supergene oxidation of copper deposits.pdf

ABSTRACTCopper oxides represent an attractive exploration target

because even low-grade prospects have the potential toproduce low-cost copper in an environmentally friendlyfashion. Derived from hypogene and/or supergene sulfides,copper oxides comprise a series of distinct assemblages thatcharacterize a variable pH, oxidizing geochemicalenvironment known as the oxide zone. Development ofoxide copper minerals is a function of source-rock andhost-rock mineralogy, pyrite and other (copper) sulfideabundance and distribution, fracture density anddistribution, phreatic and/or vadose zone occurrence andstability, and maturity of the weathering profile.

The paragenesis of copper oxide mineral formationreflects local, dynamic changes in supergene solutioncomposition attributable to reaction between host-rockmineral components and dissolved species. Especiallyimportant are the concentrations of Fe+++ (vs. Fe++), SO4=,H+, and Cu++ (vs. Cu+). Because mineral assemblages, eventhose that are metastable, represent the geochemicalenvironment in which they formed, identification andmapping of copper oxides is useful in interpreting thegeochemical history of an oxide zone. Furthermore,practical application of oxide zone geochemistry issignificant in the recognition and solution of problemsassociated with weathering-engendered metals oxidationand transport from mine wastes.

SPECIAL NOTE: Readers will find more information about thecopper oxide minerals mentioned in this article by referring to theSEG web site [http://www.segweb.org]. Photographs showingmineral relationships and paragenetic associations allow readersto further understand the nature of copper oxide assemblagesand their geochemical and physical settings.

HSOCIETY OF ECONOMIC GEOLOGISTSHAPRIL 2000 NUMBER 41

Supergene Oxidation of Copper Deposits:Zoning and Distribution of Copper Oxide Minerals

WILLIAM X. CHVEZ, JR. (SEG 1990) MINERALS & ENVIRONMENTAL ENGINEERING DEPARTMENT NEW MEXICO SCHOOL OF MINES SOCORRO, NEW MEXICO, USA 87801TEL. +1.505.835.5317 / FAX: +1.505.835.5252 E-MAIL: [email protected]

NEWSLETTERSEGSEGNEWSLETTER

RESUMENOxidos de cobre comprenden una fuente importante del metal rojo,

especialmente en yacimientos aptos para tratamiento del tipo lixiviacin recuperacin por solventeselectrowinning. Este artculo describe la zonaciny ocurrencia de los xidos de cobre derivados por procesos suprgenosafectando a un protolito con sulfuros de cobre y fierro, hospedado por variasasociaciones mineralgicas de alteracin. Los yacimientos considerados sonprincipalmente prfidos de cobre y molibdeno, y sistemas tipo skarn.

Geoquimcamente, el mineral ms importante que influye la distribucin delos productos de meteorizacin de un yacimiento metalfero del tipo prfido decobre es la pirita. Este mineral genera, en cantidades importantes, cidosulfrico (SO4= y H+) y fierro (Fe+++ y Fe++). Estos componentes de solucionesmetericas (suprgenas) funcionan como lixiviantes, produciendo mobilizacinde cobre y otros metales bsicos desde el volumen de la roca lixiviada yresultando en la formacin de la capa lixiviada (leached capping; vase Figura1). Estos componentes acumulan, influido por la geoqumica de la roca huspedy de las soluciones que transportan estos componentes, en forma de xidos y/osulfuros, formando un volumen de roca enriquecida en metales y azufre.

En la zona de xidos, minerales que contienen cobre oxidado (Cu++, conmenor Cu+ y cobre nativo) comprenden la fuente principal de cobre. Laparagnesis de los xidos refleja los cambios geoqumicos en las soluciones queproveen el cobre con respeto al tiempo. As, la precipitacin de los xidossigue, por lo general, la secuencia detallada en las figuras 3 y 4. Desarrollo de lasecuencia vertical y/o lateral de xidos de cobre es una funcin de (1) el tiempodisponible para meteorizacin e acumulacin (maturity of supply and storage)de metales derivados de los sulfuros (madurz del perfil de meteorizacin), (2)composicin y reactividad de la roca(s) fuente y de la roca(s) husped (3) pH desoluciones transportadores de metales, (4) distribucin y densidad de estructuras(fracturas, zonas de fracturamiento), y (5) estabilidd tectnico y fluctuacinvertical del nivel fretico. Aplicaciones de la geoqumica de la zona de xidos esimportante en la solucin de problemas ambientales asociados con desechos deminas, especialmente oxidacin y lixiviacin desde relaves,desmontes, y pilas de lixiviacin abandonadas. to page 10 . . .

10 S E G N E W S L E T T E R N 41 APRIL 2000

INTRODUCTION AND BACKGROUNDDespite low metal prices, mining and exploration for copper

continue at a significant pace. Recovery of copper by leachingmethods is economically more attractive than by conventional oremilling, so many companies are concentrating their mining andexploration efforts on copper oxide minerals. This article describesthe nature and distribution of copper minerals occurring in oxideaccumulations associated with weathering of copper sulfidedeposits, with emphasis on minerals that occur in the supergeneoxide zones of porphyry copper and skarn ore deposits. Copperoxides are defined as those copper minerals containing oxidizedanions, especially copper oxides, sensu strictu, sulfates, phosphates,carbonates, and arsenates.

The oxidation of sulfide minerals, especially pyrite, is critical indetermining the geochemical environment that characterizes aweathering sulfide-bearing rock volume. Sulfide destruction createssolutions containing hydrogen ions, metal ions, and sulfate; thesesolutions must be at least partially neutralized if the metals ofeconomic significance are to be redeposited. One of the mostimportant factors influencing the generation of the acid sulfate-bearing solutions is the ratio of reduced sulfur to metal in sulfideminerals before oxidation.

Weathering results in significant geochemical changes in theoxidation state of a sulfide-bearing mineral deposit because most ore

deposits are characterized by minerals containing base metals andreduced Fe and S. Figure 1 shows a schematic model of thecomponents of an oxidizing rock volume containing sulfides and thelocation of the oxide zone. In examples considered in this article,the pre-oxidation sulfide assemblage (protore) consists of pyrite andchalcopyrite, and contains sufficient pyrite to overcome at leastsome neutralizing capacity of host-rock minerals. The oxide zoneconsists of the rock volume in which copper oxide minerals arestable and are the dominant copper minerals.

