Skarns or tactites are coarse-grained metamorphic rocks that form by replacement of carbonate-bearing rocks during regional or contact metamorphism and metasomatism. Skarns may form by metamorphic recrystallization of impure carbonate protoliths, bimetasomatic reaction of different lithologies, and infiltration metasomatism by magmatic-hydrothermal fluids. Skarns tend to be rich in calcium-magnesium-iron-manganese-aluminium silicate minerals, which are also referred to as calc-silicate minerals. These minerals form as a result of alteration which occurs when hydrothermal fluids interact with a protolith of either igneous or sedimentary origin. In many cases, skarns are associated with the intrusion of a granitic pluton found in and around faults or shear zones that commonly intrude into a carbonate layer composed of either dolomite or limestone. Skarns can form by regional or contact metamorphism and therefore form in relatively high temperature environments. The hydrothermal fluids associated with the metasomatic processes can originate from a variety of sources; magmatic, metamorphic, meteoric, marine, or even a mix of these. The resulting skarn may consist of a variety of different minerals which are highly dependent on both the original composition of the hydrothermal fluid and the original composition of the protolith. If a skarn has a respectable amount of ore mineralization that can be mined for a profit, it can be classified as a skarn deposit.
Etymology Skarn is an old Swedish mining term originally used to describe a type of silicate gangue, or waste rock, associated with iron-ore bearing sulfide deposits apparently replacing Palaeoproterozoic age limestones in Sweden's Persberg mining district.
Petrology Skarns are composed of calcium-iron-magnesium-manganese-aluminum silicate minerals. Skarn deposits are economically valuable as sources of metals such as tin, tungsten, manganese, copper, gold, zinc, lead, nickel, molybdenum and iron. A skarn is formed by a variety of metasomatic processes during metamorphism between two adjacent lithologic units. Skarns can form in almost any rock type such as shale, granite, or basalt but the majority of skarns are found in carbonate rocks containing limestone or dolomite. It is common to find skarns near plutons, along faults and major shear zones, in shallow geothermal systems, and on the bottom of the sea floor. The specific mineralogy of skarns are highly related to the mineralogy of the protolith. Skarn mineralogy is dominated by garnet and pyroxene with a wide variety of calc-silicate and associated minerals, including idocrase, wollastonite, actinolite, magnetite or hematite, epidote and scapolite. Because skarns are formed from silica-rich aqueous fluids replete with incompatible elements, a variety of uncommon mineral types are found in skarns, such as: tourmaline, topaz, beryl, corundum, fluorite, apatite, barite, strontianite, tantalite, anglesite, and others.
Classification Skarns can be subdivided depending on specific criteria. One way to classify a skarn is by its protolith. If the protolith is of sedimentary origin, it can be referred to as an exoskarn and if the protolith is igneous, it can be called an endoskarn. Further classification can be made based on the protolith by observing the skarn's dominant composition and the resulting alteration assemblage. If the skarn contains minerals such as olivine, serpentine, phlogopite, magnesium clinopyroxene, orthopyroxene, spinel, pargasite, and minerals from the humite group, it is characteristic of a dolomitic protolith and can be classed as a magnesian skarn. The other class, called calcic skarns, are the replacement products of a limestone protolith with dominant mineral assemblages containing garnet, clinopyroxene, and wollastonite. Rocks that contain garnet or pyroxene as major phases, and that are also fine-grained, lack iron, and have skarn-like appearances, are generally given the term "skarnoid". Skarnoid is therefore the intermediate stage of a fine-grained hornfels and a coarse-grained skarn.
Skarn ore deposits Metal ore deposits that have skarn as gangue are called skarn deposits and can form by any combination of closed metamorphism or open system metasomatism, although most skarn deposits are thought to be related to magmatic-hydrothermal systems. Skarn deposits are classified by their dominant economic element, e.g., a copper (Cu) skarn deposit or a molybdenum (Mo) skarn deposit.
Fe (Cu, Ag, Au) skarn deposits The tectonic setting for calcic Fe skarns tends to be the oceanic island arcs. The host rocks tend to range from gabbro to syenite associated with intruding limestone layers. The tectonic setting for magnesium Fe skarns tends to be the continental margin. The host rocks tend to be granodiorite to granite associated with intruding dolomite and dolomitic sedimentary rocks. Magnetite is the principal ore in these types of skarn deposits which its grade yields from 40 to 60%. Chalcopyrite, bornite and pyrite constitute minor ores.
Cu (Au, Ag, Mo, W) skarn deposits The tectonic setting for Cu deposits tends to be the Andean-type plutons intruding older continental-margin carbonate layers. The host rocks tend to be quartz diorite and granodiorite. Pyrite, chalcopyrite and magnetite are typically found in higher abundances.
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