Biotite

Biotite is a common group of phyllosilicate minerals within the mica group, with the approximate chemical formula Template:Chem2. It is primarily a solid-solution series between the iron-endmember annite, and the magnesium-endmember phlogopite; more aluminous end-members include siderophyllite and eastonite. Biotite was regarded as a mineral species by the International Mineralogical Association until 1998, when its status was changed to a mineral group.<ref name="Minerals_Net">{{#invoke:citation/CS1|citation |CitationClass=web }}</ref><ref>{{#invoke:citation/CS1|citation |CitationClass=web }}</ref> The term biotite is still used to describe unanalysed dark micas in the field. Biotite was named by J.F.L. Hausmann in 1847 in honor of the French physicist Jean-Baptiste Biot, who performed early research into the many optical properties of mica.<ref>Template:Cite book "Zur Bezeichnung des sogenannten einachsigen Glimmers ist hier der Name Biotit gewählt worden, um daran zu erinnern, daß Biot es war, der zuerst auf die optische Verschiedenheit der Glimmerarten aufmerksam machte." (For the designation of so-called uniaxial mica, the name "biotite" has been chosen in order to recall that it was Biot who first called attention to the optical differences between types of mica.)</ref>

Members of the biotite group are sheet silicates. Iron, magnesium, aluminium, silicon, oxygen, and hydrogen form sheets that are weakly bound together by potassium ions. The term "iron mica" is sometimes used for iron-rich biotite, but the term also refers to a flaky micaceous form of haematite, and the field term Lepidomelane for unanalysed iron-rich Biotite avoids this ambiguity. Biotite is also sometimes called "black mica" as opposed to "white mica" (muscovite) – both may form in the same rocks, and in some instances side by side.

Properties

Like other mica minerals, biotite has a highly perfect basal cleavage, and consists of flexible sheets, or lamellae, which easily flake off. It has a monoclinic crystal system, with tabular to prismatic crystals with an obvious pinacoid termination. It has four prism faces and two pinacoid faces to form a pseudohexagonal crystal. Although not easily seen because of the cleavage and sheets, fracture is uneven. It appears greenish to brown or black, and even yellow when weathered. It can be transparent to opaque, has a vitreous to pearly luster, and a grey-white streak. When biotite crystals are found in large chunks, they are called "books" because they resemble books with pages of many sheets. The color of biotite is usually black and the mineral has a hardness of 2.5–3 on the Mohs scale of mineral hardness.

Biotite dissolves in both acid and alkaline aqueous solutions, with the highest dissolution rates at low pH.<ref>Template:Cite journal</ref> However, biotite dissolution is highly anisotropic with crystal edge surfaces (h k0) reacting 45 to 132 times faster than basal surfaces (001).<ref>Template:Cite journal</ref><ref>Template:Cite journal</ref>

• Biotite mica 2 (31739438210).jpg

  Flaky biotite sheets.

• BiotitaEZ.jpg

  Thick biotite sample featuring many sheets.

• Biotite1.jpg

  Biotite crystal exhibiting pseudohexagonal shape.

Optical properties

In thin section, biotite exhibits moderate relief and a pale to deep greenish brown or brown color, with moderate to strong pleochroism. Biotite has a high birefringence which can be partially masked by its deep intrinsic color.<ref name="min-in-thin">{{#invoke:citation/CS1|citation |CitationClass=web }}</ref> Under cross-polarized light, biotite exhibits extinction approximately parallel to cleavage lines, and can have characteristic bird's eye maple extinction, a mottled appearance caused by the distortion of the mineral's flexible lamellae during grinding of the thin section. Basal sections of biotite in thin section are typically approximately hexagonal in shape and usually appear isotropic under cross-polarized light.<ref name="min-rock-sec">Template:Cite book</ref>

• Muscovite and Biotite2a.jpg

  Biotite (in brown) and muscovite in an orthogneiss thin section under plane-polarized light.

• Thin Section of Biotite (test) (cropped to Biotite).jpg

  Biotite in thin section under cross-polarized light.

• Sagenitic biotite.JPG

  Basal section of biotite, with needle-like rutile inclusions, in thin section under plane-polarized light.

