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Clay is a type of soil or rock composed of very fine particles that are plastic when wet and coherent when dry. Learn about the formation, classification, and applications of clay in various industries, such as pottery, cement, paper, and drilling.
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clay mineral, any of a group of important hydrous aluminum silicates with a layer (sheetlike) structure and very small particle size. They may contain significant amounts of iron, alkali metals, or alkaline earths.
The term clay is generally applied to (1) a natural material with plastic properties, (2) particles of very fine size, customarily those defined as particles smaller than two micrometres (7.9 × 10−5 inch), and (3) very fine mineral fragments or particles composed mostly of hydrous-layer silicates of aluminum, though occasionally containing magnesium and iron. Although, in a broader sense, clay minerals can include virtually any mineral of the above-cited particle size, the definition adapted here is restricted to represent hydrous-layer silicates and some related short-range ordered aluminosilicates, both of which occur either exclusively or frequently in very fine-size grades.
The development of X-ray diffraction techniques in the 1920s and the subsequent improvement of microscopic and thermal procedures enabled investigators to establish that clays are composed of a few groups of crystalline minerals. The introduction of electron microscopic methods proved very useful in determining the characteristic shape and size of clay minerals. More recent analytical techniques such as infrared spectroscopy, neutron diffraction analysis, Mössbauer spectroscopy, and nuclear magnetic resonance spectroscopy have helped advance scientific knowledge of the crystal chemistry of these minerals.
Clay minerals are composed essentially of silica, alumina or magnesia or both, and water, but iron substitutes for aluminum and magnesium in varying degrees, and appreciable quantities of potassium, sodium, and calcium are frequently present as well. Some clay minerals may be expressed using ideal chemical formulas as the following: 2SiO2·Al2O3·2H2O (kaolinite), 4SiO2·Al2O3·H2O (pyrophyllite), 4SiO2·3MgO·H2O (talc), and 3SiO2·Al2O3·5FeO·4H2O (chamosite). The SiO2 ratio in a formula is the key factor determining clay mineral types. These minerals can be classified on the basis of variations of chemical composition and atomic structure into nine groups: (1) kaolin-serpentine (kaolinite, halloysite, lizardite, chrysotile), (2) pyrophyllite-talc, (3) mica (illite, glauconite, celadonite), (4) vermiculite, (5) smectite (montmorillonite, nontronite, saponite), (6) chlorite (sudoite, clinochlore, chamosite), (7) sepiolite-palygorskite, (8) interstratified clay minerals (e.g., rectorite, corrensite, tosudite), and (9) allophane-imogolite. Information and structural diagrams for these groups are given below.
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Kaolinite is derived from the commonly used name kaolin, which is a corruption of the Chinese Gaoling (Pinyin; Wade-Giles romanization Kao-ling), meaning “high ridge,” the name of a hill near Jingdezhen where the occurrence of the mineral is known as early as the 2nd century bce. Montmorillonite and nontronite are named after the localities Montmorillon and Nontron, respectively, in France, where these minerals were first reported. Celadonite is from the French céladon (meaning grayish yellow-green) in allusion to its colour. Because sepiolite is a light and porous material, its name is based on the Greek word for cuttlefish, the bone of which is similar in nature. The name saponite is derived from the Latin sapon (meaning soap), because of its appearance and cleaning ability. Vermiculite is from the Latin vermiculari (“to breed worms”), because of its physical characteristic of exfoliation upon heating, which causes the mineral to exhibit a spectacular volume change from small grains to long wormlike threads. Baileychlore, brindleyite, corrensite, sudoite, and tosudite are examples of clay minerals that were named after distinguished clay mineralogists—Sturges W. Bailey, George W. Brindley, Carl W. Correns, and Toshio Sudō, respectively.
