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Article

Mineralogy and Mineral Chemistry of Dioritic Dykes, Quartz Diorite Enclaves and Pyroxene of the Sungun Cu-Mo Porphyry Deposit, East Azerbaijan, Iran

by
Amin Allah Kamali
1,*,
Mohsen Moayyed
2,
Benoit M. Saumur
3 and
Mohammad Fadaeian
4
1
Research Center for Conservation of Culture Relics (RCCCR), Research Institute of Cultural Heritage & Tourism, Tehran 11369-13431, Iran
2
Department of Earth Sciences, University of Tabriz, Tabriz 51664-14766, Iran
3
Département des Sciences de la Terre et de l’Atmosphère, Université du Québec à Montréal, 201 Avenue du Président-Kennedy, Case Postale 8888, Succursale Centre-Ville, Montréal, QC H3C 3P8, Canada
4
Department of Geology, Payame Noor University, Tehran 19395-4697, Iran
*
Author to whom correspondence should be addressed.
Minerals 2022, 12(10), 1218; https://doi.org/10.3390/min12101218
Submission received: 22 July 2022 / Revised: 29 August 2022 / Accepted: 29 August 2022 / Published: 27 September 2022
(This article belongs to the Special Issue Minerals of Alkaline Igneous Rocks: Chemical and Isotopic Features as Tracers of Magmatic Processes)
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Abstract

:
The Sungun Cu-Mo porphyry deposit forms part of the Ahar–Arasbaran Magmatic Belt (AAMB). Its host Miocene porphyry stock is quartz monzonitic in composition and is cut by intermediate dykes that post-date mineralization. These dykes contain pyroxene and enclaves of ambiguous origin. Dykes of microdiorite are observed within quartz diorite dykes, whereas later diorite dykes contain three different kinds of enclaves (diorite, quartz diorite and hornfels) of sizes between 1 and 10 cm. Enclaves consist of plagioclase, hornblende and biotite, with accessory sphene, quartz and apatite. Chlorite compositions in microdiorite are within the chamosite range, whereas they are within the clinochlore range in diorite enclaves. Microprobe analyses of pyroxene indicate an augitic composition (Fs13.38-22.79Wo29.1-33.57En48.53-56.61), consistent with an igneous origin. Hornblende of the diorite enclaves formed at pressures ranging between 3 and 5.3 kilobars and temperatures between 714 and 731 °C. Average oxygen fugacity during rock formation is −14.75. Such high oxygen fugacities suggest that the diorite formed near the boundaries of a convergent margin. Amphibole compositions suggest that the diorite enclaves are sub-alkaline to mildly alkaline, consistent with reported whole-rock chemistry of the Sungun magmas. Pyroxenes were formed at pressures ranging between 11 and 15 kilobars (33–45 km) and temperatures between 1100 and 1400 °C. The amount of Fe3+ in clinopyroxene is also consistent with high oxygen fugacity within their environment of crystallization. Overall, these results have implications for our understanding of the origin of the Sungun Cu-Mo porphyry magmas and their mineral deposits in a lower-crustal setting.

1. Introduction

Porphyry deposits, suppliers of ~75% of the world’s copper and significant proportions of Mo, Au and Re, are formed in subduction-related magmatic arcs [1] and, to some extent, in post-subduction collisional zones [2]. They are associated with magmas of intermediate to felsic composition (mostly andesitic to dacitic), having calc-alkaline to alkaline affinity [1]. In modern environments, porphyry-related deposits are usually found within active subduction zones and, in ancient environments, these ores are associated with former collision zones [1,2]. The global distribution of known Cu-Au porphyry deposits shows a clear spatial relationship with volcanic arc terranes at convergent plate margins (e.g., [1,3]). The Sungun Cu-Mo porphyry deposit, which is the focus of this study, was formed in a post-collisional environment [4]. Studies of the Sungun plutonic rocks and deposit, thus, provide the opportunity to document petrological and geochemical controls that affect mineralization in such environments.
The Sungun Cu-Mo deposit, situated 32 km north of the Varzaghan, East Azerbaijan Province, contains ore reserves of 740 Mt at 0.65 % Cu and ~0.01% Mo and is located within the Cenozoic Ahar–Arasbaran Magmatic Belt (AAMB) of northwestern Iran. The AAMB is part of the Alborz-Azerbaijan-Lesser Caucasus Magmatic Belt, which resulted from the subduction and subsequent collision along the southern margin of Eurasia [5] (Figure 1). The Alborz-Azerbaijan belt hosts many world-class porphyry copper deposits, such as Haft Cheshme, Ali Javad, Sieh Kemer Mianeh, Sahibdivan Meshkin Shahr and Sonajil Harris. These deposits are associated with calc-alkaline to shoshonitic stocks and dykes containing rocks exhibiting typical porphyritic textures [4,6,7]. The host Cenozoic volcanic and plutonic rocks of this belt have medium to high K, calc-alkaline to alkaline composition and the deposits show common characteristics regarding their geology, host rocks, ages, alteration and mineralization [8,9,10]. A notable characteristic of Sungun is the presence of eight generations of dykes that cross-cut the deposit ([11,12] and references therein) and these dykes are genetically linked to the magmatic-hydrothermal system that generated the deposit [4] and, therefore, may provide clues with regards to temperature–pressure conditions in the magmatic plumbing system.
Among the dyke generations observed at Sungun, diorite dykes (“Pulse 1” of [11]) contain several types of enclaves; these include enclaves of quartz diorite, diorite, microdiorite and hornfels, with the former three sharing mineralogical and geochemical characteristics with their host dykes. Pyroxene also occurs within these dykes, yet is poorly understood from a petrogenic point of view. This paper aims to elucidate the source and genesis of the Sungun enclaves and pyroxene and constrain physical and chemical conditions for their formation, (i.e., pressure, temperature, oxygen fugacity) based on field observations, petrographic features and mineral chemistry. Our results also have implications for our understanding of the genesis of the Sungun deposit, notably with respect to temperatures of alteration and the documentation of a number of magmatic episodes.

2. General Geology

The Oligocene Sungun porphyry has been the subject of several geological and metallogenic studies [4,13,14]. Dated at 20.69 and 21 Ma by Ar-Ar ad U-Pb (SHRIMP), respectively [15], it was emplaced within a 500 m thick sequence of folded upper Cretaceous limestone with intercalations of shale and Eocene volcaniclastic rocks and sandstones [14,16]. Quartz monzonite, which hosts Cu-Mo mineralization, represents the earliest and most voluminous magmatic phase of the Sungun porphyry [17]. The interaction of the Sungun porphyry stock with surrounding Cretaceous limestone produced skarn zones in the northern and eastern periphery of the porphyry; this skarn contains clinopyroxene that was also analyzed in this study. Hornfels are usually observed along the edges of the eastern occurrences of skarn along topographic scars.
Alteration and mineralization are concentric and centered on the Sungun intrusion and interpreted as coeval with its emplacement [8]. Documented hydrothermal alteration consists of an early phase of potassic and propylitic alteration. This early event is associated with the hypogene copper mineralization, precipitated as chalcopyrite and bornite, as both dissemination and veinlets. Molybdenite associated with quartz veins is associated with the early potassic event but located within internal portions of the Sungun intrusion. These events were followed sequentially by phyllic, silicic and argillic stages of alteration.
The initial phase of quartz monzonite magmatism was followed by pulses of diorite and, finally, andesitic magmatism [8,16]. This later activity is associated with the emplacement of multiple generations of dykes within both the voluminous quartz monzonite body and surrounding carbonate country rocks. Rocks exposed at the Sungun Copper Mine include the mineralized Sungun porphyry as well as eight groups of cross-cutting and lithologically distinct post-mineralization dykes(Figure 2). In order of emplacement, these include quartz diorite (DK1a, DK1b, DK1c), diorite (DK3), gabbrodiorite, microdiorite, lamprophyre and dacite [4,11]. Relative ages and cross-cutting relationships were documented during detailed field studies, core logging and the identification of sequences of alteration [11].
Previous geochemical studies show that the Sungun dykes and porphyry have a common origin, with bulk rock compositions more consistent with the post-collisional magmatic arc domain compared to magmas from continental active margins [4,11,14]. However, the dykes are compositionally slightly more mafic than the porphyry. 87Sr/86Sr and 143Nd/144Nd ratios for the porphyry and dykes, with the exception of microdiorite and lamprophyric dykes, are consistent with a mantle source and closed-system fractionation [4]. At a maximum pressure of 19 kbar, gravitational separation of the magmas within a lower-crustal magmatic chamber gave rise to a dioritic magma. This magma then rose and settled into another chamber at a maximum of 6 kbar (~18 km), where it fractionated and gravitationally separated. These magmas rose again in sequence, thereby creating the more felsic and earlier Sungun porphyry and the subsequent intermediate Sungun dykes [16,18].
Among the eight groups of Sungun dykes discussed earlier, only four of these groups are relevant to this study: from oldest to youngest, these are the DK1a, DK1b and DK1c groups consisting of quartz diorite and DK3 consisting of diorite. Based on age determinations by [9,15], the emplacement age for DK1a ranges between 20.57 and 19.85 Ma. DK1a and DK1b dykes contain microdiorite enclaves as well as DK1b autobreccia (Figure 3a,c). DK1c dykes have been observed in the pit section of boreholes, but it is exhalant in the eastern skarn section of the mine. DK3 dykes contain abundant hornfels enclaves and autoliths (Figure 3e,g).

