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Anorthite
Anorthite
Anorthite
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Anorthite
Anorthite crystals in a basalt vug from Vesuvius (size:6.9 × 4.1 × 3.8 cm)
General
CategoryTectosilicate minerals
GroupFeldspar group
SeriesPlagioclase feldspar series
FormulaCaAl2Si2O8
IMA symbolAn[1]
Strunz classification9.FA.35
Crystal systemTriclinic
Crystal classPinacoidal (1)
(same H-M symbol)
Space groupP1
Unit cella = 8.1768, b = 12.8768
c = 14.169 [Å]; α = 93.17°
β = 115.85°, γ = 92.22°; Z = 8
Identification
Formula mass278.203 g·mol−1
ColorWhite, grayish, reddish
Crystal habitAnhedral to subhedral granular
TwinningCommon
CleavagePerfect [001] good [010] poor [110]
FractureUneven to conchoidal
TenacityBrittle
Mohs scale hardness6
LusterVitreous
StreakWhite
DiaphaneityTransparent to translucent
Specific gravity2.72–2.75
Optical propertiesBiaxial (−)
Refractive indexnα = 1.573–1.577 nβ = 1.580–1.585 nγ = 1.585–1.590
Birefringenceδ = 0.012–0.013
2V angle78° to 83°
Melting point1550 ± 2°C[2]
References[3][2][4][5]

Anorthite (< an 'not' + ortho 'straight') is the calcium endmember of the plagioclase feldspar mineral series. The chemical formula of pure anorthite is CaAl2Si2O8. Anorthite is found in igneous rocks.

Mineralogy

[edit]
Anorthite crystals (white) in lava from Miyake Island, Japan (size: 2.4 × 1.7 × 1.7 cm)

Anorthite is the calcium-rich endmember of the plagioclase solid solution series, the other endmember being albite (NaAlSi3O8). Pure anorthite, containing no sodium, is rare on Earth.[6] Anorthite also refers, however, to plagioclase compositions with more than 90 molecular percent of the anorthite endmember (and up to 10 molecular percent of the albite endmember). The composition of plagioclases is often expressed as a molar percentage of An%, or (for a specific quantity) Ann, where n = Ca/(Ca + Na) × 100.[7] This equation predominantly works in a terrestrial context; exotic locales and in particular Lunar rocks may need to account for other cations, such as Fe2+, to explain differences between optically and structurally derived An% data observed in Lunar anorthites.[8]

At standard pressure, pure anorthite (An100) melts at 1550 ± 2 °C (2822 °F).[2]

Occurrence

[edit]

Anorthite is a compositional variety of plagioclase. It occurs in mafic igneous rock. It also occurs in metamorphic rocks of granulite facies, in metamorphosed carbonate rocks, and corundum deposits.[3] Its type localities are Monte Somma and Valle di Fassa, Italy. It was first described in 1823.[5] It is more rare in surficial rocks than it normally would be due to its high weathering potential in the Goldich dissolution series.

It also makes up much of the lunar highlands; the Genesis Rock, collected during the 1971 Apollo 15 mission, is made of anorthosite, a rock composed largely of anorthite. Anorthite was discovered in samples from comet Wild 2, and the mineral is an important constituent of Ca-Al-rich inclusions in rare varieties of chondritic meteorites.

See also

[edit]

References

[edit]
Revisions and contributorsEdit on WikipediaRead on Wikipedia

Anorthite

View on Grokipedia
from Grokipedia
Anorthite is the calcium endmember of the series, characterized by the CaAl₂Si₂O₈ and recognized as a key rock-forming in igneous and metamorphic environments. This triclinic exhibits a vitreous luster, colorless to white or grayish hues, and a Mohs of 6 to 6.5, with perfect cleavage parallel to the {001} plane. As the most calcic member of the group, anorthite forms a continuous series with (NaAlSi₃O₈), where compositions range from nearly pure anorthite (An₉₀–An₁₀₀) to more sodic intermediates, influencing its role in classifying . It typically occurs in and ultramafic igneous rocks such as and , as well as in contact metamorphic zones and lunar anorthosites, where it can constitute up to 90-100% of the rock mass. Anorthosite, a rock composed predominantly of , is used industrially in ceramics, aggregates, and as a functional filler, while pure anorthite holds significant petrological value for understanding magmatic differentiation and crustal evolution, and it occasionally appears as a collector's specimen or minor gem material in transparent varieties.

