Geofluids / 2018 / Article

Research Article | Open Access

Volume 2018 |Article ID 4261795 |

Yan Zhang, Runsheng Han, Shuming Wen, Pingtang Wei, "Physiochemical Restrictions of Mineral Zoning of Sediment-Hosted Stratiform Copper Deposit in SW China", Geofluids, vol. 2018, Article ID 4261795, 19 pages, 2018.

Physiochemical Restrictions of Mineral Zoning of Sediment-Hosted Stratiform Copper Deposit in SW China

Academic Editor: Andri Stefansson
Received04 Nov 2017
Accepted22 Jan 2018
Published26 Feb 2018


The Chuxiong basin, located in southwest China, is well known as a mineralization area of red-bed type copper deposits in China. These deposits are characterized by mineral zoning, which is especially true for the Dayao deposits. The mineral zoning is consistent for both horizontal and vertical zoning; from the base (center) of the ore body to the top (outermost), the mineral zones are from hematite, chalcocite, chalcocite + bornite, and bornite + chalcopyrite to pyrite. We studied the mineral zoning in detail using a thermodynamic phase diagram method, such as -, pH-, and pH-Eh, and discussed the constraints on the order of the minerals precipitation under different physiochemical conditions. It is indicated that changes in temperature have little effect on pH and Eh in the formation of minerals. S2− is stable only below 473 K, and the forming temperature of chalcocite must be below 473 K. In this paper, we also explain the mineral zoning formation mechanism and propose that the main controlling factor of mineral zoning is pH. Because this mineral zoning is widespread in sediment-hosted deposits, studies on this mechanism can considerably promote better understanding of the genesis of ore deposits in order to guide the exploration.

1. Introduction

Sediment-hosted stratiform copper deposit (SSC), concerned by many researchers [111], occurs in many places around the world [7, 1215]. It is frequently labeled as “stratiform” or “stratabound” and/or “diagenetic,” which ranks the second largest source of copper after porphyry copper-type, approximately accounting for about 20–25% of the global copper reserves [6]. SSC deposits are mainly distributed in the central Africa copper belt; central Europe copper belt; Kodaro-Udokan copper belt, Russia; Dzhekagan copper belt Kazakhstan; Dongchuang copper district, China; Belt-Purcell copper belt, USA; Redstone copper belt, Canada; and Chuxiong basin-hosted copper deposits, China [11], as represented by the Zambia and Zaire copper deposits in central Africa [16], Udokan and Jezkazgan copper deposits in the former Soviet Union [17], Kupferschiefer copper deposits in Zechstein basin [18], and so on.

As early as 1960s, Carpenter [19] and White [20] began to study the zoning phenomena in the White Pine sedimentary copper deposits, Michigan, USA. Brown [21] proposed the metallogenic model of SSC deposits and believed that copper deposits of this kind occurred in the contact between red and grey clastic horizons of redox interface and had a typical sulfide zoning: chalcocite, bornite, chalcopyrite, and pyrite. In fact, mineral zonation both laterally and vertically from pyrite to chalcopyrite to bornite to chalcocite to hematite is characteristic of SSC copper deposits [11, 22]. This pattern from pyrite to copper-rich minerals (chalcocite) has been described for many deposits [1, 6, 2229]. The same mineral zoning is found in red-bed deposits widely, one of the basic broad categories in SSC deposits [1, 6, 22, 3032].

The red-bed type copper deposits in China are mainly distributed in southern Cretaceous red-bed basins, one of the most famous is Chuxiong basin, followed by Huili basin of Sichuan Province, Yuanma basin, and Hengyang basin of Hunan Province. Chuxiong basin-hosted copper deposits were formed in the layers near the redox interface marked by the transition from purple to light grey sandstones and have an obvious mineral assemblage zoning from purple to light color layers: hematite, chalcocite, bornite, chalcopyrite, and pyrite [27, 33]. It is by no accident that deposits of this kind are characteristics of such notable mineral zoning and they originate depending on their geochemical properties and their precipitation processes.

In addition, many researchers have extensively studied the red-bed type copper deposits in China and made great achievements [23, 3446]. Tu [47] put forward the geochemical model for sedimentary and reforming metallogenesis. Ran et al. [48, 49] systematically investigated the geochemistry of copper, salt, and organic matter associated deposits in Chuxiong Basin and the floor structure of copper deposits, especially in experimental studies on organic geochemistry. Zhuang et al. [50] discussed the metallogenic process of copper deposits through water-rock interaction. Wang [51] made the regional metallogenic prediction of copper deposits in Chuxiong basin. Tan [52] studied the red-bed type copper deposits from the geochemistry and metallogenic dynamics points of view. Li and Pu [43] extensively studied the red-bed type copper deposits in Lanping-Simao basin, western Yunnan Province, especially on their transformation, and further discussed the mechanisms underlying mineral activation, migration, and precipitation in the surrounding rocks using experimental geochemical method.