3. Materials and Methods

Preparation and field operations, sampling and laboratory studies were completed in the autumn and winter of 2013. Petrographic studies were performed using a BX53-P - CX31-P OLYMPUS polarizing microscope Japan Manufacturers.
Geochemical studies of various silicate minerals, such as plagioclase, amphibole, pyroxene and chlorite, were carried out in the laboratory of the Iranian Mineral Research and Technology Center (Imidro) and the Microprobe Laboratory of the University of Oklahoma, USA, using a CAMECA SX100 device, French Cameca company (20 kV, 20 nA, 2mm spot).

4. Petrography

4.1. Dykes

DK1b dykes (quartz diorite): The main minerals observed in quartz diorite dykes are plagioclase, biotite and amphibole. Plagioclase shows swinging zoning and polysynthetic twins and crystal rims exhibit sericite alteration (Figure 3b). Amphibole is observed as fine- to coarse-grained subhedral to euhedral crystals. Biotite has a weak to strong alteration and, in some cases, has been completely sericitized and chloritized. Dk1b dykes can contain enclaves of microdiorite, which are described in the following section.
DK3 dykes (diorite): These dark green diorites contain unaltered white plagioclase phenocrysts and amphibole (Figure 4a) and exhibit a microlithic porphyritic to coarsely porphyritic texture (Figure 4f). Crystal sizes vary from fine to coarse, plagioclase is subhedral and locally contains sieve texture and swinging zoning (Figure 4b). Amphiboles are subhedral to euhedral and are locally replaced by chlorite, epidote and sericite (Figure 4d), which, in order, represent a typical alteration sequence. Orthoclase, quartz, sphene, apatite and opaque minerals are minor constituents. Diorite dykes can contain large clinopyroxene (augite). These occur as coarse, subhedral to euhedral crystals and in some microscopic sections, augite crystals exhibit exsolution features (Figure 4e,f). DK3 dykes may also contain large enclaves of hornfels and diorite, described below.

4.2. Enclaves

Microdiorite enclaves in DK1b dykes: Enclaves of microdiorite are porphyritic to microlithic, often gray in color in hand sample and are mesocratic to melanocratic. The diameter of these enclaves ranges between 2 and 10 centimeters (Figure 3a). Plagioclase and ferromagnesian minerals form the bulk of the mineralogy. Plagioclase occurs as euhedral to subhedral phenocrysts with polysynthetic twinning and is often moderately to strongly altered to saussurite (Figure 3b). Such crystals form 30–40 modal % of the rock. Ferromagnesian minerals do not occur as phenocrysts and have been completely chloritized (Figure 3b). The fine-grained matrix forms 40%–50% of the rock, but its primary mineralogy is not recognizable due to extreme alteration.
Diorite enclaves in DK3 dykes: These enclaves show the same overall mineralogy as the host DK3 diorite dykes. Hand samples of these enclaves are often dark gray, have sizes ranging between 2 and 7 centimeters and show granular textures (Figure 3g). Plagioclase often occurs as medium to coarse, subhedral to euhedral crystals that have been chlorite and epidote alteration (Figure 3h). Apatite, quartz, sphene and opaques are accessory minerals.
DK1b enclaves in DK3 dykes: Quartz diorite enclaves are granular textured, exhibit sizes ranging between 3 and 10 centimeters (Figure 3d) and hand samples are often gray in color. Chilled contacts of these enclaves with quartz diorite (DK1b) are clearly visible. The main minerals include plagioclase, amphibole and biotite. Plagioclase is observed as euhedral to subhedral, medium- to coarse-grained crystals, has polysynthetic twinning, exhibits poikilitic texture and has moderate alteration. It forms a cumulate phase in some samples, forming up to 65 modal % of one particular enclave (Figure 3d). Amphibole (25–35% modal) is observed as fine to coarse, euhedral to subhedral crystals, exhibiting simple twinning and is only moderately altered. This mineral forms 25–35% of this type of the enclave and has moderate alteration (Figure 3d). Biotite (10%) is observed as medium to coarse crystals, is euhedral to subhedral and locally forms coronae around poikilitic plagioclase (Figure 3d). Apatite and quartz are accessory phases.
Hornfels enclaves in DK3 dykes: Hand samples of hornfels enclaves are gray, very hard and dense. The size of these enclaves ranges from a few millimeters up to about 5 centimeters (Figure 3f). They are fine grained and contain quartz, hornblende, epidote, chlorite, plagioclase and opaque minerals. Epidotized plagioclase and hornblende were also chloritized (Figure 3f). Mineral assemblages are consistent with metamorphism in the Hornblende Hornfels facies.

5. Mineral Chemistry of Microdiorite and Diorite Enclaves

5.1. Plagioclase Chemistry

The results of EPMA of plagioclase are shown in Table 1, based on five cations and eight oxygen atoms. In all samples, plagioclase is highly sodic albite, although some slightly calcic grains from microdiorite enclaves plot as oligoclase (Figure 5). The An content for plagioclase from microdiorite enclaves varies between 2.73% and 15.07% and that for the diorite enclaves between 2.88% and 4.89%. Average values are 7.89% and 3.82%, respectively. The composition of plagioclase in the quartz diorite dykes (DK1a, DK1b and DK1c) varies from albite-oligoclase to andesine and oligoclase to andesine; in the diorite, it varies from andesine to labradorite; in the LAM, from albite to oligoclase; and in the microdiorite (MDI), it occurs as albite [11].

5.2. Chlorite Chemistry

Chemical analyses of chlorite, together with the calculated unit cell formulae, are presented in Table 2 (based on 14 oxygen atoms) and compositions are plotted in Figure 6. In the Fe/(Mg + Fe2+) − AlIV/(Si + AlIV) diagram, chlorite of microdiorite and diorite enclaves is located in the aluminum Al-chamosite and Al-Fe clinochlore, respectively (Figure 6a). Further, in the Si − Mg/(Mg + Fe) diagram, which isolates clinochlore and chamozite endmember compositions, diorite and microdioritic enclaves are, respectively, located within the clinochlore and chamozite (Figure 6b).The chemical composition of the chlorite in the quartz diorite (DK1a and DK1b), diorite (DK3) and MDI dykes falls in the range of the pycnochlorite field and, in the dyke DK1c, it is within the pennine field [11].

5.3. Amphibole Chemistry

Amphibole is one of the most abundant and important minerals in the dioritic enclaves of the region. In this study, their chemical composition is calculated based on 13 and 23 cations (Table 3). The studied amphiboles from enclaves, based on the diagram of [22], are located in the calcic group based on (Na + K) > 0.5, Ca > 1.5 and Ti < 0.5, as well as within the sub-group of magnesiohornblende (Figure 7a). Figure 7b shows Ti changes in relation to AlIV for amphibole that have less than 0.5 Ti atoms in their structural formula. In this diagram, amounts of AlIV and Ti are reduced in the structural formula because of high Si contents. In vector diagrams of edenite, pargasite and hornblende substitution, analyzed samples show evidence for hornblende–pargasite replacement (Figure 7c). The amphibole in the Sungun dykes is a combination of hornblende–Tschermakite and ferroTschermakite [11].
The chemical composition of amphibole is a proxy for the oxygen fugacity of the magma from which it crystallized. Oxygen fugacity can be calculated based on models by [23,24] and according to cationic Fe# ratios. Values between 0 and 0.6 indicate high oxygen fugacity, 0.6 and 0.8 indicates average oxygen fugacity and ratios ~1 indicate low oxygen fugacity. The chemical composition of studied amphibole shows Fe# ratios between 0.28 and 0.33, consistent with high-oxygen-fugacity conditions. An additional oxygen fugacity model [25] was used, using the equation Log fO2 = −30930/T + 14.98 + 0.142 (P − 1)/T. Values ranging between −15 and −13 for diorite enclaves (Table 6) are, once again, consistent with high oxygen fugacity. Furthermore, the occurrence of quartz and sphene together with amphibole is indicative of high-oxygen-fugacity conditions [25] and, thus, consistent with our calculations.

