# Origins of Chalcocite Defined by Copper Isotope Values

Authors: R. Mathur; H. Falck; E. Belogub; J. Milton; M. Wilson; A. Rose; W. Powell
Journal: Geofluids
 (2018)

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## Abstract

The origin of chalcocite is explored through a comparison of the copper isotope values of this mineral from supergene enrichment, sedimentary copper/red bed, and high-temperature hypogene mineralization around the world. Data from the literature and the data presented here(n=361) reveal that chalcocite from high-temperature mineralization has the tightest cluster of values of δCu65=0±0.6 in comparison to sedimentary copper/red bed δCu65=-0.9±1.0 and supergene enrichment δCu65=+1.9±1.8. Although the errors of the means overlap, large portions of the data lie in different values, allowing for distinguishing ranges for δCu65 of <−1‰ for sedimentary copper/red bed, between -1 and +1 for high-temperature hypogene, and >+1 for supergene enrichment chalcocite. The copper isotope values of sedimentary copper/red bed and supergene enrichment chalcocite are caused by redox reactions associated with the dissolution and transport of copper, whereas the tighter range of copper isotope values for hypogene minerals is associated with processes active with equilibrium conditions.


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## Body

## 1. The Importance of Chalcocite

Chalcocite is an economically important mineral of copper. Crystallographic, trace element, mineral assemblage, and textural observations and measurements have been used to understand the origin of this mineral [1–3]. Models regarding the genesis of chalcocite vary substantially, with conditions ranging from the highest temperature hydrothermal systems to ambient temperature weathering solutions, and no single model can be used to constrain how all of the occurrences of this mineral formed.To contribute to the understanding of how chalcocite forms and what geologic processes lead to its concentration, this study analyzes copper isotope values from the literature and from new data presented here. The data are used to distinguish different types of mineral deposits ultimately related to the geological processes that lead to the generation of this essential economically significant mineral.


