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Skarn

Skarn is a coarse-grained metamorphic rock formed by the metasomatic replacement of carbonate protoliths, such as limestone or dolostone, through interaction with hot, chemically active hydrothermal fluids associated with igneous intrusions.^[1] These rocks develop in the contact zones where magma intrudes reactive sedimentary sequences, leading to the recrystallization and compositional alteration of the host material under high-temperature conditions exceeding 250°C.^[2] Characterized by calc-silicate mineralogy, skarns typically feature dominant phases like garnet (e.g., andradite, grossular) and pyroxene (e.g., diopside, hedenbergite), alongside amphiboles, epidote, and quartz.^[3] The formation of skarn occurs in distinct stages: an initial prograde phase of isochemical contact metamorphism producing hornfels or skarnoids, followed by metasomatic replacement that introduces silica, iron, and other elements from magmatic fluids, and a retrograde stage involving cooling and hydration that can deposit ore minerals.^[1] This process is driven by fluid fluxes of magmatic, metamorphic, meteoric, or marine origin, creating spatially zoned patterns where proximal zones are garnet-rich and distal zones contain more pyroxene or calcite.^[4] Skarns are classified by protolith composition into calcic (from limestone) or magnesian (from dolostone) varieties, and by dominant economic metals into types such as copper, gold, iron, tungsten, or zinc-lead skarns.^[5] They form in diverse tectonic settings, including magmatic arcs, orogenic belts, and continental rifts, at depths ranging from near-surface to over 10 km.^[3] Economically, skarns are significant as hosts to major ore deposits, yielding billions of tons of metals; for instance, iron skarns contain magnetite-rich ores exceeding 500 million tons, while tungsten skarns feature scheelite in deep-seated environments.^[4] Ore minerals commonly include chalcopyrite for copper, pyrite and pyrrhotite for sulfides, and cassiterite for tin, often concentrated during the retrograde phase.^[1] Beyond mining, skarns occasionally produce gem-quality materials like garnets or even ruby and sapphire, though their primary value lies in base and precious metal extraction.^[2] Geochemically, skarn deposits are notable for their potential to release trace elements like zinc and manganese into drainage, moderated by the buffering effect of carbonate hosts.^[1]

Fundamentals

Definition

Skarn is defined as a coarse-grained calc-silicate rock formed through metasomatic replacement of carbonate-rich protoliths by hydrothermal fluids, resulting in the introduction of silica and other components that react chemically with the original minerals.^[6] This process typically occurs in association with igneous intrusions, leading to the development of distinct calc-silicate assemblages that characterize skarn as a product of metasomatism rather than simple metamorphism.^[7] Skarn differs from related metamorphic rocks such as hornfels, which forms via contact metamorphism without significant fluid-mediated chemical exchange, lacking the metasomatic zoning and exotic element enrichment typical of skarn.^[3] In contrast to marble, which represents recrystallized pure carbonate rock dominated by calcite or dolomite without substantial silicate incorporation, skarn features pervasive replacement by calc-silicates, altering the protolith's composition fundamentally.^[8] A key feature of skarn is its internal zoning, where proximal zones near the fluid source host high-temperature minerals, grading outward to distal zones with lower-temperature assemblages reflective of decreasing thermal and chemical gradients.^[9] Skarns are prevalent in orogenic belts worldwide, spanning a broad temporal range from Precambrian to the present, often linked to convergent margin tectonics.^[3]

Etymology

The term "skarn" derives from the Swedish word skarn, literally meaning "filth" or "rubbish," stemming from Old Norse skarn for dirt or dung, and was originally applied by miners to denote hard, rubbly waste rock or silicate gangue.^[10]^[11] This usage emerged in late 18th- and early 19th-century Swedish mining contexts, particularly near iron deposits in the Persberg district of Värmland, where it described non-economic, tough calc-silicate materials accompanying magnetite and sulfide ores.^[12]^[13] The word entered formal geological nomenclature through the work of Swedish geologist Alfred Elis Törnebohm, who first published it in 1875 while describing ore-hosting rocks in the Persberg area, distinguishing subtypes like garnet-rich brunskarn (brown skarn) and pyroxene-rich grönskarn (green skarn).^[14] Scandinavian geologists subsequently brought the term into English-language literature in the early 20th century, applying it to similar metamorphic assemblages observed in international studies.^[13] Over time, the terminology broadened beyond its initial mining connotation for any hard, dark metamorphic rock to a more specific petrological meaning; by the 1930s, it had been refined in scientific usage to designate coarse-grained calc-silicate rocks formed via metasomatism, particularly those replacing carbonate protoliths near igneous intrusions.^[15]^[16]