Composition and Structure

Chemical Composition

Anorthite is a calcium with the ideal \ceCaAl2Si2O8\ce{CaAl2Si2O8}, representing its pure endmember composition. It serves as the calcium-rich endmember (An100) of the solid solution series, which extends to the sodium-rich endmember with the formula \ceNaAlSi3O8\ce{NaAlSi3O8}. In natural specimens, anorthite typically exhibits compositions exceeding 90% anorthite component (An90–An100), accompanied by minor sodium substitution for calcium to maintain charge balance within the . As a tectosilicate, anorthite belongs to the group, characterized by a three-dimensional framework of linked silica-oxygen tetrahedra with aluminum substitutions. The mineral was first described and named in 1823 by German mineralogist Gustav Rose, with the name derived from the Greek words an- (not) and orthos (straight), alluding to its oblique cleavage angles.

Crystal Structure

Anorthite crystallizes in the triclinic system with space group P1, characterized by low symmetry due to the ordered distribution of aluminum and silicon atoms in its tetrahedral sites. This ordering, approximately 95% complete, positions Al and Si alternately in the TO₄ tetrahedra (where T denotes Si or Al), which contributes to the deviation from higher symmetry groups observed in other feldspars. The unit cell parameters at ambient conditions are a ≈ 8.18 , b ≈ 12.87 , c ≈ 14.17 , α ≈ 93.11°, β ≈ 115.89°, and γ ≈ 91.28°, resulting in a of approximately 1338 ų. The framework consists of a three-dimensional network formed by corner-sharing TO₄ tetrahedra, which link to create four-membered rings and extend into double crankshaft chains parallel to the a-axis. These structural motifs, including the alternating tilt of tetrahedra in the chains, arise from the Al-Si ordering and define the overall . The cleavage properties reflect inherent weaknesses in this framework: perfect on {001}, good on {010}, and poor on {110}, corresponding to planes where the double chains and tetrahedral linkages are least resistant to separation.

Physical Properties

Mechanical and Thermal Properties

Anorthite possesses a of 6 to 6.5 on the , rendering it sufficiently durable for common geological processes while remaining scratchable by harder minerals like . Its specific gravity falls between 2.74 and 2.76, reflecting a moderate that distinguishes it among framework silicates. The mineral typically exhibits a vitreous luster, enhancing its visual appeal in crystalline forms, and appears in colorless, white, or reddish-gray hues depending on impurities and formation conditions. It shows perfect cleavage parallel to {001}, good to {010}, and conchoidal to uneven fracture. In terms of thermal behavior, anorthite melts congruently at approximately ± 2°C under standard , a property that underscores its role in high-temperature igneous and metamorphic processes. The coefficient of thermal expansion is low, around 4.8 × 10^{-6} °C^{-1}, which minimizes dimensional changes during heating and supports applications requiring thermal stability. Anorthite maintains structural integrity in high-temperature environments, exhibiting stability up to granulite facies metamorphism, where it persists under conditions of 700–1000°C and moderate pressures without significant decomposition. This resilience arises from its robust aluminosilicate framework, allowing it to form key assemblages in deep crustal rocks.

Optical Properties

Anorthite exhibits biaxial negative optical character, with refractive indices ranging from nα = 1.573–1.577, nβ = 1.580–1.585, and nγ = 1.585–1.590, values that increase with higher anorthite content in the plagioclase series. These indices contribute to moderate relief in thin sections relative to common mounting media like Canada balsam (n ≈ 1.54). The resulting birefringence is 0.012–0.013, producing low to moderate first-order interference colors under crossed polars. The optic axial angle (2V) for anorthite measures approximately 78–83°, facilitating determination of optic sign and orientation in petrographic analysis. Common twinning occurs according to the albite, pericline, and Carlsbad laws, often appearing as polysynthetic lamellae that are prominently visible under polarized light, aiding in the distinction from other feldspars. In , anorthite's are essential for identifying compositions, particularly through the Michel-Lévy method, which correlates maximum and interference colors in thin sections to estimate the anorthite percentage in solid solutions. This technique relies on the systematic variation in retardation and color sequences, where anorthite-rich displays higher-order grays and whites compared to sodic end-members.