THE WEATHERING ENVIRONMENTThe weathering environment may be considered to have three

principal geochemical domains. Although the contacts betweenthese domains are gradational, each is characterized by distinctconditions of oxidation state and pH. These three domains are (1) asource region, comprising the volume of rock undergoing oxidationand mass loss; (2) a sink region(s), where mass from the sourceregion accumulates and which includes residual (unreacted)hypogene minerals the oxide zone discussed in this papercomprises part of this geochemical sink; and (3) protolith, theessentially unreacted material comprising pre-oxidation mineralassemblages. In some cases, if warranted by the metalconcentrations, the protolith is termed protore or quasiprotore(Alpers and Brimhall, 1989). The mineralogy of the source, sink, andprotolith rock volumes varies according to whether mass transportfrom the source region to the sink region is geochemicallysignificant or minor. These geochemical domains are summarized inTable 1.

S U P E R G E N E O X I D A T I O N O F C O P P E R S U L F I D E D E P O S I T S , C O N T .

. . . from 1

Figure 1: Schematic diagram showing the weathering environment of a sulfide-bearing mineral occurrence. Three component zones comprising thesimplified weathering profile are shown, with mineral assemblages characteristic of the oxide zone displayed to the right of the diagram. See Table 2 forranges of copper values in the zone of leaching.

Table 1. Mineral Assemblages in Geochemical Domains in Highand Low Mass Flux Conditions

Well-developed copper oxide zones appear to form through twodistinct mechanisms: (1) via substantial copper addition to a volumebeing oxidized, including the formation of exotic copper deposits,and (2) through in situ oxidation of a copper-bearing sulfideresource. Importantly, the first type of copper oxide system requirescopper transportation from a source region, but the protore does notneed to have high copper content if leaching and precipitation areefficient. Conversely, the second type requires substantial protolithcopper content if the copper oxide zone developed is to be ofpotential ore grade, and requires also that removal of copper beminimal.

Distinction between these protore environments is significant inexploration for copper oxide and supergene sulfide enrichmenttargets because prospects dominated by reactive rock units are likelyto display only incipient copper enrichment unless an adjacent oreroded non-reactive source-rock volume was available to providetransported copper. For example, an eroding phyllic or argillicalteration zone of a porphyry system may provide copper to a sinkcomprising a reactive (K silicate or propylitic) rock mass, whether insitu or exotic. This is why in situ copper occurs at El Abra (seebelow), Lomas Bayas, Mantos Blancos, and Radomiro Tomic, andexotic copper occurs at Mina Sur (Extica), Huinquintipa, El Tesoro,Ichuno, and La Cascada, Chile (Mnchmeyer, 1997).

To generate the first type of copper oxide occurrence, a sourceregion must be available to supply copper via oxidation andleaching. Pyrite is the most significant source of oxidized S and,indirectly, hydrogen ions, in a sulfide-bearing rock volumeundergoing weathering. It is also a substantial, if not dominant,source of oxidized iron. As these components are intimatelyinvolved with copper mobilization from the source region, oxidationof pyrite is important to generate a well-developed copper oxide oredeposit via copper addition.

Oxidation of pyrite involves a series of stepwise processesresulting in the generation of protominerals such asschwertmannite and ferrihydrite, the solubility of which is a functionof the production of Fe+++ and Fe++, pH, and SO4= activity (Murad etal., 1994). The combination of sulfate as a complexing anion,hydrogen ions (i.e., acid conditions), and atmospheric oxygen toenhance and maintain an oxidizing environment results indestruction of sulfides, oxides, and silicate minerals (Titley, 1982;Titley and Marozas, 1995). Importantly, the relative susceptibility tooxidation of sulfide minerals determines the sequence of sulfidemineral destruction, the consequent availability of metals forsupergene transport, and the nature and zoning of resulting minerals(Bladh, 1982). Figure 2 shows the general succession of sulfidemineral destruction by chalcocite replacement, as observed fromparagenetic relationships shown by oxide-sulfide zone assemblages.Boyle (1994) shows a similar sequence for sulfide replacementwithin sulfidic tailings undergoing oxidation.

Figure 2: Paragenetic diagram showing the general succession of sulfidemineral destruction by chalcocite replacement, as observed fromparagenetic relationships shown by oxide-sulfide zone assemblages.Boyle (1994) shows a similar sequence for sulfide replacement withinsulfidic tailings undergoing oxidation.

The oxidation of sulfides other than those of iron produces onlymodest quantities of acid sulfate-bearing solutions (Anderson, 1982;Williams, 1990), a factor which is significant in determining the typesand distribution of oxide minerals developed within a zone ofweathering (see below). Therefore, pyrite oxidation is generally themost important source of the acidic solutions responsible for mineraldestruction during the weathering of a rock volume. This meansthat pyrite quantity is critical in determining oxide zone mineralogy.

Pyrite is a relatively refractory mineral in the replacement sequence;marcasite oxidizes more quickly than pyrite (Mason and Berry, 1968),and pyrrhotite oxidation is as much as two orders of magnitude fasterthan oxidation of pyrite (Nicholson and Scharer, 1994). Laboratoryobservations of Fe sulfide oxidation are corroborated by the para-geneses of oxide and sulfide minerals reported from oxide zones: itis observed that pyrite shows incipient or no significant corrosion-replacement even when other sulfides in the same oxide volumedisplay substantial oxidation, as in leached caps or gossans, or variablereplacement by oxides or sulfides as seen at Chuquicamata(Flores, 1985; G. Ossandn et al., unpub data1) and Mantos Blancos(Chvez, 1983), Chile; and Lakeshore, Arizona (Cook, 1988; Huyck,1990). Therefore, for pyrite to provide a significant source of acidsulfate-bearing solutions, weathering conditionsmust be strongly oxidizing.

1 Ossandn, G., Frraut, R., Rojas, J., and Gustafson, L.B., in review, Geology ofChuquicamata Revisited: Economic Geology.