In these researches on the mineral zoning characteristics of red-bed type copper deposits in Chuxiong basin, they pointed out that metallic minerals zoning is controlled by the oxidation-reduction conditions during the principal metallogenic epoch [53, 54]. Chen et al. [55] studied the zoning characteristics and the genesis of red-bed type deposits of the Chuxiong basin and suggested that mineral zoning resulted from the interactions of the oxidizing brine rich in cooper with the reducing sulfurous fluid, while minerals precipitation at the different stages resulted from these interactions. Gao [56] made a pH-Eh phase diagram at = 323.8 K, based on which they affirmed that minerals zoning is controlled by pH under reducing condition.

However, the physiochemical conditions for the formation of mineral assemblages in Chuxiong Basin-hosted copper deposits have not been well studied. By choosing a representative deposit, the Dayao copper deposit and using the thermodynamic phase diagram method, in this paper, we explored the restrictions on the process of hydrothermal migration and precipitation of sulfides at different pH, Eh, oxygen fugacity, and sulfur fugacity and explained the reasons for mineral assemblage zoning in the Dayao red-bed copper deposit. Moreover, based on the thermodynamic theory, we also investigated the precipitation mechanism of Cu-Fe sulfides to reveal the main controlling factors of ore-forming element zoning in the Chuxiong basin.

2. Geological Setting

The Chuxiong basin is located in the middle of Yunnan Province, China, and verges to the southwest of Yangtze block and the west side of Yuanmou ancient land. It belongs to the jointing area of the western Tethys tectonic domain as well as the southeast Indian and Eurasian plate collision and is surrounded by the Kangdian earth’s axis in the east, the south China Caledonian-Variscan fold belt in the south, the Sanjiang Tethys tectonic belt in the northwest, and the Songpan-Ganzi block in the north [41, 57]. Wang [51] divided the basin into three primary tectonic units near N-S trending, namely, the western thrust belt, central depression belt, and eastern uplift belt, and subdivided them into 11 secondary tectonic units, as shown in Figure 1(a). The basin experienced three evolution stages: namely, the downfaulted, depression, and shrinking periods, where each had a different sedimentary formation. From the Late Cretaceous, the basin stepped into its contraction stage and started to deposit red clastic rocks, which provides an important condition for copper deposits [58].

A total of 313 red-bed copper deposits (points) have been found on the mouding slope in Chuxiong basin. As seen in Figure 1(b), they form a NW arc copper belt and distribute along the margin of Yuanmou ancient continent. The copper deposits span crosses a long time period of concentrated mineralization and could be divided into 16 segments from Late Triassic to Tertiary, almost covering each layer of Cenozoic and Mesozoic. But the main copper deposits are distributed in the Aodiju segment of Gaofensi formation (8.60%) in lower Cretaceous, Liuju segment (61.00%), and Dacun segment (24.12%) of Matushan formation in upper Cretaceous, in total, accounting for 93.37% of copper reserves in the basin.

Copper deposits and prospects are widely distributed from the north to the south in Tuanshan, Dacun, Wadiju, Liuju, Hao jiahe, Tongchangqing, Geyizha, Jiziwan, and Laoqingshan within the basin. Among them, the Dayao deposit hosted by Matoushan formation (K2m) of upper Cretaceous has reserves of about 44 Mt of grades 1.2% Cu and is considered as the typical and giant copper deposit (Figure 2). The major metallic minerals of the Dayao deposit are often characterized by a zoning pattern of hematite, chalcocite, chalcocite + bornite, bornite + chalcopyrite, and pyrite. The forming mechanism of this regular pattern is a key scientific issue in studying the genesis of such type of deposits.

3. Mineral Zoning of the Red-Bed Type Copper Deposits in Chuxiong Basin

The formation of the red-bed type Dayao copper deposit includes three processes: sedimentation-diagenesis, primary reformation, and secondary reformation, among which the first two processes played important roles in the formation of the deposits.

Chen et al. [23] studied the zoning characteristics and the genesis of the red-bed copper deposits of the Chuxiong basin and concluded that there are two presenting forms (Figure 3) because of their different genesis. One is zoning along the layer (horizontal zoning) from purple sandstone to light grey sandstone within the rock, which forms the mineral assemblage zoning of hematite, chalcocite, bornite, chalcopyrite, and pyrite. This zoning generally does not cut through layers or only cut through layers in a small angle and is common in sandstone type ore deposits. The other is zoning along the vertical direction (vertical zoning) generally from the base to top, which forms the mineral assemblage zoning of hematite, chalcocite, bornite, chalcopyrite, and pyrite. This zoning usually cuts through the formation interface in a large angle and is common in shale type ore deposits.

