Andesite

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For the extinct cephalopod genus, see Andesites.
Andesite
Igneous rock
Amygdaloidal andesite.jpg
A sample of andesite (dark groundmass) with amygdaloidal vesicles filled with zeolite. Diameter of view is 8 cm.
Composition
PrimaryIntermediate: plagioclase (often andesine) and pyroxene or hornblende
SecondaryMagnetites, biotite, sphene, and quartz

Andesite (/ˈæn.dɪˌzaɪt, -də-/)[1][2][3][4] is an extrusive volcanic rock of intermediate composition. In a general sense, it is the intermediate type between basalt and rhyolite. It is fine-grained (aphanitic) to porphyritic in texture, and is composed predominantly of sodium-rich plagioclase plus pyroxene or hornblende.[5]

Andesite is the extrusive equivalent of plutonic diorite. Characteristic of subduction zones, andesite represents the dominant rock type in island arcs. The average composition of the continental crust is andesitic.[6] Along with basalts, they are a major component of the Martian crust.[7]

The name andesite is derived from the Andes mountain range, where this rock type is found in abundance.

Description[]

QAPF diagram with basalt/andesite field highlighted in yellow. Andesite is distinguished from basalt by SiO2 > 52%.
Andesite is field O2 in the TAS classification.
Photomicrograph of andesite in thin section (between crossed polars)
Andesite Mount Žarnov (Vtáčnik), Slovakia
Andesite pillar in Slovakia

Andesite is an aphanitic (fine-grained) igneous rock that is intermediate in its content of silica and low in alkali metals. It has less than 20% quartz and 10% feldspathoid by volume, with at least 65% of the feldspar in the rock consisting of plagioclase. This places andesite in the basalt/andesite field of the QAPF diagram. Andesite is further distinguished from basalt by its silica content of over 52%.[8][9][10][11] However, it is often not possible to determine the mineral composition of volcanic rocks, due to their very fine grain size, and andesite is then defined chemically as volcanic rock with a content of 57% to 63% silica and not more than about 6% alkali metal oxides. This places andesite in the O2 field of the TAS classification. Basaltic andesite, with a content of 52% to 57% silica, is represented by the O1 field of the TAS classification but is not a recognized type in the QAPF classification.[11]

Andesite is usually light to dark gray in colour, due to its content of hornblende or pyroxene minerals.[5] but can exhibit a wide range of shading. Darker andesite can be difficult to distinguish from basalt, but a common rule of thumb, used away from the laboratory, is that andesite has a color index less than 35.[12]

The plagioclase in andesite varies widely in sodium content, from anorthite to oligoclase, but is typically andesine. The pyroxene minerals that may be present include augite, pigeonite, or orthopyroxene. Magnetite, zircon, apatite, ilmenite, biotite, and garnet are common accessory minerals.[13] Alkali feldspar may be present in minor amounts. Classification of andesites may be refined according to the most abundant phenocryst. Example: hornblende-phyric andesite, if hornblende is the principal accessory mineral.

Andesite is usually porphyritic, containing larger crystals (phenocrysts) of plagioclase formed prior to the extrusion that brought the magma to the surface, embedded in a finer-grained matrix. Phenocrysts of pyroxene or hornblende are also common.[14] These minerals have the highest melting temperatures of the typical minerals that can crystallize from the melt[15] and are therefore the first to form solid crystals.

Generation of melts in island arcs[]

Andesite is typically formed at convergent plate margins but may also occur in other tectonic settings. Magmatism in island arc regions comes from the interplay of the subducting plate and the mantle wedge, the wedge-shaped region between the subducting and overriding plates.

During subduction, the subducted oceanic crust is subjected to increasing pressure and temperature, leading to metamorphism. Hydrous minerals such as amphibole, zeolites, chlorite etc. (which are present in the oceanic lithosphere) dehydrate as they change to more stable, anhydrous forms, releasing water and soluble elements into the overlying wedge of mantle. Fluxing water into the wedge lowers the solidus of the mantle material and causes partial melting.[16] Due to the lower density of the partially molten material, it rises through the wedge until it reaches the lower boundary of the overriding plate. Melts generated in the mantle wedge are of basaltic composition, but they have a distinctive enrichment of soluble elements (e.g. potassium (K), barium (Ba), and lead (Pb)) which are contributed from sediment that lies at the top of the subducting plate. Although there is evidence to suggest that the subducting oceanic crust may also melt during this process, the relative contribution of the three components (crust, sediment, and wedge) to the generated basalts is still a matter of debate.[17]

Basalt thus formed can contribute to the formation of andesite through fractional crystallization, partial melting of crust, or magma mixing, all of which are discussed next.