## 2. Types of Chalcocite Considered and Deposits Analyzed

The genesis of chalcocite can be categorized into three general models: (1) hypogene hypothermal ores that precipitate from hydrothermal fluids (>150°C), (2) red bed and stratiform “sedimentary” ores that precipitate from fluids that circulate through sedimentary basins at temperatures <150°C, and (3) supergene enrichment ores that precipitate from low to ambient temperature oxidative fluids in near-surface environments.The copper isotope composition of chalcocite in these deposits varies due to several factors. In general, the primary source of most copper deposits is a large body of magmatic rock with an isotopic composition of approximatelyδCu65‰=0‰ (where δCu65‰=((65Cu/63Cu)sample/(65Cu/63Cu)Nist976-1)∗1000) [4–6]. However, the relatively minor variations in the isotopic composition of Cu of the dominantly magmatic source material will influence the possible values of Cu within the ore solution and the associated chalcocite. More importantly, the initial isotopic composition can be affected by fractionation during leaching of Cu from the source, as well as during precipitation of secondary chalcocite. The nature of the fractionation is dependent upon the specific dissolution and precipitation processes (e.g., bonding within the solid or in solution) and the physical and chemical conditions (e.g., temperature, redox), with redox processes leading to stronger bonding environments for 65Cu in oxidized products and 63Cu in reduced products. In addition, the extent of extraction of copper from the source and the fraction of copper that is reprecipitated in the ore-forming processes affect fractionation. If 100% of the Cu is extracted and precipitated, then no evidence of fractionation will be preserved. However, if the chemical transfer is incomplete, then the various phases (primary mineral, solution, and secondary mineral) may have differing isotopic compositions based on the degree of fractionation.Copper in chalcocite that is associated with hypogene hydrothermal ores is derived from a magmatic hydrothermal fluid or is extracted from country rocks at high temperatures. Moreover, extensive studies showed that hypogene hydrothermal copper minerals such as chalcopyrite and bornite do not display appreciable fractionation (>±1‰) [7–11]. Similarly, chalcocite that precipitated from these high-temperature fluids is not anticipated to contain copper that has undergone significant copper isotope fractionation. This study includes 18 chalcocite samples from three hypogene deposits (Table 1), including an archetypal example of hypogene chalcocite at Butte, Montana [12].Table 1
Summary of deposits analyzed and sources of data considered.
Deposit
Type of chalcocite
Data source
Butte, Montana
Hypogene
Mathur et al. 2009, Wall et al. 2011
Canarico, Peru
Hypogene
Mathur et al. 2010
Rippoldsau, Germany
Hypogene
Markl et al. 2006
Coates Lake, Canada
Sedimentary Cu
This document
Coppermine, Canada
Sedimentary Cu
This document
Dikulushi, DRC
Sedimentary Cu
Haest et al. 2009
Kupferschiefer, Germany
Sedimentary Cu
Asael et al. 2009
Cu, Michigan
Sedimentary Cu
This document, Larson et al. 2003, Mathur et al. 2014
Timna, Israel
Sedimentary Cu
Asael et al. 2007, Asael et al. 2009, Asael et al. 2012
Udokan, Russia
Sedimentary Cu
This document
Bayugo, Philippines
Supergene
Braxton et al. 2012
Chuquicamata, Chile
Supergene
Mathur et al. 2009
Collahuasi, Chile
Supergene
Mathur et al. 2009
El Salvador, Chile
Supergene
Mathur et al. 2009
Inca de Oro, Chile
Supergene
Mathur et al. 2014
PCDs, Iran
Supergene
Mirenjad et al. 2010, Asadi et al. 2012
Morenci, Arizona
Supergene
Mathur et al. 2010
Ray, Arizona
Supergene
Mathur et al. 2010, Larson et al. 2003
Silver Bell, Arizona
Supergene
Mathur et al. 2010
Spence, Chile
Supergene
Palacios et al. 2010In contrast to hypogene chalcocite, the copper associated with red bed and stratiform types of chalcocite is derived from leaching of sandstones and shales at low temperatures by residual brines. The source rocks contain Cu2+ that is hosted within detrital mafic minerals or is absorbed onto Fe hydroxides which are formed as products of weathering and diagenesis. A redox shift is thought to occur during transport of copper in these formational waters because the initial state of copper in the weathered source material is Cu2+ but the copper is mobilized in the Cu+ state as CuCl0, or similar aqueous species [13, 14]. Thus, the reaction required to mobilize copper for sedimentary deposits involves the reduction of copper, which would be expected to induce isotopic fractionation favoring 63Cu, assuming that copper extraction from the source material was incomplete. Dissolved copper remains unchanged until it encounters organic material or other reductants within the sediment, where Cu1+ is fixed by sulfide or by reaction with preexisting pyrite [15].Six locations at which chalcocite occurs within “sedimentary” copper deposits (a total of 161 samples) are considered herein (Table1). Literature sources that reported chalcocite as the major phase present in the copper isotope analyses were used [16–19] along with new data from Coates Lake, Copper Mine, Michigan, and Udokan. Data from Kupferschiefer [20], Michigan [21, 22], and Coates Lake [23] provide classic examples of sedimentary copper deposits along with the prospect, Coppermine [24]. Data from each of these deposits is compiled in Table 2.Table 2