Based on the detailed field geological work, we found that because of the weak reformation the zoning in Dayao copper deposits is mainly horizontal zoning. Metal sulfide zoning ranges from grain (Figures 4 and 5) to deposit scale (Figure 6), reflecting directions of fluid flow and/or chemical gradients. It was formed during the sedimentation-diagenesis period, from purple sandstone to light grey sandstone: forming the mineral zoning of hematite + (minor) native copper, chalcocite + bornite, bornite + chalcopyrite, chalcopyrite + pyrite, and pyrite (Figures 46). The primary minerals are simple, mainly chalcocite and bornite or chalcopyrite and pyrite [23, 27].

Mineralized replacement features may follow zones with the highest prelithification permeability. The relationships of mutualistic symbiosis between chalcocite and bornite, chalcopyrite and bornite, and pyrite and chalcopyrite are common with metasomatic texture (Figure 6). The metasomatic sequence is shown as hematite, chalcocite, bornite, chalcopyrite, and pyrite. The former was replaced by the latter, so the regular level zoning pattern of the mineral assemblages is from the purple sandstone to light grey sandstone, that is, hematite zone (the purple rock zone and the margin of the ore body), hematite + chalcocite zone, chalcocite + bornite zone, bornite + chalcocite + pyrite zone, chalcopyrite + bornite zone, chalcopyrite + pyrite zone, and pyrite zone (the margin of light grey sandstone) [27]. A relatively obvious mineral zoning is also formed during the structure reformation period, but the scale of such kind of ore body is usually small and narrow.

4. Methods

Currently, studies on geological phase diagram, especially on the thermodynamics software, are mainly restricted to oxidation of the ores, such as THERMOCALC software [59] and PELE software [60]. There is no corresponding thermodynamics software to date for the low pressure and low temperature sulfide system.

To describe the paragenetic assemblage relationship of minerals, a chemical equation of the ore minerals is built. The thermodynamic data reported by Lin et al. [61] range within the interval of 100K; thus, Lagrange’s interpolation can be used to calculate the Gibbs free energy of formation of the compound which is within the interval of 50K at temperature from 373 K to 523 K.

4.1. Fluid Inclusion Temperature of the Dayao Copper Deposit

According to the studies by Ran and Liu [48] and Wu [62] on fluid inclusion temperature of the Dayao copper deposit (Table 1), the formation temperature of the deposits ranges from 373 K to 523 K, of which the ore-forming temperature in the sedimentation-diagenesis metallogenic period is 373 K–423 K, and the temperature in the reformation metallogenic period is 373 K–523 K, mostly below 473 K. Therefore, the Dayao copper deposit is generally formed at low temperature.

MineralMetallogenesisSample numbersGas-liquid ratio (%) Homogeneous temperature (°C)Source of date

QuartzDiagenesis142~3096~137120, 260~300(2)
Main reformation152~25123~209149
Minor reformation62~2597~129113

Note. Source of data: (1) Ran and Zhuang [49], tested by the center analysis room of Zhongnan University; (2) Wu [62], tested by Nanjing University.
4.2. pH-Eh Phase Diagram

In the hydrothermal solution, the stable condition and equilibrium relationship of the mineral are controlled by pH and Eh of the solution and the activity of ions in the solution. Thus, the Nernst equation can be used to calculate the Eh of the reaction equation [63]where is the Faraday constant with value of 96500 C/mol, is the perfect gas constant with value of 8.314 J/(K·mo1), is the number of electrons gained or lost in the oxidation-reduction reaction, and [oxidation state] and [reduction state] are the concentration of each kind of ions at oxidation and reduction states, respectively.

In order to construct and draw pH-Eh phase diagram in the Cu-O-S-Fe hydrothermal system [6466], the chemical equations in the solution were established first (Table 2). Then, the thermodynamic data [61, 67, 68] were put into Formula (1) to establish the expression of pH-Eh and eventually to draw the phase diagram (Figure 7). The balanced lines drawn by reactions (25), (26), and (29) are ignored because they have exceeded the stability range of water. Because the ionization constant of water changes with temperature, the abscissa (i.e., pH) needs to be set accordingly based on the ionization constants of water at 373 K, 423 K, 473 K, and 523 K, which are 12.264, 11.642, 11.302, and 11.012, respectively.