Genesis of andesite[]

Intermediate volcanic rocks are created via several processes:

  1. Fractional crystallization of a mafic parent magma.
  2. Partial melting of crustal material.
  3. Magma mixing between felsic rhyolitic and mafic basaltic magmas in a magma reservoir
  4. Partial melting of metasomatized mantle

Fractional crystallization[]

To achieve andesitic composition via fractional crystallization, a basaltic magma must crystallize specific minerals that are then removed from the melt. This removal can take place in a variety of ways, but most commonly this occurs by crystal settling. The first minerals to crystallize and be removed from a basaltic parent are olivines and amphiboles. These mafic minerals settle out of the magma, forming mafic cumulates. There is geophysical evidence from several arcs that large layers of mafic cumulates lie at the base of the crust. Once these mafic minerals have been removed, the melt no longer has a basaltic composition. The silica content of the residual melt is enriched relative to the starting composition. The iron and magnesium contents are depleted. As this process continues, the melt becomes more and more evolved eventually becoming andesitic. Without continued addition of mafic material, however, the melt will eventually reach a rhyolitic composition.

Partial melting of the crust[]

Partially molten basalt in the mantle wedge moves upwards until it reaches the base of the overriding crust. Once there, the basaltic melt can either underplate the crust, creating a layer of molten material at its base, or it can move into the overriding plate in the form of dykes. If it underplates the crust, the basalt can (in theory) cause partial melting of the lower crust due to the transfer of heat and volatiles. Models of heat transfer, however, show that arc basalts emplaced at temperatures 1100–1240 °C cannot provide enough heat to melt lower crustal amphibolite.[18] Basalt can, however, melt pelitic upper crustal material.[19] Andesitic magmas generated in island arcs, therefore, are probably the result of partial melting of the crust.

Magma mixing[]

In continental arcs, such as the Andes, magma often pools in the shallow crust creating magma chambers. Magmas in these reservoirs become evolved in composition (dacitic to rhyolitic) through both the process of fractional crystallization and partial melting of the surrounding country rock.[20] Over time as crystallization continues and the system loses heat, these reservoirs cool. In order to remain active, magma chambers must have continued recharge of hot basaltic melt into the system. When this basaltic material mixes with the evolved rhyolitic magma, the composition is returned to andesite, its intermediate phase.[21]

Partial melting of metasomatized mantle[]

High-magnesium andesites in island arcs may be primitive andesites, generated from metasomatized mantle.[22] [23] Experimental evidence shows that depleted mantle rock exposed to alkali fluids such as might be given off by a subducting slab generates magma resembling high-magnesium andesites.[24][25]

Andesite in space[]

In 2009, researchers revealed that andesite was found in two meteorites (numbered GRA 06128 and GRA 06129) that were discovered in the Graves Nunataks icefield during the US Antarctic Search for Meteorites 2006/2007 field season. This possibly points to a new mechanism to generate andesite crust.[26]

See also[]

  • Andesite line
  • List of rock types – List of rock types recognized by geologists
  • Metamorphism – Change of minerals in pre-existing rocks without melting into liquid magma
  • Oceanic crust – Uppermost layer of the oceanic portion of a tectonic plate
  • Origins of granite – common type of intrusive, felsic, igneous rock with granular structure
  • Porphyry – Textural form of igneous rock with large grained crystals in a fine matrix

References[]

