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3.5: Non-Silicate Minerals

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    6856
  • The crystal structure of non-silicate minerals (see table) does not contain silica-oxygen tetrahedra. Many non-silicate minerals are economically important and provide metallic resources such as copper, lead, and iron. They also include valuable non-metallic products such as salt, construction materials, and fertilizer.

    Mineral Group Examples Formula Uses
    Native elements gold, silver, copper Au, Ag, Cu Jewelry, coins, industry
    Carbonates calcite, dolomite CaCO3, CaMg(CO3)2 Lime, Portland cement
    Oxides hematite, magnetite, bauxite Fe2O3, Fe3O4, a mixture of aluminum oxides Ores of iron & aluminum, pigments
    Halides halite, sylvite NaCl, KCl Table salt, fertilizer
    Sulfides galena, chalcopyrite, cinnabar PbS, CuFeS2, HgS Ores of lead, copper, mercury
    Sulphates gypsum, epsom salts CaSo4·2H2O, MgSO4·7H2O Sheetrock, therapeutic soak
    Phosphates apatite Ca5(PO4)3(F,Cl,OH) Fertilizer, teeth, bones

    Common non-silicate mineral groups.

    3.4.1: Carbonates

    Calcite crystal in a shape called a rhomb like a cube squahed over toward one corner
    Figure: Calcite crystal in shape of rhomb. Note the double-refracted word “calcite” in the center of the figure due to birefringence.
    Piece of limestone rock full of small fossils
    Figure: Limestone full of small fossils

    Calcite (CaCO3) and dolomite (CaMg(CO3)2) are the two most frequently occurring carbonate minerals, and usually occur in sedimentary rocks, such as limestone and dolostone rocks, respectively. Some carbonate rocks, such as calcite and dolomite, are formed via evaporation and precipitation. However, most carbonate-rich rocks, such as limestone, are created by the lithification of fossilized marine organisms. These organisms, including those we can see and many microscopic organisms, have shells or exoskeletons consisting of calcium carbonate (CaCO3). When these organisms die, their remains accumulate on the floor of the water body in which they live and the soft body parts decompose and dissolve away. The calcium carbonate hard parts become included in the sediments, eventually becoming the sedimentary rock called limestone. While limestone may contain large, easy to see fossils, most limestones contain the remains of microscopic creatures and thus originate from biological processes.

    Calcite crystal polarize light into two waves that vibrate at right angles to each other and pass through the crystal in different paths.
    Figure: Birefringence in calcite crystals

    Calcite crystals show an interesting property called birefringence, meaning they polarize light into two wave components vibrating at right angles to each other. As the two light waves pass through the crystal, they travel at different velocities and are separated by refraction into two different travel paths. In other words, the crystal produces a double image of objects viewed through it. Because they polarize light, calcite crystals are used in special petrographic microscopes for studying minerals and rocks.

    Many non-silicate minerals are referred to as salts. The term salts used here refers to compounds made by replacing the hydrogen in natural acids. The most abundant natural acid is carbonic acid that forms by the solution of carbon dioxide in water. Carbonate minerals are salts built around the carbonate ion (CO3-2) where calcium and/or magnesium replace the hydrogen in carbonic acid (H2CO3). Calcite and closely-related polymorph aragonite are secreted by organisms to form shells and physical structures like corals. Many such creatures draw both calcium and carbonate from dissolved bicarbonate ions (HCO3) in ocean water. As seen in the mineral identification section below, calcite is easily dissolved in acid and thus effervesces in dilute hydrochloric acid (HCl). Small dropper bottles of dilute hydrochloric acid are often carried by geologists in the field as well as used in mineral identification labs.

    Other salts include halite (NaCl) in which sodium replaces the hydrogen in hydrochloric acid and gypsum (Ca[SO4] • 2 H2O) in which calcium replaces the hydrogen in sulfuric acid. Note that some water molecules are also included in the gypsum crystal. Salts are often formed by evaporation and are called evaporite minerals.

    Crystal structure of calcite showing the carbonate units of carbon surrounded by three oxygen ions and bonded above and below to two calcium ions.
    Figure: Crystal structure of calcite

    The figure shows the crystal structure of calcite (CaCO3). Like silicon, carbon has four valence electrons. The carbonate unit consists of carbon atoms (tiny white dots) covalently bonded to three oxygen atoms (red), one oxygen sharing two valence electrons with the carbon and the other two sharing one valence electron each with the carbon, thus creating triangular units with a charge of -2. The negatively charged carbonate unit forms an ionic bond with the Ca ion (blue), which as a charge of +2.

    3.4.2: Oxides, Halides, and Sulfides

    Image of limonite, a hydrated oxide of iron
    Figure: Limonite, hydrated oxide of iron

    After carbonates, the next most common non-silicate minerals are the oxides, halides, and sulfides.

