reaches a thickness of 70 kilometres (43 mi) beneath the Central Volcanic Zone.[2]

Research by S. L. de Silva indicates that before 10 mya volcanic activity already existed north of 20°30' in form of the Oxaya and Altos de Pica ignimbrites. Changes in the subduction activity 12-10 mya caused a shortening and thickening of the crust in the central Andes and the formation of melt zones in the deeper crust, associated with the Quechua phase of Andean orogeny. Since 10.6 mya these rose to the surface, forming magma chambers and calderas.[4][7] The eruptions of the Panizos ignimbrites coincide with major pulses in APVC activity.[5]

Local[]

The basement beneath Panizos is formed from two formations, Acoite and Peña Colorada. The former is a sedimentary layer, formed during arc development in the Paleozoic. The latter is Tertiary volcanic in origin, containing breccia, debris flow material, ignimbrites, lava flows and sandstone. The basement dips westward.[1] Based on neodymium isotope ratios, some of the basement rocks are about one billion years old.[2]

The volcano is part of a group with other volcanoes of the region. In this region, arc and back-arc volcanism occur in the same area and have generated some of the largest calderas in the world. These include Cerro Guacha, Pastos Grandes and Vilama.[13] A meridional lineament of volcanoes including Limitayoc and Salle extends from the southern and western margin of the central lava domes to Cerro Pululu in the south. Another lineament may form the eastern rim of the lava dome complex.[1] Other centres in the south are the Rose, Salle and West Zapaleri ignimbrites as well as the dacites of Cerro Bayo, all erupted 8.9–5.1 mya from the Vilama caldera.[14] Cerro Panizos is associated with a large-scale topographic anomaly, similar to many other volcanic centres in the region.[15]

Geologic record[]

According to Turner (1978), the ignimbrites are part of the Lipiyoc formation and the lava dome structures of the Vicuñahuasi formation. The Panizos eruption products display strong local variations, with features at different depths and different distances from the central dome complex being very dissimilar.[1]

The Cerro Corutu centre southwest of Panizos was active in the Miocene, forming an ignimbrite layer, whose exposure in the Quebrada Queñoal valley is 40 metres (130 ft) thick. It contains biotite, orthopyroxene, plagioclase and smaller amounts of quartz. Another tuff is found in Quebrada Cusi Cusi. Above these lies an eastward sloping layer of volcaniclastic material.[1] The area covered by the Panizos products had been subject to earlier eruptive activity from unknown centres between 15.4–13.4 mya, generating tuffs recognized in the San Pablo de Lípez region as outcrops.[16]

Changes in the subduction geometry since the late Miocene have caused volcanism to diminish from east to west, including cessation of activity at the Panizos centre.[14] Uturuncu volcano was last active 271,000 years ago and the Cerro Chascon-Runtu Jarita complex 85,000 years ago.[12]

Composition[]

With the exception of some andesitic products, mostly lava flows, dacite is the main component of Panizos eruptive products.[2] The rock matrix and clasts in the rock have similar minerals. Plagioclase is the main component of the lower cooling unit. Vesicles are rare in the Panizos ignimbrite, forming no more than 25%. Calling it "densely welded" is difficult at percentages of more than 10%. Pumice is also found, chemically it contains biotite, plagioclase, quartz and some orthopyroxene. In the lower units, tonalite and ilmenite are also found.[1] The Cienago and Cusi Cusi ignimbrites both contain biotite, quartz, plagioclase and Cusi Cusi also sanidine.[17]

The ignimbrites of Panizos are alumina- and potassium-rich and contain 61–66% SiO2. The Cienago ignimbrite has by one study the largest amount of SiO2 of all magmas of Panizos,[2] whereas another indicates that the Cusi Cusi ignimbrite has the highest with 69%. The Cienago ignimbrites would have 63–65% and the Panizos ones 61–66%.[17] Isotope analysis indicates high 87
Sr/86
Sr ratios and high Ba/Ta and La/Ta ratios. These are associated with arc volcanism, unlike the much lower ratios found at Galan which are typical for intraplate volcanism.[18] Along with the neodymium isotope ratios this suggests that Panizos magmas have a strong crustal component.[2] Lead isotope ratios are comparable with these of Galan and La Pacana and are linked to the domain of the crust they are constructed on.[19]

