garnet

—garnetlike, adj.

/gahr"nit/, n.

1. any of a group of hard, vitreous minerals, silicates of calcium, magnesium, iron, or manganese with aluminum or iron, varying in color: a deep-red transparent variety is used as a gem and as an abrasive.

2. a deep-red color.

[1275-1325; ME garnet, gernate < OF gernate, grenade < L granatum granular; cf. POMEGRANATE]

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Any of a group of common silicate minerals with identical crystal structure but highly variable chemical composition.

Garnets are most often found in metamorphic rocks but also occur in certain types of igneous rocks, and, usually in minor amounts, in some sedimentary rocks. They may be colourless, black, or many shades of red and green. Garnets are hard, and they fracture with sharp edges. They are used as abrasives for fine sanding and polishing of wood, leather, glass, metals, and plastics, as sandblasting agents, and in nonskid surface coatings. Garnet is the birthstone for January. Garnets have been mined in New York, Maine, and Idaho in the U.S., the world's leading producer; notable quantities have also been found in Australia, China, India, and elsewhere.

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▪ mineral

Introduction

      any member of a group of common silicate minerals that have similar crystal structures and chemical compositions. They may be colourless, black, and many shades of red and green.

General considerations

      Garnets, favoured by lapidaries since ancient times and used widely as an abrasive, occur in rocks of each of the major classes. In most rocks, however, garnets occur in only minor amounts—i.e., they are accessory minerals. Nevertheless, as a consequence of their distinctive appearances, they are frequently recognized in hand specimens and become part of the name of the rock in which they are contained—e.g., garnet mica schist.

Chemical composition

      Garnets comprise a group of silicates with the general formula A₃B₂(SiO₄)₃ in which A = Ca, Fe²⁺, Mg, Mn²⁺; B = Al, Cr, Fe³⁺, Mn³⁺, Si, Ti, V, Zr; and Si may be replaced partly by Al, Ti, and/or Fe³⁺. In addition, many analyses indicate the presence of trace to minor amounts of Na, beryllium (Be), Sr, scandium (Sc), Y, La, hafnium (Hf), niobium (Nb), molybdenum (Mo), cobalt (Co), nickel (Ni), copper (Cu), silver (Ag), Zn, cadmium (Cd), B, Ga, indium (In), Ge, tin (Sn), P, arsenic (As), F, and rare earth elements. grossular is often recorded as having a composition containing water, but the true substitution seems to involve 4 H⁺ for Si⁴⁺; and a complete series appears to exist between grossular [Ca₃Al₂(SiO₄)₃] and hydrogrossular [Ca₃Al₂(SiO₄)_{3 - x}(H₄O₄)_x]. Other hydrogarnets have been reported—e.g., hydroandradite and hydrospessartine; the general formula for hydrogarnets would be A₃B₂(SiO₄)_{3 - x}(H₄O₄)_x, and the general formula for an end-member hydrogarnet would be A₃B₂(H₄O₄)₃.

 Nearly all natural garnets exhibit extensive substitution; solid-solution (solid solution) series—some complete, others only partial—exist between several pairs of the group. In practice, the name of the end-member that makes up the largest percentage of any given specimen is usually applied—e.g., a garnet with the composition Al₄₅Py₂₅Sp₁₅Gr₉An₆ would be called almandine. End-member compositions of the garnets that are relatively common in rocks are given in the Table—>.

      Analyses of natural specimens suggest that the following solid-solution series exist: in the pyralspite subgroup, a complete series between almandine and both pyrope and spessartine; in the ugrandite subgroup, a continuous series between grossular and both andradite and uvarovite; less than a complete series between any member of the pyralspite subgroup and any member of the ugrandite subgroup; and an additional series between pyrope and andradite and one or more of the less common garnets (e.g., pyrope with knorringite [Mg₃Cr₂(SiO₄)₃] and andradite with schorlomite [Ca₃Ti₂(Fe₂, Si)O₁₂]).

      A few well-studied garnets from metamorphic rocks have been shown to be chemically zoned with layers of differing compositions. Most of the differences thus far described appear to reflect, for the most part, differences in occupants of the A structural positions.

crystal structure

 Garnets consist of groups of independent, distorted SiO₄ tetrahedrons, each of which is linked, by sharing corners, to distorted BO₆ (e.g., aluminum- and/or iron-centred) octahedrons, thus forming a three-dimensional framework. The interstices are occupied by A divalent metal ions (e.g., Ca, Fe²⁺, Mg, and Mn), so that each one is surrounded by eight oxygen atoms that are at the corners of a distorted cube. Therefore, each oxygen is coordinated by two A, one B, and one silicon cation (see figure—>). The configuration of the array is such that garnets are isometric (cubic).