6. Mineral Chemistry of Pyroxene

This section focuses on clinopyroxene, observed as in DK3-type diorite dykes and a metasomatic phase in Sungun skarn units. The general formula for pyroxene group minerals is M1M2T2O6; the M2 site can be occupied by Ca (Calcic Pyroxenes), Na (sodic pyroxenes), Mn, Fe2+ and/or Mg; the M1 position can be occupied by Al, Cr, Fe3+, Ti, Fe2+ and/or Mg; and the T position is occupied by Si and Al (e.g., [19]). Structural formulae are calculated based on six oxygen atoms and four cations. The results of the analysis are shown in Table 4. The amount of Al in T site is so elevated that it can compensate the Si4+ shortage in the T position. The amounts of AlIV and Si the T site are 0.14–0.27 and 1.73–1.86, respectively. The M1 position frequently has amounts of Mg (0.62–0.80), Fe3+ (0.05–0.22), AlIV (0.10–0.16) and Ti (0.03–0.05) and the M2 position is occupied by Ca (0.44–0.51), although others contain Fe2+ (0.20–0.33), Mg (0.05–0.18), Na (0.08–0.13), K (0.02–0.05) and Mn (0.01). The observed differences in Fe3+ can be described by various modes of oxidation during magmatic conditions. The average composition is as follows:
(Ca0.467Fe2+0.24Mg0.136Na 0.108K 0.033Mn 0.01) (Mg 0.675Fe3+0.168AlVI 0.117Ti 0.041) (Si 1.774AlIV 0.225)2O6
Al and Ti are Tschermak replacement, meaning replacement of Mg and Fe by Ti at the M2 site and replacement of Al by Si at the T site. Accordingly, Al/Ti ratios are greater than 10 (Figure 8a) and the observed correlation between Fe3+ and Al (Figure 8b) indicates that the calcium Tschermak component is the most important part of the clinopyroxene’s composition. Furthermore, a diagram of Ti-AlIV shows positive correlation that indicates a linked increase between the two elements (Figure 8c). In contrast, samples below the 1:2 line indicate that Al is located in a tetrahedral position to offset other substitutions. The Ti-Mg diagram shows a negative correlation and justifies increases in Ti through replacement of Mg (Figure 8d).
Diagrams of Ti + Cr + Na vs. Al are used to determine whether clinopyroxene is igneous or metamorphic in nature. All analyzed areas have compositions consistent with an igneous origin (Figure 9a). The classification based on the Q-J diagram [27] indicates that crystals are in the group of Ca-Mg-Fe clinopyroxene (Figure 9b). Based on the En-Wo-Fs ternary diagram, clinopyroxene are augite, whereas from the Sungun skarn, are diopside [26] (Figure 9c). In the alternate classification scheme by [28], the Ti-Na-AlIV clinopyroxene ternary diagram shows that clinopyroxene plots in the CATS range, consistent with clinopyroxene Tschermak calcium compositions (Figure 9d).
Oxygen fugacity has a special effect on changes in the liquidus temperature and magma composition [31] and is also an effective factor for controlling magmatic processes and the sequence of crystallization [32,33,34,35]. To determine the degree of oxygen fugacity in the primary magma by using clinopyroxene, the total amount of AlIV + 2Ti + Cr was used against Na + AlIV [30] (Figure 9e). Fe3+ in the octahedral position replaces elements, such as Cr and AlIV. Therefore, the clinopyroxene amount of Fe3+ in pyroxenes depends strongly on the amount of AlIV: whenever more aluminum enters into the tetrahedral position, the possibility for Fe3+ to enter M sites will increase. In the diagram (Figure 9e), the Fe3 + =0 line is a proxy for oxygen fugacity; data points that plot above the line indicate high fugacities and distance from this line indicates greater fugacity values. Fe3+ content from Sungun is, thus, consistent with high oxygen fugacity during magmatic clinopyroxene crystallization.

7. Magmatic Series and Tectonic Environment

7.1. Magma Series from Amphibole Composition

Bivariate diagrams of Al2O3 vs. TiO2 [36] are used to determine the source and nature of the magma in diorite enclaves in the region from the chemical composition of amphibole. Studied samples are largely located within the sub-alkaline field, with only a few transitional samples plotting within the sub-alkaline and alkaline field (Figure 10a,b). These data are consistent with previously reported whole-rock geochemistry showing the calc-alkalic to alkalic nature of the Sungun magmas [18].

7.2. Temperature Estimates from Chlorite

Temperatures estimated from Sungun chlorite compositions are provided in Table 5 for several chlorite geothermometers [37,38,39,40,41]. The estimates obtained from models by [37,40] are most applicable to diagenetic, hydrothermal and metamorphic environments because the tetrahedral structure of aluminum is independent from bulk rock chemistry:
T (°C) = −61.92 + 321.98AlIV
The authors of [40] categorized geo-thermometers for chlorite formed in hydrothermal environments saturated in aluminum (i.e., in the presence of other aluminum minerals). They corrected the tetrahedral structure of aluminum and rewrote Equation (1):
AlcIV = AlIV + 0.7Fe/(Fe + Mg)T = 106AlcIV + 18
The correction to Equation (2) proposed by [41], which is applicable to similar temperature ranges, is only applicable for low-Fe chlorite (Fe > 0.6). The [40] model is, thus, the most appropriate for this study.
The authors of [42] studied combinations of chlorite in the meta-volcanic rocks of the Barton Greenstone belt, which includes basalt and dacite, and they proposed a chlorite geo-thermometer equation with a correction of 0.31 for the Fe/(Fe+Mg) ratio:
TX97-AlIV (°C) = 106.99 × ((AlIVO28) + 1.33 × (0.31 − Fe/(Fe+Mg))) – 61.92 if
Fe⁄((Fe + Mg)) < 0.31
TX97-AlIV (°C) = 106.99 × ((AlIVO28) + 1.33 × (0.31 − Fe/(Fe + Mg))) – 61.92 if
Fe⁄((Fe+Mg)) > 0.31
Several experimental correction factors were used in chlorite geo-thermometers to reduce the effect of bulk rock composition and contamination from other aluminum phases (e.g., [37,43]). For most experimental chlorite geo-thermometers, the amount of AlIV is estimated by using the 28-oxygen normalization method; however, in other models, a normalization to 14-oxygen is preferred. Nevertheless, the application of both chlorite normalizations (i.e., differences in sites of octahedral occupation) to the same geo-thermometer generates only minor variations in modeled temperatures.
Results from the two favored chlorite geothermometers ([37,40] Table 5) indicate temperatures ranging between 263 °C and 311 °C for DK1b diorite enclaves and between 230 °C and 258 °C for DK3 microdiorite enclaves.
Table
Table 5. Results of the thermometry calculations of chlorites in the diorite and microdiorite enclaves.
Table 5. Results of the thermometry calculations of chlorites in the diorite and microdiorite enclaves.
Sample [37][40][43][39][38][44][41][45][42][46]
b1 271319328241337280305251206231
b2 255303305209313244285237188217
b3 258306309214317249289238188218
b4 260309312219321255298240188220
b5DK1b260309313219321255291240189220
b6 265313320229328267292246201226
b7 272320330244338282306253211233
b8 244291289189297218282227177207
b9 268316325237333274296250206229
b10 273322332248341286295253209233
Average 263311316225325261294244196223
Max 273322332248341286306253211233
Min 244291289189297218282227177207
k1 229257266165266183248237267219
k2 232259270169270189252239270221
k3 228255264163264180246236267218
k4 233260271170271191258240271222
k5 238266279178279203267245277227
k6 229256265164265182256236266219
k7 226253260160260174257233262215
k8DK3230257267166267185264238270220
k9 235263274173274195266241272224
k10 225252259158258172252232260214
k11 231258268167268187261238269221
k12 222249255155255166249231261213
k13 222248254154254165258230260212
k14 240267282182282208275247282229
k15 237265277176277200264244276226
Average 230258267167267185258238269220
Max 240267282182282208275247282229
Min 222248254154254165246230260212

7.3. Pressure and Temperature Estimates from Amphibole

Experimental results show that the composition of amphibole depends on pressure, temperature, oxygen partial pressure (fugacity), total composition of the rock and coeval formation of other mineral phases [47,48]. In this study, to estimate of crystallization pressure of selected amphiboles, four conventional methods were used based on Al in hornblende [48,49,50,51]; results are presented in Table 6. Pressure estimates obtained from these models range between 3.0 and 5.3 kilobars (approximate depths of 9 to 16 kilometers) and standard deviations generally indicate that the degree of variation for each of these methods is negligible.
In all of the above models, the pressure of formation is determined solely from the total amount of Al and other parameters, such as temperature, are not considered. Many formulae have been proposed for calculating pressure. The model by [52] is appropriate for conditions consistent with convergent margins:
P (kbar) = −3.01 + 4.76(Al total)
The above formula allows for the determination of peak pressures of crystallization [51]. High amounts of magnetite and ilmenite indicate high oxygen fugacity and the amphiboles that crystallize in such conditions tend to show more reliable results for geothermobarometry [47,48]. Plagioclase and hornblende grains that are adjacent and equilibrated with each other are useful for thermometry and the usage of this pair of minerals in igneous rocks is independent to the presence or absence of quartz.
The calculation of the temperature in the formula presented by [53] (Table 6) shows that the temperature range for the diorite enclaves is between 714 and 731 °C. This temperature indicates mineral replacement in diorite enclaves occurs within Dk3 diorite dykes during late magmatic stages. Diagrams of the main elements of amphibole compared to (Na + K)A and total aluminum Al (total), which, respectively, show the temperature [54] and pressure [48] conditions of amphibole crystallization, provide insight on the pressure and temperature conditions at the time of crystallization. Experimental studies have shown that atomic amounts of Al (total) and (Na + K)A depend on the temperature of the system and often exhibit high positive correlation with each other [55,56]. Analysis of these diagrams shows a positive correlation between amounts of Al(total) and (Na + K)A, consistent with such temperature increases for the dioritic enclaves (Figure 10c). According to these diagrams, amounts of Mg and Si decrease with increasing Al total. Decreases in Si are accompanied by increases in Ti (Figure 11), indicating substitution associated with increasing pressure. With respect to (Na + K)A, negative correlations with Si and Mg are consistent with increasing temperatures (Figure 11). Mg decreases are likely related to replacement by Fe.

7.4. Pressure and Temperature Estimates from Pyroxene

The Winpyrox application by [57] was used for the thermobarometric analysis of pyroxene. The chemical composition of pyroxenes is an important index for measuring temperature and pressure in igneous rocks. Experiential research shows that the amount of AlIV in clinopyroxene depends on pressure [58]. The authors of [59] proposed a model for the estimation of temperature and pressure of clinopyroxene formation based on XPT and YPT indexes, which can be calculated with the following equations:
XpT = 0.446 SiO2 + 0.187 TiO2   0.404 Al2O3 + 0.346 FeO (tot)   0.052 MnO + 0.309 MgO + 0.431 CaO    0.446 Na2O
YpT = 0.369 SiO2+ 0.535 TiO2   0.317 Al2O3+ 0.323 FeO (tot) + 0.235 MnO    0.516 MgO − 0.167 CaO   0.153 Na2O
Using these indexes, we estimate pressures ranging between 11 and 15 kbar for the Sungun clinopyroxene (Figure 12a) and a temperature of formation ranging between 1250 °C and 1300 °C (Figure 12b). These are consistent with results from other geothermometers and geobarometers provided in Table 7 and Table 8.