There are some compositional variations in various stages of volcanism at Cerro Panizos. The Cienago ignimbrite is a highly evolved magma. Magmas from the Panizos ignimbrite display only weak variations that may be linked to temperature differences in the magma chamber. The magmas of the Panizos ignimbrite underwent strong crystallization between eruptions and crystals are often heavily modified. The formation of all magmas was initiated by the interaction of mafic mantle melts with the crust.[2] The mantle component is up to 50% of the main Panizos ignimbrite.[19]

A notable feature of Cerro Panizos is the presence of so-called orbs, which are rocks with concentric layers of igneous material surrounding them.[20] They are known from plutonic rocks, but orbs in erupted magmas are only known from Akagi volcano, Japan. In Panizos they are found in the upper part of the lower cooling unit of the Cerro Panizos ignimbrite and are associated with pumice and megacrysts in the surrounding rock. Buried within the ignimbrites and lavas, some orbs contain layers of biotite, bronzite, ilmenite and plagioclase around a centimetre-sized xenolith or orthopyroxene core. The layering is not disturbed by irregular shapes of the cores. These orbs most likely formed from material crystallizing around pre-existent cores during rapid changes in magma temperature that occurred shortly before the end of the first phase of the Cerro Panizos eruption through changes in magma water content. Opening of ring vents then delivered the orb-containing magma to the surface.[20]

Climate and hydrography[]

Panizos has an arid climate, although some stream erosion is visible. Some stream valleys are known, clockwise from northeast, as Quebrada Buenos Aires, Quebrada Cienago, Quebrada Paicone Quebrada Pupusayo, Quebrada Cusi Cusi, Quebrada Cuevas and Quebrada Garcia.[1] The dissection is particularly pronounced on the Argentine side of the complex.[10]

Oxygen isotopic analysis of magmas from other APVC centres support the notion that the area of the APVC has been subject to arid climate for the duration of its active phase.[21]

Eruptive history[]

Two ignimbrite eruptions have taken place in Panizos.[2] A number of lava flows also formed.[22] Volcanic activity took place in the Late Miocene.[1] The main Cerro Panizos ignimbrite lies on top three older ignimbrite layers.[1] Potassium-argon dating has yielded ages of 9.7 ± 0.4, 8.49 ± 0.2 and 9.4 mya. Dates often differ between newly established and old established dates, presumably due to xenolith contamination.[1]

The Cusi Cusi tuff is 12.4 mya old[1] or more than 10 million years old and has been associated with the Panizos centre.[17] The first recorded ignimbrite in the area is named Quebrada Cienago ignimbrite after the valley where it is exposed. It contains biotite quartz dacite and is formed from four units, two ashfall deposits and two ignimbrite flows. Some of these have undergone reworking. It was emplaced 7.9 mya.[1] After the emplacement of the Cienago ignimbrite, eruption of dacite lava flows continued.[20]

Erupted 6.71 ± 0.04 mya,[23] the Panizos ignimbrite proper is a complex structure with several cooling units and an interlayered pyroclastic deposit, which contains pumice, sandstone boulders up to two metres thick and has carved channels into the lower unit. At the edge of the plateau the upper and lower cooling units are 0–50 metres (0–164 ft) and 160 metres (520 ft) thick. In the plateau centre, the lower unit is completely hidden beneath the now more than 100 metres (330 ft) thick upper unit. The lower unit begins with one metre of lapilli and above it thick ignimbrite layers that become increasingly non-welded farther up with vapour phase components appearing.[1] There was no prior Plinian fallout.[24] Orbs and two differently coloured pumices are located in the upper section of the lower unit, with some xenoliths. The upper cooling unit contains two types of pumice, one strongly welded and the other weakly so, and is much richer in lithic fragments. The upper unit was erupted in several discrete flows from the central complex. Some pumice fall layers are embedded in the upper unit.[1]

Based on the structure, the main Panizos ignimbrite was probably erupted in a steady eruption at first, from either one vent or several smaller ones in close association. Either a column collapse or a change in vent geometries triggered a temporary pause which separates the upper and lower cooling units. After a short timespan, the eruption restarted, this time through several eruption flows and a more unsteady regimen with a lower flow rate. Based on welding patterns, the eruption commenced in the southern sector later covered by lava domes and migrated northward. Calculations indicate that the main Panizos ignimbrite has minimum volumina of 950 cubic kilometres (230 cu mi) outside of the calderas and 652 cubic kilometres (156 cu mi) dense rock equivalent. This ignimbrite flow was of comparatively low fluidity,[1] likely due to its high crystal content.[25] The amount of vesicles present in the lower cooling unit is inferior to 20% of volume.[26]