Copper isotope data from sedimentary copper type deposits where cc means chalcocite and some samples reported trace bn (bornite).
Sample
Location
Phase
δ
C
u
6
5 (per mil)
1
Udokan, Russia
cc
-
0.32
2
Udokan, Russia
cc
-
0.04
3
Udokan, Russia
cc-bn
0.4
4
Udokan, Russia
bn-cc
-
0.34
5
Udokan, Russia
bn-cc
-
1.33
6
Udokan, Russia
cc-bn
-
0.61
7
Udokan, Russia
cc
-
0.18
8
Udokan, Russia
cc
-
1.82
9
Udokan, Russia
cc
-
0.13
10
Udokan, Russia
cc
-
1.61
11
Udokan, Russia
cc
-
1.07
12
Udokan, Russia
cc
-
0.57
13
Udokan, Russia
cc
-
0.68
14
Udokan, Russia
cc
-
1.27
15
Udokan, Russia
cc
-
0.53
16
Udokan, Russia
cc
-
0.77
17
Udokan, Russia
cc
-
0.04
18
Udokan, Russia
cc
-
0.07
19
Udokan, Russia
cc
-
1.07
20
Udokan, Russia
cc
-
0.66
21
Udokan, Russia
cc
-
0.74
22
Udokan, Russia
cc
-
0.16
23
Udokan, Russia
cc
-
0.66
24
Udokan, Russia
cc
-
0.41
9098
Coates Lake, Canada
cc
-
3.67
9110
Coates Lake, Canada
cc
-
0.40
9430
Coates Lake, Canada
cc
-
1.22
NWT 743 B1/5
Coates Lake, Canada
cc
-
0.28
JP77 7X1 2122 R2 #42
Coates Lake, Canada
cc
0.08
JP77 36984-4 3381.5 #38
Coates Lake, Canada
cc
-
0.31
NWT JP77 74121225 #45 R8
Coates Lake, Canada
cc
-
0.27
JP77 COATES 36984-1 1638 #36
Coates Lake, Canada
cc
-
0.72
NWT 7371
Coates Lake, Canada
cc
-
0.26
NWT 7Y3 B1/11
Coates Lake, Canada
cc
-
0.49
NWT JP77 644 3379 #39
Coates Lake, Canada
cc
-
0.20
JP77 781 422 #43 R4
Coates Lake, Canada
cc
-
0.38
9097 cc
Coates Lake, Canada
cc
-
2.01
7371
Coates Lake, Canada
cc
0.43
#41
Coates Lake, Canada
cc
0.96
45 r8
Coates Lake, Canada
cc
0.62
43 r4
Coates Lake, Canada
cc
0.90
7352
Coates Lake, Canada
cc
0.70
7358 A
Coates Lake, Canada
cc
0.14
#38
Coates Lake, Canada
cc
0.36
NWT 7356
Coates Lake, Canada
cc
-
0.24
NWT 7361A
Coates Lake, Canada
cc
-
0.78
JP77 36984.2 2289 #37
Coates Lake, Canada
cc
-
0.54
NWT 9410
Coates Lake, Canada
cc
-
0.60
9410
Coates Lake, Canada
cc
0.28
NWT KQ 74-11964
Coates Lake, Canada
cc
-
0.78
CM32619
Baltic Mine, Michigan, USA
cc
0.47
CM32620
Baltic Mine, Michigan, USA
cc
-
0.18
CM32621
Baltic Mine, Michigan, USA
cc
0.03
CM32622
Baltic Mine, Michigan, USA
cc
-
0.05
jk 10 h12
Coppermine, Canada
cc
-
0.69
cool rock
Coppermine, Canada
cc
-
1.35
ly 03 h16
Coppermine, Canada
cc
0.07
dn 04
Coppermine, Canada
cc
-
1.11
nr 02
Coppermine, Canada
cc
-
0.51
h13
Coppermine, Canada
cc
-
0.55
dt 02 h8
Coppermine, Canada
cc
-
0.07
rd 04
Coppermine, Canada
cc
-
1.23
rd 04-2
Coppermine, Canada
cc
-
1.24
h23
Coppermine, Canada
cc
-
0.01
ct 02 h3
Coppermine, Canada
cc
-
1.49
ly03
Coppermine, Canada
cc
-
0.10
h16
Coppermine, Canada
cc
-
0.25
jk01
Coppermine, Canada
cc
-
0.02The copper for supergene-type chalcocite is derived by oxidative weathering of rocks or ores containing Cu sulfide (e.g., chalcopyrite CuFeS2). The oxidized copper is transported downward toward the water table, where it is reprecipitated [25]. Near-surface oxidation zones in porphyry copper deposits are a classic example of this process. Commonly, some Cu remains in the leached capping. This incomplete oxidation reaction results in fractionated copper through the weathered profile. A reduction reaction of copper at the water table where fresh metallic surfaces of pyrite and other sulfides are present results in the precipitation of the reduced copper. Due to the increased pH at the water table and effective removal of copper via precipitation onto sulfide minerals, a majority of the copper is thought to be recovered from the oxidative solutions [26]. Late stage covellite (CuS) normally accompanies supergene chalcocite, further demonstrating the reductive nature of the reaction. Since reduction at the water table is essentially complete, fractionation preserved in the chalcocite from supergene enrichment will be due to the oxidation stage weathering and so would be expected to favor 65Cu. Continual reworking of the previous supergene enrichment layers due to uplift and erosion has been modeled [27, 28] to illustrate how larger degrees of fractionation would evolve.A total of 182 samples from 10 locations are considered (Table1). Any data from the following sources that had listed chalcocite as an analyzed phase was included [27, 29–36]. Data from Morenci, Ray, Chuquicamata, and Spence provide type examples of supergene enrichment in classic porphyry copper deposits.