8. Discussion and Conclusions

Previous studies on samples of Sungun dykes and Sungun porphyry show that they have bulk rock compositions more consistent with the post-collisional magmatic arc domain than magmas from continental active margins [4,11]. Similarities between REE patterns of the dykes and the porphyry suggest that their magmas share a common origin. However, the dykes are compositionally slightly more mafic and younger in age. All samples, with the exception of the micro-diorite and lamprophyric, plot in similar 87Sr/86Sr versus 143Nd/144Nd space, showing ratios consistent with a mantle source [4]. The isotope ratio of these rocks originated mainly from the melt extraction from a mantle source within a closed system. Thermobarometry of the dykes indicates that their magmas formed from the extraction of an intermediate magma and another magma of mixed crustal-mantle affinity. At a maximum pressure of 19 kbar, gravitational separation of the magmas within a lower-crustal magmatic chamber gave rise to the dioritic magma. This magma then rose and settled into another chamber at a maximum of 6 kbar (~18 km), where it fractionated and gravitationally separated. These magmas rose again in sequence, thereby creating the more felsic and earlier Sungun porphyry and the subsequent more mafic Sungun dykes [16,18].
Dioritic dykes in the eastern skarn part of the Sungun copper deposit contain abundant clinopyroxene. Although previous workers proposed that these were inherited from the skarn [26], our work shows that the crystals are augitic, contrasting with the diopsidic composition of clinopyroxene from the skarn. We propose that they are magmatic in origin. Substitution mechanisms of studied clinopyroxenes depend on variations in physical and chemical conditions and the distribution of Al and Ti minerals in the source magma. Pressures of formation of clinopyroxene in diorite dykes are estimated between 11 and 15 kilobars and temperatures of 1200 °C, consistent with early stage, lower-crustal (maximum 19 kbar) magmatic activities deduced from dyke thermobarometry [11]. High Fe3+ contents are consistent with high oxygen fugacities during early magmatic conditions.
Results stemming from the mineral analyses of enclaves described in this work constrain the later-stage cooling and retrograde alteration processes that occurred in Sungun magmas. Amphibole crystallization occurred at fairly well-constrained temperatures (714–731 °C), at pressures ranging between 3.0 and 5.3 kbar (9–16 km), as later dioritic magmas rose upwards in the crust. Amphiboles within the enclaves consist of calcic amphibole and a sub-group of magnesio-hornblende; such compositions, along with high-cationic Fe, reflect high oxygen fugacity at the time of crystallization and are, thus, consistent with a supra-subduction-zone (magmatic arc) environment. As the system cooled, later hydrothermal alteration and chloritization occurred at much lower temperatures: the retrograde formation of chlorite in microdiorite and diorite occurred at approximately 272 °C and 257 °C, respectively.
Recent petrologic studies on intrusive rocks in the Sungun Cu-Mo porphyry deposit show that the main stock of the intrusion and its peripheral dykes consist of, in order of abundance, quartz monzonite, quartz diorite, gabbro diorite, microdiorite, dacite and lamprophyre [11]. Generally, enclaves observed in late dykes consist of quartz diorite, diorite, hornfels and microdiorite. These findings have implications for our understanding of the genesis of the intrusion and its deposit. Indeed, previous work has documented that the stock consists of an early quartz monzonitic magma pulse, followed by a dioritic/granodioritic pulse [13]. In contrast, our results suggest that the intrusion consists of multiple pulses expressed as several sequential episodes of magma intrusion that are more lithologically diverse than previously described. Furthermore, the temperature of chloritization documented here is consistent but at the lower temperature range of previous estimates for propylitic hydrothermal alteration at Sungun [8].

Author Contributions

Conceptualization, A.A.K. and M.M.; methodology, A.A.K., M.M., B.M.S. and M.F.; field investigation, A.A.K. and M.M.; data curation, A.A.K., M.M., B.M.S. and M.F.; writing—original draft preparation A.A.K., M.M., B.M.S. and M.F.; writing—review and editing, A.A.K., M.M., B.M.S. and M.F.; supervision, A.A.K., M.M. and B.M.S.; funding acquisition, A.A.K., M.M., B.M.S. and M.F. All authors have read and agreed to the published version of the manuscript.

Funding

BMS acknowledges research funding from the Natural Sciences and Engineering Research Council of Canada (Discovery Grant RGPIN-2021-03306).

Acknowledgments

Particular thanks go to Jamshid Ahmadian (Payame Noor University) for precise EPMA analyses. Funding for this study was provided by the University of Tabriz.

Conflicts of Interest

The authors declare no conflict of interest.

