Template:Refimprove
Anorthosite from Poland
Lunar anorthosite from Apollo 15 landing site
Anorthosite /ænˈɔr/ is a phaneritic, intrusive igneous rock characterized by a predominance of plagioclase feldspar (90–100%), and a minimal mafic component (0–10%). Pyroxene, ilmenite, magnetite, and olivine are the mafic minerals most commonly present.
Anorthosite on Earth can be divided into two types: Proterozoic anorthosite (also known as massif or massif-type anorthosite) and Archean anorthosite. These two types of anorthosite have different modes of occurrence, appear to be restricted to different periods in Earth's history, and are thought to have had different origins.
Lunar anorthosites constitute the light-coloured areas of the Moon's surface and have been the subject of much research.[1]
Proterozoic anorthosite[]
Age[]
Proterozoic anorthosites were emplaced during the Proterozoic Eon (ca. 2,500-542 Ma).
Mode of occurrence[]
Anorthosite from southern Finland
Anorthosite plutons occur in a wide range of sizes. Some smaller plutons, exemplified by many anorthosite bodies in the U.S. and Harris in Scotland, cover only a few dozen square kilometres. Larger plutons, like the Mt. Lister Anorthosite, in northern Labrador, Canada, cover several thousands of square kilometres.
Many Proterozoic anorthosites occur in spatial association with other highly distinctive, contemporaneous rock types (the so-called 'anorthosite suite' or 'anorthosite-mangerite-charnockite complex'). These rock types include iron-rich diorite, gabbro, and norite; leucocratic mafic rocks such as leucotroctolite and leuconorite; and iron-rich felsic rocks, including monzonite and rapakivi granite. Importantly, large volumes of ultramafic rocks are not found in association with Proterozoic anorthosites.
Occurrences of Proterozoic anorthosites are commonly referred to as 'massifs'. However, there is some question as to what name would best describe any occurrence of anorthosite together with the rock types mentioned above. Early works used the term 'complex' The term 'plutonic suite' has been applied to some large occurrences in northern Labrador, Canada; however, it has been suggested (in 2004-2005) that 'batholith' would be a better term. 'Batholith' is used to describe such occurrences for the remainder of this article.
The areal extent of anorthosite batholiths ranges from relatively small (dozens or hundreds of square kilometres) to nearly Template:Convert, in the instance of the Nain Plutonic Suite in northern Labrador, Canada.
Major occurrences of Proterozoic anorthosite are found in the southwest U.S., the Appalachian Mountains, eastern Canada, across southern Scandinavia and eastern Europe. Mapped onto the Pangaean continental configuration of that eon, these occurrences are all contained in a single straight belt, and must all have been emplaced intracratonally. The conditions and constraints of this pattern of origin and distribution are not clear. However, see the Origins section below.
Anorthosites are also common in layered intrusions. Anorthosite in these layered intrusions can form as cumulate layers in the upper parts of the intrusive complex[2] or as later-stage intrusions into the layered intrusion complex.[3]
Physical characteristics[]
Since they are primarily composed of plagioclase feldspar, most of Proterozoic anorthosites appear, in outcrop, to be grey or bluish. Individual plagioclase crystals may be black, white, blue, or grey, and may exhibit an iridescence known as labradorescence on fresh surfaces. The feldspar variety labradorite is commonly present in anorthosites. Mineralogically, labradorite is a compositional term for any calcium-rich plagioclase feldspar containing between 50–70 molecular percent anorthite (An 50–70), regardless of whether it shows labradorescence. The mafic mineral in Proterozoic anorthosite may be clinopyroxene, orthopyroxene, olivine, or, more rarely, amphibole. Oxides, such as magnetite or ilmenite, are also common.
Most anorthosite plutons are very coarse grained; that is, the individual plagioclase crystals and the accompanying mafic mineral are more than a few centimetres long. Less commonly, plagioclase crystals are megacrystic, or larger than one metre long. However, most Proterozoic anorthosites are deformed, and such large plagioclase crystals have recrystallized to form smaller crystals, leaving only the outline of the larger crystals behind.