## 3. The Behavior of Copper Isotopes and Predicted Differences for Redox Reactions

While many reactions can result in a shift in copper isotope values, redox reactions have been documented to produce the most substantial changes; redox reactions that result in oxidized copper favor the65Cu isotope, whereas reactions that result in reduced copper favor the 63Cu isotope due to stronger bonding environments for each isotope [33, 37–39]. Experimental and empirical data support the magnitude and direction of copper isotope fractionation during the redox reactions [33, 38, 39].In the case of oxidative reactions, the weathering of copper sulfide in supergene enrichment environments has been studied in the greatest detail. Solutions that leach copper during oxidation from the copper sulfide mineral become enriched in the65Cu isotope due to a stronger bonding environment [33, 38, 39]. Although the degree of enrichment (fractionation factor) is different for a variety of copper sulfides (chalcopyrite, chalcocite, bornite, and enargite), in each case, the reactions produce cupric copper (Cu+2) in solution which always has greater δCu65‰ than the starting mineral. This phenomenon has been traced in natural aqueous solutions such as rivers, lakes, groundwater, and seawater [28, 40–43].Reduction reactions involving copper have not been as thoroughly studied. Laboratory experiments that reduce copper from oxidized solutions have resulted in precipitated solids that have lowerδCu65‰ values than the starting solutions [38]. Modeling of copper isotopes in sedimentary copper deposits by Asael et al. [16] showed that the reduction of copper during transfer to solution should favor the lighter copper isotope. Thus, the available data indicate that reduction reactions favor the lighter copper isotope and that the products of the reduction have lower δCu65‰ values than the starting materials. Furthermore, current models of copper behavior during redox reactions would predict that supergene enrichment copper mineralization would be associated with higher copper isotope values than that of sedimentary copper deposits.


## 4. Methods for Cu Isotope Data Presented

A total of 68 new Cu isotope measurements from chalcocite are presented. The chalcocite samples were handpicked from veins or disseminations. X-ray diffraction techniques were used to identify mineral species present and those methods are described by Mathur et al. (2005). Approximately 30–40 milligrams of powdered chalcocite was dissolved in 15 ml Teflon jars containing 4 ml of heated aqua regia for 12 hours. Complete dissolution was visually confirmed. The solutions were dried and copper was separated using ion exchange chromatography described by Mathur et al. (2009).Isotope measurements were conducted on ICP-MS multicollectors at the University of Arizona and the Pennsylvania State University. Solutions were measured at 100 ppb and mass bias was corrected for by standard-sample-standard bracketing using the NIST 976 standard. Instrumentation setup and run conditions are described in detail by Mathur et al. (2005). Errors for the analyses presented are0.1‰ and 2σ and error calculation is described by Mathur et al. (2005). Internal cent standards were measured at both locations during the analytical sessions and the 1838 cent δCu65=0.02±0.1 (2σ, n=14).