Above the Panizos ignimbrite, a lava flow platform and a set of lava domes were emplaced. A last manifestation is the Cerro La Ramada lava flow, with an age of 6.1 mya.[1] A tephra layer found in the Coastal Cordillera and dated 6.66 ± 0.13 mya may also be linked to the Panizos complex.[27] The much younger (1.9±0.2–1.7±0.5 mya) Laguna Colorada ignimbrite is sometimes called Panizos, generating confusion.[28]

See also[]

References[]

  1. ^ a b c d e f g h i j k l m n o p q r Ort, Michael H. (June 1993). "Eruptive processes and caldera formation in a nested downsagcollapse caldera: Cerro Panizos, central Andes Mountains". Journal of Volcanology and Geothermal Research. 56 (3): 221–252. Bibcode:1993JVGR...56..221O. doi:10.1016/0377-0273(93)90018-M.
  2. ^ a b c d e f g h i Ort, Michael H.; Coira, Beatriz L.; Mazzoni, Mario M. (15 April 1996). "Generation of a crust-mantle magma mixture: magma sources and contamination at Cerro Panizos, central Andes". Contributions to Mineralogy and Petrology. 123 (3): 308–322. Bibcode:1996CoMP..123..308O. doi:10.1007/s004100050158. S2CID 140723693.
  3. ^ Troise, Claudia; de Natale, Giuseppe; Kilburn, Christopher R. J. (2006). Mechanisms of activity and unrest at large calderas. London: Geological Society. p. 54. ISBN 978-1-86239-211-3. Retrieved 2 December 2015.
  4. ^ a b c d 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, 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.
  6. ^ a b Lipman, Peter W. (8 December 1997). "Subsidence of ash-flow calderas: relation to caldera size and magma-chamber geometry". Bulletin of Volcanology. 59 (3): 198–218. Bibcode:1997BVol...59..198L. doi:10.1007/s004450050186. S2CID 44012497.
  7. ^ a b c de Silva, S.L. (May 1989). "Geochronology and stratigraphy of the ignimbrites from the 21°30′S to 23°30′S portion of the Central Andes of northern Chile". Journal of Volcanology and Geothermal Research. 37 (2): 93–131. doi:10.1016/0377-0273(89)90065-6.
  8. ^ Francis, P. W.; Hawkesworth, C. J. (1 October 1994). "Late Cenozoic rates of magmatic activity in the Central Andes and their relationships to continental crust formation and thickening". Journal of the Geological Society. 151 (5): 845–854. Bibcode:1994JGSoc.151..845F. doi:10.1144/gsjgs.151.5.0845. S2CID 129179678. Retrieved 3 December 2015.
  9. ^ 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 3 December 2015.
  10. ^ a b c Ort, M.; Coira, B.; Mazzoni, M.; Fisher, R.V.; Merodio, J.C. (1989). "CENTRO EMISOR VOLCANICO CERRO PANIZOS, JUJUY". Informacion Tecnologica (in Spanish): 291–300. ISSN 0716-8756. Retrieved 21 December 2015.
  11. ^ Leyrit; Montenat, Christian (2000). Volcaniclastic rocks, from magmas to sediments : [Pierre Bordet (1914–1996) in memoriam]. Amsterdam [u.a.]: Gordon and Breach Science Publ. ISBN 978-90-5699-278-1. Retrieved 2 December 2015.
  12. ^ a b Deroin, Jean-Paul; Téreygeol, Florian; Cruz, Pablo; Guillot, Ivan; Méaudre, Jean-Charles (1 August 2012). "Integrated non-invasive remote-sensing techniques and field survey for the geoarchaeological study of the Sud Lípez mining district, Bolivia". Journal of Geophysics and Engineering. 9 (4): S40–S52. Bibcode:2012JGE.....9S..40D. doi:10.1088/1742-2132/9/4/S40.
  13. ^ España, 6th International symposium on Andean geodynamics, Universitat de Barcelona, 12–14 septembre 2005 ; organisateurs, Institut de recherche pour le développement, Universitat de Barcelona, Instituto geológico y minero de (2005). Géodynamique andine : résumés étendus. Paris: Institut de recherche pour le développement. p. 414. ISBN 978-2-7099-1575-5. Retrieved 2 December 2015.
