Gabbro

Gabbro (/ˈɡæb.roʊ/) is a phaneritic (coarse-grained), mafic intrusive igneous rock formed from the slow cooling of magnesium-rich and iron-rich magma into a holocrystalline mass deep beneath the Earth's surface. Slow-cooling, coarse-grained gabbro is chemically equivalent to rapid-cooling, fine-grained basalt. Much of the Earth's oceanic crust is made of gabbro, formed at mid-ocean ridges. Gabbro is also found as plutons associated with continental volcanism. Due to its variant nature, the term gabbro may be applied loosely to a wide range of intrusive rocks, many of which are merely "gabbroic". By rough analogy, gabbro is to basalt as granite is to rhyolite.

Gabbro specimen
Photomicrograph of a thin section of gabbro

Etymology

The term "gabbro" was used in the 1760s to name a set of rock types that were found in the ophiolites of the Apennine Mountains in Italy.[1] It was named after Gabbro, a hamlet near Rosignano Marittimo in Tuscany. Then, in 1809, the German geologist Christian Leopold von Buch used the term more restrictively in his description of these Italian ophiolitic rocks.[2] He assigned the name "gabbro" to rocks that geologists nowadays would more strictly call "metagabbro" (metamorphosed gabbro).[3]

Petrology
Mineral assemblage of igneous rocks

Gabbro is a coarse-grained (phaneritic) igneous rock that is relatively low in silica and rich in iron, magnesium, and calcium. Such rock is described as mafic. Gabbro is composed of pyroxene and calcium-rich plagioclase, with minor amounts of hornblende, olivine, and accessory minerals.[4] When present, hornblende is typically found as a rim around augite crystals or as large grains enclosing smaller grains of other minerals (poikilitic grains).[5][6]

QAPF diagram with the gabbroid/dioritoid fields highlighted in yellow. Gabbroids are distinguished from dioritoids by an anorthosite content of greater than 50% of their plagioclase.
QAPF diagram with the gabbro field highlighted in yellow. Gabbro is distinguished from diorite by an anorthosite content of greater than 50% of its plagioclase and from anorthite by a mafic mineral content greater than 10%.

Geologists use rigorous quantitative definitions to classify coarse-grained igneous rocks, based on the mineral content of the rock. For igneous rocks composed mostly of silicate minerals, and in which at least 10% of the mineral content consists of quartz, feldspar, or feldspathoid minerals, classification begins with the QAPF diagram. The relative abundances of quartz (Q), alkali feldspar (A), plagioclase (P), and feldspathoid (F), are used to plot the position of the rock on the diagram.[7][8][9] The rock will be classified as either a gabbroid or a dioritoid if quartz makes up less than 20% of the QAPF content, feldspathoid makes up less than 10% of the QAPF content, and plagioclase makes up more than 65% of the total feldspar content. Gabbroids are distinguished from dioritoids by an anorthite (calcium plagioclase) fraction of their total plagioclase of greater than 50%.[10]

The composition of the plagioclase cannot easily be determined in the field, and then a preliminary distinction is made between dioritoid and gabbroid based on the content of mafic minerals. A gabbroid typically has over 35% mafic minerals, mostly pyroxenes or olivine, while a dioritoid typically has less than 35% mafic minerals, which typically includes hornblende.[11]

Gabbroids form a family of rock types similar to gabbro, such as monzogabbro, quartz gabbro, or nepheline-bearing gabbro. Gabbro itself is more narrowly defined, as a gabbroid in which quartz makes up less than 5% of the QAPF content, feldspathoids are not present, and plagioclase makes up more than 90% of the feldspar content. Gabbro is distinct from anorthosite, which contains less than 10% mafic minerals.[12][7][8]

Coarse-grained gabbroids are produced by slow crystallization of magma having the same composition as the lava that solidifies rapidly to form fine-grained (aphanitic) basalt.[7][8]