Hierarchy of sulfide mineral destruction via supergene chalcocite replacement

Rapid Slow

Sphalerite, BorniteGalena, Sulfosalts, Enargite

Arsenopyrite, Chalcopyrite, Pyrrhotite, PentlanditeMarcasite, Pyrite

Dominantly In SituOxidation

Low total sulfide volumes or low S/metal sulfides

Quasi-in situ oxidation andprecipitation of hematite;hematite> to goethite,jarosite

Atacamite, brochantite, native copper, chalcosiderite, cuprite, tenorite, paramelaconite, malachite, phosphates; local alunite; residual chalcopyrite, bornite, pyrite

Bornite, hypogene chalcocite, chalcopyrite, pyrite

Dominantly TransportedFe and Cu

Reactive sulfides with jarosite, goethite hematite;

Residual pyrite, chalcopyrite; alunite, Al-Fe sulfates

Chalcanthite, bonattite, antlerite, brochantite, posnjakite; local native copper

Chalcocite, covellite, pyrite, chalcopyrite

Also: alunite, As-Fe oxides, arsenates

Pyrite, chalcopyrite; traces of bornite, pyrrhotite

Source

Sink

Protolith

APRIL 2000 N 41 S E G N E W S L E T T E R 11

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Other sources of acidic solutions, albeit generally minorcompared to sulfides, include magnetite and Fe-bearing silicates.Silicate minerals that contain Fe++ are susceptible to oxidation, andminerals such as biotite, Fe amphiboles, Fe pyroxenes, and Fe-bearing garnets (e.g., the La Democrata skarn system in the Cananeadistrict, Mxico) may contribute to the generation of acid solutionsduring weathering. This is because ferric iron, produced duringmafic mineral oxidation, generates goethite plus hydrogen ions viareactions such as:

Fe+++ + 3H2O = Fe(OH)3(s) + 3H+ (aq) (1)

The same type of reaction explains why magnetite, a commoncomponent of ore deposits, is capable of producing acid solutionseven from mineralized rocks having scant or no sulfide minerals.

LEACHED CAPPINGS:SOURCES OF METALS

The metals that ultimately accumulate in the oxide or sulfideenrichment zone are derived from the volume of rock that hasundergone oxidation and metal removal, referred to as the leachedcapping (developed from disseminated and fracture-controlled

sulfides; Locke, 1926) or gossan (developed from massive sulfidebodies, including skarn-hosted sulfides).

The extent to which the leached capping, oxide volume, andsulfide enrichment volume are developed depends on the amount ofacid-producing sulfides in the rock volume, the neutralizing capacityof the minerals in the host rocks, the density and extent of host-rockfracturing, and the nature and duration of local and regionalweathering conditions (Lpez and Titley, 1995). Although removalof metals from the leached capping may be very efficient, residualcopper and iron are always present in detectable quantities andcomprise the geochemical anomaliesboth positive and negativeimportant to minerals exploration and to environmentalconsiderations of waste-rock disposal.

Table 2 provides examples of the residual copper values reportedfrom leached rock volumes over porphyry copper deposits. Coppercontributed from rock masses undergoing oxidation and removal ofmetals and sulfate is transported by acid solutions, dominantly ascupric copper. Figure 3 shows the general parageneses for copperphases related to different protolith sulfide assemblages for relativelyreactive protoliths.

Copper is mobile at low pH, so copper occurrence in someenvironments may be represented by cupric ion as well as byminerals. Although copper oxide minerals display a wide range of


. . . from 11

Figure 3: Oxidation path diagram showing paragenesis of copper oxides derived from low to moderate total pyrite protoliths. Note that the endingparagenesis, developed in geochemically mature copper oxide zones, comprises a series of Cu + Fe Mn oxides, dominated by hematite (rather thangoethite or jarosite).

Table 2. Copper Content of Leached Cap Volumes

DISTRICT LEACHED CAP COPPER CONTENT

Cananea, MxicoX0 to low X00 ppm Cu derived from pyriticprotolith with jarositic-goethite dominantcapping

Cerro Colorado, ChileUp to 2,000 ppm, as contamination from relichypogene sulfides and residual supergenechalcocite Cu oxides

Quebrada Blanca, Chile700 to 1,500 ppm in a hematitic leached cap,probably derived from the incomplete oxidationof former chalcocite

La Escondida, ChileLess than ~100 ppm in superleached cap,enhanced through chloride activity andessentially inert host rocks

El Abra, Chile

No leached cap in well-developed K silicatestable protolith with cp + bn + cc protore(~0.65% Cu) and in situ chrysocolla +brochantite + pseudomalachite + neotociteCu-oxide zone (avg ~0.55% Cu)

Morenci, Arizona X0 to 800 ppm Cu; protore Cu concentrationapproximately 1,2001,500 ppm

Tyrone, New Mexico200 to 400 ppm in jarositic to goethitic leachedcap developed from pyritic protolith containing7001,200 ppm copper

Santa Rita, New Mexico

X0 to low X00 ppm Cu in hematitic to goethiticleached cap developed over phyllic-argillicalteration of monzonitic hosts; local nativecopper

Radomiro Tomic, Chile Up to 1,000 ppm in poorly developed leachedvolumes derived from K silicate protolith

Lomas Bayas, ChileLeached and oxidized rock volumes contain X00ppm copper with residual Cu values to >1,000ppm as sulfates, chlorides

Cerro Colorado, PanamNo significant leached cap in humid, high-rainfall(>4,000 mm/year), steep terrain; protolithcopper concentrations 4,0009,000 ppm

stability, specific suites of copper oxides are useful in limiting theinterpretations concerning weathering environments and the genesisof copper oxide minerals (Locke, 1926; Schwartz, 1934). Thisindicates that copper oxide minerals represent broad conditions ofoxidation and pH; nonetheless, the mineralogy of a given oxideassemblage is very useful in assessing the Eh-pH conditions ofcopper oxide formation, including those conditions responsible forcopper transportation and deposition. The following sectiondescribes the formation of copper oxides and associated minerals inthe oxide zone of a weathering mineral deposit containingdisseminated and fracture-controlled sulfides.

COPPER OXIDE ZONE DEVELOPMENTThe oxide zone is defined as the rock volume representing a

redox environment transitional between the very oxidized conditionspresent in the leached capping and the reduced conditionscharacterizing the supergene sulfide zone. Oxide zone mineralogyreflects variably oxidized and reduced conditions, with mineralzoning exhibited on both large and small scale. Table 3 listsminerals commonly found in the oxide zone and leached capping ofporphyry copper deposits.