  14. ^ a b Coira, B.; Kay, S. Mahlburg; Viramonte, J. (August 1993). "Upper Cenozoic Magmatic Evolution of The Argentine Puna—A Model for Changing Subduction Geometry". International Geology Review. 35 (8): 677–720. Bibcode:1993IGRv...35..677C. doi:10.1080/00206819309465552.
  15. ^ Perkins, Jonathan P.; Finnegan, Noah J.; Henderson, Scott T.; Rittenour, Tammy M. (16 June 2016). "Topographic constraints on magma accumulation below the actively uplifting Uturuncu and Lazufre volcanic centers in the Central Andes". Geosphere. 12 (4): 1078. Bibcode:2016Geosp..12.1078P. doi:10.1130/GES01278.1. ISSN 1553-040X.
  16. ^ Jiménez, Néstor; López-Velásquez, Shirley (November 2008). "Magmatism in the Huarina belt, Bolivia, and its geotectonic implications". Tectonophysics. 459 (1–4): 85–106. Bibcode:2008Tectp.459...85J. doi:10.1016/j.tecto.2007.10.012.
  17. ^ a b c 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. ^ Hedenquist, J. W.; Ramos, Víctor A. (1998). "Cordillera de Los Andes, Geological and Mining Potential : the New Tectonic Approach". Mendoza: GRK Servicios Mineros. pp. 31–32. Retrieved 2 December 2015.
  19. ^ a b Lindsay, J. M. (1 March 2001). "Magmatic Evolution of the La Pacana Caldera System, Central Andes, Chile: Compositional Variation of Two Cogenetic, Large-Volume Felsic Ignimbrites". Journal of Petrology. 42 (3): 459–486. doi:10.1093/petrology/42.3.459.
  20. ^ a b c Ort, Michael H. (August 1992). "Orbicular volcanic rocks of Cerro Panizos: Their origin and implications for orb formation". Geological Society of America Bulletin. 104 (8): 1048–1058. Bibcode:1992GSAB..104.1048O. doi:10.1130/0016-7606(1992)104<1048:OVROCP>2.3.CO;2.
  21. ^ 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.
  22. ^ Schweizerbart, E. (1996). Zentralblatt für Mineralogie (3–4 ed.). p. 1311. Retrieved 2 December 2015.
  23. ^ Soler, M.M.; Caffe, P.J; Coira, B.L.; Onoe, A.T.; Kay, S. Mahlburg (July 2007). "Geology of the Vilama caldera: A new interpretation of a large-scale explosive event in the Central Andean plateau during the Upper Miocene". Journal of Volcanology and Geothermal Research. 164 (1–2): 27–53. Bibcode:2007JVGR..164...27S. doi:10.1016/j.jvolgeores.2007.04.002.
  24. ^ Cas, Ray A. F.; Wright, Heather M. N.; Folkes, Christopher B.; Lesti, Chiara; Porreca, Massimiliano; Giordano, Guido; Viramonte, Jose G. (16 November 2011). "The flow dynamics of an extremely large volume pyroclastic flow, the 2.08-Ma Cerro Galán Ignimbrite, NW Argentina, and comparison with other flow types". Bulletin of Volcanology. 73 (10): 1583–1609. Bibcode:2011BVol...73.1583C. doi:10.1007/s00445-011-0564-y. S2CID 129502026.
  25. ^ 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". Geological Society of America Bulletin. 123 (5–6): 821–840. doi:10.1130/B30280.1.
  26. ^ Gottsmann, J.; Lavallée, Y.; Martí, J.; Aguirre-Díaz, G. (July 2009). "Magma–tectonic interaction and the eruption of silicic batholiths". Earth and Planetary Science Letters. 284 (3–4): 426–434. Bibcode:2009E&PSL.284..426G. doi:10.1016/j.epsl.2009.05.008.
  27. ^ 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.
  28. ^ 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". Geological Society of America Bulletin. 123 (5–6): 821–840. doi:10.1130/B30280.1.

Additional sources[]


Retrieved from ""