Subtypes

There are a number of subtypes of gabbro recognized by geologists. Gabbros can be broadly divided into leucogabbros, with less than 35% mafic mineral content; mesogabbros, with 35% to 65% mafic mineral content; and melagabbros with more than 65% mafic mineral content. A rock with over 90% mafic mineral content will be classified instead as an ultramafic rock. A gabbroic rock with less than 10% mafic mineral content will be classified as an anorthosite.[8][13]

A more detailed classification is based on the relative percentages of plagioclase, pyroxene, hornblende, and olivine. The end members are:[8][13]

  • Normal gabbro (gabbro sensu stricto[8]) is composed almost entirely of plagioclase and clinopyroxene (typically augite), with less than 5% each of hornblende, olivine, or orthopyroxene.
  • Norite is composed almost entirely of plagioclase and orthopyroxene, with less than 5% each of hornblende, clinopyroxene, or olivine.
  • Troctolite is composed almost entirely of plagioclase and olivine, with less than 5% each of pyroxene or hornblende.
  • Hornblende gabbro is composed almost entirely of plagioclase and hornblende, with less than 5% each of pyroxene or olivine.

Gabbros intermediate between these compositions are given names such as gabbronorite (for a gabbro intermediate between normal gabbro and norite, with almost equal amounts of clinopyroxene and orthopyroxene) or olivine gabbro (for a gabbro containing significant olivine, but almost no clinopyroxene or hornblende). A rock similar to normal gabbro but containing more orthopyroxene is called an orthopyroxene gabbro, while a rock similar to norite but containing more clinopyroxene is called a clinopyroxene norite.[8]

A gabbro landscape – the main ridge of the Cuillin, Isle of Skye, Scotland
Cizlakite sample

Gabbros are also sometimes classified as alkali or tholleiitic gabbros, by analogy with alkali or tholeiitic basalts, of which they are considered the intrusive equivalents.[14] Alkali gabbro usually contains olivine, nepheline, or analcime, up to 10% of the mineral content,[15] while tholeiitic gabbro contains both clinopyroxene and orthopyroxene, making it a gabbronorite.[14]

Gabbroids

Gabbroids (also known as gabbroic-rocks[8]) are a family of coarse-grained igneous rocks similar to gabbro:[10]

  • Quartz gabbro contains 5% to 20% quartz in its QAPF fraction. One example is the cizlakite at Pohorje in northeastern Slovenia,[16]
  • Monzogabbro contains 65% to 90% plagioclase out of its total feldspar content.
  • Quartz monzogabbro combines the features of quartz gabbro and monzogabbro. It contains 5% to 20% quartz in its QAPF fraction, and 65% to 90% of its feldspar is plagioclase.
  • Foid-bearing gabbro contains up to 10% feldspathoids rather than quartz. "Foid" in the name is usually replaced by the specific feldspathoid that is most abundant in the rock. For example, a nepheline-bearing gabbro is a foid-bearing gabbro in which the most abundant feldspathoid is nepheline.
  • Foid-bearing monzogabbro resembles monzogabbro, but containing up to 10% feldspathoids in place of quartz. The same naming conventions apply as for foid-bearing gabbro, so that a gabbroid might be classified as a leucite-bearing monzogabbro.[8]

Gabbroids contain minor amounts, typically a few percent, of iron-titanium oxides such as magnetite, ilmenite, and ulvospinel. Apatite, zircon, and biotite may also be present as accessory minerals.[6]

Gabbro is generally coarse-grained, with crystals in the size range of 1 mm or larger. Finer-grained equivalents of gabbro are called diabase (also known as dolerite), although the term microgabbro is often used when extra descriptiveness is desired. Gabbro may be extremely coarse-grained to pegmatitic.[8] Some pyroxene-plagioclase cumulates are essentially coarse-grained gabbro,[17] and may exhibit acicular crystal habits.[18]

Gabbro is usually equigranular in texture, although it may also show ophitic texture[6] (with laths of plagioclase enclosed in pyroxene[19]).

Distribution
Zuma Rock, Nigeria, a massive, nearly uniform, intrusion of gabbro and granodiorite.