References

  1. Sillitoe, R.H. Porphyry copper systems. Econ. Geol. 2010, 105, 3–41. [Google Scholar] [CrossRef]
  2. Richards, J.P. Postsubduction porphyry Cu-Au and epithermal Au deposits: Products of remelting of subduction-modified lithosphere. Geology 2009, 37, 247–250. [Google Scholar] [CrossRef]
  3. Logan, J.M.; Mihalynuk, M.G. Tectonic controls on early Mesozoic paired alkaline porphyry deposit belts (Cu-Au ± Ag-Pt-Pd-Mo) within the Canadian Cordillera. Econ. Geol. 2014, 109, 827–858. [Google Scholar] [CrossRef]
  4. Kamali, A.A.; Moayyed, M.; Amel, N.; Hosseinzadeh, M.R.; Mohammadiha, K.; Santos, J.F.; Brenna, M. Post-mineralization, cogenetic magmatism at the sungun cu-mo porphyry deposit (Northwest Iran): Protracted melting and extraction in an arc system. Minerals 2018, 8, 588. [Google Scholar] [CrossRef]
  5. Nabavi, M.H. An Introduction to the Geology of Iran; Geological Survey of Iran: Tehran, Iran, 1976. [Google Scholar]
  6. Moayyed, M. Petrologic Studies of Tertiary Volcano-Plutonic Belt in Western Alborz-Azerbaijan, with a Special Focus on Hashtchin Area, Iran. Ph.D. Thesis, University of Shahid Beheshti, Tehran, Iran, 2001. [Google Scholar]
  7. Osanloo, M.; Ataei, M. Using 2d lerchs and grossmann algorithm to design final pit limits of sungun copper deposit of Iran. Int. J. Eng. 2000, 13, 81–89. [Google Scholar]
  8. Hezarkhani, A.; Williams-Jones, A.E. Controls of alteration and mineralization in the Sungun porphyry copper deposit, Iran; evidence from fluid inclusions and stable isotopes. Econ. Geol. 1998, 93, 651–670. [Google Scholar] [CrossRef]
  9. Hassanpour, S. Metallogeny and Mineralization of Copper and Gold in Arasbaran Zone (Eastern Azerbaijan). Ph.D. Thesis, Shahid Beheshti University, Tehran, Iran, 2010. (In Persian with English Abstract). [Google Scholar]
  10. Jamali, H.; Dilek, Y.; Daliran, F.; Yaghubpur, A.; Mehrabi, B. Metallogeny and tectonic evolution of the Cenozoic Ahar—Arasbaran volcanic belt, northern Iran. Int. Geol. Rev. 2010, 52, 608–630. [Google Scholar] [CrossRef]
  11. Kamali, A.A.; Moayyed, M.; Amel, N.; Mohammad, F.; Brenna, M.; Saumur, B.M.; Santos, J.F.J.F. Mineralogy, mineral chemistry and thermobarometry of post-mineralization dykes of the Sungun Cu–Mo porphyry deposit (Northwest Iran). Open Geosci. 2020, 12, 764–790. [Google Scholar] [CrossRef]
  12. Richards, J.P.; Wilkinson, D.; Ullrich, T. Geology of the Sari Gunay Epithermal Gold Deposit, Northwest Iran. Econ. Geol. 2006, 101, 1455–1496. [Google Scholar] [CrossRef]
  13. Hezarkhani, A. Petrology of the intrusive rocks within the Sungun porphyry copper deposit, Azerbaijan, Iran. J. Asian Earth Sci. 2006, 27, 326–340. [Google Scholar] [CrossRef]
  14. Kamali, A.; Moayyed, M.; Amel, N.; Hosainzadeh, M.R. Mineral chemistry and geochemistry of lamprophyric dykes in the Sungun Cu-Mo porphyry deposit (Varzaghan-Northwestern Iran). J. Geosci. 2017, 26, 73–90. [Google Scholar]
  15. Aghazadeh, M.; Hou, Z.; Badrzadeh, Z.; Zhou, L. Temporal–spatial distribution and tectonic setting of porphyry copper deposits in Iran: Constraints from zircon U–Pb and molybdenite Re–Os geochronology. Ore Geol. Rev. 2015, 70, 385–406. [Google Scholar] [CrossRef]
  16. Mehrpartou, M. Contributions to the Geology, Geochemistry, Ore Genesis and Fluid Inclusion Investigations on Sungun Cu-Mo Porphyry Deposit (North-West of Iran). Ph.D. Thesis, Hamburg University, Hamburg, Germany, 1993. [Google Scholar]
  17. Kamali, A.; Moayyed, M.; Amel, N.; Hosseinzadeh, M.R. Mineralogy and Mineral Chemistry of Quartz-Dioritic Dykes of Sungun Mo- Cu Porphyry Deposit (NW Iran). Iran. J. Crystallogr. Mineral. 2017, 25, 123–138. [Google Scholar]
  18. Kamali, A.A. Petrology and Mineral Chemistry of Post Mineralization Dykes of Sungun Cu-Mo Porphyry Deposit, North of Varzegan, East-Azerbaijan. Ph.D. Thesis, University of Tabriz, Tabriz, Iran, 2016. [Google Scholar]
  19. Deer, W.A.; Howie, R.A.; Zussman, J. An Introduction to the Rock-Forming Minerals, 2nd ed.; Pearson: London, UK, 1992; ISBN 0582300940. [Google Scholar]
  20. Moazen, M. Chlorite-Chloritoid-Garnet Equilibria and Geothermometry in the Sanandaj-Sirjan Me-Tamorphic Belt, Southern Iran. Iran. J. Sci. Technol. Trans. A Sci. 2004, 28, 65–78. [Google Scholar]
  21. Chabu, M. The geochemistry of phlogopite and chlorite from the Kipushi Zn-Pb-Cu deposit, Shaba, Zaire. Can. Mineral. 1995, 33, 547–558. [Google Scholar]
  22. Leake, B.E.; Woolley, A.R.; Arps, C.E.S.; Birch, W.D.; Gilbert, M.C.; Grice, J.D.; Hawthorne, F.C.; Kato, A.; Kisch, H.J.; Krivovichev, V.G. Report. Nomenclature of amphiboles: Report of the subcommittee on amphiboles of the international mineralogical association commission on new minerals and mineral names. Mineral. Mag. 1997, 61, 295–321. [Google Scholar] [CrossRef]
  23. Anderson, J.L.; Smith, D.R. The effects of temperature and fO2 on the Al-in-hornblende barometer. Am. Mineral. 1995, 80, 549–559. [Google Scholar] [CrossRef]
  24. Speer, J.A. Micas in Igneous Rocks. Rev. Mineral. Geochemistry 1984, 13, 299–356. [Google Scholar]
  25. Wones, D.R. Significance of the Assemblage Titanite+ Magnetite+ Quartz in Granitic Rocks. Am. Mineral. 1989, 74, 744–749. [Google Scholar]
  26. Alavi, G. Study of the skarn deposits around the Sheyvar-Dagh batolith and comparison with the Sungun porphyry skarn. Geology. Tabriz 2014. [Google Scholar]
  27. Morimoto, N. Nomenclature of pyroxenes. Mineral. J. 1989, 14, 198–221. [Google Scholar] [CrossRef]
  28. Papike, J.J. Amphiboles and pyroxenes: Characterization of other than quadrilateral components estimates of ferric iron from microprobe data. Geol. Soc. Am. Abstr. Programs 1974, 6, 1053–1054. [Google Scholar]
  29. Berger, J.; Femenias, O.; Mercier, J.C.C.; Demaiffe, D. Ocean-floor hydrothermal metamorphism in the Limousin ophiolites (western French Massif Central): Evidence of a rare preserved Variscan oceanic marker. J. Metamorph. Geol. 2005, 23, 795–812. [Google Scholar] [CrossRef]
  30. Schweitzer, E.L.; Papike, J.J.; Bence, A.E. Statistical analysis of clinopyroxenes from deep-sea basalts. Am. Mineral. 1979, 64, 501–513. [Google Scholar] [CrossRef]
  31. France, L.; Ildefonse, B.; Koepke, J.; Bech, F. A new method to estimate the oxidation state of basaltic series from microprobe analyses. J. Volcanol. Geotherm. Res. 2010, 189, 340–346. [Google Scholar] [CrossRef]
  32. Botcharnikov, R.E.; Koepke, J.; Holtz, F.; McCammon, C.; Wilke, M. The effect of water activity on the oxidation and structural state of Fe in a ferro-basaltic melt. Geochim. Cosmochim. Acta 2005, 69, 5071–5085. [Google Scholar] [CrossRef]
  33. Kilinc, A.; Carmichael, I.S.E.E.; Rivers, M.L.; Sack, R.O. The ferric-ferrous ratio of natural silicate liquids equilibrated in air. Contrib. Mineral. Petrol. 1983, 83, 136–140. [Google Scholar] [CrossRef]
  34. Kress, V.C.; Carmichael, I.S.E.E. The compressibility of silicate liquids containing Fe2O3 and the effect of composition, temperature, oxygen fugacity and pressure on their redox states. Contrib. Mineral. Petrol. 1991, 108, 82–92. [Google Scholar] [CrossRef]
  35. Moretti, R. Polymerisation, basicity, oxidation state and their role in ionic modelling of silicate melts. Ann. Geophys. 2005, 48, 583–608. [Google Scholar] [CrossRef]
  36. Molina, J.F.; Scarrow, J.H.; Montero, P.G.; Bea, F. High-Ti amphibole as a petrogenetic indicator of magma chemistry: Evidence for mildly alkalic-hybrid melts during evolution of Variscan basic—Ultrabasic magmatism of Central Iberia. Contrib. Mineral. Petrol. 2009, 158, 69–98. [Google Scholar] [CrossRef]
  37. Cathelineau, M.; Nieva, D. A chlorite solid solution geothermometer the Los Azufres (Mexico) geothermal system. Contrib. Mineral. Petrol. 1985, 91, 235–244. [Google Scholar] [CrossRef]
  38. Jowett, E.C. Fitting iron and magnesium into the hydrothermal chlorite geothermometer. In Proceedings of the GAC/MAC/SEG Joint Annual Meeting, Toronto, ON, Canada, 27–29 May 1991. Program with Abstracts 16. [Google Scholar]
  39. Kavalieris, I.; Walshe, J.L.; Halley, S.; Harrold, B.P. Dome-related gold mineralization in the Pani volcanic complex, North Sulawesi, Indonesia; a study of geologic relations, fluid inclusions, and chlorite compositions. Econ. Geol. 1990, 85, 1208–1225. [Google Scholar] [CrossRef]
  40. Kranidiotis, P.; MacLean, W.H. Systematics of chlorite alteration at the Phelps Dodge massive sulfide deposit, Matagami, Quebec. Econ. Geol. 1987, 82, 1898–1911. [Google Scholar] [CrossRef]