Table 3. Minerals Commonly Found in the Oxide Zone ofCopper Deposits

Alunite . . . . . . . . . . . . . . . . . . . . . . . . . . . . . KAl3(SO4)2(OH)6Antlerite . . . . . . . . . . . . . . . . . . . . . . . . . . . . Cu3SO4(OH)4Atacamite (paratacamite, botallackite) . . . . . Cu2Cl(OH)3Bonattite . . . . . . . . . . . . . . . . . . . . . . . . . . . . CuSO43H2OBrochantite . . . . . . . . . . . . . . . . . . . . . . . . . . Cu4SO4(OH)6Ceruleite . . . . . . . . . . . . . . . . . . . . . . . . . . . . Cu2Al7(AsO4)4(OH)1312H2OChalcanthite (compare to krhnkite) . . . . . . . CuSO45H2OChalcosiderite (compare to turquoise) . . . . . CuFe6(PO4)4(OH)84H2OChenevixite . . . . . . . . . . . . . . . . . . . . . . . . . . Cu2 Fe+++2(AsO4)2(OH)4H2OChrysocolla (mineraloid) . . . . . . . . . . . . . . . . Cu(Fe,Mn)Ox-SiO2- H2O, with

copper content varying from ~20-40 wt-% Cu

Copiapite. . . . . . . . . . . . . . . . . . . . . . . . . . . . Fe5(SO4)6(OH)220H2OCoquimbite . . . . . . . . . . . . . . . . . . . . . . . . . . Fe2(SO4)39H2OGoethite . . . . . . . . . . . . . . . . . . . . . . . . . . . . -FeOOHJarosite. . . . . . . . . . . . . . . . . . . . . . . . . . . . . KFe3(SO4)2(OH)6Krhnkite. . . . . . . . . . . . . . . . . . . . . . . . . . . . Na2Cu(SO4)22H2OLavendulan . . . . . . . . . . . . . . . . . . . . . . . . . . NaCaCu++5(AsO4)4Cl5H2OLibethenite . . . . . . . . . . . . . . . . . . . . . . . . . . Cu2PO4(OH)Paramelaconite . . . . . . . . . . . . . . . . . . . . . . . Cu4O3 (see tenorite (CuO) and

cuprite (Cu2O))Poitevinite . . . . . . . . . . . . . . . . . . . . . . . . . . . (Cu,Fe,Zn)SO4H2OPosnjakite . . . . . . . . . . . . . . . . . . . . . . . . . . . Cu4SO4(OH)6H2OPseudomalachite (see libethenite) . . . . . . . . Cu5(PO4)2(OH)4Scorodite (see chenevixite) . . . . . . . . . . . . . Fe+++AsO42H2OTurquoise . . . . . . . . . . . . . . . . . . . . . . . . . . . CuAl6(PO4)4(OH)84H2OVoltaite . . . . . . . . . . . . . . . . . . . . . . . . . . . . . K2Fe8Al(SO4)1218H2OWroewolfeite (Langite) . . . . . . . . . . . . . . . . . Cu4SO4(OH)62H2O

Copper oxide minerals form (1) though direct precipitation assupergene solutions reach saturation with a specific mineralcomponent(s), or (2) via replacement of sulfides, oxides, or silicateminerals. In most environments, oxidation of hypogene sulfideswith high S/metal (S/Me) mole ratios, such as pyrite, marcasite, andpyrrhotite, results in at least incipient destruction of the originalsulfide and the resultant dissolution of iron as Fe+++ and sulfur asSO4=. However, oxidation of sulfide-bearing rocks with low totalpyrite content and of minerals with S/Me ratios of approximatelyunity, such as chalcopyrite, idaite (Cu3FeS4), pentlandite, enargite,and arsenopyrite, usually results in the formation of combined Feand metal oxides having geochemically limited mobilities becausethere is insufficient acidity generated during weathering to ensurecomplete removal of the original mineralcomponents. For this reason, chalcopyrite


to page 14 . . .


oxidation generally leads to the development of local hematite goethite halos adjacent to the replaced mineral grain, accompaniedby copper oxides that are stable in the near-neutral to moderatelylow pH range.

Figure 4 shows reaction paths for copper oxide minerals formedwithin (1) reactive host rock and (2) relatively non-reactive hostrock, starting with a protolith containing pyrite, chalcopyrite, andminor bornite. The geochemical reactivity of host rocks is significant(Marozas, 1982; Pinson, 1992) because the quantity of silicateminerals available for acid neutralization directly influences the localleaching and oxide zone geochemical environment. Although theabundance of reactive minerals is important in determining how arock mass will react to acidic solutions, reaction kinetics may inhibitthe ability of a reactive protolith to neutralize acid, sulfate-bearingsolutions. The relatively slow reaction of most silicates with acidicsolutions generated via pyriticsulfide oxidation is especiallynotable in mine environmentalremediation studies in whichreactive silicates comprise part ofthe acid-buffering component of amine waste (Walder and Chvez,1995).

The mineralogy of the host rockplays a very significant geochem-ical role in the development of thegangue and ore mineral assem-blages occurring in the copperoxide zone. This is because host-rock silicates and oxides, compris-ing the volumetrically dominantminerals in the weathering environ-ment, offer exchangeable cationsand thus are capable of consuminghydrogen ions via hydrolysis. Thegreater the quantity of reactive sili-cates and oxides such as feldspars,mafic minerals, and carbonates, thegreater the ability of a wall rock toneutralize acid, sulfate-bearingsolutions. This buffering capacity islimited in rock that has alreadybeen subjected to phyllic, argillic,and advanced argillic alteration,because phyllosilicates and clayscharacteristic of these assemblageshave only limited capacity toexchange cations for H+.

In Figure 4, arrows show thesequential development of copperoxide and associated sulfides, withpaths determined by protolithsulfide ratios and the completenessof weathering reactions. The pathslead to oxide assemblages that are

mineralogically distinct because the geochemical conditions thatform the various assemblages are dictated by specific combinationsof sulfide and host-rock mineralogy, structural setting of theweathering rock mass, and lithologic variations.

These geochemical conditions produce the mappable mineralassemblages characteristic of the oxide zone. Interpretation of theenvironment of formation of the mineral assemblages is animportant part of the economic evaluation of copper oxide (andsulfide) prospects. For example, chalcocite oxidation and leachingproduces an assemblage of Fe oxides referred to as live limonites;this term really refers to red hematite-dominant Fe oxideassemblages, generated as a result of copper removal by supergenesolutions derived from residual acid production. Thus, thegeneration of red hematite during oxidation of supergene sulfideshaving very minor iron may be explained by the oxidation ofchalcocite in low-pyrite or high-pyrite environments, as in thefollowing reactions.


. . . from 13

Figure 4: Paragenesis of copper oxides starting with a pyrite-dominant protolith. Copper oxide assemblagesare a function of successive oxidation-mobilization-accumulation cycles, with paths shown for geochemicallyreactive and nonreactive host rocks. Lower tier shows mineral assemblages resulting from various oxidationscenarios, beginning with a supergene sulfide assemblage. The oxidation of sulfidic mine wastes mimics thatshown here for natural systems, with corresponding applications for environmental remediation of abandonedminesites.