Nearly all gabbros are found in plutonic bodies, and the term (as the International Union of Geological Sciences recommends) is normally restricted just to plutonic rocks, although gabbro may be found as a coarse-grained interior facies of certain thick lavas.[20][21] Gabbro can be formed as a massive, uniform intrusion via in-situ crystallisation of pyroxene and plagioclase, or as part of a layered intrusion as a cumulate formed by settling of pyroxene and plagioclase.[22] An alternative name for gabbros formed by crystal settling is pyroxene-plagioclase adcumulate.

Gabbro is much less common than more silica-rich intrusive rocks in the continental crust of the Earth. Gabbro and gabbroids occur in some batholiths but these rocks are relatively minor components of these very large intrusions because their iron and calcium content usually makes gabbro and gabbroid magmas too dense to have the necessary buoyancy.[23] However, gabbro is an essential part of the oceanic crust, and can be found in many ophiolite complexes as layered gabbro underling sheeted dike complexes and overlying ultramafic rock derived from the Earth's mantle. These layered gabbros may have formed from relatively small but long-lived magma chambers underlying mid-ocean ridges.[24]

Layered gabbros are also characteristic of lopoliths, which are large, saucer-shaped intrusions that are primarily Precambrian in age. Prominent examples of lopoliths include the Bushveld Complex of South Africa, the Muskox intrusion of the Northwest Territories of Canada, the Rum layered intrusion of Scotland, the Stillwater complex of Montana, and the layered gabbros near Stavanger, Norway.[25] Gabbros are also present in stocks associated with alkaline volcanism of continental rifting.[26]

Uses

Gabbro often contains valuable amounts of chromium, nickel, cobalt, gold, silver, platinum, and copper sulfides.[27][28][29] For example, the Merensky Reef is the world's most important source of platinum.[30]

Gabbro is known in the construction industry by the trade name of black granite.[31] However, gabbro is hard and difficult to work, which limits its use.[32]

See also
  • Peridotite – Coarse-grained ultramafic igneous rock type
  • Igneous differentiation – Geologic process in formation of some igneous rocks
  • Fractional crystallisation – Process of rock formation