  41. De Caritat, P.; Hutcheon, I.A.N.; Walshe, J.L. Chlorite geothermometry: A review. Clays Clay Miner. 1993, 41, 219–239. [Google Scholar] [CrossRef]
  42. Xie, X.; Byerly, G.R.; Ferrell, R.E., Jr. IIb trioctahedral chlorite from the Barberton greenstone belt: Crystal structure and rock composition constraints with implications to geothermometry. Contrib. Mineral. Petrol. 1997, 126, 275–291. [Google Scholar] [CrossRef]
  43. Cathelineau, M. Cation site occupancy in chlorites and illites as function of temperature. Clay Miner. 1988, 23, 471–485. [Google Scholar] [CrossRef]
  44. Hillier, S.; Velde, B. Octahedral Occupancy and the Chemical Composition of Diagenetic (Low-Temperature) Chlorites. Clay Miner. 1991, 26, 149–168. [Google Scholar] [CrossRef]
  45. Zang, W.; Fyfe, W.S. Chloritization of the Hydrothermally Altered Bedrock at the Igarapé Bahia Gold Deposit, Carajás, Brazil. Miner. Depos. 1995, 30, 30–38. [Google Scholar] [CrossRef]
  46. El-Sharkawy, M.F. Talc Mineralization of Ultramafic Affinity in the Eastern Desert of Egypt. Miner. Depos. 2000, 35, 346–363. [Google Scholar] [CrossRef]
  47. Esawi, E.K. AMPH-CLASS: An Excel spreadsheet for the classification and nomenclature of amphiboles based on the 1997 recommendations of the International Mineralogical Association. Comput. Geosci. 2004, 30, 753–760. [Google Scholar] [CrossRef]
  48. Hammarstrom, J.M.; Zen, E. Aluminum in hornblende: An empirical igneous geobarometer. Am. Mineral. 1986, 71, 1297–1313. [Google Scholar]
  49. Hollister, L.S.; Grissom, G.C.; Peters, E.K.; Stowell, H.H.; Sisson, V.B. Confirmation of the empirical correlation of Al in hornblende with pressure of solidification of calc-alkaline plutons. Am. Mineral. 1987, 72, 231–239. [Google Scholar]
  50. Johnson, M.C.; Rutherford, M.J. Experimental calibration of the aluminum-in-hornblende geobarometer with application to Long Valley caldera (California) volcanic rocks. Geology 1989, 17, 837–841. [Google Scholar] [CrossRef]
  51. Schmidt, M.W. Amphibole composition in tonalite as a function of pressure: An experimental calibration of the Al-in-hornblende barometer. Contrib. Mineral. Petrol. 1992, 110, 304–310. [Google Scholar] [CrossRef]
  52. lNonn Spnpn, J.A.; Vyhnal, C.R.; McSween, H.Y.; Speer, J.A. Hornblende chemistry in southern Appalachian granitoids: Implications for aluminum hornblende thermobarometry and magmatic epidote stability. Am. Mineral. 1991, 76, 176–188. [Google Scholar]
  53. Blundy, J.D.; Holland, T.J.B. Calcic amphibole equilibria and a new amphibole-plagioclase geothermometer. Contrib. Mineral. Petrol. 1990, 104, 208–224. [Google Scholar] [CrossRef]
  54. Humphreys, M.C.S.; Edmonds, M.; Christopher, T.; Hards, V. Chlorine variations in the magma of Soufrière Hills Volcano, Montserrat: Insights from Cl in hornblende and melt inclusions. Geochim. Cosmochim. Acta 2009, 73, 5693–5708. [Google Scholar] [CrossRef]
  55. Rutherford, M.J.; Devine, J.D. Magmatic conditions and magma ascent as indicated by hornblende phase equilibria and reactions in the 1995--2002 Soufriere Hills magma. J. Petrol. 2003, 44, 1433–1453. [Google Scholar] [CrossRef]
  56. Scaillet, B.; Evans, B.W. The 15 June 1991 Eruption of Mount Pinatubo. I. Phase Equilibria and Pre-eruption P-T-fO2-fH2O Conditions of the Dacite Magma. J. Petrol. 1999, 40, 381–411. [Google Scholar] [CrossRef]
  57. Yavuz, F. WinPyrox: A Windows program for pyroxene calculation classification and thermobarometry. Am. Mineral. 2013, 98, 1338–1359. [Google Scholar] [CrossRef]
  58. Thompson, R.N. Some high-pressure pyroxenes. Mineral. Mag. 1974, 39, 768–787. [Google Scholar] [CrossRef]
  59. Soesoo, A. A multivariate statistical analysis of clinopyroxene composition: Empirical coordinates for the crystallisation PT-estimations. GFF 1997, 119, 55–60. [Google Scholar] [CrossRef]
  60. Nimis, P. A Clinopyroxene Geobarometer for Basaltic Systems Based on Crystal-Structure Modeling. Contrib. Mineral. Petrol. 1995, 121, 115–125. [Google Scholar] [CrossRef]
  61. Nimis, P.; Ulmer, P. Clinopyroxene Geobarometry of Magmatic Rocks Part 1: An Expanded Structural Geobarometer for Anhydrous and Hydrous, Basic and Ultrabasic Systems. Contrib. Mineral. Petrol. 1998, 133, 122–135. [Google Scholar] [CrossRef]
  62. Nimis, P. Clinopyroxene Geobarometry of Magmatic Rocks. Part 2. Structural Geobarometers for Basic to Acid, Tholeiitic and Mildly Alkaline Magmatic Systems. Contrib. Mineral. Petrol. 1999, 135, 62–74. [Google Scholar] [CrossRef]
  63. Putirka, K.D. Thermometers and Barometers for Volcanic Systems. Rev. Mineral. Geochem. 2008, 69, 61–120. [Google Scholar] [CrossRef]
  64. Bertrand, P.; Mercier, J.-C.C. The Mutual Solubility of Coexisting Ortho- and Clinopyroxene: Toward an Absolute Geothermometer for the Natural System? Earth Planet. Sci. Lett. 1985, 76, 109–122. [Google Scholar] [CrossRef]
  65. Nimis, P.; Taylor, W.R. Single Clinopyroxene Thermobarometry for Garnet Peridotites. Part I. Calibration and Testing of a Cr-in-Cpx Barometer and an Enstatite-in-Cpx Thermometer. Contrib. Mineral. Petrol. 2000, 139, 541–554. [Google Scholar] [CrossRef]
  66. Negro, A.D.; Carbonin, S.; Salviulo, G.; Piccirillo, E.M.; Cundari, A. Crystal Chemistry and Site Configuration of the Clinopyroxene from Leucite-Bearing Rocks and Related Genetic Significance: The Sabatini Lavas, Roman Region, Italy. J. Petrol. 1985, 26, 1027–1040. [Google Scholar] [CrossRef]
  67. Molina, G.; Zanazzi, P.F.; Mineralogy, P.Z.-E.J. Intracrystalline Fe2+ − Mg Ordering in Augite: Experimental Study and Geothermometric Applications. Eur. J. Mineral. 1991, 3, 863–876. [Google Scholar] [CrossRef] [Green Version]
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Figure 1. Regional tectonic map of Iran [12] showing the location of the study area.
Figure 1. Regional tectonic map of Iran [12] showing the location of the study area.
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Figure 2. Geological map of the Sungun Copper Mine [11].
Figure 2. Geological map of the Sungun Copper Mine [11].
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Figure 3. Hand sample (left) and thin section (right) photographs of representative samples from Sungun post-mineralization dykes. All photomicrographs are in plane polarized light. (a,b) Microdiorite enclaves in DK1b dykes: (a) Mingled contact between a fine-grained microdiorite sheet and a medium-grained quartz diorite. (b) Photomicrograph showing the contact between the microdiorite and a quartz diorite. (c,d) Quartz diorite enclaves: (c) irregular mingled contact between a fine-grained autolith and a medium-grained quartz diorite. (d) Boundary between the quartz diorite and its enclave. (e,f) Hornfels enclaves in DK3 dykes: (e) hornfels xenolith within an outcrop of fine-grained diorite. (f) Photomicrograph showing the boundary between the dyke and enclave of hornfels in microscopic scale. (g,h) Diorite enclaves in DK3 dykes: (g) DK3 xenolith in the dioritic dykes. (h) Photomicrograph of the contact of DK3 xenolith with the host diorite dyke.
Figure 3. Hand sample (left) and thin section (right) photographs of representative samples from Sungun post-mineralization dykes. All photomicrographs are in plane polarized light. (a,b) Microdiorite enclaves in DK1b dykes: (a) Mingled contact between a fine-grained microdiorite sheet and a medium-grained quartz diorite. (b) Photomicrograph showing the contact between the microdiorite and a quartz diorite. (c,d) Quartz diorite enclaves: (c) irregular mingled contact between a fine-grained autolith and a medium-grained quartz diorite. (d) Boundary between the quartz diorite and its enclave. (e,f) Hornfels enclaves in DK3 dykes: (e) hornfels xenolith within an outcrop of fine-grained diorite. (f) Photomicrograph showing the boundary between the dyke and enclave of hornfels in microscopic scale. (g,h) Diorite enclaves in DK3 dykes: (g) DK3 xenolith in the dioritic dykes. (h) Photomicrograph of the contact of DK3 xenolith with the host diorite dyke.
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Figure 4. (a) A hand specimen from the dioritic dykes (coarse plagioclase (plg), epidote (Epi) and amphibole (Amp)); (b) plagioclase phenocrysts exhibiting twinning; (c) euhedral amphiboles and plagioclase. (d) Alteration in amphibole and plagioclase in diorite dykes; (e,f) pyroxene in diorite dykes (DK3).
Figure 4. (a) A hand specimen from the dioritic dykes (coarse plagioclase (plg), epidote (Epi) and amphibole (Amp)); (b) plagioclase phenocrysts exhibiting twinning; (c) euhedral amphiboles and plagioclase. (d) Alteration in amphibole and plagioclase in diorite dykes; (e,f) pyroxene in diorite dykes (DK3).