A low total residual pyrite environment results in the formation ofsubstantial ferrous sulfate, which participates in oxidation reactionsas follows:

Cu2S(s) + 2Fe++SO4(aq) + H2O + 3O2 = chalcocite + ferrous sulfate

Fe2O3(s) + 2CuSO4(aq) + H2SO4red hematite + cupric sulfate (2)

If residual pyrite content of an oxidizing protore is relativelyhigh, this results in generation of ferric sulfate, which participates inoxidation reactions as follows:

Cu2S(s) + Fe+++2(SO4)3(aq) + 2H2O + 2.5O2 = chalcocite + ferric sulfate

Fe2O3(s) + 2CuSO4(aq) + 2H2SO4red hematite + cupric sulfate (3)

In each environment, copper is liberated and hematite takes theplace of the now oxidized and dissolved copper sulfide. At leasttraces of copper remain associated with the newly generated redhematite. This copper may occur as geochemical copper adsorbedonto the surface of iron oxides or as minute grains of distinct copperminerals admixed with the red hematite. The association ofabundant hematitic Fe oxides with trace copper is common inleached environments, which otherwise show no obvious copperoxide occurrence. These oxides are termed almagre or sangre detoro in Central and South America, and may contain economicallyimportant quantities of copper. In some cases, the copper mayoccur as cuprite or native metal, rendering copper recovery difficult(e.g., portions of the Ray, Arizona, oxide zone). In cases wherepyrite was present in stoichiometric excess (usually greater than 57vol % pyrite), its oxidation may produce enough acid to removeessentially all iron and copper, such that supergene iron oxideabundance and copper content may each be minor.

With the descent of metal-bearing, acid sulfate-rich fluids,hypogene sulfides may be replaced initially by chalcocite, djurleite(Cu1.96S) or digenite (Cu1.8S), with subsequent replacement of thesesulfides by copper oxides as availability of reduced sulfur diminishesas sulfides are consumed. Covellite develops in environments thatlack abundant dissolved Cu++, usually by in situ oxidation andreplacement of chalcopyrite or bornite, rarely pyrite. Hence, theparagenesis of sulfide replacement may involve several coppersulfides prior to ultimate copper oxide development. Replacementof sulfide assemblages having low S/Me ratios or high coppercontents (covellite, chalcocite, digenite, bornite) may result in thedirect precipitation of copper oxides e.g., at Radomiro Tomic(Arcuri and Brimhall, 1998); Quebrada M in the El Salvador district,Chile, and Morenci, Arizona because the local geochemicalenvironment is moderately low to near-neutral pH, which isfavorable for copper oxides that are stable in the range of pH 4 to 9(Fig. 3; see also Anderson, 1982).

COPPER OXIDE PARAGENESIS AND ZONING

The paragenetic sequence of copper oxide minerals observedfrom many oxidized copper-bearing orebodies reveals that a specificseries of progresive mineralogic changes takes place duringsupergene oxidation, transport, and precipitation. This section

discusses copper mineral paragenesis and spatial zoning in thecontext of mineralogic associations, protolith compositions, andhost-rock alteration assemblages.

Copper deposits in which pyrite is a volumetrically significantcomponent are characterized by copper oxide assemblages reflectinglow pH environments. Pyrite rarely shows direct replacement bycopper oxides because the microenvironment developed by pyriteoxidation is usually so acidic that only copper sulfates and anattendant series of iron sulfates, such as jarosite, coquimbite,copiapite, melanterite, and voltaite, are stable. For example, if pyritecontents are such that the neutralizing capacity of host rock isexceeded and pH of


representing an in situ replacement assemblage with little or nosignificant copper addition or transport.

In systems characterized by near-neutral or slightly alkaline pHenvironments, cuprite replaces chalcocite (e.g., Cerro Colorado,Copucha (Sierra Gorda), and El Abra, Chile; locally at Ray, Arizona,and Santa Rita, New Mexico). Cuprite represents an intermediatereplacement product in many oxide zones, and is almost alwaysreplaced by other copper oxide minerals. Native copper usuallyoccurs with cupriteEl Abra, Chile; Santa Rita, New Mexico; Ray,Arizona; Piedras Verdes, Mexico (Dreier and Braun, 1995); SanJorge, Argentina (Williams et al., 1999)but rarely directly replaceschalcocite. Native copper occurs generally at greater depth thancuprite (Anderson, 1982).

Malachite and azurite are common constituents of copper oxidezones in which carbonate is available from sedimentary sources(notably in oxidized skarn systems, e.g., Christmas, Koski and Cook,1982; Morenci, Arizona, and Cananea, Mexico, Velasco, 1966),atmospheric sources, and/or indigenous bacteria cells (Enders,2000). Carbonates, along with the mineraloid chrysocolla, generallycomprise paragenetically late minerals, replacing earlier oxides andsulfides and occurring as transported constituents occupyingotherwise clean fractures, including fractures showing no evidenceof prior mineralization (e.g., southern Per coastal batholith).

In geochemically mature copper oxide systems developed undernear-neutral to alkaline pH conditions, malachite and chrysocolla aretypically the most important copper minerals, with tenorite,paramelaconite, and neotocite are volumetrically minor. This isprobably because carbonates and silicates are most stable in a well-developed oxidation environment in which sources of low pHsolutions have been consumed, and because indigenous andatmospheric sources of silica and carbonate, respectively, are readilyavailable. Incipient and generally subeconomic fracture-controlledcopper carbonates and chrysocolla occur paragenetically late inoxidized copper deposits at Cerro Colorado and Cerro Chorcha,Panam; along the southern Per coastal batholith and in adjacentnorthern Chile, and in late-stage oxidation assemblages in thesouthwest United States. Exotic copper deposits (Newberg, 1967;Angita, 1997; Mote and Brimhall, 1997; Mnchmeyer, 1997) arealmost exclusively chrysocolla dominant, with minor atacamite,copper wad, tenorite, and/or Fe-Mn-Cu oxides (including neotocite).

Tenorite and paramelaconite, the black copper oxides, occur inthe upper zones of copper systems in which high host-rockreactivity and low pyrite content produce alkaline to neutral pHenvironments. If carbonate is available to buffer low pH solutionsproduced through sulfide oxidation, tenorite and paramelaconitemay occur in local environments characterizing oxidized pyriticsulfide systems, especially skarns (e.g., Morenci, Arizona). At ElAbra, Chile, tenorite and paramelaconite comprise the constituentminerals in neotocite; along with chrysocolla, neotocite occurs insurface outcrops and at shallow depths of the El Abra oxide orebodywithin reactive host rock comprising biotite-stable diorite porphyry.The tenorite and paramelaconite association grades with increasingdepth to the assemblage cuprite native copper (A. Moraga, pers.comm., 1999); this assemblage is replaced by and grades with depthto brochantite. This change with depth is consistent with a gradualchange in copper oxidation state, decreasing with increasing

distance from the former erosional surface. The observedparagenesis, in which black copper oxides replace the assemblagecuprite +native copper brochantite, supports the argument that theoccurrence of tenorite paramelaconite neotocite indicates themost oxidized zones of a weathering, low total sulfide protolith.

