Forsterite (Olivine) - Mineral Properties, Photos and Occurence

Author: Vic Ridgley
Published: 24.02.2019 03:28
Last updated: 26.01.2021 10:29

Olivine is the most common mineral on Earth and very important rock forming mineral. The common term olivine refers to olivine group minerals and to IMA valid mineral forsterite. This article will focus on forsterite, which is very popular gem and forms crystals popular among collectors.

Olivine Group Minerals

Olivine is the group name for the minerals with the generic formula X2SiO4. Olivine structure can accomodate various divalent cations: minerals of the olivine group include a common (ternary) solid-solution series, forsterite (Mg2SiO4) – fayalite (Fe2SiO4) – tephroite (Mn2SiO4). Much more rare are liebenbergite (Ni2SiO4), larnite (Ca2SiO4), kirschteinite (CaFeSiO4) and monticellite (CaMgSiO4).

Gemmy forsterite (peridot) crystals from Mogok, Myanmar
Gemmy forsterite (peridot) crystals from Mogok, Myanmar. Size of both aprox. 3 x 1.5 cm, photo: Albert Russ

Forsterite is the only common mineral from the olivine group, natural fayalite and tephroite are quite uncommon. Other minerals from the olivine group are explicitly rare. Actually, rock-forming olivine is one of the most common minerals on Earth, but most of it is located inside Earth's upper mantle (as peridotite rock), so we do not see it that much on the surface. Minerals of the forsterite-fayalite solid solution are also present in many meteorites.

Crystal Structure of Forsterite

The forsterite crystallizes in the orthorhombic system and belongs to the nesosilicates. Its structure consist of isolated SiO4 tetrahedrons. Majority of natural forsterites contains 10-25 % of fayalite (Fe2+) component, pure forsterite is rare. Most forsterites form compact granular masses, only few select localities produce large, euhedral, prismatic stubby crystals with wedge-shaped terminations and striations parallel to the direction of elongation.

Regular impurities include quite high amount of Fe, and significantly smaller amount of Ni, Co and Ca. The olivine structure contains two cation positions - usualy labeled as M1 and M2 - which are not exactly the same. This is the reason why some minerals of the olivine group have only limited miscibility and others form complete solid solutions.

Aggregate of the green forsterite grains from Lanzarote, Canary Islands, Spain
Typical aggregate of the forsterite grains from Lanzarote, Canary Islands, Spain. Size: 6 x 4 cm, photo: Albert Russ

Given the abundance of Mg and Fe in the upper mantle and crust, one might ask why the olivine series is so dominated by Mg, and not more equally apportioned between Mg and Fe. One apparent reason is the charge flexibility of Fe. To be accommodated in fayalite, iron must remain in its Fe2+ state. If it should be oxidized to Fe3+, it will no longer fit in the olivine (fayalite) lattice, and is functionally expelled from (or not incorporated in) that structure. By default, the concentration of Mg in olivine rises. Observations of eruptions at the Stromboli volcano in Italy have positively established that escaping gases were undergoing oxidation from Fe2+ to Fe3+, enriching the residual magma in Mg and giving rise to abundant forsterite in the cooling rock.


Forsterite (Mg2SiO4) has two polymorphs: wadsleyite and ringwoodite. Both are high-pressure forms, stable in the upper mantle of Earth, with wadsleyite considered stable at depths of 410 to 520 km, and ringwoodite stable at depths of 520 to 660 km.

Wadsleyite is identified as the expected phase transition of forsterite-bearing rocks impacted by a high-velocity meteorite impact, such as was found in the Peace River Meteorite in Alberta, Canada in 1963.

Green grain of gemmy forsterite in basalt from British Columbia, Canada
Big grain of gemmy forsterite in basalt hostrock from British Columbia, Canada. Photo: Philippe Belley

Ringwoodite, in addition to its Mg2SiO4 formula, is capable of incorporating abundant hydroxide (OH) ions in its crystal lattice, leading to speculation that the suspected large volume of ringwoodite in the upper mantle may contain as much as 3 times the water content of the world’s surface oceans.

Physical Properties of Forsterite

Forsterite colors include greenish-yellow, yellowish-green, olive green, light green, yellow-brown, brown and black. Whites, grays and oranges are rare. Pure forsterite, a rare species, is very light yellow or colorless. The

Forsterite is soluble in HCl, transparent to translucent, with perfect cleavage on {010} and imperfect cleavage on {100}, a vitreous to resinous/greasy luster, white streak, conchoidal fracture and a hardness of 6.5-7.0.

Green forsterite crystal from Sapat Gali, Mansehra District, Pakistan
Nice forsterite crystal in matrix from Sapat Gali, Mansehra District, Pakistan. Size: 8 x 5 cm, photo: Albert Russ

Pure forsterite has about 25 % lover density then fayalite (Fo = 3.21; Fa = 4.39); also pure forsterite is not pleochroic. However, most olivines in thin sections are pleochroic because of significant iron content.

Varietal Names

Olivine is alternatively still known as chrysolite - the name easily confused with chrysotile - natural asbestos mineral from serpentinite group. Gemmy olivine is often labeled as peridot. Rock forming olivine with dominant forsterite is sometimes still labeled with the obsolete name hortonolite.

