feldspar

feldspar

, felspar

any of a group of hard rock-forming minerals consisting of aluminium silicates of potassium, sodium, calcium, or barium: the principal constituents of igneous rocks. The group includes orthoclase, microcline, and the plagioclase minerals

Collins Discovery Encyclopedia, 1st edition © HarperCollins Publishers 2005

feldspar

[′fel‚spär]

(mineralogy)

A group of silicate minerals that make up about 60% of the outer 9 miles (15 kilometers) of the earth's crust; they are silicates of aluminum with the metals potassium, sodium, and calcium, and rarely, barium.

McGraw-Hill Dictionary of Scientific & Technical Terms, 6E, Copyright © 2003 by The McGraw-Hill Companies, Inc.

feldspar

A group of igneous minerals, all of which are softer than quartz, having the chemical composition of calcium silicates, potassium silicates, or sodium-aluminum silicates.

McGraw-Hill Dictionary of Architecture and Construction. Copyright © 2003 by McGraw-Hill Companies, Inc.

The following article is from The Great Soviet Encyclopedia (1979). It might be outdated or ideologically biased.

Feldspar

 

the most widely distributed group of rock-forming minerals, constituting more than 50 percent of earth and lunar rocks; they are also found in meteorites. The composition of feldspars is basically determined by the component ratio in a ternary system: NaAlSi₃O₈—KAlSi₃O₈—CaAl₂Si₂O₈; that is, feldspars are aluminosilicates of Na, K, and Ca, with admixtures of Ba, Sr, Pb, Fe, Li, Rb, Cs, Eu, Ce, and other elements. All feldspars have a basic three-dimensional framework composed of tetrahedral (Al, Si)O₄ groups in which one-third to one-half of the Si atoms are replaced by Al. Univalent K⁺ and Na⁺ cations, with an Al/Si ratio of 1:3, or bivalent Ca²⁺ and Ba²⁺ cations, with an Al/Si ratio of 1: 2, are arranged in the large vacancies within this framework.

Two series of solid solutions are differentiated in the feldspar group: anorthoclases, or alkali feldspars (KAISi₃O₈—NaAlSi₃O₈), and plagioclases (NaAlSi₃O₈–CaAl₂Si₂O₈). The barium feldspar BaAl₂Si₂O₈, known as celsian, is rare, as are solid solutions with compositions between KAlSi₃O₀ and BaAl₂Si₂O₈, known as hyalophane and containing up to 10–30 percent Ba.

Figure 1

Many feldspar varieties result from complex variation in composition (see Figure 1), the ordering of Al and Si distribution according to structural position, the decomposition of solid solutions, and submicroscopic twinning. The following are examples of potassium feldspars: (1) sanidine, with monoclinic symmetry and disordered Si and Al distribution; (2) maximum microcline (triclinic), with fully ordered Si and Al distribution; (3) intermediate microclines; and (4) orthoclase (assumed to be pseudomonoclinic), composed of submicroscopic twinned triclinic domains.

High-temperature anorthoclases are disordered and form a continuous series of solid solutions. Low-temperature anorthoclases decompose to yield perthites—regular intergrowths of microcline or orthoclase—and sodium feldspars, or albite. All plagioclase varieties are high-temperature (disordered with respect to Al and Si distribution), low-temperature (ordered), or intermediate.

Changes in the degree of ordering and the composition of plagioclases occur with the retention of triclinic symmetry with extremely complex structural changes and the formation of two unmixed regions, which in many oligoclases and labradorites is accompanied by iridescence.

Precise determination of the composition and structural state (ordering) of feldspars is carried out by means of optical orientation diagrams and diagrams of optic axial angles, measured on a Fedorov, or universal, stage, as well as by X-ray methods (diffractometry).

Plagioclases and microclines are nearly always polysynthetically twinned; that is, they form microscopic intergrowths of several elements in accordance with various characteristic laws of twinning.

The tabular or prismatic habit of feldspars in rocks is determined by well-developed {010} and {001} faces, along which perfect cleavage is formed at a right or nearly right angle, as well as by {110} faces. Feldspars have a hardness of 6–6.5 on Mohs’ scale and a density of 2,500-2,800 kg/m³. They have no color of their own; the varied coloration (gray, pink, red, green, black) is due to the presence of very fine inclusions of hematite, iron hydroxides, hornblende, pyroxene, and other minerals; the bluish green color of amazonite and the green color of microcline are associated with the electron center of Pb, substituting for K. Bands of Pb²⁺, Fe³⁺, Ce³⁺, and Eu²⁺ are distinguished in the luminescence spectra of feldspars. Electron paramagnetic resonance spectra of feldspars are used to determine the electron centers Ti³⁺ and the hole centers Al—O^-—A1, formed through the entrapment of an electron or hole, respectively, by lattice defects.

Feldspars serve as the basis for rock classification. The most important types of rocks are chiefly composed of feldspars: (1) intrusive rocks—granites, syenites (alkali feldspars and plagioclases), gabbros, and diorites (plagioclases); (2) effusive rocks—andesites and basalts; and (3) metamorphic rocks—gneiss, crystalline schists, contact- and regional-metamorphosed rocks, and pegmatites. In sedimentary rocks, feldspars occur as fragmented grains and new formations (authigenic feldspars). Only plagioclases are present in lunar rocks (lunar basalts, gabbros, anorthosites).

Because of the wide variations in composition and properties, feldspars are valuable in the geological and petrographie studies of magmatic and metamorphic rock masses. The isotope ^40.K/⁴⁰Ar ratio of anorthoclases is used to determine the absolute age of rocks.

Alkali feldspars in pegmatites and small-veined rocks are used in the production of ceramics, glass, porcelain, and faience. Feldspar rocks (labradorites) are used as facing material. Amazonite and moonstone (iridescent oligoclase) are decorative stones.

REFERENCES

Deer, W. A., R. A. Howie, and J. Zussmann. Porodoobrazu-iushchie mineraly, vol. 4. Moscow, 1966. (Translated from English.)
Marfunin, A. S. Polevye shpaty—fazovye vzaimootnosheniia, opticheskie svoistva, geologicheskoe raspredelenie. Moscow, 1962.

A. S. MARFUNIN

The Great Soviet Encyclopedia, 3rd Edition (1970-1979). © 2010 The Gale Group, Inc. All rights reserved.