Editing Mineral (section)

====Phyllosilicates====
[[File:Muscovite-Albite-122886.jpg|right|upright=1.15|thumb|Muscovite, a mineral species in the mica group, within the phyllosilicate subclass]]
Phyllosilicates consist of sheets of polymerized tetrahedra. They are bound at three oxygen sites, which gives a characteristic silicon:oxygen ratio of 2:5. Important examples include the [[mica]], [[Chlorite group|chlorite]], and the [[kaolinite]]-[[Serpentine group|serpentine]] groups. In addition to the tetrahedra, phyllosilicates have a sheet of octahedra (elements in six-fold coordination by oxygen) that balance out the basic tetrahedra, which have a negative charge (e.g. [Si<sub>4</sub>O<sub>10</sub>]<sup>4−</sup>) These tetrahedra (T) and octahedra (O) sheets are stacked in a variety of combinations to create phyllosilicate layers. Within an octahedral sheet, there are three octahedral sites in a unit structure; however, not all of the sites may be occupied. In that case, the mineral is termed dioctahedral, whereas in other case it is termed trioctahedral.<ref>{{harvnb|Dyar|Gunter|2008}}, p. 110</ref> The layers are weakly bound by [[van der Waals forces]], [[hydrogen bond]]s, or sparse [[ionic bond]]s, which causes a crystallographic weakness, in turn leading to a prominent basal cleavage among the phyllosilicates.<ref>{{harvnb|Chesterman|Lowe|2008}}, p. 525</ref>

The kaolinite-serpentine group consists of T-O stacks (the 1:1 clay minerals); their hardness ranges from 2 to 4, as the sheets are held by hydrogen bonds. The 2:1 clay minerals (pyrophyllite-talc) consist of T-O-T stacks, but they are softer (hardness from 1 to 2), as they are instead held together by van der Waals forces. These two groups of minerals are subgrouped by octahedral occupation; specifically, kaolinite and pyrophyllite are dioctahedral whereas serpentine and talc trioctahedral.<ref>{{harvnb|Dyar|Gunter|2008}}, pp. 110–13</ref>

Micas are also T-O-T-stacked phyllosilicates, but differ from the other T-O-T and T-O-stacked subclass members in that they incorporate aluminium into the tetrahedral sheets (clay minerals have Al<sup>3+</sup> in octahedral sites). Common examples of micas are [[muscovite]], and the [[biotite]] series. Mica T-O-T layers are bonded together by metal ions, giving them a greater hardness than other phyllosilicate minerals, though they retain perfect basal cleavage.{{sfn|Nesse|2000|p=238}} The chlorite group is related to mica group, but a [[brucite]]-like (Mg(OH)<sub>2</sub>) layer between the T-O-T stacks.<ref>{{harvnb|Dyar|Gunter|2008}}, pp. 602–05</ref>

Because of their chemical structure, phyllosilicates typically have flexible, elastic, transparent layers that are electrical insulators and can be split into very thin flakes. Micas can be used in electronics as insulators, in construction, as optical filler, or even cosmetics. Chrysotile, a species of serpentine, is the most common mineral species in industrial asbestos, as it is less dangerous in terms of health than the amphibole asbestos.<ref>{{harvnb|Dyar|Gunter|2008}}, pp. 593–95</ref>