Chemical reactionspH-Eh expressions
523 K473 K423 K373 K

(1) 2H2O = O2 + 4H+ + 4e1.129 − 0.104pH1.142 − 0.094pH1.166 − 0.084pH1.167 − 0.074pH
(2) H2 = 2H+ + 2e−0.104pH−0.094pH−0.084pH−0.074pH
(3) = + H+pH = 5.40pH = 4.56pH = 3.73pH = 2.98
(4) S + 4H2O = + 7H+ + 6e0.367 − 0.121pH0.340 − 0.110pH0.33 − 0.098pH0.288 − 0.086pH
(5) S + 4H2O = + 8H+ + 6e0.462 − 0.138pH0.411 − 0.125pH0.38 − 0.112pH0.325 − 0.099pH
(6) H2S = S + 2H+ + 2e0.233 − 0.104pH0.220 − 0.094pH0.211 − 0.084pH0.205 − 0.074pH
(7) H2S = HS + H+pH = 7.61pH = 7.09pH = 6.71pH = 6.57
(8) HS + 4H2O = + 9H+ + 8e0.305 − 0.117pH0.280 − 0.106pH0.268 − 0.094pH0.235 − 0.083pH
(9) HS = S2− + H+pH = 11.43pH = 11.28pH = 11.30pH = 11.68
(10) S2− + 4H2O = + 8H+ + 8e0.157 − 0.104pH0.148 − 0.094pH0.149 − 0.084pH0.127 − 0.074pH
(11) 3Fe + 4H2O = Fe3O4 + 8H+ + 8e−0.085 − 0.104pH−0.903 − 0.094pH−0.091 − 0.084pH−0.112 − 0.074pH
(12) 2Fe3O4 + H2O = 3Fe2O3 + 2H+ + 2e0.24 − 0.104pH0.22 − 0.094pH0.21 − 0.084pH0.17 − 0.074pH
(13) Fe2+ = Fe3+ + e0.950.940.900.86
(14) 2Fe2+ + 3H2O = Fe2O3 + 6H+ + 2e1.602 − 0.341pH1.352 − 0.282pH1.282 − 0.252pH1.142 − 0.222pH
(15) 3Fe2+ + 4H2O = Fe3O4 + 8H+ + 2e2.258 − 0.456pH1.918 − 0.376pH1.818 − 0.336pH1.628 − 0.296pH
(16) 2Fe3+ + 3H2O = Fe2O3 + 6H+pH = 1.18pH = 1.11pH = 1.34pH = 1.3
(17) 2Cu + 4H2O = Cu2O + 2H+ + 2e0.46 − 0.104pH0.45 − 0.094pH0.46 − 0.084pH0.44 − 0.074pH
(18) Cu2O + H2O = 2CuO + 2H+ + 2e0.67 − 0.104pH0.65 − 0.094pH0.62 − 0.084pH0.62 − 0.074pH
(19) Cu+ = Cu2+ + e0.370.320.270.22
(20) Cu+ + e = Cu−0.30−0.36−0.41−0.45
(21) 2Cu+ + H2O = Cu2O + 2H+pH = 9.53pH = 9.05pH = 8.65pH = 7.86
(22) Cu2+ + H2O = CuO + 2H+pH = 6.23pH = 6.32pH = 6.58pH = 6.60
(23) 2Cu2+ + H2O = Cu2O + 2H+ + 2e0.622 − 0.104pH0.532 − 0.094pH0.462 − 0.084pH0.362 − 0.074pH
(24) Fe2+ + 2H2S = FeS2 + 4H+ + 2e
(25) Fe2+ + S2 + 2e = FeS2
(26) Cu+ + = Cu2+ + + e−0.63−0.67−0.72−0.77
(27) 2FeS2 + Cu2+ + 4H+ + 4e = CuFeS2 + Fe2+ + 2H2S−0.16 + 0.104pH−0.15 + 0.094pH−0.14 + 0.084pH−0.14 + 0.074pH
(28) 2CuFeS2 + 3Cu2+ = Cu5FeS4 + Fe2+ + 4e−0.59−0.59−0.59−0.6
(29) 2Cu+ + S2− = Cu2S
(30) 15Cu2S + 2Fe3O4 + 7H+ + 9HS = 6Cu5FeS4 + 8H2O + 2e−4.86 + 0.364pH−4.34 + 0.329pH−3.96 + 0.294pH−2.1 + 0.259pH

4.3. PH- Phase Diagram

The pH- equation diagram of each chemical reaction is listed in Table 2. Take reaction as an example; its equation is . Then Eh of each reaction can be calculated by inputting the values of pH and into the equation (Table 3) and used to draw the phase diagram (Figure 8).

= 523 K = 473 K = 423 K = 373 K

(3)pH = 5.40pH = 4.56pH = 3.73pH = 2.98
(4)−29.3 − 0.65pH−34.1 − 0.68pH−39.8 − 0.67pH−47.5 − 0.65pH
(5)−25.6 − 1.31pH−31.1 − 1.32pH−37.2 − 1.33pH−45.5 − 1.35pH
(7)pH = 7.61pH = 7.09pH = 6.71pH = 6.57
(8)−31.7 − 0.50pH−36.7 − 0.51pH−42.8 − 0.48pH−50.4 − 0.49pH
(9)pH = 11.43pH = 11.26pH = 11.30pH = 11.68
(28)−66.1 + 4pH−73.7 + 4pH−83.6 + 4pH−95.5 + 4pH
(30)−230.3 + 18pH−233.3 + 18pH−244.1 + 18pH−176.6 + 18pH

4.4. - Phase Diagram

The oxygen fugacity and sulfur fugacity are calculated using the formula below:where or delta is under standard conditions.