The paragenetic paths shown in Figures 3 and 4 summarize theobservations above. Oxidation products for arsenic-bearing ores,common components of hydrothermal ore deposits, are summarizedin Figure 3. Arsenopyrite, when oxidized in an environmentcontaining pyrite, yields the iron arsenate scorodite characteristic ofthe upper portions of an oxide zone. Similarly, enargite oxidation inthe presence of pyrite produces scorodite (Summitville, Colorado; LaCandelaria breccia at Morenci, Arizona; La Grande, Collahuasidistrict, Chile). In a low pyrite environment, enargite is replaced bya series of apple green to pastel blue copper arsenates such aschenevixite, ceruleite, and lavendulan (e.g., in the weatheredepithermal Cu-Au-As systems at El Guanaco and La Grande, Chile,and in the oxide zone at Chuquicamata, Chile).

EXAMPLES OF COPPER OXIDEDEPOSITS

The following examples of settings in which copper oxides ofeconomic importance have developed demonstrate that both themineralogy and amount of copper oxides vary significantly.

Systems Displaying Limited Copper MobilityEl Abra. The El Abra porphyry copper deposit of northern Chile

is an example of supergene oxidation generated within a reactivehost-rock environment (Fig. 5). This world-class ore depositcomprises a well-developed, fracture-controlled copper oxideorebody derived from essentially in situ oxidation of a low-pyrite,chalcopyrite + bornite + chalcocite protolith assemblage hosted bydioritic intrusions. Host-rock alteration consists of ubiquitous biotitewith subordinate K feldspar replacement and veining. Incipientwhite phyllosilicate overprint of the K silicate assemblage occurslocally and distal to the K silicate assemblages.

Copper oxides at El Abra comprise assemblages characteristic ofmoderate-pH weathering environments because insufficient pyritewas available for production of low-pH supergene solutions. Theoxide orebody outcrops, with surface and near-surface oxidescomprising chrysocolla, paramelaconite (Cu4O3, similar inoccurrence to tenorite, CuO), and neotocite, shown by X-raydiffraction studies to be a physical mixture of Fe and Cu oxides,notably tenorite. This assemblage gives way at depth to brochantiteand copper phosphates, such as pseudomalachite. Suprajacent toand within the weakly developed chalcocite enrichment volume andin the upper portions of the hypogene sulfide zone, cuprite, nativecopper, brochantite, and chrysocolla are developed. This latterassemblage displays a typical paragenetic sequence in whichchalcocite is replaced by the sequence:

Chalcocite cupritenative copper brochantite chrysocolla

Because copper grades in the oxide zone are essentially the sameas those in the hypogene protolith, it is interpreted that the El Abracopper oxide-copper sulfide orebody represents in situ oxidation ofthe hypogene sulfide assemblage, with copper transport limited toperhaps several tens of meters. The development of copper oxidesfrom oxidation of a low-pyrite, reactive protolith containing lowS/Me ratio minerals at El Abra is similar to that observed atRadomiro Tomc (Acuri and Brimhall, 1998, 1999), and other


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northern Chile ore deposits hosted byintermediate volcanic rocks, such as theatacamite-chrysocolla assemblages at MantosBlancos (Chvez, 1983) and Michilla (Soto andDreyer, 1985). An exotic copper oxideresource (Ichuno) exists adjacent to theprincipal copper oxide orebody at El Abra.This occurrence may be explained by aneroded copper source rock, possibly a phyllicalteration assemblage, formerly locatedsuprajacent to the present potassic core of theEl Abra porphyry system (A. Moraga and A.Molina, pers. comm., 1999).

Piedras Verdes. Dreier and Braun (1995)describe the occurrence of incipient copperoxide development from the Piedras Verdesporphyry copper deposit, Sonora, Mexico(Fig. 6). This occurrence comprises a low-grade, low total sulfide protolith hosted by analteration assemblage of biotite + K feldspar +quartz + tourmaline, with adjacent pyriticprotolith hosted by a phyllic alterationassemblage. Protolith copper concentrationsare on the order of 1,500 ppm, aschalcopyrite.

Piedras Verdes represents an excellentexample of the control of copper oxidedevelopment by alteration mineralogy. Wherereactive K silicate assemblages exist,weathering has resulted in the in situdevelopment of a hematitic-goethitic oxideassemblage of nearer-surface chrysocolla,neotocite, and tenorite, changing with depthto cuprite + native copper. Copper-oxide-zone copper grades atPiedras Verdes are


to page 18 . . .

Figure 6: Vertical south-north cross section through a portion of the Piedras Verdes porphyry copperdeposit, Sonora, Mxico, simplified from figure 4 of Dreier and Braun (1995). Upper diagram showsgeneral alteration mineral assemblage distribution, with host rock consisting of quartz-biotite schistand minor granodiorite porphyry. Dashed line shows base of significant supergene-derived host-rockalteration, thickening in the portion of the deposit characterized by phyllic alteration and developedonly to a limited extent in K silicate stable assemblages. Lower diagram depicts copper oxide andsulfide zones. Piedras Verdes copper oxides are well developed within the K silicate stablealteration assemblages but show only incipient occurrence in the phyllic zone. Copper sulfides,dominated by chalcocite, are found subjacent to phyllic assemblages but are weakly developed inthe K silicate stable assemblages. Protore sulfides consist of pyrite chalcopyrite molybdenite.

Figure 5: Generalized vertical cross section through the El Abra porphyry system, II Region, northern Chile. In situ development of copperoxides from a low pyrite, K silicate stable, (bn + cp + cc)-bearing protolith engendered near-neutral pH stable minerals and no significantcopper grade enhancement in the oxide zone. The copper oxide zone consists of up to approximately 200 m of mineralized host rock,beginning at the present topographic surface. Upper and lower portions of the El Abra oxide zone may be defined on the basis of dominantcopper mineralogy, as shown; the lower oxide zone displays a gradational contact with underlying and erratically-developed chalcociteenrichment. Simplified from Hawley, Moraga, and Molina (pers. comm., 1999)


essentially equal to those of the hypogene sulfides fromwhich they were derived, indicating that no significantcopper transport has taken place (Dreier and Braun, 1995).This spatial distribution of copper oxides and similarity inhypogene-supergene copper oxide grades mimics thatobserved in portions of the copper oxide zone at San Jorge,Argentina (Williams et al., 1999), and at El Abra, and isinterpreted to indicate restricted copper mobility within aweakly mineralized, reactive protolith. The copper oxideminerals observed also indicate a near-neutral pHenvironment of formation (Anderson, 1982). Notably, wherethere is phyllic alteration with high pyrite content,weathering-generated oxidation is deeper and betterdeveloped, resulting in the formation of a moderatelydeveloped chalcocite resource. Dreier and Braun (1995)report that oxidation of the chalcocite enrichment blanketyielded an in situ assemblage of chrysocolla, neotocite,tenorite, and malachite.