## 5. Data and Its Implications

The histogram in Figure1 compares the distribution of copper isotope values of 361 chalcocite samples from three distinct environments of formation: supergene enrichment (182 samples), sedimentary copper deposits (161 samples), and hypogene ores (18 samples). Each datum has an error on the order of ±0.1‰ and data are binned at 0.5‰ increments. All data reported here were compared to the NIST 976 standard with mass bias controlled by standard bracketing.Figure 1
Histogram plot combined with a cartoon model of copper isotope values of chalcocite formed in three different environments. Data from the supergene group show the largest range and overlap the ranges of the other two deposit types.The mean values and 1-sigma variations for supergene enrichment chalcocite areδCu65=+1.9±1.8‰  (n=182), for sedimentary copper chalcocite are δCu65=-0.9±1.0‰ (n=161), and for hypogene chalcocite is δCu65=-0.001±0.6‰  (n=18). Although the three populations show considerable overlap in the weakly fractionated range, 64% of the sedimentary copper measurements are less than -0.8‰, and 65% of the chalcocite from supergene enrichment has δCu65 values greater than +1‰. The data portrayed in this manner indicates that the copper isotopic composition of chalcocite can be related to deposit types, with values less than -1‰ most likely related to sedimentary copper deposits, whereas values greater than +1‰ are most likely formed under supergene processes. To further detail variations in copper isotope compositions between the two genetically distinct, lower temperature deposits, a deposit specific comparison is presented in Figure 2, with 1σ variations calculated by the standard deviations of all presented data. It is significant that the deposit types have little overlap and lie completely within the ranges suggested above. Despite the fact that range boundaries are approximate and that none of the limiting values define sharp divide, this approach provides a statistically valid means for differentiating chalcocite from sedimentary and supergene processes based on copper isotope composition.Figure 2
Mean and 1σ error plot of specific deposit types comparing the supergene and sedimentary chalcocite from the presented data.Note that the variation associated with the supergene enrichment deposits is significantly larger than that for the other environments of mineralization and almost twice that of sedimentary copper deposits. This most likely reflects the fact that these supergene systems are still active, with continued mobilization and migration of copper with associated evolution of copper isotopic compositions; that is, the active supergene enrichment blanket is continuing to weather and lose65Cu during oxidation as is evident at Morenci where the top of the enrichment blanket contains chalcocite with lower copper isotope values than that found at deeper levels [30].It is interesting to note that theδCu65 range of high-temperature hypogene chalcocite directly overlaps the 0±1‰ range in δCu65 that has been documented in other copper-rich sulfide minerals (bornite, chalcopyrite) from high-temperature hypogene mineralization, as compiled by Wall et al. (2011) and Saunders et al. (2015). The overlap in isotopic composition of high-temperature hypogene chalcocite with that of high-temperature hypogene chalcopyrite and bornite suggests that the processes that lead to copper isotope variations at elevated temperature are broadly similar regardless of the resulting copper mineral assemblage. Several studies [44–46] suggest that the range of copper isotope values may be related to changes in pH or Eh or the partitioning of Cu between liquid and vapor phases as the hydrothermal solution cools. Overprinting high-temperature events could potentially lead to greater degrees of fractionation; however, none of the samples here have petrographic evidence to suggest this. Additional experimental work is needed to resolve the roles of different mechanisms that lead to these small but measurable copper isotope variations and to decide whether they vary systematically throughout a deposit as suggested by Mathur et al. (2012) and Li et al. [10].


