Clinoptilolite is a zeolite, which makes it a member of the tectosilicate group. Zeolites are framework silicates in which all silica tetrahedra are completely polymerized with other silica or with atoms proxying for silicon in tetrahedral sites. One of the noteworthy features of zeolites is the large pores or channels that are formed within the structures. These channels are filled with water and with exchangeable cations to balance negative charges in the zeolite structural framework. Because of this porous structure and the substitution of Al³⁺ for Si⁴⁺ in the tetrahedral framework, clinoptilolite and other zeolites have significant cation exchange capacities (CEC), on the order of 100 to 300 cmol of charge per kg. As with most zeolites, however, exchange selectivity is restricted by channel size. Larger ions may be selectively excluded. These “ion sieving” properties of zeolites are important properties exploited in a number of industrial and other uses.

Cristobalite is a polymorph of quartz. It has the same composition, SiO2, but a different structure. It commonly forms at higher temperatures than quartz.

Sodalite is a member of the Feldspathoid group of the Tectosilicates. It has a composition of Na8Si6Al6O24Cl2 and is in the isometric crystal class. The structure of sodalite is interesting in that it is a silicate that contains a large accessory anion, in this case, chlorine. The silica tetrahedral backbone structure is such that it produces large cage-like cavities in which the Cl is housed.

Albite is classified as a Feldspar Group Tectosilicate and is the sodic end member of both the plagioclase (Na-Ca) and the alkali (Na-K) feldspar series. The plagioclase series ranges in chemical composition from pure NaAlSi3O8 to pure CaAl2Si2O8 (Anorthite) while the alkali series ranges from albite to orthoclase KAlSi3O8.

Albite is comprised of an interconnected framework of three SiO4 and one AlO4 tetrahedra, with all oxygens shared between tetrahedra. The remaining negative charge is balanced by Na+, which fills larger voids in the structure. The silicon to oxygen ratio is 1:2. The exact structure of albite changes based on the ordering of the Al within the framework. High albite (formed at high temperatures) is triclinic and has a highly disordered Al/Si ordering. A monoclinic variety known as monalbite with a totally disordered Al/Si distribution also is known. Low albite, which forms at lower temperatures, is highly ordered and has a triclinic (C_1) structure. Na+ fills no less than 90%, and K plus Ca no more than 10%, of available voids. Albite exhibits twinning which can be seen as grooves on both the crystal and cleavage surfaces.

Anorthite, CaAl2Si2O8, is classified as a plagioclase group feldspar tectosilicate, with 45 to 50% of the Si4+ in the tetrahedra framework substituted by Al3+. This large charge deficit is balanced mainly by the addition of Ca to the feldspar structure. Up to 10% of the Ca may be replaced by Na, in proportion to the total charge on the structure. Albite is the sodic end member of an isomorphous solid solution series, containing sodium and no calcium. Anorthite, the other end member, contains calcium and is one of the rarer members of the plagioclase series. The solid solution is not complete in that miscibility gaps exist. Anorthite exhibits a triclinic crystal system with prismatic structure.

Quartz has a formula unit composition of SiO₂ and is classified as a Tectosilicate. Alpha-quartz is the most common polymorph of the silica minerals. Other polymorphs include beta-quartz, tridymite, cristobalite, and silica glass, which has a short-range ordered structure.

All four oxygens in quartz are polymerized to additional silica groups; all silica tetrahedra are polymerized to four other tetrahedra. In its characteristic crystal form, quartz has a hexagonal structure.