For the reactions in which oxygen and sulfur participated simultaneously, the Gibbs-Duhem Equations (i.e., stoichiometric coefficient) of oxygen and sulfur are used to for calculation at certain points and subsequently to draw the balanced line of each reaction and calculate its slope. Table 4 lists , , and slope of each reaction and Figure 9 shows the - phase diagram of each reaction.

Chemical reactions = 373 K = 423 K = 473 K = 523 K

(1) 3Fe + 2O2 = Fe3O4−69.1−59.9−52.7−46.8
(2) 2Fe3O4 + 1/2O2 = 3Fe2O3−53.7−45.7−39.3−34.2
(3) Fe + 1/2S2 = FeS−37.9−32.5−28.3−24.9
(4) FeS + 1/2S2 = FeS2−25.0−20.5−16.9−14.0
(5) 3FeS + 2O2 = Fe3O4 + 1/2S2,
(6) 3FeS2 + 2O2 = Fe3O4 + 3S2,
(7) 2FeS2 + 3/2O2 = Fe2O3 + 2S2,
(8) 2Cu + 1/2O2 = Cu2O−39.1−33.6−29.3−25.9
(9) Cu2O + 1/2O2 = 2CuO−29.6−24.8−20.8−17.7
(10) 2Cu + 1/2S2 = Cu2S−34.3−29.7−26.1−23.2
(11) Cu2S + 1/2O2 = Cu2O + S2,
(12) Cu2S + 1/2O2 = 2CuO + S2,
(13) 2FeS + 5CuFeS2 + 4O2 = Cu5FeS4 + 2Fe3O4 + 4S2,
(14) 3FeS + CuFeS2 + 2O2 = CuFeS2+ Fe3O4 + 3/2S2,
(15) 3FeS2 + CuFeS2 + 2O2 = CuFeS2 + Fe3O4 + 3S2,
(16) FeS2 + 5CuFeS2 + S2 = Cu5FeS4 + 5FeS2−14.3−12.7−11.1−8.6
(17) Cu2S + 2Fe3O4 + 1/2O2 = Cu2S + 3Fe2O3−42.4−40.8−39.3−34.2
(18) 2FeS2 + CuFeS2 + 3/2O2 = CuFeS2 + Fe2O3 + 2S2,
(19) 2FeS2 + Cu5FeS4 + 3/2O2 = Cu5FeS4 + Fe2O3 + 2S2,
(20) Cu2S + Fe2O3 + 1/2O2 = Cu2O + Fe2O3 + S2,
(21) 3Cu5FeS4 + 2O2 = Cu2S + Fe3O4 + 9/4S2,
(22) 5CuFeS2 + Fe2O3 + 15/4O2 = Cu5FeS4 + 7/2Fe2O3 +3S2,
(23) 4S2 = S8−8.2−6.5−5.1−4.1

5. Results

5.1. Constraints of pH, Eh, and on Sulfide Precipitation

The range of pH, Eh, and of metal sulfides and the following cognition can be obtained from Figures 7 and 8.

(1) S2− can only exist stably in the hydrothermal solution at temperature below 473 K. When the temperature of hydrothermal solution is higher than 473 K, the chalcocite (Cu2S) is not precipitated.

(2) The formation of mineral assemblage zoning was controlled by multiple factors including Eh and pH. From FeS2, CuFeS2, and Cu5FeS4 to Cu2S, pH increases and Eh decreases; in other words, the environment turns from acidic to alkaline and from relatively oxidation state into strong reduction state.

(3) Variation of temperature has different impacts on Eh or pH for different sulfide. For FeS2 and Cu2S, temperature change has no significant impacts on Eh and pH of mineral precipitation. For CuFeS2 and Cu5FeS4, although temperature change has no significant effects on Eh, alkalinity increases with temperature decreasing because of the precipitation of volatile components during the migration process of the ore-forming hydrothermal fluid. In addition, decrease in HCl and H2O contents could reduce metal carrying ability, leading to mineral precipitation.

(4) has little effect on mineral precipitation. The range of suitable for FeS2 formation is wide, but that of suitable to form other minerals is basically the same.

The scope of pH for mineral precipitation mentioned above is in accordance with that reported by Zhao and Zhang [69]. For example, the scope of pH is 2.5~8 for Fe2+ and Cu2+; both are amphoteric elements which migrate in dissolved state at strong acidic or alkaline conditions. Thus, CuFeS2 is precipitated in nearly neutral conditions. The scope of pH is <2.5 for Cu+, an alkaline element which has low electrovalence and great radius and is easy to migrate in acidic medium, so Cu2S is easy to precipitate in alkaline condition. Because both bivalent copper and cuprous ions are present in Cu5FeS4, they are precipitated at neutral to alkaline conditions.