Petrology

Mineral Composition

Skarn deposits are characterized by a mineral assemblage dominated by calc-silicate minerals, primarily garnet and pyroxene, which form through metasomatic replacement of carbonate protoliths.^[7] Garnet in skarns typically occurs as grossular (Ca_3Al_2(SiO_4)_3) to andradite (Ca_3Fe_2(SiO_4)_3) solid solutions, with compositions varying based on the iron and aluminum content of the metasomatizing fluids; andradite is prevalent in iron-rich environments, while grossular dominates in aluminous settings.^[7] Pyroxenes are chiefly diopside (CaMgSi_2O_6) in magnesian skarns and hedenbergite (CaFeSi_2O_6) in more ferruginous ones, reflecting the calcium and divalent cation availability during formation.^[7] Ore minerals in skarns include magnetite (Fe_3O_4), which is common in iron skarns as an early prograde phase, chalcopyrite (CuFeS_2) associated with copper deposits, and scheelite (CaWO_4) in tungsten-bearing examples.^[7] These minerals precipitate during metasomatic stages, with paragenetic sequences progressing from prograde (high-temperature) assemblages—such as early garnet followed by pyroxene and magnetite—to retrograde (lower-temperature) phases involving amphiboles, epidote, and sulfides like chalcopyrite.^[7] Fluid inclusions trapped in these minerals indicate formation from saline hydrothermal fluids, typically with salinities of 10–50% NaCl equivalent, suggesting involvement of magmatic brines.^[17] Mineral variations occur depending on skarn type; calcic skarns frequently contain vesuvianite (Ca_{19}(Al,Mg,Fe)_{13}Si_{18}O_{68}(OH,F)_{10}), a complex calc-silicate enriched in aluminum, fluorine, and boron, which forms in proximal zones near the intrusive contact.^[18] Magnesian skarns, though less common, feature forsterite (Mg_2SiO_4) as a high-temperature prograde mineral, often altered to serpentine during retrograde stages.^[17] Accessory minerals include allanite, an REE-bearing epidote-group phase, which incorporates trace rare earth elements (primarily light REE like La and Ce) and serves as a reservoir for these elements in certain skarns.^[19]

Textures and Structures

Skarn rocks typically exhibit massive and granular textures resulting from extensive recrystallization during metasomatism, often appearing as coarse-grained assemblages that reflect high-temperature metamorphic conditions. These textures are commonly granoblastic, with equidimensional mineral grains interlocking to form a dense fabric, though nematoblastic variants occur where elongated crystals align due to directed fluid flow. Banded or veined structures arise from episodic fluid infiltration, creating layered alternations of calc-silicate minerals or quartz veins that crosscut the host rock, highlighting the role of metasomatic replacement in shaping the rock's fabric.^[20]^[21]^[22] Zonation is a hallmark structural feature of skarns, manifesting as systematic spatial variations in mineral assemblages from proximal to distal zones relative to the igneous intrusion. Commonly, a garnet-rich core transitions outward to pyroxene- and epidote-dominated margins, with zone widths ranging from centimeters near contacts to kilometers in extensive systems, influenced by host rock purity and fluid migration paths. This zoning reflects gradients in temperature, fluid composition, and reaction progress, often more pronounced in coarse-grained limestones than in finer or impure carbonates.^[23]^[24]^[3] Deformation features in skarns vary with depth and rheology; in deeper settings, ductile folding preserves bedding parallel to intrusive contacts, accommodating strain without fracturing, while shallower environments promote brittle hydrofracturing that facilitates vein development and fluid ingress. These structures underscore the interplay between host rock plasticity and metasomatic stresses.^[3]^[25] Associated retrograde alteration overprints prograde assemblages with hydrous minerals such as chlorite and amphibole, forming along fractures or pervasive fronts as cooling fluids introduce water and volatiles. This alteration imparts a finer-grained, often schistose texture to the otherwise massive skarn, marking a shift from anhydrous calc-silicates to more hydrated phases.^[1]^[25]^[26]