While many Proterozoic anorthosite plutons appear to have no large-scale relict igneous structures (having instead post-emplacement deformational structures), some do have igneous layering, which may be defined by crystal size, mafic content, or chemical characteristics. Such layering clearly has origins with a rheologically liquid-state magma.
Chemical and isotopic characteristics[]
The composition of plagioclase feldspar in Proterozoic anorthosites is most commonly between An40 and An60 (40-60% anorthite). This compositional range is intermediate, and is one of the characteristics which distinguish Proterozoic anorthosites from Archean anorthosites. Mafic minerals in Proterozoic anorthosites have a wide range of composition, but are not generally highly magnesian.
The trace-element chemistry of Proterozoic anorthosites, and the associated rock types, has been examined in some detail by researchers with the aim of arriving at a plausible genetic theory. However, there is still little agreement on just what the results mean for anorthosite genesis; see the 'Origins' section below. A very short list of results, including results for rocks thought to be related to Proterozoic anorthosites.[4]
Some research has focused on neodymium (Nd) and strontium (Sr) isotopic determinations for anorthosites, particularly for anorthosites of the Nain Plutonic Suite (NPS). Such isotopic determinations are of use in gauging the viability of prospective sources for magmas that gave rise to anorthosites. Some results are detailed below in the 'Origins' section.
Origins of Proterozoic anorthosites[]
The origins of Proterozoic anorthosites have been a subject of theoretical debate for many decades. A brief synopsis of this problem is as follows. The problem begins with the generation of magma, the necessary precursor of any igneous rock.
Magma generated by small amounts of partial melting of the mantle is generally of basaltic composition. Under normal conditions, the composition of basaltic magma requires it to crystallize between 50 and 70% plagioclase, with the bulk of the remainder of the magma crystallizing as mafic minerals. However, anorthosites are defined by a high plagioclase content (90–100% plagioclase), and are not found in association with contemporaneous ultramafic rocks. This is now known as 'the anorthosite problem'. Proposed solutions to the anorthosite problem have been diverse, with many of the proposals drawing on different geological subdisciplines.
It was suggested early in the history of anorthosite debate that a special type of magma, anorthositic magma, had been generated at depth, and emplaced into the crust. However, the solidus of an anorthositic magma is too high for it to exist as a liquid for very long at normal ambient crustal temperatures, so this appears to be unlikely. The presence of water vapour has been shown to lower the solidus temperature of anorthositic magma to more reasonable values, but most anorthosites are relatively dry. It may be postulated, then, that water vapour be driven off by subsequent metamorphism of the anorthosite, but some anorthosites are undeformed, thereby invalidating the suggestion.
The discovery, in the late 1970s, of anorthositic dykes in the Nain Plutonic Suite, suggested that the possibility of anorthositic magmas existing at crustal temperatures needed to be reexamined. However, the dykes were later shown to be more complex than was originally thought. In summary, though liquid-state processes clearly operate in some anorthosite plutons, the plutons are probably not derived from anorthositic magmas.
Many researchers have argued that anorthosites are the products of basaltic magma, and that mechanical removal of mafic minerals has occurred. Since the mafic minerals are not found with the anorthosites, these minerals must have been left at either a deeper level or the base of the crust. A typical theory is as follows: partial melting of the mantle generates a basaltic magma, which does not immediately ascend into the crust. Instead, the basaltic magma forms a large magma chamber at the base of the crust and fractionates large amounts of mafic minerals, which sink to the bottom of the chamber. The cocrystallizing plagioclase crystals float, and eventually are emplaced into the crust as anorthosite plutons. Most of the sinking mafic minerals form ultramafic cumulates which stay at the base of the crust.