Mantos Blancos. The Mantos Blancos district ofAntofagasta province, northern Chile (Chvez, 1983, 1984),hosts a generally low-pyrite, andesite- to rhyolite-hostedseries of bornite + digenite + chalcopyrite covellite specularite orebodies. Figure 7 shows a portion of the Noraorebody, and the general occurrence of copper oxidescomprising paratacamite (mapped locally as atacamite) andchrysocolla. Host-rock alteration comprises well-developedalbitization with subordinate but geochemically importantchloritization, specular hematite development, and localreplacement by carbonates. Because albitic feldspar andchlorite were available for hydrolysis, and because onlylimited amounts of pyrite were available for acid generation,the oxide assemblage at Mantos Blancos is characteristic of anear-neutral pH environment, and the copper oxides arethought to represent only local (tens of meters) metalmobility.

The occurrence of specularite relics within some oxidevolumes indicates that acidic solutions capable oftransporting cupric ion did not react on a wholesale basiswith Mantos Blancos host rocks because specularite wouldhave been destroyed during such interaction. The near-surface occurrence of chrysocolla and subjacent atacamite atMantos Blancos suggests high chloride activity relative tothat of available sulfate; this is similar to the mineral zoningand paragenesis described by Arcuri and Brimhall (1998,1999) for the Radomiro Tomic deposit immediately north ofChuquicamata.

Quetena. Figure 8 shows the Quetena skarn-brecciasystem, northern Chile, in which exotic malachite andatacamite are developed in carbonate clast conglomeratesderived from erosion of silty limestones. The protolithmineral assemblage at Quetena consists of pyrite-dominantsulfides in marble skarn and hornfels derived from intercalatedlimestones and mudstones, with locally developed whitephyllosilicate replacement of siliciclastic components within thelimestones. Malachite and atacamite occur as millimeter-scalecoatings on carbonate clasts; these minerals form interlayered rinds,indicating that conditions favoring carbonate and chloride

precipitation alternated, despite the obvious carbonate source withinthe local wall rock and gravels. This is probably because source-rock carbonates, although serving as pH buffers, had elevated localsulfide contents of 4 to 5 vol percent pyrite. Under such conditions,acidic solutions were generated during weathering and were capableof liberating and transporting copper from protolith chalcopyrite into

SUPERGENE OX IDAT ION OF COPPER SULF IDE DEPOS ITS , CONT.

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Figure 7: Schematic east-west cross section through the Mantos Blancos Cu-Agsystem, II Region, northern Chile. Host andesites and rhyolites have been albitizedand variably chloritized, so rocks have substantial capacity for acid-neutralizinghydrolysis reactions. Such reactions buffer low pH solutions generated viaweathering-related destruction of protolith sulfides and determine the resultingatacamite + chrysocolla oxide mineral assemblage. Copper transport distanceswere very restricted in this environment, probably limited to several tens of metersand generally along through-going fractures. Scant but widespread native copperand silver occur within the copper oxide zone and generally below atacamite-chrysocolla.

Figure 8: Generalized vertical cross section through the Quetena skarn-brecciasystem southwest of Chuquicamata, Chile. Holocene gravels derived fromcarbonates and calcareous clastic sedimentary rocks conducted acid copper-bearing solutions near or at gravel-bedrock contact, forming incipiently developedmalachite + atacamite + anhydrite as clast coatings. Although supergene solutionpH was likely very low during initial oxidation of pyrite-bearing protolith, transportdistances for copper were restricted by the highly reactive paleochannel gravels;maximum transport distances at Quetena are on the order of 200 m.

the alluvial gravels developed on hill slopes adjacent to the erodingskarn-breccia system. Paragenetically latest anhydrite occurs asmillimeter-scale patinas covering copper oxides, probably the resultof gypsum dehydration. The maximum copper transport distance atQuetena is on the order of 200 m.

Systems with Evidence for Enhanced Copper MobilityOne of the best-developed leached cappingcopper oxide zone

copper sulfide enrichment zone sequences is shown by the giantChuquicamata porphyry system, northern Chile (Little, 1926; G.Ossandn et al., unpub. data). Jarrell (1944) described theoccurrence of copper oxides in the near-surface environment,suggesting that in-place oxidation of supergene sulfides producedthe thick and well-developed copper oxide zones in the originalChuquicamata orebody. Because the Chuquicamata orebodycomprises two mineralogically distinct ore types, supergeneoxidation and consequent development of copper oxide mineralassemblages are also spatially and mineralogically distinct. Figure 9is a schematic west-east vertical cross section through theChuquicamata mine area, showing the general distribution of oxideminerals in the upper parts of the orebody.

Detailed mapping (J. Rojas de la Rivera, pers. comm., 1999)shows that two general alteration zones can be defined, comprisingK silicates (with chalcopyrite + bornite + digenite) and phyllic withincipient advanced argillic alteration (with pyrite + enargite +covellite). These alteration assemblages appear to have developedwithin a single intrusive rock unit. The Domeyko fault zone (WestFissure in Figure 9), has faulted the Chuquicamata orebody alongits western margin, forming an abrupt contact against the phyllicalteration assemblage.

Within the K silicate assemblage, weathering has produced onlylimited oxidation, with an assemblage of hematite > goethite,atacamite, and local turquoise-chalcosiderite typical of near-neutralpH conditions. However, the depth of enrichment is greatlyenhanced in the phyllic alteration assemblage, with oxidation on theorder of nearly 1 km deep, resulting in a well-developed low pH,stable assemblage of natrojarosite, goethite, chalcanthite, krhnkite,and antlerite. Below this deeply oxidized rock column is a well-developed supergene chalcocite covellite enrichment zone thatdisplays an apparently gradual and poorly defined contact withhypogene pyrite + enargite + covellite tennantite.