Formation

Metasomatic Processes

Skarn formation primarily occurs through metasomatic processes driven by the interaction of hydrothermal fluids with carbonate-rich protoliths, leading to the replacement of primary minerals with calc-silicate assemblages. These processes involve the infiltration of reactive fluids that transport and deposit elements such as silicon, iron, and metals, resulting in significant mass transfer and mineralogical transformation. The overall metasomatism is divided into prograde and retrograde stages, each characterized by distinct temperature conditions, fluid compositions, and reaction pathways.^[27]^[1] The prograde stage represents the initial high-temperature phase of metasomatism, occurring at temperatures typically between 400°C and 700°C, as inferred from fluid inclusions in calc-silicate minerals like garnet and pyroxene. During this stage, anhydrous calc-silicate minerals such as garnet, pyroxene, and wollastonite form through the reaction of carbonate rocks with silica- and metal-bearing fluids. These fluids, primarily of magmatic origin with possible contributions from metamorphic devolatilization or meteoric water, are dominated by H₂O-CO₂ mixtures and exhibit neutral to acidic pH, buffered by the carbonate host rocks. Salinities range from 10 to 60 wt% NaCl equivalent, enabling the transport of metals like copper, zinc, and iron via chloride complexes through mechanisms of infiltration along fractures or diffusion across reaction fronts. Mass balance calculations indicate net gains in silicon, iron, water, and metals, coupled with losses of carbon dioxide, as carbonates are decarbonated and reformed into silicates. A representative reaction is the metasomatic replacement of limestone by silica-rich fluids: CaCO₃ + SiO₂ → CaSiO₃ (wollastonite) + CO₂, which exemplifies the addition of silica and expulsion of CO₂ gas.^[27]^[3]^[1] Following prograde metasomatism, the retrograde stage ensues as the system cools to 200–400°C, promoting hydration and sulfidation reactions that overprint the earlier assemblages. In this phase, prograde minerals are partially replaced by hydrous silicates such as amphibole, epidote, and chlorite, alongside the precipitation of sulfide minerals like pyrite and chalcopyrite. The fluids evolve with increased sulfur content and may incorporate more meteoric water, leading to lower temperatures and higher water/rock ratios that facilitate the breakdown of anhydrous phases. This stage is marked by metasomatic alteration along structural features, where mass transfer involves the addition of hydrogen, sulfur, and water, resulting in the mobilization and redeposition of metals into ore zones. For instance, prograde pyroxene can react with sulfur-bearing fluids to form sulfides and hydrous silicates: CaMgSi₂O₆ (diopside) + H₂S → Mg-sulfide + hydrous Ca-silicate + H₂O, highlighting the shift toward more volatile-rich conditions. Fluid inclusion studies confirm these lower temperatures, tying retrograde alterations to the cooling of the hydrothermal system.^[27]^[28]^[3]