Occurrence and Formation

Natural Habitats

Anorthite primarily occurs in igneous rocks, such as and , where its calcium-rich composition facilitates association with other minerals. These environments include layered intrusions and volcanic settings, with notable examples in the Bushveld Complex of and oceanic basalts. In metamorphic terrains, anorthite is present in rocks of granulite facies, particularly within contact aureoles surrounding igneous intrusions. It also appears in the contact aureole of the Laramie Anorthosite Complex in Wyoming, USA, highlighting its role in thermal metamorphism of surrounding sediments. Extraterrestrially, anorthite is a dominant mineral in the lunar highlands, exemplified by the ferroan anorthosite known as the Genesis Rock (sample 15415), collected during the Apollo 15 mission in 1971 from the Hadley-Apennine region. This sample consists predominantly of anorthite (approximately 97%), representing primordial lunar crust. Anorthite particles have also been identified in samples from comet 81P/Wild 2, returned by the Stardust mission in 2006, within refractory inclusions that indicate high-temperature nebular processing. The type localities for anorthite are Monte Somma at the Vesuvius complex and Valle di Fassa, both in , where it was first described in from ejecta and metamorphic enclaves. Pure anorthite crystals are rare, typically forming as small, translucent individuals up to several centimeters; more commonly, it appears as massive aggregates or the primary component of rocks, such as those in the of New York.

Geological Significance

Anorthite forms primarily through the of calcium-rich magmas in basic igneous environments, where it appears as an early-phase in the differentiation sequence of gabbroic and basaltic melts. In these settings, high CaO/Na₂O ratios in hydrous basalts promote the precipitation of with anorthite contents exceeding An₉₀, often as cumulate layers in layered intrusions. Additionally, anorthite develops during high-grade in granulite-facies conditions, typically above 700°C, where it stabilizes in calcic paragenesis involving reactions among aluminosilicates, pyroxenes, and carbonates. As an indicator mineral, anorthite signals calcic conditions during , reflecting the initial stages of fractional in primitive, compositions before sodium enrichment shifts toward more albitic . In metamorphic contexts, its presence denotes advanced grades, with assemblages like anorthite + + indicating equilibration at elevated temperatures and pressures in the deep crust. Anorthite serves as a key component in plutons, which are interpreted as remnants of early crustal differentiation processes, particularly in terranes where hydrous underplating of basaltic magmas facilitated the accumulation of high-An plagioclase at lower crustal depths of 25–28 km. These plutons contribute to the stabilization and growth of during the , linking anorthite-rich rocks to the planet's formative magmatic episodes. Geothermometry involving anorthite relies on exsolution textures in coexisting pyroxenes or equilibrium partitioning with mafic minerals, yielding crystallization temperatures of 1100–1180°C and pressures up to 9 kbar in anorthositic systems. For instance, pyroxene exsolution lamellae in anorthite-bearing assemblages provide constraints on cooling paths, while plagioclase composition in equilibrium with melt or amphibole refines temperature estimates under hydrous conditions. Beyond Earth, the prevalence of high-anorthite plagioclase (An₉₅–₉₉) in the lunar highlands underscores its role in planetary geology, where flotation of buoyant crystals atop a crystallizing magma ocean generated the ferroan anorthosite crust, comprising over 90% plagioclase with minimal mafic contaminants. This process, driven by density contrasts in an FeO-enriched residual melt, implies a protracted solidification lasting hundreds of millions of years and offers insights into the thermal evolution of airless bodies.