This theory has many appealing features, of which one is the capacity to explain the chemical composition of high-alumina orthopyroxene megacrysts (HAOM). This is detailed below in the section devoted to the HAOM. However, on its own, this hypothesis cannot coherently explain the origins of anorthosites, because it does not fit with, among other things, some important isotopic measurements made on anorthositic rocks in the Nain Plutonic Suite. The Nd and Sr isotopic data shows the magma which produced the anorthosites cannot have been derived only from the mantle. Instead, the magma that gave rise to the Nain Plutonic Suite anorthosites must have had a significant crustal component. This discovery led to a slightly more complicated version of the previous hypothesis: Large amounts of basaltic magma form a magma chamber at the base of the crust, and, while crystallizing, assimilating large amounts of crust.[5]
This small addendum explains both the isotopic characteristics and certain other chemical niceties of Proterozoic anorthosite. However, at least one researcher has cogently argued, on the basis of geochemical data, that the mantle's role in production of anorthosites must actually be very limited: the mantle provides only the impetus (heat) for crustal melting, and a small amount of partial melt in the form of basaltic magma. Thus anorthosites are, in this view, derived almost entirely from lower crustal melts.[6]
High-alumina orthopyroxene megacrysts[]
The high-alumina orthopyroxene megacrysts (HAOM) have, like Proterozoic anorthosites, been the subject of great debate, although a tentative consensus about their origin appears to have emerged. The peculiar characteristic worthy of such debate is reflected in their name. Normal orthopyroxene has chemical composition (Fe,Mg)2Si2O6, whereas the HAOM have anomalously large amounts of aluminium (up to about 9%) in their atomic structure.
Because the solubility of aluminium in orthopyroxene increases with increasing pressure, many researchers,[7] have suggested that the HAOM crystallized at depth, near the base of the Earth's crust. The maximum amounts of aluminium correspond to a Template:Convert depth.
Other researchers consider the chemical compositions of the HAOM to be the product of rapid crystallization at moderate or low pressures.[8]
Archaean anorthosite[]
Smaller amounts of anorthosite were emplaced during the Archaean eon (ca 3,800-2,400 Ma), although most have been dated between 3,200 and 2,800 Ma. They are distinct texturally and mineralogically from Proterozoic anorthosite bodies. Their most characteristic feature is the presence of equant megacrysts of plagioclase surrounded by a fine-grained mafic groundmass.
Economic value of anorthosite[]
The primary economic value of anorthosite bodies is the titanium-bearing oxide ilmenite. However, some Proterozoic anorthosite bodies have large amounts of labradorite, which is quarried for its value as both a gemstone and a building material. Archean anorthosites, because they are calcium-rich, have large amounts of aluminium substituting for silicon; a few of these bodies are mined as ores of aluminium.
Anorthosite was prominently represented in rock samples brought back from the Moon, and is important in investigations of Mars, Venus, and meteorites.
See also[]
References[]
- ↑ PSRD: The Oldest Moon Rocks
- ↑ Template:Cite map
- ↑ Topinka, Lyn (2003-01-26). "America's Volcanic Past: Minnesota". USGS/Cascades Volcano Observatory. Archived from the original on 10 January 2009. http://web.archive.org/web/20090110104310/http://vulcan.wr.usgs.gov/LivingWith/VolcanicPast/Places/volcanic_past_minnesota.html. Retrieved 2009-02-13.
- ↑ Bédard (2001); Emslie et al. (1994); Xue and Morse (1994); Emslie and Stirling (1993); and Xue and Morse (1993).
- ↑ Emslie et al. (1994).
- ↑ Bédard (2001).
- ↑ Longhi et al. (1993); Emslie (1975).
- ↑ e.g. Xue and Morse, (1994).
Bibliography[]
- Bédard, Jean H. (2001). "Parental magmas of the Nain Plutonic Suite anorthosites and mafic cumulates: a trace element modelling approach". Contributions to Mineralogy and Petrology 141 (6): 747–771. doi:10.1007/s004100100268
doi:10.1007/s004100100268. Bibcode: 2001CoMP..141..747B Bibcode: 2001CoMP..141..747B.