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Figure 5. Plagioclase phenocryst compositions for each of the diorite and microdiorite enclaves [19].
Figure 5. Plagioclase phenocryst compositions for each of the diorite and microdiorite enclaves [19].
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Figure 6. Compositional variations of chlorites in terms of (a) Fe/(Mg+Fe2+) versus AlIV/(Si+AlIV) [20]. (b) Mg/(Mg+Fe) versus Si [21] from diorite and microdiorite enclaves (cations/28 oxygen atoms).
Figure 6. Compositional variations of chlorites in terms of (a) Fe/(Mg+Fe2+) versus AlIV/(Si+AlIV) [20]. (b) Mg/(Mg+Fe) versus Si [21] from diorite and microdiorite enclaves (cations/28 oxygen atoms).
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Figure 7. (a) Major-element data for amphiboles from diorite enclaves plotted on the Mg/(Mg+Fe2+) vs. Si classification diagram [22]. (b) Al (AlIV) plotted vs. Ti for amphibole from the diorite enclaves [22]. (c) Exchange vectors diagram of Edenite–Pargazite and Hornblende based on AlIV amounts vs. (Na+K) for diorite enclaves [22].
Figure 7. (a) Major-element data for amphiboles from diorite enclaves plotted on the Mg/(Mg+Fe2+) vs. Si classification diagram [22]. (b) Al (AlIV) plotted vs. Ti for amphibole from the diorite enclaves [22]. (c) Exchange vectors diagram of Edenite–Pargazite and Hornblende based on AlIV amounts vs. (Na+K) for diorite enclaves [22].
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Figure 8. Pyroxene xenolith compositions (a) Ti vs. Al diagram, in which most samples are located in the Al/Ti zone > 10, (b) Fe3+ vs. Al IV diagram where a strong linear correlation between these two cations is observed. (c) Ti vs. Al IV diagram, showing a broad positive correlation between the two, (d) Ti vs. Mg diagram showing a negative correlation, revealing the increase in Ti at the expense of Mg.
Figure 8. Pyroxene xenolith compositions (a) Ti vs. Al diagram, in which most samples are located in the Al/Ti zone > 10, (b) Fe3+ vs. Al IV diagram where a strong linear correlation between these two cations is observed. (c) Ti vs. Al IV diagram, showing a broad positive correlation between the two, (d) Ti vs. Mg diagram showing a negative correlation, revealing the increase in Ti at the expense of Mg.
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Figure 9. (a) Al diagram vs. Ti-Na- Cr to distinguish igneous from metamorphic pyroxene; all clinopyroxenes are located in igneous field [29]. (b) The Q-J clinopyroxene classification diagram [27]. (c) Wo-En-Fs ternary diagrams of pyroxene [27]. (d) Clinopyroxene ternary diagram of Ti-Na- AlIV, studied samples are located exclusively in the CATS field. (e) An estimation of oxygen fugacity from pyroxene crystals compositions in diorite dykes [30].
Figure 9. (a) Al diagram vs. Ti-Na- Cr to distinguish igneous from metamorphic pyroxene; all clinopyroxenes are located in igneous field [29]. (b) The Q-J clinopyroxene classification diagram [27]. (c) Wo-En-Fs ternary diagrams of pyroxene [27]. (d) Clinopyroxene ternary diagram of Ti-Na- AlIV, studied samples are located exclusively in the CATS field. (e) An estimation of oxygen fugacity from pyroxene crystals compositions in diorite dykes [30].
Minerals 12 01218 g009
Minerals 12 01218 g010 550
Figure 10. (a) Al2O3 vs. TiO2 and (b) Na2O vs. TiO2 diagram for amphibole [36]. The dioritic enclave samples are dominantly located in subalkaline fields. (c) (Na+K) A vs. (Al) total in amphiboles and diorite enclaves.
Figure 10. (a) Al2O3 vs. TiO2 and (b) Na2O vs. TiO2 diagram for amphibole [36]. The dioritic enclave samples are dominantly located in subalkaline fields. (c) (Na+K) A vs. (Al) total in amphiboles and diorite enclaves.
Minerals 12 01218 g010
Minerals 12 01218 g011 550
Figure 11. The Al (total) vs. Ti, Mg, Si and (Na+K) A diagram vs. the Ti, Mg, Si for the study of chemical composition changes in dioritic enclaves. Associated inferred pressure and temperature changes are indicated with red arrows.
Figure 11. The Al (total) vs. Ti, Mg, Si and (Na+K) A diagram vs. the Ti, Mg, Si for the study of chemical composition changes in dioritic enclaves. Associated inferred pressure and temperature changes are indicated with red arrows.
Minerals 12 01218 g011
Minerals 12 01218 g012 550
Figure 12. Estimations of (a) crystallization pressure and (b) crystallization temperature of clinopyroxene.
Figure 12. Estimations of (a) crystallization pressure and (b) crystallization temperature of clinopyroxene.
Minerals 12 01218 g012
Table
Table 1. Representative analyses of plagioclase from diorite and micro diorite enclaves.
Table 1. Representative analyses of plagioclase from diorite and micro diorite enclaves.
Xen-DK1bXen-DK3
SamplePl1Pl2Pl3Pl4b1b2b3b4b5K1K2K3K4K5K6K7K8K9
SiO267.2865.116666.7664.1466.0667.4167.4666.8767.3566.4467.6266.7866.4366.8267.2664.1167.33
TiO20.0200.03000.030.0100000.020.050.050.020.020.080.03
Al2O320.6521.4721.3720.7322.0320.5320.1820.0421.2120.3120.5619.962020.1720.2519.9120.3520.28
FeO0.040.030.030.030.090.040.030.020.050.330.390.350.30.360.40.132.920.23
MnO00.010.020.0100.02000.010.030.020.030.0100.0200.050.02
MgO000.010.010.020.01000.0100.010000.0400.640.08
CaO1.322.321.821.713.181.320.850.581.820.610.830.610.630.970.980.70.860.87
Na2O10.7110.3210.4810.699.7410.6911.0111.3210.4410.699.9911.1810.9310.8910.2110.4710.8710.93
K2O0.150.090.070.080.250.10.120.10.130.630.580.170.320.20.420.190.150.38
Total100.1799.3599.82100.0299.4598.8199.6299.54100.5399.9698.8299.9499.0299.0799.1698.68100.03100.15
Formula 8 (O)
Si2.942.882.92.932.852.932.962.962.922.962.942.962.962.942.952.972.862.95
Ti000000000000000000
Al1.061.121.111.071.151.071.041.041.091.051.071.031.041.051.051.041.071.05
Fe2+0000000000.010.010.010.010.010.0100.110.01
Mn000000000000000000
Mg00000000000000000.040.01
Ca0.060.110.090.080.150.060.040.030.080.030.040.030.030.050.050.030.040.04
Na0.910.890.890.910.840.920.940.960.880.910.860.950.940.940.870.90.940.93
K0.010000.010.010.010.010.010.040.030.010.020.010.020.010.010.02
Total4.9854.994.99554.9954.984.994.975554.974.965.085
Ab92.8688.5290.8891.4883.5193.0795.2296.6790.5793.4392.296.1695.1394.2292.5995.3594.9793.72
Or0.840.480.410.461.420.590.690.590.723.643.540.961.861.142.521.130.872.14
An6.3118.718.0715.076.344.082.748.712.934.262.883.014.644.893.524.164.14
Table
Table 2. Representative major-element compositions of chlorite from studied diorite and microdiorite enclaves.
Table 2. Representative major-element compositions of chlorite from studied diorite and microdiorite enclaves.
Xen-DK1bXen-DK3
Sample b1b2b3b4b5b6b7b8b9b10k1k2k3k4k5k6k7k8k9k10k11k12k13k14k15
SiO2 25.4326.4526.2526.3026.1426.0625.6127.0125.9025.5929.4129.2029.4229.2028.9528.9729.0529.0728.4828.9528.6730.1529.0028.9128.75
TiO20.040.040.010.030.070.090.020.050.030.080.010.020.000.030.010.010.010.020.020.010.000.020.000.020.01
Al2O319.1418.6718.5318.8218.8319.1219.2717.8519.3919.6818.5918.6918.5718.6018.8518.1317.8318.2018.2617.7318.0218.2317.3418.8318.66
FeO30.2129.9330.4631.0230.6730.2630.1129.7330.1530.3216.8416.8716.6217.0317.3216.7416.6716.6316.9716.5016.6916.5716.0917.1617.04
MnO0.580.540.540.580.570.580.560.520.560.590.460.460.430.520.510.490.490.490.500.470.480.480.500.470.47
MgO11.4812.0311.8011.6311.4911.8511.8812.6011.8411.4421.2821.1521.3321.2221.1221.0421.1021.4020.6920.9820.9422.1121.3521.4620.98
CaO0.060.080.180.060.070.120.130.140.100.070.160.140.150.150.150.150.140.120.100.150.170.170.150.150.14
K2O0.000.010.010.010.000.010.000.010.010.000.020.010.010.010.010.010.010.000.010.010.020.020.010.010.02
F0.000.000.000.000.060.000.030.000.000.140.090.040.240.170.070.170.040.090.180.110.260.350.030.120.03
Cl0.010.000.010.010.010.000.010.000.010.010.000.000.000.010.000.000.000.000.010.010.010.000.000.010.00
O=F0.000.000.000.000.030.000.010.000.000.060.040.020.100.070.030.070.020.040.080.050.110.150.010.050.01
O=Cl0.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.00
Total86.9587.7587.7988.4687.8888.0987.6187.9187.9987.8686.8286.5686.6786.8786.9685.6485.3285.9885.1484.8785.1587.9584.4687.0986.09
14(O)
Si2.792.862.852.842.842.812.782.912.802.782.982.972.992.972.942.983.002.982.963.002.973.023.022.932.95
Ti0.000.000.000.000.010.010.000.000.000.010.000.000.000.000.000.000.000.000.000.000.000.000.000.000.00
Al2.472.382.372.392.412.432.472.272.472.522.222.242.222.232.262.202.172.202.232.172.202.152.132.252.25