Geological Settings

Skarns primarily form at the contacts between felsic to intermediate intrusive bodies, such as granites and diorites, and carbonate host rocks like limestones and dolomites, within convergent tectonic margins where magmatic activity is driven by subduction processes.^[29]^[30] These settings facilitate the metasomatic alteration of carbonates by hot, reactive fluids derived from the cooling intrusions, leading to the development of calc-silicate mineral assemblages along the intrusive-country rock interfaces.^[6] The depth of skarn formation varies significantly, influencing their structural and mineralogical characteristics. Epizonal skarns develop at shallow crustal levels, typically less than 5 km, and may exhibit explosive brecciation or phreatic features due to volatile-rich fluids interacting with near-surface carbonates.^[6] In contrast, mesozonal skarns form at greater depths exceeding 10 km, often in association with regional metamorphism and higher pressures, resulting in more pervasive alteration zones.^[29]^[13] Tectonically, skarns are predominantly associated with Phanerozoic orogenic belts, such as the Andes and the North American Cordillera, where they link to subduction-related plutonism and terrane accretion.^[29]^[30] Precambrian shields also host skarn occurrences, particularly in stable cratonic margins with evolved granitic intrusions, though they are less common in extensional or anorogenic environments.^[13] While fluid circulation often follows fractures and lithologic boundaries in these settings, the overall framework is dominated by compressional tectonics.^[31] Although most skarns involve carbonate protoliths, non-carbonate variants, such as aluminous skarns, occur in pelitic rocks adjacent to S-type granites, where aluminum-rich sediments undergo metasomatism to produce spessartine- and almandine-bearing assemblages.^[13] These are typically found in post-orogenic or cratonic settings following major tectonic events, contrasting with the more common calcic skarns in arc environments.^[32]

Classification

Protolith and Composition

Skarns are classified primarily according to the nature of their protolith and the resulting bulk chemical composition, which dictate the dominant mineral assemblages formed during metasomatism.^[7] Calcic skarns develop from limestone protoliths and are characterized by high calcium oxide (CaO) contents, with bulk CaO typically ranging from 1 to 50 wt% (mean ~18 wt%), alongside dominant calcium silicate minerals such as garnet (grossular-andradite) and pyroxene (diopside-hedenbergite).^[27] These skarns reflect the Ca-rich nature of the original carbonate host, leading to metasomatic replacement dominated by calc-silicate phases.^[4] Magnesian skarns, in contrast, form from dolomitic protoliths and feature elevated magnesium oxide (MgO) levels, with Mg-rich minerals including forsterite, diopside, periclase, and humite-group minerals like chondrodite.^[27] This composition arises from the Mg-bearing dolomite, promoting the stabilization of magnesium silicates during fluid-rock interaction.^[4] Such skarns often exhibit lower iron content compared to calcic varieties due to the protolith's influence on available cations.^[7] Aluminous or distal skarns originate from aluminous protoliths such as shales or volcanic rocks, which introduce high aluminum contents and result in minerals like aluminous amphiboles, idocrase, kyanite, and tourmaline.^[7] These skarns typically occur farther from the intrusive source and have lower buffering capacity against metasomatic fluids, leading to more variable and Al-enriched assemblages.^[27] Skarns are further distinguished as endoskarns or exoskarns based on the protolith type relative to the igneous intrusion. Endoskarns replace igneous hosts, such as granodiorite, forming within hornfels-altered zones with minerals like biotite, amphibole, and pyroxene-plagioclase intergrowths.^[7] Exoskarns, the more common variety, involve replacement of sedimentary protoliths, particularly carbonates, yielding zones of garnet, pyroxene, and wollastonite.^[4] The protolith composition in these cases influences mineral zoning patterns, with calcic exoskarns showing progressive Ca-silicate sequences outward from the intrusion.^[27]

Associated Metals

Skarns are classified based on their dominant economic metals, which are primarily introduced during the retrograde stage of metasomatism, with distinct mineralogical expressions reflecting the ore-forming processes.^[3]^[4] Fe-skarns are dominated by magnetite as the primary ore mineral, forming massive to disseminated bodies within calc-silicate gangue, and are often barren of other metals or associated with minor Cu and Au.^[33] These deposits represent the most abundant skarn type globally, with major examples exceeding 500 million tons in reserves.^[33] Cu-skarns feature chalcopyrite and pyrite as the principal sulfides, frequently accompanied by Au and Ag, and are typically linked to underlying porphyry copper systems that provide the metal source.^[3]^[34] Au-skarns contain native gold or electrum as the key economic phases, with subtypes distinguished by oxidation state: reduced variants associated with ilmenite and pyrrhotite, and oxidized ones linked to magnetite and pyrite.^[3]^[35] Other skarn types include W-skarns with scheelite as the tungsten host, Mo-skarns featuring molybdenite, Zn-Pb skarns rich in sphalerite and galena, and Sn-skarns containing cassiterite.^[4]^[3]