- Emslie, R. F. (1 May 1975). "Pyroxene megacrysts from anorthositic rocks: new clues to the sources and evolution of the parent magmas". Canadian Mineralogist 13 (2): 138–145. ISSN 00084476
ISSN 00084476. http://canmin.geoscienceworld.org/cgi/content/abstract/13/2/138.
- Emslie, R. F.; Stirling, J. A. R. (1 December 1993). "Rapakivi and related granitoids of the Nain Plutonic Suite: geochemistry, mineral assemblages and fluid equilibria". Canadian Mineralogist 31 (4): 821–847. ISSN 00084476
ISSN 00084476. http://canmin.geoscienceworld.org/cgi/content/abstract/31/4/821.
- Emslie, R. F.; Hamilton, M. A.; Theriault, R. J. (1994). "Petrogenesis of a Mid-Proterozoic Anorthosite-Mangerite-Charnockite-Granite (AMCG) Complex: Isotopic and Chemical Evidence from the Nain Plutonic Suite". Journal of Geology 102 (5): 539–558. doi:10.1086/629697
doi:10.1086/629697. Bibcode: 1994JG....102..539E Bibcode: 1994JG....102..539E.
- Longhi, John; Fram, M. S.; Vander Auwera, J.; Montieth, J. N. (1 October 1993). "Pressure effects, kinetics, and rheology of anorthositic and related magmas". American Mineralogist 78 (9–10): 1016–1030. http://ammin.geoscienceworld.org/cgi/content/abstract/78/9-10/1016.
- Norman, M. D.; Borg, L. E.; Nyquist, L. E.; Bogard, D. D. (2003). "Chronology, geochemistry, and petrology of a ferroan noritic anorthosite clast from Descartes breccia 67215: Clues to the age, origin, structure, and impact history of the lunar crust". Meteoritics and Planetary Science 38 (4): 645–661. doi:10.1111/j.1945-5100.2003.tb00031.x
doi:10.1111/j.1945-5100.2003.tb00031.x. Bibcode: 2003M&PS...38..645N Bibcode: 2003M&PS...38..645N. http://www.ingentaconnect.com/content/arizona/maps/2003/00000038/00000004/art00011.
- Wood, J. A.; Dickey, J. S. Jr.; Marvin, U. B.; Powell, B. N. (1970). "Lunar Anorthosites". Science 167 (3918): 602–604. doi:10.1126/science.167.3918.602
doi:10.1126/science.167.3918.602. PMID 17781512 PMID 17781512. Bibcode: 1970Sci...167..602W Bibcode: 1970Sci...167..602W.
- Xue, S.; Morse, S. A. (1993). "Geochemistry of the Nain massif anorthosite, Labrador: Magma diversity in five intrusions". Geochimica et Cosmochimica Acta 57 (16): 3925–3948. doi:10.1016/0016-7037(93)90344-V
doi:10.1016/0016-7037(93)90344-V. Bibcode: 1993GeCoA..57.3925X Bibcode: 1993GeCoA..57.3925X.
- Xue, S.; Morse, S. A. (1994). "Chemical characteristics of plagioclase and pyroxene megacrysts and their significance to the petrogenesis of the Nain Anorthosites". Geochimica et Cosmochimica Acta 58 (20): 4317–4331. doi:10.1016/0016-7037(94)90336-0
doi:10.1016/0016-7037(94)90336-0. Bibcode: 1994GeCoA..58.4317X Bibcode: 1994GeCoA..58.4317X.
External links[]
- Anorthosite Complexes (web archive)
- How does anorthosite crystallize?
- History of the Emplacement and Deformation of Anorthosite Bodies in the Eastern Marcy Massif, Adirondacks Mountains, New York
- Anorthosite – Lunar Highland Rock
- Lunar Anorthosite Specimen 60025 Photomicrographs
- Mercury – Evidence for Anorthosite and Basalt from mid-Infrared Spectroscopy