5.2. Constraints of and on Sulfide Precipitation

It is clear from Figure 9 and Table 5 that stable - range of the 22 kinds of minerals and their assemblage as well as the trend of the redox block distribution by parsing the phase diagram. By comparing and analyzing the trend of the redox block distribution in the phase diagram and the mineral assemblage zoning based on the redox trend in Dayao copper deposit, one could find that the permutation and assemblage of mineral in the phase diagram are consistent with the redox trend which reflects the mineral zoning on the geological occurrence (Table 5). Taking = 423 K as an example, the fact can be explained as follows (Figure 9).

Redox state blockThe area of approximate trapezoid under the (8), (11), and (12) balance lines and coordinate axisThe area of polygon under the (3), (13), (20), (8), (11), and (12) balance linesThe area of approximate triangle under the (5), (6), (7), (13), and (23) balance linesThe area of approximate trapezoid under (3), (5), (6), (7), and (23) balance lines and coordinate axis

Lithology (rock color)PurpleAmaranthPale red or light greyLight grey off-white
Cementing patterns of different type sandstonesFerruginous, calcium argillaceous, which contains a large quantity of hematite, calcite, dolomite, and clay mineral Ferruginous, calcium argillaceous, which contains a large quantity of hematite, calcite, dolomite, and clay mineral 
Copper sulfide mineral assemblage
Copper sulfide mineral assemblagePrincipal siliceous cementation which contains recrystallization, secondary overgrowing quartz/pyrite, etc.
Redox zoningStrong oxidizing zoneOxidizing zoneOxidizing-reducing transitive zoneReducing zone
Typical mineral assemblage
(the minerals marked by italic are the typical minerals for each zoning)
Iron and copper oxide such as hematite,
cuprite, and tenorite
Iron oxide + copper sulfide such as hematite, magnetite, and chalcociteIron oxide + copper sulfide such as hematite,
magnetite, bornite, and chalcopyrite
Iron and copper sulfide such as chalcopyrite, pyrrhotite, and pyrite

(1) At the same temperature, each mineral and its assemblage have their own respective scopes of and , indicating that the ranges of and control the distribution of minerals and their assemblage. The cementing patterns of different type sandstones, mineral assemblage features, and obvious differences among the oxidizing-reducing environments are corresponding to the zoning features of the mineral assemblage (Table 5).

(2) When temperature falls, the scopes of and of mineral precipitation also decrease correspondingly (Figure 9), and the redox effect becomes weaker. The mineral stability range (the block occupied in the phase diagram) shifts towards native Fe and Cu with temperature declining. Oxidation-reduction area of the transition block occupied by chalcocite is always large, indicating that chalcocite precipitated fugacity has a very wide range.

(3) Zones of Cu2S minerals, bornite, chalcopyrite, and pyrite are arranged across redox boundaries with chalcocite on the oxidized side and pyrite on the reduced side. It is manifested by the light-purple interactive zone that the lower right area in Figure 9 is purple-amaranthine sandstone zone with abundant oxide minerals; the upper left area is light grey off-white sandstone zone with abundant reductive minerals; and nearly triangular-shaped zone between the above two zones is the light-purple interactive zone. Therefore, the mineral assemblages along with the evolution from the lower right strong oxidizing zone towards the upper left reducing zone in Figure 9 have the following main features: strong oxidizing zone, oxidizing zone, oxidizing-reducing transitive zone, and weak reducing zone to reducing zone. Sulfur and oxygen fugacity, lithology, mineral assemblage, and redox blocks have one-to-one corresponding relationship (Table 5).

6. Discussions

6.1. The Correspondence between Thermodynamic Phase Diagram and Geological Features

From the three phase diagrams (Figures 79), we can obtain Tables 6 and 7 and listed the pH, Eh, , and conditions for the precipitation of each sulfide mineral. The geological features of Dayao copper deposit have been testified in the thermodynamic calculation and the phase diagrams (Figures 7, 8, and 9 and Tables 5, 6, and 7).


373 K
 Eh(−0.07, 0.33)(−0.61, 0.06)(−0.43, 0.06)(−0.80, −0.33)
 pH(0, 2.7)(1, 10)(1, 10)(6.4, 12.2)
(−63.1, −47.5)(−63.1, −55)(−63.1, −56.8)(−63.14, −56.2)
(−25.0, −8.7)(−38.4, −25.0)(−18.2, −8.7)(−34.3, −8.7)
423 K
 Eh(−0.07, 0.33)(−0.59, 0.07)(−0.80, −0.59)(−0.80, 0.12)
 pH(0, 2.6)(0.8, 8.8)(7, 10.7)(10.7, 11.6)
(−55.5, −39.8)(−55.5, −41.7)(−55.5, −46.1)(−55.5, −48)
(−20.5, −6.5)(−32.5, −20.5)(−12.7, −6.5)(−29.7, −6.5)
473 K
 Eh(−0.08, 0.34)(−0.59, 0.07)(−0.80, −0.59)(−0.80, −0.08)
 pH(0, 2.4)(0.8, 8.2)(6.3, 10.1)(10.1, 11.3)
(−48.6, −34.1)(−48.6, −36.4)(−48.6, −41)(48.6, −42.3)
(−16.9, −5.1)(−28.3, −16.9)(−11.1, −5.1)(−26.1, −5.1)
523 K
 Eh(−0.08, 0.34)(−0.58, 0.08)(−0.80, 0.59)(−0.80, −0.20)
 pH(0, 2.3)(0.7, 7.6)(7.6, 9.4)(9.4, 11.0)
(−43.4, −29.3)(−43.4, −30.8)(−43.4, −35.8)(−43.4, −37)
(−14.0, −4.1)(−24.9, −14.0)(−8.6, −4.1)(−23.2, −4.1)