Economic Geology

Deposit Types

Skarn ore deposits are categorized into genetic subtypes based on their spatial relationship to the causative intrusion, fluid oxidation states, and associations with other deposit systems, which influence their mineralization styles and economic potential. Proximal skarns form directly adjacent to igneous intrusion contacts, where high-temperature fluids promote intense metasomatism, resulting in high-grade concentrations of metals such as copper, often exceeding 1-5% Cu in zones rich in garnet and pyroxene.^[27] In contrast, distal skarns develop along extended fluid pathways away from the intrusion, typically kilometers distant, featuring disseminated mineralization like gold in pyroxene-dominant assemblages with lower grades around 5-10 g/t Au.^[3] These spatial variations arise from decreasing temperature and fluid flux with distance, leading to zoned mineralogy from proximal garnet-rich to distal pyroxene- or wollastonite-rich skarns.^[4] Oxidation state variants further distinguish skarn subtypes, reflecting the redox conditions of the host rocks and fluids. Reduced skarns, commonly associated with gold, occur in graphitic or carbonaceous host rocks that buffer fluids to low oxygen fugacity, producing pyrrhotite-bearing assemblages with ilmenite-series plutons and high-grade Au mineralization (e.g., 5-15 g/t Au).^[3] Oxidized skarns, prevalent in carbonate-rich hosts without significant carbon, involve magnetite-series plutons and pyrite-dominant sulfides, favoring base metal enrichment such as in copper or tungsten systems.^[4] These variants control sulfide mineralogy and metal partitioning, with reduced types often yielding higher precious metal grades due to stability of native gold under low fO₂ conditions.^[27] Associated systems highlight hybrid deposit models that integrate skarn formation with other hydrothermal styles. Skarn-porphyry hybrids, such as copper-molybdenum systems, combine proximal skarn metasomatism with porphyry-style stockwork veining near the intrusion, yielding large-tonnage deposits (10-100 Mt) at 1-2% Cu and 0.01-0.1% Mo.^[27] Replacement skarns, involving selective metasomatic alteration of evaporitic or carbonate sequences, form stratabound ores where fluids dissolve and precipitate metals along favorable beds, often in Fe or Zn-Pb systems with grades of 1-5% for base metals.^[36] Overall, skarn deposits typically range from 10-100 million tonnes in size, with base metal grades of 1-5% and gold at 5-10 g/t, though extremes reach over 500 Mt for iron skarns.^[4]