The structure of clay minerals has been determined largely by X-ray diffraction methods. The essential features of hydrous-layer silicates were revealed by various scientists including Charles Mauguin, Linus C. Pauling, W.W. Jackson, J. West, and John W. Gruner through the late 1920s to mid-1930s. These features are continuous two-dimensional tetrahedral sheets of composition Si2O5, with SiO4 tetrahedrons (Figure 1) linked by the sharing of three corners of each tetrahedron to form a hexagonal mesh pattern (Figure 2A). Frequently, silicon atoms of the tetrahedrons are partially substituted for by aluminum and, to a lesser extent, ferric iron. The apical oxygen at the fourth corner of the tetrahedrons, which is usually directed normal to the sheet, forms part of an adjacent octahedral sheet in which octahedrons are linked by sharing edges (Figure 3). The junction plane between tetrahedral and octahedral sheets consists of the shared apical oxygen atoms of the tetrahedrons and unshared hydroxyls that lie at the centre of each hexagonal ring of tetrahedrons and at the same level as the shared apical oxygen atoms (Figure 4). Common cations that coordinate the octahedral sheets are Al, Mg, Fe3+, and Fe2+; occasionally Li, V, Cr, Mn, Ni, Cu, and Zn substitute in considerable amounts. If divalent cations (M2+) are in the octahedral sheets, the composition is M2+/3 (OH)2O4 and all the octahedrons are occupied. If there are trivalent cations (M3+), the composition is M3+/2 (OH)2O4 and two-thirds of the octahedrons are occupied, with the absence of the third octahedron. The former type of octahedral sheet is called trioctahedral, and the latter dioctahedral. If all the anion groups are hydroxyl ions in the compositions of octahedral sheets, the resulting sheets may be expressed by M2+(OH)2 and M3+(OH)3, respectively. Such sheets, called hydroxide sheets, occur singly, alternating with silicate layers in some clay minerals. Brucite, Mg(OH)2, and gibbsite, Al(OH)3, are typical examples of minerals having similar structures. There are two major types for the structural “backbones” of clay minerals called silicate layers. The unit silicate layer formed by aligning one octahedral sheet to one tetrahedral sheet is referred to as a 1:1 silicate layer, and the exposed surface of the octahedral sheet consists of hydroxyls. In another type, the unit silicate layer consists of one octahedral sheet sandwiched by two tetrahedral sheets that are oriented in opposite directions and is termed a 2:1 silicate layer (Figure 5). These structural features, however, are limited to idealized geometric arrangements.
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Real structures of clay minerals contain substantial crystal strains and distortions, which produce irregularities such as deformed octahedrons and tetrahedrons rather than polyhedrons with equilateral triangle faces, ditrigonal symmetry modified from the ideal hexagonal surface symmetry, and puckered surfaces instead of the flat planes made up by the basal oxygen atoms of the tetrahedral sheet. One of the major causes of such distortions is dimensional “misfits” between the tetrahedral and octahedral sheets. If the tetrahedral sheet contains only silicon in the cationic site and has an ideal hexagonal symmetry, the longer unit dimension within the basal plane is 9.15 Å, which lies between the corresponding dimensions 8.6 Å of gibbsite and 9.4 Å of brucite. To fit the tetrahedral sheet into the dimension of the octahedral sheet, alternate SiO4 tetrahedrons rotate (up to a theoretical maximum of 30°) in opposite directions to distort the ideal hexagonal array into a doubly triangular (ditrigonal) array (Figure 2B). By this distortion mechanism, tetrahedral and octahedral sheets of a wide range of compositions resulting from ionic substitutions can link together and maintain silicate layers. Among ionic substitutions, those between ions of distinctly different sizes most significantly affect geometric configurations of silicate layers.
Learn about clay minerals, a group of hydrous aluminum silicates with a layer (sheetlike) structure and very small particle size. Find out how they are classified, composed, and used in various fields of science and industry.
Clay is a type of fine-grained natural soil material containing clay minerals (hydrous aluminium phyllosilicates, e.g. kaolinite, Al 2 Si 2 O 5 4). Most pure clay minerals are white or light-coloured, but natural clays show a variety of colours from impurities, such as a reddish or brownish colour from small amounts of iron oxide.
Learn the meaning, synonyms, examples, and history of the word clay, an earthy material used for various purposes. Find out how to pronounce clay and its related phrases and words.
May 1, 2023 · Learn about clay minerals, a group of hydrous aluminosilicates that are formed from the weathering and alteration of silicate minerals. Discover their chemical composition, structure, types, formation, properties, uses, and importance in soil science, industry, and environment.
Apr 27, 2021 · This video covers where clay comes from (geology), what clay is (chemistry and mineralogy), and what makes it such a special material (biology, genetics, and chemistry).
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