Fe(2+)2.772.712.762.802.782.732.742.682.722.751.431.431.411.451.471.441.441.421.471.431.451.391.401.461.46
Mn0.050.050.050.050.050.050.050.050.050.050.040.040.040.040.040.040.040.040.040.040.040.040.040.040.04
Mg1.881.941.911.871.861.911.922.021.911.853.223.213.233.213.203.233.253.273.203.253.243.303.313.243.21
Ca0.010.010.020.010.010.010.020.020.010.010.020.020.020.020.020.020.020.010.010.020.020.020.020.020.02
K0.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.00
F0.000.000.000.000.020.000.010.000.000.050.030.010.080.060.020.060.010.030.060.040.090.110.010.040.01
Cl0.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.000.00
Al(IV)1.211.141.151.161.161.191.221.091.201.221.021.031.011.031.061.021.001.021.041.001.030.980.981.071.05
Al(VI)1.261.241.221.231.251.251.251.181.271.291.201.211.211.191.201.181.171.171.191.171.181.161.141.181.20
Table
Table 3. Representative major-element compositions of amphibole from studied diorite enclave.
Table 3. Representative major-element compositions of amphibole from studied diorite enclave.
SampleX1X2X3X4X5X6X7X8X9X10
SiO243.1645.1945.2046.1546.4144.6345.2646.0644.3845.36
TiO22.101.811.841.521.621.721.691.571.831.61
Al2O310.138.798.637.577.459.078.768.299.198.39
FeO12.9512.3812.2311.7211.4412.5412.4812.4912.8012.47
MnO0.340.360.420.330.300.350.320.330.360.34
MgO14.0315.1715.0915.6816.0814.8414.9815.3914.2115.01
CaO10.8310.7810.7910.6810.7610.6910.7110.7210.8810.64
Na2O1.851.701.661.481.551.751.661.621.711.58
K2O0.620.530.540.450.460.580.580.530.610.57
Total98.0798.8098.4897.6598.1698.2598.5299.1098.0398.04
T
Si6.286.496.516.686.676.456.526.596.466.57
Al1.721.491.471.291.261.551.481.401.541.43
Ti0.000.030.020.030.070.010.000.020.000.00
Total8.008.008.008.008.008.008.008.008.008.00
C
Al0.010.000.000.000.000.000.010.000.030.00
Ti0.230.170.180.130.110.180.180.150.200.17
Fe3+1.431.381.331.271.291.401.331.341.291.32
Mg3.043.253.243.383.453.203.223.283.083.24
Fe2+0.150.110.150.140.080.120.180.150.270.19
Mn2+0.040.040.050.040.040.040.040.040.040.04
Total4.904.954.954.974.964.944.954.964.924.96
B
Ca1.691.661.671.661.661.661.651.641.701.65
Na0.310.340.330.350.340.350.350.360.300.35
Total2.002.002.002.002.002.002.002.002.002.00
A
Na0.210.130.130.070.090.150.120.090.180.09
K0.120.100.100.080.080.110.110.100.110.11
Total0.330.230.230.150.170.250.220.190.290.20
Table
Table 4. EPMA analysis results of pyroxene of diorite dyke and Sungun skarn [26] (chemical composition of pyroxenes and structural formula based on 6 oxygen atoms).
Table 4. EPMA analysis results of pyroxene of diorite dyke and Sungun skarn [26] (chemical composition of pyroxenes and structural formula based on 6 oxygen atoms).
Sample Sungun DK3
point123456789102345678910
SiO251.1551.6651.5352.3151.8952.1751.3551.0351.5551.6447.9946.6846.5549.9647.4148.3847.2847.5246.32
TiO20.070.030.130.080.070.020.080.020.120.081.251.621.681.141.221.271.571.681.31
Al2O30.570.590.630.280.140.130.270.470.640.277.848.317.95.98.037.38.147.788.85
Cr2O30000000000000000000
FeO14.3112.9314.3913.4414.2413.8214.9313.6714.3914.6313.5314.0612.9512.113.3812.6513.1612.8413.77
MnO0.060.260.080.370.130.060.170.160.090.260.30.360.350.470.440.370.370.380.34
MgO9.0810.249.2410.749.269.688.699.449.248.9613.3612.7213.6516.1915.2715.7315.1415.2813.51
CaO23.6123.5923.5422.6623.7723.6323.5723.2823.5423.7111.8111.9812.5811.2311.2611.3111.2111.612.12
Na2O0.980.610.570.540.440.480.580.080.520.331.411.761.561.141.651.591.661.41.56
K2O0000000.040.02000.861.010.840.390.570.50.640.590.94
Total99.8399.91100.11100.4299.9499.9999.6898.17100.0999.8898.3598.598.0698.5299.2399.199.1799.0798.72
Si (T)1.961.971.971.981.991.991.981.991.971.991.811.761.751.861.751.791.751.771.73
Al (T)0.030.030.030.010.010.010.010.010.030.010.190.240.250.140.250.210.250.230.27
Fe3+ (T)0.020.0100.01000.01000000000000
Total (T)2222222222222222222
Al (M1)00000000.01000.160.130.10.120.10.110.110.110.12
Fe3+ (M1)0.110.080.060.050.040.040.0600.060.030.110.20.20.050.210.170.20.160.22
Ti (M1)00000000000.040.050.050.030.030.040.040.050.04
Cr (M1)0000000000000000000
Mg (M1)0.520.580.530.610.530.550.50.550.530.510.70.630.650.80.650.690.650.690.62
Fe2+ (M1)0.330.330.40.340.420.40.410.440.40.44000000000
Mn (M1)00.0100000.01000.01000000000
Total (M1)0.960.990.9910.9910.98111111111111
Mg (M2)00000000000.050.080.120.110.20.180.190.160.14
Fe2+ (M2)0000.030000.01000.320.240.210.330.20.220.210.240.21
Mn (M2)0000.010000.01000.010.010.010.010.010.010.010.010.01
Ca (M2)0.970.960.960.920.980.970.970.970.970.980.480.480.510.450.450.450.440.460.49
Na (M2)0.070.050.040.040.030.040.040.010.040.020.10.130.110.080.120.110.120.10.11
K (M2)00000000000.040.050.040.020.030.020.030.030.04
Total (M2)1.041.011.0111.0111.02111111111111
Wo53.3851.4651.148.5950.850.3651.6249.3450.950.630.8333.5334.226.733029.129.929.8833.57
En28.5631.0827.9132.0427.5428.726.4827.8427.826.6148.5349.5351.6353.6256.6156.3156.1954.7752.06
Fs18.0617.462119.3721.6620.9421.9122.8221.3122.7920.6416.9414.1719.6413.3814.5913.9215.3414.37
Q1.811.871.891.891.921.921.891.971.91.931.551.441.481.681.491.541.491.541.45
J0.150.090.080.080.070.070.090.010.080.050.210.260.230.170.240.230.240.20.23
Table
Table 6. Results of geothermobarometery and oxygen fugacity from amphibole in the diorite enclaves (DK3).
Table 6. Results of geothermobarometery and oxygen fugacity from amphibole in the diorite enclaves (DK3).
SampleP1 (kbar)P2 (kbar)P3 (kbar)P4 (kbar)T1 (oC)T2 (oC)T3 (oC)T4 (oC)fO2
X14.8155.0343.8865.256754750768747−13.63
X23.5593.6272.834.068732731743725−14.67
X33.4523.5062.743.966732732743725−14.75
X42.5722.5191.9993.133708709716700−15.51
X52.4272.3571.8782.997715716723707−15.64
X63.8513.9533.0754.344739737750732−14.42
X73.5623.6292.8324.07727727738720−14.67
X83.1063.1182.4483.638720720729712−15.05
X94.0074.1283.2064.491729727741722−14.28
X103.2793.3122.5943.803721721731714−14.91
Average3.4633.51832.74883.9766727.7727738.2720.4−14.753
Max4.8155.0343.8865.256754750768747−13.63
Min2.4272.3571.8782.997708709716700−15.64
P1 = −3.92 + 5.03 * Al(total) [47]; P2 = −4.76 + 5.64 * Al(total) [48]; P3 = −3.46 + 4.23 * Al(total) [49]; p4 = −3.01 + 4.76 * Al(total) [50].
Table
Table 7. Results of geobarometry calculations for clinopyroxene.
Table 7. Results of geobarometry calculations for clinopyroxene.
Rock
Type		Sample
No.		[60][61][62][63]
ErrorKbar± 1.75± 1.70± 1.00± 2.80
113.7214.6616.0117.87
214.8215.7322.8619.07
313.6414.4124.5319.49
412.2212.8924.0918.13
DK3511.5612.5824.4816.38
613.2114.1125.2018.25
712.9013.8425.3618.24
813.4414.3525.6618.16
912.4013.2525.1116.96
1013.7614.5425.3818.09
Max14.8215.7325.6619.49
Min11.5612.5816.0116.38
Average13.1714.0623.3618.04
Table
Table 8. Results of the geothermometry calculations for clinopyroxene.
Table 8. Results of the geothermometry calculations for clinopyroxene.
Rock
Type		Sample
No.		[64][65][66][66][67]
Error°C±50±30±30±30±30
11431.001104.001172.00816.00894.00
21425.001068.001171.00854.00901.00
31427.001054.001178.00867.00903.00
41419.001069.001185.00863.00902.00
DK351446.001170.001176.00716.00882.00
61446.001125.001204.00833.00896.00
71446.001136.001197.00809.00892.00
81446.001113.001194.00831.00896.00
91440.001119.001185.00812.00893.00
101427.001083.001196.00865.00903.00
Max1446.001170.001204.00867.00903.00
Min1419.001054.001171.00716.00882.00
Average1434.831105.421186.08820.75895.58
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Kamali, A.A.; Moayyed, M.; Saumur, B.M.; Fadaeian, M. Mineralogy and Mineral Chemistry of Dioritic Dykes, Quartz Diorite Enclaves and Pyroxene of the Sungun Cu-Mo Porphyry Deposit, East Azerbaijan, Iran. Minerals 2022, 12, 1218. https://doi.org/10.3390/min12101218

AMA Style

Kamali AA, Moayyed M, Saumur BM, Fadaeian M. Mineralogy and Mineral Chemistry of Dioritic Dykes, Quartz Diorite Enclaves and Pyroxene of the Sungun Cu-Mo Porphyry Deposit, East Azerbaijan, Iran. Minerals. 2022; 12(10):1218. https://doi.org/10.3390/min12101218

Chicago/Turabian Style

Kamali, Amin Allah, Mohsen Moayyed, Benoit M. Saumur, and Mohammad Fadaeian. 2022. "Mineralogy and Mineral Chemistry of Dioritic Dykes, Quartz Diorite Enclaves and Pyroxene of the Sungun Cu-Mo Porphyry Deposit, East Azerbaijan, Iran" Minerals 12, no. 10: 1218. https://doi.org/10.3390/min12101218

APA Style

Kamali, A. A., Moayyed, M., Saumur, B. M., & Fadaeian, M. (2022). Mineralogy and Mineral Chemistry of Dioritic Dykes, Quartz Diorite Enclaves and Pyroxene of the Sungun Cu-Mo Porphyry Deposit, East Azerbaijan, Iran. Minerals, 12(10), 1218. https://doi.org/10.3390/min12101218

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