    Oxides consist of metal ions covalently bonded with oxygen. The most familiar oxide is rust, which is a combination of iron oxides (Fe2O3) and hydrated oxides. Hydrated oxides form when the iron is exposed to oxygen and water. Iron oxides are important for producing metallic iron. When iron oxide or ore is smelted, it produces carbon dioxide (CO2) and metallic iron.

    The red color in rocks is usually due to the presence of iron oxides. For example, the red sandstone cliffs in Zion National Park and throughout Southern Utah consist of white or colorless grains of quartz coated with iron oxide which serve as cementing agents holding the grains together.

    A red form of hematite called oolitic showing a mass of small round nodules
    Figure: Oolitic hematite

    Other iron oxides include limonite, magnetite, and hematite. Hematite occurs in many different crystal forms. The massive form shows no external structure. Botryoidal hematite shows large concentric blobs. Specular hematite looks like a mass of shiny metallic crystals. Oolitic hematite looks like a mass of dull red fish eggs. These different forms of hematite are polymorphs and all have the same formula, Fe2O3.

    Other common oxide minerals include:

    • Ice (H2O), an oxide of hydrogen
    • Bauxite (Al2H2O4), hydrated oxides of aluminum, an ore for producing metallic aluminum
    • Corundum (Al2O3), which includes ruby and sapphire gemstones.
    Crystals of halite showing cubic crystal habit
    Figure: Halite crystal showing cubic habit

    The halides consist of halogens in column VII, usually fluorine or chlorine, ionically bonded with sodium or other cations. These include halite or sodium chloride (NaCl), common table salt; sylvite or potassium chloride (KCl); and fluorite or calcium fluoride (CaF2).

    Photo of salt crust at the Bonneville Salt Flats in Utah with mountains in the background.
    Figure: Salt crystals at the Bonneville Salt Flats
    Purplish crystals of fluorite. The second image shows the deep blue fluorescence of fluorite under ultraviolet light.
    Figure: Fluorite. B shows fluorescence of fluorite under UV light

    Halide minerals usually form from the evaporation of seawater or other isolated bodies of water. A well-known example of halide mineral deposits created by evaporation is the Bonneville Salt Flats, located west of the Great Salt Lake in Utah (see figure).

    Cubic crystals of iron pyrite, called "fools gold"
    Figure: Cubic crystals of pyrite

    Many important metal ores are sulfides, in which metals are bonded to sulfur. Significant examples include galena (lead sulfide), sphalerite (zinc sulfide), pyrite (iron sulfide, sometimes called “fool’s gold”), and chalcopyrite (iron-copper sulfide). Sulfides are well known for being important ore minerals. For example, galena is the main source of lead, sphalerite is the main source of zinc, and chalcopyrite is the main copper ore mineral mined in porphyry deposits like the Bingham mine (see chapter 16). The largest sources of nickel, antimony, molybdenum, arsenic, and mercury are also sulfides.

    3.4.3: Sulfates

    A clear crystal of gypsum
    Figure: Gypsum crystal

    Sulfate minerals contain a metal ion, such as calcium, bonded to a sulfate ion. The sulfate ion is a combination of sulfur and oxygen (SO42). The sulfate mineral gypsum (CaSO4ᐧ2H2O) is used in construction materials such as plaster and drywall. Gypsum is often formed from evaporating water and usually contains water molecules in its crystalline structure. The ᐧ2H2O in the formula indicates the water molecules are whole H2O. This is different from minerals like amphibole, which contain a hydroxide ion (OH) that is derived from water but is missing a hydrogen ion (H+). The calcium sulfate without water is a different mineral than gypsum called anhydrite (CaSO4).

    3.4.4: Phosphates

    A crystal of apatite
    Figure: Apatite crystal

    Phosphate minerals have a tetrahedral phosphate unit (PO4-3) combined with various anions and cations. In some cases arsenic or vanadium can substitute for phosphorus. Phosphates are an important ingredient of fertilizers as well as detergents, paint, and other products. The best known phosphate mineral is apatite, Ca5(PO4)3(F,Cl,OH), variations of which are found in teeth and bones. The gemstone turquoise [CuAl6(PO4)4(OH)8·4H2O ] is a copper-rich phosphate mineral that, like gypsum, contains water molecules.

    3.4.5: Native Element Minerals

    Metallic native copper
    Figure: Native copper
    Native sulfur deposited around the vent of a volcanic fumarole
    Figure: Native sulfur deposited around a volcanic fumarole

    Native element minerals, usually metals, occur in nature in a pure or nearly pure state. Gold is an example of a native element mineral; it is not very reactive and rarely bonds with other elements so it is usually found in an isolated or pure state. The non-metallic and poorly-reactive mineral carbon is often found as a native element, such as graphite and diamonds. Mildly reactive metals like silver, copper, platinum, mercury, and sulfur sometimes occur as native element minerals. Reactive metals such as iron, lead, and aluminum almost always bond to other elements and are rarely found in a native state.