Because the host-rock phyllic alteration assemblage has onlyminor capacity to neutralize acidity, solutions generated from theoxidation of protolith with very high pyrite content produced a verylow pH, stable copper and iron oxide assemblage, dominated bysulfates. These solutions were also able to transport copper awayfrom the near-surface environment until they reacted with reducedsulfur, producing the exceptionally well developed chalcocite covellite enrichment volume at Chuquicamata. Lateral transport ofcopper at the southern margin of the Chuquicamata orebodyproduced the economically important Mina Sur (Extica) exoticcopper deposit (Angita, 1997; Mnchmeyer, 1997), which is apaleodrainage system containing copper transported at least 6 kmaway from the Chuquicamata mine area. This scale of coppertransport is similar to that noted in the mineralized gravels of the Huinquintipa Este sector of the Collahuasi district north of Chuquicamata and the Damiana copper resource within the El Salvador district, Chile (Mote andBrimhall, 1997).


Figure 9: Simplified east-west vertical profile of the Chuquicamata, Chile ore deposit, modified slightly from Jos Rojas (pers. comm., 1999). As with thePiedras Verdes system, alteration mineral assemblages control copper and iron oxide distribution and zoning. Protolith at Chuquicamata appears to havebeen a single, large-scale intrusive unit of intermediate composition (Ossandn et al., unpub. data), so copper and iron oxide distributions are a functionof fracture density and alteration mineralogy, including sulfide types and abundance, rather than protolith composition. Although the contact betweensupergene and hypogene mineral assemblages is difficult to define, the vertical column of preserved leaching-oxidation-enrichment at Chuquicamataapproaches 1 km.

to page 20 . . .


EXPLORATION IMPLICATIONSCopper oxide zones are the product of sulfide destruction

produced by weathering under oxidizing conditions. Supergenesulfides produced by the same process are not preserved unlessdevelopment of an oxide profile is limited by water table ascent orthe onset of an arid climate (Alpers and Brimhall, 1989), lack ofacid-generating sulfides in a source region, and/or presence ofreactive silicates and oxides. Current exploration for copper oredeposits favors oxide targets because the leaching technologiesdeveloped for metal recovery permit mining of relatively low gradematerials. Consequently, knowledge of the mineral zoning andmineralogic composition of copper oxide deposits is important inexploration and economic evaluation of these systems.

Copper oxide occurrences display consistent vertical and lateralzoning patterns that mimic the hand specimen-scale paragenesisshown by individual copper oxide minerals. Weathering-derivedcopper mineral distribution is characterized by a supergenegeochemical stratigraphy comprising copper oxides, iron manganese oxides, and copper sulfides. This stratigraphy begins atthe surface with a leached rock volume typified by the occurrenceof iron oxides and residual copper and manganese minerals.Depending on the distribution of fractures in the host-rock mass,leached zones may occur within and below both copper oxide andcopper sulfide horizons. Indigenous copper oxide zones, generatedvia in situ oxidation of a sulfide-bearing rock, are usually developedso that the most reduced copper oxides (native copper and cuprite)are formed in the lower portions of the oxide column, suprajacent toand replacing supergene copper sulfides.

As oxidation continues, hydroxy-sulfates are developed at theexpense of native copper and cupite, so brochantite, antlerite, andrelated sulfates comprise minerals in the topographic middle of anoxide column. As oxidation matures and acid-generating mineralsare consumed, supergene solution pH becomes more moderate, andthe upper parts of the geochemical stratigraphy develop chlorides,silicates, and phosphates. Contacts between mineral sub-zoneswithin the copper oxide zone are gradational, and may be erratic iftectonic and/or structural settings allow the phreatic zone andcapillary fringe to vary vertically and/or laterally. Very soluble ironand copper sulfates develop throughout the oxide zone column ifoxidizing pyritic sulfides continue to supply acidic solutions.

This bottom-to-top copper oxide zoning is mappable vertically,and in exotic systems, laterally (Angita, 1997; Mnchmeyer, 1997).Interpretation of the distribution and mineralogy of copper oxidesencountered in surface outcrops and in drill hole intervals permitsdevelopment of a model for the geochemical environment(s)responsible for metals oxidation, transport, and precipitation withina sampled oxidation profile. Copper oxide prospects may then beevaluated for their potential for the occurrence of a target oremineral assemblage. For example, in exploration for large-tonnage,low-grade deposits, green copper oxides are a more metallurgicallyfavorable target than a cuprite-native copper mineral assemblage.Exploration for brochantite-antlerite-chrysocolla would target themiddle of a well-developed copper oxide zone or the upperportions of a weathering profile showing only incipientdevelopment.

The lateral mineral zoning at the margins of a weathered sulfideore deposit, including exotic mineral occurrences, can be used toassess the geochemical maturity of the oxidation environment andthe direction(s) from which supergene solutions deposited copperminerals. Integration of geochronologic results with studies oflandform development, geomorphology, and the distribution ofcopper oxides and sulfides (e.g., Clark, 1967; Sillitoe and McKee,1996) provides complementary information useful in assessing thegeologic history of an exploration target, and the consequenteconomic potential of copper oxide ore deposit occurrence.Metallurgical studies will dictate which portions of a copper oxideassemblage, if any, are economically extractable if host-rockreactivity is recognized to be high. At the termination of mining,understanding copper oxide mineral genesis is useful in directingefforts at mine remediation and ultimate recovery of copper frommine wastes.

ACKNOWLEDGMENTSIt is a pleasure to acknowledge thoughtful and constructive

reviews of the initial draft of this manuscript by Jeff W. Hedenquist,Pepe Perell, and David Hopper. Continued study of supergenecopper ore deposits by the author has benefited by the contributionsof New Mexico School of Mines graduate students J.A. Amarante, D.Djikine, W. Jonas, A. Mioduchowski, P. Pinson, W. Seibert III, and C.Spencer. Discussions with D. S. Andrews, W. Glvez, A. Moraga, A.Molina, W. Orquera, J. Pizarro C., J. Rojas de la Rivera, F. Ramrezand J. Vega E. were instrumental in developing ideas concerning theparagenesis of weathering copper deposits. Roger Nordin and RafaelChavarra of Compaa Minera Boliden and Fernando Len P. ofMinera Lomas Bayas provided useful commentary on coppermineralogy and the depths of oxidation in some areas of northernChile. Field observations by R. Ayala F., S. Enders, J.W. Hawley,R.M. North, R. Stegen, and S.R. Titley were especially useful ininterpreting southwest North America oxidized orebodies.

Erich U. Petersen suggested the idea of using the SEG web pageto include additional information and photographic documentationof copper oxide mineralogy; his savvy and skill are muy agradecido.The patience and support of Noel C. White during the developmentand review of this article are appreciated and gratefullyacknowledged.

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copper sulfideabundance

y h y fierro fe y fe

cobre y fierro

cobre y molibdeno

thecopper oxide minerals

y sistemas tipo skarn

mineral assemblages

influido por