Naming and Discovery

The naming history of forsterite is quite complex. The earliest undisputed name was chrysolit, assigned by Johann Gottschalk Wallerius in 1747. In 1755, Antoine d’Argenville referred to it as peridot ordinaire, and in 1758 Axel Cronstedt called it gulgron topas. In 1772, Rome d’Lisle named it chrysolite ordinaire. In 1789, Abraham Gottlieb Werner renamed the Wallerius chrysolit as olivine. In 1823 Frederic Walchner named the specimen hyalosiderite. The following year, a sample of actual forsterite may have been described from Mount Somma at Vesuvius, Italy and Serve-Dieu Armand Levy formally named forsterite after Adolarius Jacob Forster, a German collector and mineral dealer. Other names continued to ‘plague’ the mineral, with Charles Upham calling it boltonite in 1835 and an unidentified Romanovski using glinkit in 1847.

Grainy olivine nodule (peridotite xenolith) in basalt hostrock from British Columbia, Canada
Typical olivine nodule (peridotite xenolith) in basalt hostrock from British Columbia, Canada. Photo: Philippe Belley


The olivine minerals are characteristic of mafic and ultramafic rocks found beneath the Earth’s crust, in the upper 400 km of the Earth’s mantle. At mantle depths, these rocks fall into 3 natural classes: dunites, peridotites and eclogites. Dunite is dominated by olivine, and the olivine is typically > 92% forsterite. Peridotite is a commonly a mixture of olivine and pyroxene, and the olivine content, even if only 50% of the mixture, amounts to > 88% forsterite. Eclogite is high pressure and high temperature rock, consisting of garnet (pyrope) and pyroxene (omphacite).

Left: Perfect forsterite crystal from Sapat Gali, Mansehra District, Pakistan. Size: 4 x 2 cm. Anton Watzl collection, photo: Albert Russ
Collecting forsterite in columnar basalt lava flow - British Columbia, Canada. Photo: Philippe Belley

Melting of these rocks in deep structural environments will generate mafic and ultramafic rocks capable of rising into the lower crust, differentially recrystallizing into the suite of mafic and ultramafic rocks generally known under a variety of names. Current practice for classifying mafic rocks relies on the relative proportions of olivine-pyroxene-plagioclase; for ultramafic rocks, the relative proportions of olivine-orthopyroxene-clinopyroxene.

Since olivine has an extremely high melting point, crystallization from a melt containing magnesium and silica usually results in the early precipitation of olivine, along with orthopyroxene, as cumulate crystals settling into the floor of the magma chamber, wherever that chamber develops.

Green olivine sand on the lava beach
Green olivine grains are typical for some lava beaches on Iceland, Hawaii or Canary Islands. Photo: Brocken Inaglory

Forsterite is more or less present in many mafic and ultramafic rocks, however, rarely forms bigger grains or crystals. Big nodules made of olivine grains are present in some basalts. These are peridotite xenoliths - parts of mantle rocks (peridotite) transported to the surface by low-viscosity magma (basalt).

A secondary, less common occurence of forsterite, is in the marbles resulted from metamorphism of limestones, dolostones and oceanic serpentinites containing high levels of magnesium. Some marbles are one of the few environments with very pure and often almost colorless forsterite.


Forsterite – or better say its gemmy variety peridote – is widely used as a gemstone. Forsterite has pleasing yellow green color, quite uncommon for other gems.

Faceted gemmy forsterite (peridot) from British Columbia, Canada
Faceted gemmy forsterite (peridot) up to 1.85 carats from British Columbia, Canada. Photo: Philippe Belley

One forsterite characteristic – superior mechanical properties – is animating the idea of using it as a biomaterial substrate for medical implants. The idea behind a biomaterial is that it is an engineered material created by materials scientists, suitable for a medical application, and not a material produced by an organic biological system. Such biomaterials may be biologically inert materials placed in the body as platforms, anchors, sensors, and so forth.

Occurrence of Forsterite

Prominent forsterite localities in Europe include: At Monte Somma on Vesuvius, Campania, Italy; Ojamo, Lohja, Finland; Mreog Ramsdel in Norway; at Forstberg, Germany, and in Smrčí, Czech Republic.

Forsterite aggregate in basalt
Peridotite xenolith in basalt, composed mostly of green forsterite, from Smrčí, Czech Republic. Size: 9 x 7.5 cm, photo: Zbyněk Buřival

In Russia, large crystals from the Kovdor Massif, Kola Peninsula and at Zlatoust and Mt. Itkul, Ural Mountains. In Pakistan, exceptional gemmy crystals from Sapat Gali, 24 km northeast of Naran, Northwest Frontier Province. Incredibly huge gems are produced in Myanmar (Burma), in the Mogok District and at Pyaung Gaung.

In Egypt, large gem crystals from the Island of Zabargad (Zabirgetor St. Johns), in the Red Sea. In the U.S., in Arizona, on Peridot Mesa, southwest of San Carlos, Gila County and at Buell Park, Apache County. In Tanzania, at Kingiti, Mpapwa.