S systemH2SH2S + HSH2S + HSHS + S2−
pHAcidWeak acid neutralNeutral-weak alkalinityAlkalinityWeak acid alkalinity
EhWeak reductionReductionReductionReductionOxidation
CementQuartzQuartz + carbonateQuartz + carbonateQuartz + carbonateCarbonate + clay
Temperature variationMediumMedium-low temperatureMedium-lowLowMedium

During the early stage of the diagenetic period, recrystallization of quartz and extensive pyritization took place and the purple sandstone was discolored and changed into the light grey sandstone zone in the red-bed type copper deposits, Chuxiong basin. During the reformatting diagenetic period, silicification developed and changed the purple sandstone into discolor and formed off-white quartz sandstone or dissolved and transported the copper from the sandstone body that contains metal elements (or sandstone ore body). Both two processes could take place in (weak) acidic conditions (Table 7).

Theoretic results and phase diagrams are consistent with both the macrogeological and microgeological characteristics of copper mineralization. Macroscopically (Figures 3 and 6), the mineral zoning is characterized as light-purple interactive zone and mainly indicates the cementation pattern of the sandstones and the features of the mineral assemblage (Tables 5 and 7). Purple-red sandstone cement belonged to iron and calcium mud, which contains a large amount of hematite, calcite, dolomite, and clay minerals, representing an oxidizing and alkaline environment. The light grey-greyish white sandstone mainly consisted of siliceous cement, containing recrystallization and overgrowth of quartz and pyrite and other minerals, which represents a reduction of acidic medium environment. The zone of a large number of copper sulfide between purple-red sandstone and the light grey-greyish white sandstone represents the redox and acid-base transition zone.

6.2. Interpretation of Mineral Zoning and Metallogenic Process by Thermodynamic Phase Diagrams

A large number of studies have shown that the precipitation of sulfide minerals in SSC copper deposits is caused by reduction [1, 2, 6, 9, 25, 26, 28, 46, 7686], which is true for the red-bed copper deposit in Chuxiong basin [37, 4850].

The Chuxiong basin is a Mesozoic and Cenozoic red basin with copper and polymetallic, coal, oil, and gas formations and their associated deposits [87]. The occurrence and development of paleo-continental rift in the Kangdian region brought up a Chuxiong basin, deposited cycles and ore-bearing formations of coal, evaporate, and copper, and formed the associated organic (T3-J), copper (K2), and saline (K2-E) deposits [87]. There commonly exist veinlike, spotted, and cloud dry asphalt in host rock, structures, especially in rich ores, with organic carbon showing positive correlation with Cu and Ag content in Haojiahe deposit [70]. Geochemical studies of the strata by [70] show that in Mesozoic strata of the region copper abundance tends to increase, whereas organic carbon abundance tends to decrease from the lower part upward. Studies on organic geochemistry indicate that the origin, type, and maturity of organic matter are different among coal-bearing, copper-bearing, and evaporate formations in the Mesozoic continental Chuxiong basin [88]. Many scholars believed that organic matter and the evaporates played an important role for the red-bed type copper deposits in Chuxiong basin [89, 90].

Previous studies have shown that the δ34S values of sulfides from the red-bed type copper deposits in Chuxiong basin are mainly distributed in two intervals [51, 7075] (Figure 10). It shows that δ34S values of sulfides in diagenetic period vary between and in all of the ore deposits, which is essentially the same as the δ34S values of sulfides which varied in the range from to of samples in the bottom part of the Kupferschiefer profile from the Sangerhausen basin [91]. Upon TSR, the effect of isotopic fractionation is low and the resulting sulfides have values above [92]. The δ34S values of sulfides in diagenetic period from the red-bed type copper deposits in Chuxiong basin are in accordance with a contribution of TSR to sulfide precipitation. The distribution range of S isotopic compositions of sulfides in transformation period are entirely different, as shown in Figure 10, varying between and in Dayao and Haojiahe ore deposits. This indicates that, in addition to sulfate reduction, the sulfur of deep seated magma source is involved in mineralization in these two deposits.