   Garnets commonly occur as well-developed crystals. The typical forms of the crystals have 12 or 24 sides and are called dodecahedrons (see photograph—>) and trapezohedrons (see photograph—>), respectively, or they are combinations of such forms (see photograph—>). All tend to be nearly equant. A few studies have led to the suggestion that these crystal habits can be correlated with chemical composition—i.e., that dodecahedrons are most likely to be grossular-rich; that trapezohedrons tend to be pyrope-, almandine-, or spessartine-rich; and that combinations are generally andradite-rich. In any case, many garnets have individual faces that are not well developed, and thus the crystals are roughly spherical. Garnet also occurs in fine to coarse granular masses.

Physical properties

      The diverse garnets can be distinguished from other common rock-forming minerals rather easily since they do not physically resemble any of them. All garnets have vitreous to resinous lustres. Most are translucent, although they may range from transparent to nearly opaque. Garnets lack cleavage but tend to be brittle. They have Mohs hardness values of 6¹/₂ to 7¹/₂; their specific gravities (specific gravity), which vary with composition, range from about 3.58 (pyrope) to 4.32 (almandine). Their habits, also noteworthy, have already been described.

      A garnet's predominant end-member constituent can only be defined absolutely by, for example, chemical analysis or differential thermal analysis (DTA), a method based on the examination of the chemical and physical changes resulting from the application of heat to a mineral. Nonetheless, in many rocks a garnet can be named tentatively as to its probable composition after only macroscopic examination if its colour is considered in conjunction with the identity of its associated minerals and geologic occurrence. This is true despite the fact that even individual garnet species may assume several different colours: almandine's colour range is deep red to dark brownish red; pyrope may be pink to purplish or deep red to nearly black; spessartine may be brownish orange, burgundy, or reddish brown; grossular may be nearly colourless, white, pale green, yellow, orange, pink, yellowish brown, or brownish red; and andradite may be honey yellow or greenish yellow, brown, red, or nearly black.

      The availability of garnets of several colours, along with properties that make them rather durable and relatively easily worked, is responsible for their widespread use as gemstones.

Origin and occurrence

       Common occurrences of rock-forming garnetsThe rock-forming garnets are most common in metamorphic rocks (metamorphic rock). A few occur in igneous rocks, especially granites and granitic pegmatites. Garnets derived from such rocks occur sporadically in clastic sediments and sedimentary rocks. Typical occurrences of the common rock-forming garnets are given in the Table (Common occurrences of rock-forming garnets).

      Garnets commonly contain many inclusions—i.e., fragments of other rocks and minerals. Pinwheel garnet and snowball garnet are designations sometimes applied to those garnets whose inclusions appear to have been rotated. These garnets occur sporadically in foliated metamorphic rocks. Although their presence in diverse rocks has been interpreted variously, present-day consensus appears to be that they represent rotation during growth under conditions of dynamic metamorphism that involved differential pressures.

      Iron-rich garnets are frequently weathered to rusty masses that consist largely of limonite, and spessartine has weathered to masses of manganese oxide ores under tropical conditions (e.g., in India and Brazil). Garnets as a group, however, are relatively resistant to most weathering processes. Consequently, they occur in some sandy sediments and sandstones. Indeed, the red-coloured grains that are commonly found along some beaches are garnets.

Uses

      The hardness, lack of cleavage, and tendency to break into irregular grains have led to the recovery, crushing, and size-sorting of garnet for use in abrasives (abrasive) such as sandpaper. In addition, as previously mentioned, garnets are used as gemstones. Transparent red and reddish purple pyrope from the Middle East and from the former Czechoslovakia have been utilized in this capacity for centuries. Green andradite is cut, polished, and marketed as the highly prized stone demantoid. In addition, rhodolite is a pale rose-red garnet made up of two parts pyrope and one part almandine. Essonite (hessonite), also called hessonite (cinnamon garnet), is a gem form of grossular. Synthetic garnets with certain compositions, many of which do not have natural representatives, serve important functions because they are ferrimagnetic or antiferromagnetic or because they possess properties particularly suitable for use in lasers.

R.V. Dietrich

Additional Reading

W.A. Deer, R.A. Howie, and J. Zussman, Rock-forming Minerals, 5 vol. (1962–63), with a 2nd ed. in progress (1978– ); Paul H. Ribbe (ed.), Orthosilicates, 2nd ed. (1982).R.V. Dietrich

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