  1. ^ "andesite". Merriam-Webster Dictionary.
  2. ^ "andesite". CollinsDictionary.com. HarperCollins.
  3. ^ "andesite". The American Heritage Dictionary of the English Language (5th ed.). Boston: Houghton Mifflin Harcourt.
  4. ^ "andesite". Dictionary.com Unabridged. Random House.
  5. ^ Jump up to: a b Macdonald, Gordon A.; Abbott, Agatin T.; Peterson, frank L. (1983). Volcanoes in the sea : the geology of Hawaii (2nd ed.). Honolulu: University of Hawaii Press. p. 127. ISBN 0824808320.
  6. ^ Rudnick, Roberta L.; Fountain, David M. (1995). "Nature and composition of the continental crust: A lower crustal perspective". Reviews of Geophysics. 33 (3): 267–309. Bibcode:1995RvGeo..33..267R. doi:10.1029/95RG01302.
  7. ^ Cousins, Claire R.; Crawford, Ian A. (2011). "Volcano–Ice Interaction as a Microbial Habitat on Earth and Mars" (PDF). Astrobiology. 11 (7): 695–710. Bibcode:2011AsBio..11..695C. doi:10.1089/ast.2010.0550. hdl:10023/8744. PMID 21877914.
  8. ^ Le Bas, M. J.; Streckeisen, A. L. (1991). "The IUGS systematics of igneous rocks". Journal of the Geological Society. 148 (5): 825–833. Bibcode:1991JGSoc.148..825L. CiteSeerX 10.1.1.692.4446. doi:10.1144/gsjgs.148.5.0825. S2CID 28548230.
  9. ^ "Rock Classification Scheme - Vol 1 - Igneous" (PDF). British Geological Survey: Rock Classification Scheme. 1: 1–52. 1999.
  10. ^ "CLASSIFICATION OF IGNEOUS ROCKS". Archived from the original on 30 September 2011.
  11. ^ Jump up to: a b Philpotts, Anthony R.; Ague, Jay J. (2009). Principles of igneous and metamorphic petrology (2nd ed.). Cambridge, UK: Cambridge University Press. pp. 139–143. ISBN 9780521880060.
  12. ^ Philpotts and Ague 2009, p. 139
  13. ^ Blatt, Harvey; Tracy, Robert J. (1996). Petrology : igneous, sedimentary, and metamorphic (2nd ed.). New York: W.H. Freeman. p. 57. ISBN 0-7167-2438-3.
  14. ^ Blatt and Tracy 1996, p.57
  15. ^ Tilley, C. E. (1957). "Norman Levi Bowen 1887-1956". Biographical Memoirs of Fellows of the Royal Society. 3: 6–26. doi:10.1098/rsbm.1957.0002. JSTOR 769349. S2CID 73262622.
  16. ^ Tatsumi, Y. (1995). Subduction Zone Magmatism. Oxford: Blackwell Scientific.[page needed]
  17. ^ Eiler, J.M. (2003). Inside the Subduction Factory. San Francisco: AGU Geophysical Monograph 138.[page needed]
  18. ^ Petford, Nick; Gallagher, Kerry (2001). "Partial melting of mafic (amphibolitic) lower crust by periodic influx of basaltic magma". Earth and Planetary Science Letters. 193 (3–4): 483–99. Bibcode:2001E&PSL.193..483P. doi:10.1016/S0012-821X(01)00481-2.
  19. ^ Annen, C.; Sparks, R.S.J. (2002). "Effects of repetitive emplacement of basaltic intrusions on thermal evolution and melt generation in the crust". Earth and Planetary Science Letters. 203 (3–4): 937–55. Bibcode:2002E&PSL.203..937A. doi:10.1016/S0012-821X(02)00929-9.
  20. ^ Troll, Valentin R.; Deegan, Frances M.; Jolis, Ester M.; Harris, Chris; Chadwick, Jane P.; Gertisser, Ralf; Schwarzkopf, Lothar M.; Borisova, Anastassia Y.; Bindeman, Ilya N.; Sumarti, Sri; Preece, Katie (2013-07-01). "Magmatic differentiation processes at Merapi Volcano: inclusion petrology and oxygen isotopes". Journal of Volcanology and Geothermal Research. Merapi eruption. 261: 38–49. Bibcode:2013JVGR..261...38T. doi:10.1016/j.jvolgeores.2012.11.001. ISSN 0377-0273.
  21. ^ Reubi, Olivier; Blundy, Jon (2009). "A dearth of intermediate melts at subduction zone volcanoes and the petrogenesis of arc andesites". Nature. 461 (7268): 1269–1273. Bibcode:2009Natur.461.1269R. doi:10.1038/nature08510. PMID 19865169. S2CID 4417505.
  22. ^ Kelemen, P.B., Hanghøj, K., and Greene, A.R. "One View of the Geochemistry of Subduction-Related Magmatic Arcs, with an Emphasis on Primitive Andesite and Lower Crust." In Treatise on Geochemistry, Volume 3. Editor: Roberta L. Rudnick. Executive Editors: Heinrich D. Holland and Karl K. Turekian. pp. 659. ISBN 0-08-043751-6. Elsevier, 2003., p.593-659
  23. ^ Beier, Christoph; Haase, Karsten M.; Brandl, Philipp A.; Krumm, Stefan H. (11 April 2017). "Primitive andesites from the Taupo Volcanic Zone formed by magma mixing". Contributions to Mineralogy and Petrology. 172 (5): 33. Bibcode:2017CoMP..172...33B. doi:10.1007/s00410-017-1354-0. S2CID 133574938.
  24. ^ Wood, Bernard J.; Turner, Simon P. (June 2009). "Origin of primitive high-Mg andesite: Constraints from natural examples and experiments". Earth and Planetary Science Letters. 283 (1–4): 59–66. Bibcode:2009E&PSL.283...59W. doi:10.1016/j.epsl.2009.03.032.
  25. ^ Mitchell, Alexandra L.; Grove, Timothy L. (23 November 2015). "Erratum to: Melting the hydrous, subarc mantle: the origin of primitive andesites". Contributions to Mineralogy and Petrology. 170 (5–6). doi:10.1007/s00410-015-1204-x.
  26. ^ Day, James M. D.; Ash, Richard D.; Liu, Yang; Bellucci, Jeremy J.; Rumble, Douglas; McDonough, William F.; Walker, Richard J.; Taylor, Lawrence A. (2009). "Early formation of evolved asteroidal crust". Nature. 457 (7226): 179–82. Bibcode:2009Natur.457..179D. doi:10.1038/nature07651. PMID 19129845. S2CID 4364956. Lay summary – Newswise (January 7, 2009).

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