Han et al. [27] proposed that coal-copper-salt three-color sedimentary formation and basin fluid were formed during the Middle and Late Yanshan Period. The fluids Cu-bearing from basin basement ascended along the faults, derived the organic matter from the coal bed, mobilized the copper from the preexisting stratiform copper deposits and strata, and formed the reductive fluid rich in Cu. The oxidative fluid of high salinity, which resulted from deep cycling of meteoric water and leaching of gypsum bed mixed the reductive fluid rich in Cu and caused intense redox reaction. was reduced into H2S that reacted with copper to form the orebodies.

Combining the study of the phase diagrams (Figures 79 and Tables 5–7) and the deposit geologic features can better explain the reason for the mineral zoning. We inferred that the formation of the red-bed copper deposit in Chuxiong basin experienced the following processes.

During the sedimentation-diagenesis metallogenic epoch, the reducing fluid that contains copper from basin basement migrated towards the oxidizing purple sandstone that contains ferruginous and calcium argillaceous cements in the permeable stratum of the sandstone and shale. Water-rock interactions occurred between the fluid and the purple sandstone, changed the purple sandstone into light grey sandstone containing siliceous calcium cements, and formed the recrystallized or secondary growth quartz sandstone. Meanwhile, the redox, double decomposition, and replacement reactions took place in the ore body that is close to the light grey zone within the light-purple transitive zone.

(1) Formation of Pyrite Zone. Initially, the fluid containing a large amount of reducing constituent content is characterized as high temperature and low pH. The hematite and magnetite in the purple sandstone were reduced into pyrite (reactions (6) and (7) in Table 4). The conditions for pyrite formation are acid, weak reduction, and medium .

(2) Formation of Chalcopyrite Zone. Because of the low pH and large amount of copper in fluid, the new formed pyrite reacts with H+ and Cu2+ (reaction (27) in Table 2) to produce chalcopyrite. Therefore, the formation of chalcopyrite resulted in the increase of fluid pH. The conditions for chalcopyrite formation are weak acid neutral, reduction, and medium .

(3) Formation of Bornite Zone. Because the formation of chalcopyrite is the acid consumption reaction, fluid acidity became neutral-weak alkalinity. Partial chalcopyrite is metasomatic to form bornite (reaction (28) in Table 2). The conditions for bornite formation are neutral-weak alkalinity, reduction, and medium-high .

(4) Formation of Chalcocite Zone. Along with the migration of fluid, the release of pressure makes volatile components separate out continuously, with decrease in some components, such as HCl and H2O, and increase in the alkalinity of fluid. Addition to chalcocite on a wide range of sulfur and oxygen fugacity conditions can precipitate when the sulfur fugacity cannot meet the precipitation conditions of bornite, chalcopyrite, and chalcocite precipitate. The conditions for its formation are alkalinity, reduction, and medium .

Therefore, the mineral zoning is mainly controlled by the geochemical environment. Among the various physical and chemical conditions, pH is the vital factors controlling the order of different sulfide precipitation and explaining mineral zoning. The Eh and determine the precipitation interval of sulfides, while has little effect on mineral precipitation.

7. Conclusions

The calculations of the Eh, pH, , and within the principal metallogenic temperature of the Dayao red-bed type copper deposits and the analysis of phase diagrams resulted in the following conclusions:

(1) The zoning pattern and mineral assemblage shown in the phase diagram are in accordance with the macroscopic and microscopic geological features of the deposits.

(2) The temperature variation has almost no impact on the Eh and pH of FeS2 and Cu2S precipitation. Although the Eh is almost not affected with the falls of temperature for CuFeS2 and Cu5FeS4 precipitation, CuFeS2 and Cu5FeS4 precipitate with pH increasing. The value scope of and of the mineral precipitation decreases correspondingly with temperature decreasing.

(3) The scope of and of chalcocite is relatively wide. Because S2− can only exist stably in hydrothermal fluid below 473 K, the forming temperature of chalcocite is below 473 K. This explains why the chalcocite is the main mineral of the red-bed type that formed at low temperature.

(4) Among the various physical and chemical conditions, pH is the vital factors controlling the order of different sulfide precipitation and explaining mineral zoning. The Eh and determine the precipitation interval of sulfides, while has little effect on mineral precipitation.

Since this paper only discussed the restrictions of Eh, pH, , and , which have played roles in elements migration and precipitation. The problems regarding temperature, pressure, water-rock reaction, migration of copper and iron in hydrothermal system, migration pattern, and driving pattern of fluid remained for the future research.

Conflicts of Interest

The authors declare that they have no conflicts of interest.


This study was supported jointly by the National Natural Science Foundation of China (nos. U1133602 and 41572060), China Postdoctoral Science Foundation (2017M610614), projects of YM Lab (2011) and Innovation Team of Yunnan Province and KMUST (2008 and 2012), and Yunnan and Kunming University of Science and Technology Postdoctoral Sustentation Fund.


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