Major Examples

Skarn deposits exhibit a global distribution strongly tied to convergent plate margins, with the majority concentrated in the circum-Pacific orogenic belt, including key regions such as the Andes of Peru, the Great Basin of Nevada in the USA, and the Canadian Cordillera. This pattern reflects their formation through metasomatism associated with subduction-related calc-alkaline intrusions. Precambrian examples are less common but notable in Sweden, where deposits like the Yxsjöberg tungsten skarn formed around 1.789 Ga during Paleoproterozoic orogenic events.^[37]^[38]^[39] A classic example of an Fe-skarn is the Iron Springs deposit in the Iron Springs mining district of southwestern Utah, USA, which represents the largest iron deposits in the western United States and produced over 100 million tons of high-grade magnetite ore averaging around 50% Fe (as of 1966), with estimated reserves at that time up to 200 million tons at 40-60% Fe. The ore occurs as massive magnetite replacements in Jurassic limestones surrounding Miocene quartz monzonite laccoliths, highlighting the district's role in contact metasomatic iron mineralization; the district is now largely depleted.^[40]^[41] The Antamina deposit in north-central Peru exemplifies a world-class Cu-Zn skarn, recognized as the largest of its type globally, with proven and probable reserves of approximately 500 million tonnes of ore grading 1.2% Cu and 1.0% Zn (as of 2024), alongside minor Mo and Ag; ongoing expansions are boosting production in 2025-2026. Hosted in Cretaceous carbonates intruded by Miocene diorite stocks, the deposit features zoned skarn mineralization with proximal Cu-rich garnet skarn transitioning to distal Zn-rich pyroxene skarn, supporting large-scale open-pit mining operations.^[42]^[43]^[44] For Au-skarn deposits, the Fortitude mine in Lander County, Nevada, USA, stands out as a high-grade example within the Battle Mountain-Eureka trend, where approximately 11 million tonnes of ore were mined at an average of 5.14 g/t Au and 25 g/t Ag, with the skarn formed by replacement of Carboniferous-Permian carbonates by Eocene intrusions. The mineralization is stratabound, dominated by pyrrhotite, pyrite, and chalcopyrite in calc-silicate altered host rocks, contributing significantly to Nevada's gold production.^[45]^[46] The Cantung deposit in the Northwest Territories, Canada, illustrates a prominent W-skarn, featuring scheelite mineralization in a large exoskarn body developed in Cambrian dolomites adjacent to a Cretaceous granite intrusion; the E-zone orebody comprises approximately 4.2 million tonnes at 1.6% WO₃, part of historical resources exceeding 10 million tonnes at grades around 1-1.5% WO₃, with total historical production of about 5 million tonnes of ore. This high-grade scheelite skarn has been a major tungsten producer, though the mine entered permanent closure in 2025, underscoring past economic viability in a remote Arctic setting.^[47]^[48]^[49] An example of a Zn-Pb skarn is the Big Gossan deposit in the Ertsberg district of Papua, Indonesia, where high-grade replacement mineralization occurs in Miocene limestones intruded by quartz monzonite, featuring sphalerite and galena in distal skarn zones with elevated Zn/Pb ratios alongside Cu-Au. The deposit's zoning, with Zn-Pb enrichment in upper breccias and fractures, demonstrates the lateral variability in metasomatic systems associated with porphyry-skarn complexes.^[50]

Economic Significance

Skarn deposits play a vital role in the global mineral supply chain, historically contributing approximately 10% of the world's copper, 5% of gold, and 20% of tungsten production (as of the 1990s), with skarns remaining significant for tungsten where they account for over 70% of historical global output.^[27] Iron skarns have been historically significant, particularly in 19th-century Sweden, where deposits in the Bergslagen region supported substantial iron output that bolstered the country's early industrial economy.^[51] Production trends for skarn deposits show a decline in established districts such as the United States, where older mines have largely depleted shallow resources, contrasted by rising output in developing regions like China and Peru.^[38] China dominates tungsten production from skarns, accounting for over 80% of global supply as of 2025, while Peru's skarn-hosted copper deposits, such as Antamina, drive increasing contributions to base metal markets.^[52] Historical global output from skarn deposits exceeds 1 billion tonnes of ore, underscoring their long-term economic impact.^[4] Byproducts like silver, molybdenum, and rare earth elements (REE) often enhance the economic viability of skarn operations, with these metals recovered as co-products from primary tungsten, copper, or iron mineralization.^[27] For instance, molybdenum accompanies many copper skarns, while REE enrichments occur in iron and tungsten varieties, adding value amid fluctuating primary metal prices.^[53] Looking ahead, skarn deposits hold future potential through underexplored deep extensions beneath known surface occurrences, where advanced geophysical methods could uncover additional resources.^[5] However, environmental challenges persist in mining carbonate-hosted skarns, including risks of acid mine drainage from sulfide oxidation once buffering carbonates are depleted, necessitating sustainable practices to mitigate impacts on water quality and local ecosystems.^[1]