Synthesis and Uses

Laboratory Synthesis

Anorthite can be synthesized hydrothermally using oxide precursors such as , , and , or gels derived from them, under controlled pressure and temperature conditions to promote . Typical synthesis involves mixing the precursors in stoichiometric ratios (CaO:Al₂O₃:SiO₂ = 1:1:2) and subjecting the mixture to hydrothermal treatment at temperatures ranging from 700°C to 1200°C and pressures of 1–3 kbar for durations of hours to months, yielding single crystals or polycrystalline material. Solid-state represents another common method for producing polycrystalline anorthite, where mixtures of powders or natural materials like kaolin and CaCO₃ are ball-milled, pressed into pellets, and heated in air or inert atmospheres. This process typically requires temperatures exceeding 1400°C for several hours to achieve phase purity, as lower temperatures may result in incomplete reaction or residual phases; the high temperature facilitates and densification without melting, given anorthite's of approximately 1550°C. Sol-gel methods enable the production of nanoscale or fine-grained anorthite by starting with metal alkoxides, such as (TEOS) for silica, aluminum isopropoxide for alumina, and for calcium, followed by and to form a gel network. The dried gel is then calcined at temperatures around 900–1100°C to crystallize anorthite, often with dopants like B₂O₃ to lower the required temperature and enhance homogeneity at the atomic scale. Synthesis of pure anorthite faces challenges, including the potential contamination by (NaAlSi₃O₈) if sodium impurities are present in precursors, which can form solid solutions or separate phases under non-equilibrium conditions. Additionally, achieving full Al-Si tetrahedral order in the is difficult, as synthetic anorthite often exhibits high disorder, particularly in the core of crystals grown rapidly, requiring prolonged annealing times (up to 110 days) at elevated temperatures to approach natural ordering levels. Recent advances include the use of spark plasma sintering (SPS) for consolidating anorthite powders into dense ceramics, where mixtures of kaolin and CaCO₃ are heated rapidly (50°C/min) to 850–1100°C under 50 MPa for 10 minutes, achieving up to 90 wt.% anorthite phase purity and low —significantly outperforming conventional at the same temperatures. This technique, demonstrated in studies around 2021–2022, reduces energy use and processing time while minimizing secondary phases. More recent developments as of 2025 include plasma synthesis using natural raw materials such as quartz sand and , enabling efficient production at reduced temperatures, and dolomite-induced eutectic synthesis for anorthite from industrial byproducts like ash.

Applications in Industry and Science

Anorthite-rich materials or anorthite-based compositions are utilized in the and ceramics industries, where their high and fluxing properties facilitate the production of durable materials with enhanced and low . In , the of anorthite phases improves mechanical strength and resistance to , making it suitable for applications requiring high-temperature stability. Specifically, anorthite-based compositions are employed in the manufacture of , contributing to denser microstructures and reduced temperatures while maintaining excellent pyroplastic deformation resistance. Additionally, in refractories, anorthite's low thermal conductivity and structural integrity support its use in high-temperature environments, such as furnace linings and insulating composites. In scientific research, anorthite serves as a valuable analog for , particularly in lunar studies; for instance, high-purity megacrystic anorthite from Miyake-jima, , has been identified as an effective simulant for the Moon's anorthositic crust due to its close compositional match (approximately 95% anorthite) and spectroscopic properties. This material aids in simulating lunar for mission planning and resource utilization experiments as of 2025. Furthermore, porous anorthite ceramics, often synthesized at the nanoscale, function as supports in catalytic processes, leveraging their high surface area and thermal stability to enhance reaction efficiency in applications like and insulation. Anorthite also finds niche roles in gemology and geochronology. In gemology, faceted anorthite gems, derived from rare transparent crystals, are prized by collectors for their scarcity and subtle play of light, though they lack vibrant coloration and are typically small in size. These specimens highlight anorthite's triclinic structure, which allows for intriguing optical effects in high-quality cuts. In geochronology, anorthite-bearing rocks, such as anorthosites, are analyzed using ⁴⁰Ar/³⁹Ar dating methods to determine cooling histories and impact events, providing precise timelines for igneous and metamorphic processes with a closure temperature of approximately 275 °C for anorthite grains. This technique has been instrumental in dating lunar samples and terrestrial xenoliths, revealing geomagnetic and thermal evolution insights.

References

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