Silicate minerals are rock-forming made up of silicate groups. They are the largest and most important class of minerals and make up approximately 90 percent of Earth's crust.
In mineralogy, the crystalline forms of silica () are usually considered to be tectosilicates, and they are classified as such in the Dana system (75.1). However, the Nickel-Strunz system classifies them as (4.DA). Silica is found in nature as the mineral quartz and its polymorphs.
On Earth, a wide variety of silicate minerals occur in an even wider range of combinations as a result of the processes that have been forming and re-working the crust for billions of years. These processes include partial melting, crystallization, fractionation, metamorphism, weathering, and diagenesis.
Living organisms also contribute to this geologic cycle. For example, a type of plankton known as construct their ("frustules") from silica extracted from seawater. The frustules of dead diatoms are a major constituent of deep ocean sediment, and of diatomaceous earth.
General structure
A silicate mineral is generally an inorganic compound consisting of subunits with the formula SiO
2+ n2 n−. Although depicted as such, the description of silicates as anions is a simplification. Balancing the charges of the silicate anions are metal cations, M
x+. Typical cations are Mg
2+, Fe
2+, and Na
+. The Si-O-M linkage between the silicates and the metals are strong, polar-covalent bonds. Silicate anions (SiO
2+ n2 n−) are invariably colorless, or when crushed to a fine powder, white. The colors of silicate minerals arise from the metal component, commonly iron.
In most silicate minerals, silicon is tetrahedral, being surrounded by four oxides. The coordination number of the oxides is variable except when it bridges two silicon centers, in which case the oxide has a coordination number of two.
Some silicon centers may be replaced by atoms of other elements, still bound to the four corner oxygen corners. If the substituted atom is not normally tetravalent, it usually contributes extra charge to the anion, which then requires extra . For example, in the mineral orthoclase , the anion is a tridimensional network of tetrahedra in which all oxygen corners are shared. If all tetrahedra had silicon centers, the anion would be just neutral silica . Replacement of one in every four silicon atoms by an aluminum atom results in the anion , whose charge is neutralized by the potassium cations .
Main groups
In
mineralogy, silicate minerals are classified into seven major groups according to the structure of their silicate anion:
[Deer, W.A.; Howie, R.A., & Zussman, J. (1992). An introduction to the rock forming minerals (2nd edition ed.). London: Longman ][Hurlbut, Cornelius S.; Klein, Cornelis ||1985). Manual of Mineralogy, Wiley, (20th edition ed.). ]
Tectosilicates can only have additional cations if some of the silicon is replaced by an atom of lower valence such as aluminum. Al for Si substitution is common.
Nesosilicates or orthosilicates
Nesosilicates (from Greek 'island'), or orthosilicates, have the orthosilicate ion, present as isolated (insular) tetrahedra connected only by interstitial
. The Nickel–Strunz classification is 09.A –examples include:
Sorosilicates
Sorosilicates (from Greek 'heap, mound') have isolated
pyrosilicate anions , consisting of double tetrahedra with a shared oxygen vertex—a silicon:oxygen ratio of 2:7. The Nickel–Strunz classification is 09.B. Examples include:
Cyclosilicates
Cyclosilicates (from Greek 'circle'), or ring silicates, have three or more tetrahedra linked in a ring. The general formula is (Si
xO
3 x)
2 x−, where one or more silicon atoms can be replaced by other 4-coordinated atom(s). The silicon:oxygen ratio is 1:3. Double rings have the formula (Si
2 xO
5 x)
2 x− or a 2:5 ratio. The Nickel–Strunz classification is 09.C. Possible ring sizes include:
(red: Si, blue: O)]]
]]
]]
]]
]]
Some example minerals are:
-
3-member single ring
-
4-member single ring
-
6-member single ring
-
9-member single ring
-
6-member double ring
The ring in axinite contains two B and four Si tetrahedra and is highly distorted compared to the other 6-member ring cyclosilicates.
Inosilicates
Inosilicates (from Greek genitive: 'fibre'), or chain silicates, have interlocking chains of
silicon tetrahedra with either , 1:3 ratio, for single chains or , 4:11 ratio, for double chains. The Nickel–Strunz classification is 09.D – examples include:
Single chain inosilicates
Double chain inosilicates
Phyllosilicates
Phyllosilicates (from Greek 'leaf'), or sheet silicates, form parallel sheets of silicate tetrahedra with or a 2:5 ratio. The Nickel–Strunz classification is 09.E. All phyllosilicate minerals are
, with either
water or
hydroxyl groups attached. Many phyllosilicates are clay-forming and may be further classified as 1:1 clay minerals (one tetrahedral sheet and one octahedral sheet) and 2:1 clay minerals (one octahedral sheet between two tetrahedral sheets). Below is a list of phyllosilicate minerals and their chemical formulas, organized by mineralogical group:
(red: Si, blue: O)]]
-(KF)-apophyllite-(KOH) series]]
-(Fe)-pyrosmalite-(Mn) series]]
]]
]]
Tectosilicates
Tectosilicates, or "framework silicates," have a three-dimensional framework of silicate
tetrahedra with in a 1:2 ratio. This group comprises nearly 75% of the crust of the
Earth.
Tectosilicates, with the exception of the quartz group, are
. The Nickel–Strunz classifications are 9.F (tectosilicates without zeolitic ), 9.G (tectosilicates with zeolitic ), and 4.DA (quartz/silica group). Below is a list of the tectosilicate mineral species that currently have articles on Wikipedia, with their chemical formulas and important varieties:
See also
External links