References
  1. Bortolotti, V. et al. Chapter 11: Ophiolites, Ligurides and the tectonic evolution from spreading to convergence of a Mesozoic Western Tethys segment in F. Vai, G.P. and Martini, I.P. (editors) (2001) Anatomy of an Orogen: The Apennines and Adjacent Mediterranean Basins, Dordrecht, Springer Science and Business Media, p. 151. ISBN 978-90-481-4020-6
  2. Bortolotti, V. et al. Chapter 11: Ophiolites, Ligurides and the tectonic evolution from spreading to convergence of a Mesozoic Western Tethys segment in F. Vai, G.P. and Martini, I.P. (editors) (2001) Anatomy of an Orogen: The Apennines and Adjacent Mediterranean Basins, Dordrecht, Springer Science and Business Media, p. 152. ISBN 978-90-481-4020-6
  3. Gabbro at SandAtlas geology blog. Retrieved on 2015-07-09.
  4. Allaby, Michael (2013). "gabbro". A dictionary of geology and earth sciences (Fourth ed.). Oxford: Oxford University Press. ISBN 9780199653065.
  5. Jackson, Julia A., ed. (1997). "gabbro". Glossary of geology (Fourth ed.). Alexandria, Virginia: American Geological Institute. ISBN 0922152349.
  6. Blatt, Harvey; Tracy, Robert J. (1996). Petrology : igneous, sedimentary, and metamorphic (2nd ed.). New York: W.H. Freeman. p. 53. ISBN 0716724383.
  7. 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.
  8. "Rock Classification Scheme - Vol 1 - Igneous" (PDF). British Geological Survey: Rock Classification Scheme. 1: 1–52. 1999.
  9. Philpotts, Anthony R.; Ague, Jay J. (2009). Principles of igneous and metamorphic petrology (2nd ed.). Cambridge, UK: Cambridge University Press. pp. 139–143. ISBN 978-0-521-88006-0.
  10. Jackson 1997, "gabbroid".
  11. Blatt & Tracy 1996, p. 71.
  12. Jackson 1997, "gabbro".
  13. Philpotts & Ague 2009, p. 142.
  14. Allaby 2013, "gabbro".
  15. Jackson 1997, "alkali gabbro".
  16. Le Maitre, R. W.; et al., eds., 2005, Igneous Rocks: A Classification and Glossary of Terms, Cambridge Univ. Press, 2nd ed., p. 69, ISBN 9780521619486
  17. Beard, James S. (1 October 1986). "Characteristic mineralogy of arc-related cumulate gabbros: Implications for the tectonic setting of gabbroic plutons and for andesite genesis". Geology. 14 (10): 848–851. Bibcode:1986Geo....14..848B. doi:10.1130/0091-7613(1986)14<848:CMOACG>2.0.CO;2.
  18. Nicolas, Adolphe; Boudier, Françoise; Mainprice, David (April 2016). "Paragenesis of magma chamber internal wall discovered in Oman ophiolite gabbros". Terra Nova. 28 (2): 91–100. Bibcode:2016TeNov..28...91N. doi:10.1111/ter.12194. S2CID 130338632.
  19. Wager, L. R. (October 1961). "A Note on the Origin of Ophitic Texture in the Chilled Olivine Gabbro of the Skaergaard Intrusion". Geological Magazine. 98 (5): 353–366. Bibcode:1961GeoM...98..353W. doi:10.1017/S0016756800060829. S2CID 129950597.
  20. Arndt, N.T.; Naldrett, A.J.; Pyke, D.R. (1 May 1977). "Komatiitic and Iron-rich Tholeiitic Lavas of Munro Township, Northeast Ontario". Journal of Petrology. 18 (2): 319–369. doi:10.1093/petrology/18.2.319.
  21. Gill, Robin (2010). Igneous rocks and processes: a practical guide. Oxford: Wiley‐Blackwell. ISBN 978-1-4443-3065-6.
  22. Emeleus, C. H.; Troll, V. R. (August 2014). "The Rum Igneous Centre, Scotland". Mineralogical Magazine. 78 (4): 805–839. Bibcode:2014MinM...78..805E. doi:10.1180/minmag.2014.078.4.04. ISSN 0026-461X.
  23. Philpotts & Ague 2009, p. 102.
  24. Philpotts & Ague 2009, pp. 370–374.
  25. Philpotts & Ague 2009, pp. 95–99.
  26. Philpotts & Ague 2009, p. 99.
  27. Iwasaki, I.; Malicsi, A.S.; Lipp, R.J.; Walker, J.S. (August 1982). "By-product recovery from copper-nickel bearing duluth gabbro". Resources and Conservation. 9: 105–117. doi:10.1016/0166-3097(82)90066-9.
  28. Lachize, M.; Lorand, J. P.; Juteau, T. (1991). "Cu-Ni-PGE Magmatic Sulfide Ores and their Host Layered Gabbros in the Haymiliyah Fossil Magma Chamber (Haylayn Block, Semail Ophiolite Nappe, Oman)". Ophiolite Genesis and Evolution of the Oceanic Lithosphere. Petrology and Structural Geology. 5: 209–229. doi:10.1007/978-94-011-3358-6_12. ISBN 978-94-010-5484-3.
  29. Arnason, John G.; Bird, Dennis K. (August 2000). "A Gold- and Platinum-Mineralized Layer in Gabbros of The Kap Edvard Holm Complex: Field, Petrologic, and Geochemical Relations". Economic Geology. 95 (5): 945–970. doi:10.2113/gsecongeo.95.5.945.
  30. Philpotts & Ague 2009, pp. 384–390.
  31. Winkler, Erhard M. (1994). Stone in architecture : properties, durability (3rd completely rev. and extended ed.). Berlin: Springer-Verlag. p. 101. ISBN 9783540576266.
  32. National Research Council (1 January 1982). Conservation of Historic Stone Buildings and Monuments. p. 80. doi:10.17226/514. ISBN 978-0-309-03275-9.
Wikimedia Commons has media related to Gabbro.
This article is issued from Wikipedia. The text is licensed under Creative Commons - Attribution - Sharealike. Additional terms may apply for the media files.