Most olivine found at Earth’s surface is in dark-colored igneous rocks. It usually crystallizes in the presence of plagioclase and pyroxene to form gabbro or basalt. These types of rocks are most common at divergent plate boundaries and at hot spots within the centers of tectonic plates.
Olivine has a very high crystallization temperature compared to other minerals. That makes it one of the first minerals to crystallize from a magma. During the slow cooling of a magma, crystals of this mineral may form and then settle to the bottom of the magma chamber because of their relatively high density. This concentrated accumulation of this mineral can result in the formation of olivine-rich rocks such as dunite in the lower parts of a magma chamber.
Crystals of this mineral are sometimes formed during the metamorphism of a dolomitic limestone or dolomite. The dolomite contributes magnesium, and silica is obtained from quartz and other impurities in the limestone. When olivine is metamorphosed, it is transformed into serpentine.
This mineral is one of the first minerals to be altered by weathering. Because it is so easily altered by weathering and its not a common mineral in sedimentary rocks and is only an abundant constituent of sand or sediment when the deposit is very close to the source.
Olivine is the name given to a group of silicate minerals that have a generalized chemical composition of A2SiO4. In that generalized composition, “A” is usually Mg or Fe, but in unusual situations can be Ca, Mn, or Ni.
The chemical composition of most olivine falls somewhere between pure forsterite (Mg2SiO4) and pure fayalite (Fe2SiO4). In that series, Mg and Fe can substitute freely for one another in the mineral’s atomic structure – in any ratio. This type of continuous compositional variation is known as a “solid solution” and is represented in a chemical formula as (Mg,Fe)2SiO4.
The name “olivine” is used instead of “forsterite” or “fayalite” because a chemical analysis or other detailed testing is needed to determine which one is dominant – if either is dominant. The name “olivine” serves as a quick, convenient, and inexpensive way to put a name on the material. A list of the more common mineral derivatives of and their composition is given in the table below.
Olivine receives its name from its usual olive-green color. Many geology students remember the color of olivine by using a rhyme: “olivine is green.” That rhyme is true with most classroom specimens; however, there are rare iron-rich olivines (fayalites) that are brownish in color.
Olivine in Earth’s Mantle
Olivine is thought to be an important mineral in Earth’s mantle. Its presence as a mantle mineral has been inferred by a change in the behavior of seismic waves as they cross the Moho – the boundary between Earth’s crust and mantle.
The presence of this mineral in Earth’s interior is also confirmed by the presence of olivine in xenoliths, which are thought to be pieces of the upper mantle delivered to Earth’s surface in the magmas of deep-source volcanic eruptions. Olivine is also an abundant mineral in the lower portion of many ophiolites. These are slabs of oceanic crust (with part of the upper mantle attached) that have been thrust up onto an island or a continent.
Physical Properties of Olivine
|Color||Usually olive green, but can be yellow-green to bright green; iron-rich specimens are brownish green to brown|
|Diaphaneity||Transparent to translucent|
|Cleavage||Poor cleavage, brittle with conchoidal fracture|
|Mohs Hardness||6.5 to 7|
|Specific Gravity||3.2 to 4.4|
|Diagnostic Properties||Green color, vitreous luster, conchoidal fracture, granular texture|
|Chemical Composition||Typically (Mg, Fe)2SiO4. Ca, Mn, and Ni rarely occupy the Mg and Fe positions.|
|Uses||Gemstones, a declining use in bricks and refractory sand|
Olivine is usually green in color but can also be yellow-green, greenish yellow, or brown. It is transparent to translucent with a glassy luster and a hardness between 6.5 and 7.0. It is the only common igneous mineral with these properties. The properties of olivine are summarized in the table.
Olivine has been identified in a large number of stony and stony-iron meteorites. These meteorites are thought to have originated from the mantle of a rocky planet that used to occupy an orbit between Mars and Jupiter – or they might be from an asteroid that was large enough to have developed a differentiated internal structure consisting of a rock mantle and a metallic core.
Pallasites are thought to represent the part of an asteroid or planet that was near the mantle-core boundary where rocky materials of the mantle were mixed with the metallic materials of the core. Pallasites typically have distinct crystals of olivine (usually fayalite) surrounded by a nickel-iron matrix. A photograph of a slice from a pallasite meteorite is shown on this page.
Olivine Rain on a Developing Star
In 2011, NASA’s Spitzer Space Telescope observed what is believed to have been tiny crystals of olivine falling like rain through the dusty cloud of gas of a developing star. This “olivine rain” was thought to have occurred as strong air currents lifted newly crystallized particles of olivine from the surface of the forming star, high into its atmosphere, and then dropped them when the currents lost their momentum. The result was a rain of glittering green olivine crystals.
Uses of Olivine
Olivine is a mineral that is not often used in industry. This mineral is used in metallurgical processes as a slag conditioner. High-magnesium olivine (forsterite) is added to blast furnaces to remove impurities from steel and to form a slag.
This mineral has also been used as a refractory material. It is used to make refractory brick and used as a casting sand. Both of these uses are in decline as alternative materials are less expensive and easier to obtain.
Olivine and the Gemstone Peridot
Olivine is also the mineral of the gemstone known as “peridot.” It is a yellow-green to green gemstone that is very popular in jewelry. Peridot serves as a birthstone for the month of August. The most valued colors are dark olive green and a bright lime green. These specimens are of the mineral forsterite because the iron-rich fayalite is usually a brownish, less desirable color.
Much of the world’s peridot used in mass-production jewelry is mined at the San Carlos Reservation in Arizona. There, a few basalt flows containing nodules of granular form of this mineral are the source of the peridot. Most of the stones produced there are a few carats or less in size and often contain visible crystals of chromite or other minerals. They are cut in Asia and returned to the United States in commercial jewelry.
Higher quality and larger peridot crystals are mined in Pakistan and Myanmar. There, crystals of this mineral are found in metamorphic rocks. These are usually found in association with serpentine or dolomitic marble.
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