References

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[36]
Skarn Copper Deposits | INN - Investing News Network
Mar 24, 2011 · The largest copper skarns are associated with mineralized porphyry copper plutons, or bodies of intrusive igneous rock. These deposits can ...
[37]
Discrimination of Mineralization Types of Skarn Deposits by ... - MDPI
Compared with the average oxygen fugacity for all intrusions associated with skarns, Au and Sn skarn intrusions are more reduced, while Cu, Zn, and Mo skarn ...
[38]
Fingerprinting involvement of evaporites in magmatic-hydrothermal ...
Evaporites can be involved in the formation of Fe skarn systems and may play a critical role in ore-forming processes.
[39]
Skarn Deposits in the Circum-Pacific Belts - AusIMM
In more than 20 coastwise countries of this region, there exist thousands skarn deposits of different types. According to the differences of major metallic ...
[40]
Tungsten skarn potential of the Yukon-Tanana Upland, eastern ...
In this paper, we present an assessment for undiscovered W skarn resources for parts of the lesser-explored western (Alaskan) portion of the YTU.
[41]
U‐Pb age of the Yxsjöberg Tungsten‐Skarn deposit, Sweden: GFF
U‐Pb dating of titanite that formed during the skarnification of the limestones yields an age of 1789±2 Ma. This age is not compatible with an exhalati ve ...
[42]
Crystallization and alteration of quartz monzonite, Iron Springs mining district, Utah; relation to associated iron deposits | Economic Geology | GeoScienceWorld
### Summary of Iron Springs Skarn Deposit Size and Reserves
[43]
Iron Springs - PorterGeo Database - Ore Deposit Description
Jul 30, 2013 · The ore has predominantly had direct shipping grades which have averaged 53% Fe, although the ores vary between 40 and 60% Fe. They are soft and ...
[44]
[PDF] NI 43-101 Technical Report on Antamina Mining Operation Peru
Dec 31, 2024 · Peru. February 2025. Page 1-3. 1.5. Geology and Mineralization. The Antamina deposit is considered to be an example of a giant skarn deposit.
[45]
(PDF) The Geology of the Antamina Copper-Zinc Skarn Deposit, Peru
Feb 18, 2016 · The Antamina Cu-Zn deposit has 990 Mt of resources including 500 Mt of reserves at 1.2% Cu, 1.0% Zn, according to Redwood (1999) . Besides ...
[46]
Alteration zonation of the Fortitude gold skarn deposit, Lander ...
Jan 1, 1991 · It contains about 11 Mt (12 million st) of minable ore grading 5.14 g/t (0.149 oz per st) and is the distal portion of a continuous skarn system ...Missing: tonnage | Show results with:tonnage
[47]
PorterGeo Database - Ore Deposit Description
Mineralisation at Fortitude-Phoenix is basically a 30 m thick, stratabound gold-silver bearing, sulphide replacement of pervasively calc-silicate/skarn altered ...
[48]
The Cantung E Zone Scheelite Skarn Orebody, Tungsten, Northwest ...
The unusually large (4.2 million metric tons) and high-grade (1.6% WO3) Cantung E zone exoskarn scheelite orebody developed in a dolomite-poor, ...Missing: tonnage | Show results with:tonnage
[49]
Major Mines & Projects | Cantung Mine - Mining Data Online
Cantung is a typical skarn-type deposit, albeit of an unusually large size for a tungsten bearing skarn. As with most skarns, the mineralization is related to a ...
[50]
(PDF) Genesis of Pyrite-Au-As-Zn-Bi-Te Zones Associated with Cu ...
Aug 7, 2025 · Pyrite-Au-As-Zn-Bi-Te occurrences are also distributed in faults and fractures to the north and south of the Big Gossan skarn Cu-Au deposit. At ...
[51]
[PDF] Characterization of Fe-rich skarns and fluorapatite-bearing ...
Several centuries of mining have led to prosperity for Sweden. In 16c, the iron mines in the district accounted for 38 % of the world's iron production.
[52]
The Challenge of Tungsten Skarn Processing by Froth Flotation
The use of the Petrov process was also avoided in the Cantung Canadian formerly exploited scheelite mine, where gravity pre-concentration allowed rejecting the ...
[53]
A special issue devoted to skarn deposits - Introduction
Aug 7, 2025 · Skarn mineral deposits are sources of economically important metals such as Cu, Mo, Ag, Au, W, Fe, Pb, Zn, U, REE, F, B, In, and Sn (Einaudi ...