Structure

Like other micas, biotite has a crystal structure described as TOT-c, meaning that it is composed of parallel TOT layers weakly bonded to each other by cations (c). The TOT layers in turn consist of two tetrahedral sheets (T) strongly bonded to the two faces of a single octahedral sheet (O). It is the relatively weak ionic bonding between TOT layers that gives biotite its perfect basal cleavage.Template:Sfn

The tetrahedral sheets consist of silica tetrahedra, which are silicon ions surrounded by four oxygen ions. In biotite, one in four silicon ions is replaced by an aluminium ion. The tetrahedra each share three of their four oxygen ions with neighboring tetrahedra to produce a hexagonal sheet. The remaining oxygen ion (the apical oxygen ion) is available to bond with the octahedral sheet.Template:Sfn

The octahedral sheet in biotite is a trioctahedral sheet having the structure of a sheet of the mineral brucite, with magnesium or ferrous iron being the usual cations. Apical oxygens take the place of some of the hydroxyl ions that would be present in a brucite sheet, bonding the tetrahedral sheets tightly to the octahedral sheet.Template:Sfn

Tetrahedral sheets have a strong negative charge, since their bulk composition is AlSi₃O₁₀^5-. The trioctahedral sheet has a positive charge, since its bulk composition is M₃(OH)₂⁴⁺ (M represents a divalent ion such as ferrous iron or magnesium) The combined TOT layer has a residual negative charge, since its bulk composition is M₃(AlSi₃O₁₀)(OH)₂⁻. The remaining negative charge of the TOT layer is neutralized by the interlayer potassium ions.Template:Sfn

Because the hexagons in the T and O sheets are slightly different in size, the sheets are slightly distorted when they bond into a TOT layer. This breaks the hexagonal symmetry and reduces it to monoclinic symmetry. However, the original hexahedral symmetry is discernible in the pseudohexagonal character of biotite crystals.

• Mica T.png

  View of tetrahedral sheet structure of biotite. The apical oxygen ions are tinted pink.

• Mica tO.png

  View of trioctahedral sheet structure of biotite. The binding sites for apical oxygen are shown as white spheres. Red spheres are hydroxide ions.

• Mica tOs.png

  View of trioctahedral sheet structure of mica emphasizing magnesium or iron sites

• Mica tri.png

  View of biotite structure looking at surface of a single layer

• Mica tri side.png

  View of biotite structure looking along sheets

Occurrence

Members of the biotite group are found in a wide variety of igneous and metamorphic rocks. For instance, biotite occurs in the lava of Mount Vesuvius and in the Monzoni intrusive complex of the western Dolomites. Biotite in granite tends to be poorer in magnesium than the biotite found in its volcanic equivalent, rhyolite.<ref name="CTV74">Template:Cite book</ref> Biotite is an essential phenocryst in some varieties of lamprophyre. Biotite is occasionally found in large cleavable crystals, especially in pegmatite veins, as in New England, Virginia and North Carolina USA. Other notable occurrences include Bancroft and Sudbury, Ontario Canada. It is an essential constituent of many metamorphic schists, and it forms in suitable compositions over a wide range of pressure and temperature. It has been estimated that biotite comprises up to 7% of the exposed continental crust.<ref>Template:Cite journal</ref>

An igneous rock composed almost entirely of dark mica (biotite or phlogopite) is known as a glimmerite or biotitite.<ref name="glimmerite">Template:Cite journal</ref>

Biotite may be found in association with its common alteration product chlorite.<ref name="min-rock-sec"/>

The largest documented single crystals of biotite were approximately Template:Convert sheets found in Iveland, Norway.<ref>Template:Cite journal</ref>

• Biotite Granite student sample.jpg

  Biotite-bearing granite samples (small black minerals).

• Biotite Gneiss.JPG

  Biotite-bearing gneiss sample.

• Biotite and chlorite gneiss mg 7971.jpg

  Gneiss sample bearing biotite and chlorite (green), a common alteration product of biotite.

• Sheet mica, Namibia.jpg

  Glimmerite from Namibia.

Uses

Biotite is used extensively to constrain ages of rocks, by either potassium-argon dating or argon–argon dating. Because argon escapes readily from the biotite crystal structure at high temperatures, these methods may provide only minimum ages for many rocks. Biotite is also useful in assessing temperature histories of metamorphic rocks, because the partitioning of iron and magnesium between biotite and garnet is sensitive to temperature.

Bibliography

• Template:Cite book