## 6. Transportation of Copper and Precipitation of Chalcocite in Lower Temperature Solutions

The hydrothermal systems being considered involve metal migration at <150°C in mixtures of brine, diagenetic, and meteoric fluids associated with typical sedimentary copper and supergene enrichment processes [15, 25]. Geochemical modeling of reaction kinetics and equilibrium of the observed mineral assemblages greatly enhanced our understanding of how and why metals move in these environments. In general, these studies identify the controls of copper transfer and precipitation in these systems as complicated and impacted by many interrelated variables such as pH, Eh, salinity, temperature, bulk chemistry of the solution, and bulk chemistry of the substrate that initiates precipitation [47–50]. Coupled with isotopic studies of these ores and host rocks, the reaction sources and pathways can be identified.The copper in chalcocite (Cu2S) from supergene enrichment and sedimentary copper deposits is hypothesized to be mobilized and transported by two different redox reactions. For supergene enrichment, copper is oxidized from preexisting copper minerals, which are exposed to meteoric fluids during uplift and erosion. These fluids are dominantly strongly acidic due to oxidation of pyrite accompanying the Cu sulfides. The acid allows ready transport of Cu2+. As all of the deposits examined are still in the process of developing, the reaction has not been completed and some Cu is left behind in the leached zone. Thus, the source of the copper is well understood.In contrast, copper sources in sedimentary copper deposits are much debated [13, 15]. However, it is agreed that a likely source of the metal is Cu2+ adsorbed onto Fe oxides within sandstones. The following two reactions (Davies, 1978) describe how copper adheres to the adsorption of sites of Fe-oxide surfaces (see (1)) and how it is transported (see (2)) from adsorption sites:(1)SOH+Cu+2aq⟶SO-Cu+2+H+where S is the surface of the Fe oxide or other minerals (2)H++SO-Cu+2+2Cl-+e-⟶CuCl2-aq+SOH. With regard to the associated fractionation of copper isotopes, it is important to note that copper is transported in two different redox states. In these near-neutral solutions, Cu2+ is soluble, and transport is as CuCl0 or related complex ions [13]. Although many different copper molecules are likely formed in association with carbonates, sulfates, and organic ligands, it is the isotopic proportioning potential of the two redox reactions and the likelihood of partial extraction that will control the measured variations in the copper isotopes. As shown in Figures 1 and 2, the supergene enrichment chalcocite preserves a heavier copper isotope value, which most likely represents the transportation and concentration of oxidized copper in the supergene. In contrast, the reduction reactions that led to the transport of copper in the sedimentary copper resulted in chalcocite that has significantly lower copper isotope values.The data presented here indicate that redox reactions associated with copper transport are the primary means by which copper fractionates in low-temperature systems. At the deposition site, precipitation processes appear to have a negligible contribution to the degree of isotopic differentiation through fractionation. For supergene enrichment copper deposits, the oxidized copper molecule is reduced during the formation of chalcocite when the oxidized waters interact with the water table and hypogene sulfide minerals. This reduction process is highly effective in removing copper from solution [47], and the essentially complete precipitation of dissolved copper results erases the record of redox fractionation in this process. In sedimentary copper deposits, copper that is transported via CuCl complexes (such as CuCl2- and CuCl32-) does not change redox state upon precipitation. Thus, fractionation due to electron transfer during precipitation is not thought to occur in the sedimentary copper chalcocite.


## 7. Conclusions

Despite the chemical complexity of the systems from which chalcocite is produced, copper isotope values in chalcocite provide a means by which the three major sources of chalcocite may be differentiated: (1)δCu65 values less than -1.0 are most likely associated with sedimentary copper deposits; (2) δCu65 values greater than -1.0 are most likely associated with supergene enrichment; and (3) a tightly clustered population of δCu65 at 0.0 is most consistent with hypogene ores. These distinct variations in δCu65 values in chalcocite are controlled predominantly by redox reactions at low temperature and equilibrium type reactions at high temperatures. Therefore, copper isotope values in chalcocite can provide insights into the genesis of chalcocite and can be used to develop improved mineralization models.



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