# Disseminated Gold–Sulfide Mineralization in Metasomatites of the Khangalas Deposit, Yana–Kolyma Metallogenic Belt (Northeast Russia): Analysis of the Texture, Geochemistry, and S Isotopic Composition of Pyrite and Arsenopyrite

^{1}

^{2}

^{3}

^{*}

## Abstract

**:**

^{+}prevails, isomorphically entering the crystal lattice or its defects. Isotope characteristics of hydrothermal sulfides (δ

^{34}S = −2.0 to −0.6‰) indicate that mantle/magmatic sulfur was involved in the formation of the deposit, though the participation of sulfur from the host rocks of the Verkhoyansk clastic complex cannot be ruled out. The Khangalas deposit has much in common with other gold deposits of the Yana–Kolyma metallogenic belt, and from this point of view, the results obtained will help to better reveal their gold potential and understand their origin.

## 1. Introduction

## 2. Regional Geology and Mineralization

#### 2.1. Regional Tectonic Framework

_{3}–K

_{1}). Also present are mafic (162 ± 4 Ma, whole rock, Rb–Sr [34]), intermediate, and felsic dikes of the Nera–Bohapcha complex (151–145 Ma, U–Pb SHRIMP-II, zircons [23]). According to Parfenov et al. [35] and Parfenov and Kuzmin [33], the emplacement of the Late Jurassic granitoids was related to collision events. More recent data indicate that subduction processes were involved in their formation [36,37]. Tectonic structures, magmatism, and ore deposits of the YKMB were closely related to the Late Jurassic to earliest Early Cretaceous subduction, accretionary events at the eastern active continental margin of the Siberian craton [33]. The Upper Indigirka sector of the YKMB includes, from northeast to southwest, the Inyali–Debin, Olchan–Nera, Adycha–Taryn, and Adycha metallogenic zones. The Olchan–Nera zone hosts the Khangalas orogenic gold deposit.

#### 2.2. Geology of the Khangalas Deposit

#### 2.2.1. Structures and Host Rocks

_{3}) deposits. In the lower part of the section, with a thickness of more than 350 m, these are mainly massive brownish-gray and gray sandstones with thin siltstone interbeds. The upper part is dominated by a more than 450 m thick sequence of dark gray to black siltstones with included pebbles of sedimentary, igneous, and metamorphic rocks. The limbs of the anticline are made of Lower Triassic (T

_{1}) deposits (mainly dark gray shales, mudstones, and siltstones with rare interlayers of light gray sandstones with a thickness of 680–750 m) and Middle Triassic (T

_{2}a) sediments of the Anisian stage (alternating sandstones and siltstones with a thickness of 700–800 m). The Ladinian strata (T

_{2}l) consist of interbedded siltstones and sandstones with a total thickness of 850–950 m. The main ore-controlling tectonic structure is the Khangalas fault with a NW strike. This is represented at the Khangalas deposit by five extensive (up to 1400 m) mineralized ore zones (Severnaya, Promezhutochnaya, Centralnaya, Yuzhnaya, Zimnyaya) with low-sulfidation Au-type mineralization localized in the Dvoinaya anticline crest (Figure 1 and Figure 2A). The ore zones are up to 32 m thick and dip to the SW, S, and SE at 30°–50° to 70°–80° [25]. No evidence of magmatic activity is observed within the Khangalas deposit. Geophysical data suggest the presence of a granitoid pluton at depth [38]. The mineralization formed as a result of progressive fold-and-thrust deformations in the Verkhoyansk–Kolyma fold belt. These were initiated by orogenic processes in late Late Jurassic–early Early Cretaceous [25].

#### 2.2.2. Mineralization

## 3. Materials and Methods

_{2}for Fe and S, FeAsS for As, Fe-Ni-Co alloy for Co, Ni, Au-Ag alloy of fineness for Au and Ag, CuSbS

_{2}for Sb, and PbS for Pb. The detection limits 0.01%. Trace elements in pyrite were studied on 9 grains of pyrite-3 and arsenopyrite-1 using a New Wave Research UP-213 laser ablation system (USA) coupled with an Agilent 7700x quadrupole mass spectrometer (Agilent Technologies, Santa Clara, CA, USA) (analyst D.A. Artemiev, Institute of Mineralogy, Ural Branch of the Russian Academy of Sciences, Miass). The measurements were carried out using a 213 nm Nd:YAG UV laser with fluence set at 1.8–5.5 J/cm

^{2}(1.8–3.0 J/cm

^{2}for pyrite, 3.0–4.5 J/cm

^{2}arsenopyrite) and a rate of flow of He carrier gas at 0.5–0.65 L/min. Mass spectrometer settings were: RF power 1550 W, carrier gas Ar, flow rate 0.85–0.95 L/min, plasma-forming gas (Ar) flow rate 15 L/min, and auxiliary gas (Ar) flow rate 0.9 L/min. Data were acquired by singe spot and line analyses using a laser spot diameter of 25 to 80 µm and a frequency of 5–10 Hz. The analysis time for each sample was 90 s, comprising a 30 s measurement of background (laser off) and a 60 s analysis with laser on. Pre-ablation was performed for 3–4 s before each analysis. Between the analyses, and between analysis and pre-ablation, blowing with gas was done for 60–90 s.

^{232}Th

^{16}O/

^{232}Th) was kept below 0.2%. The

^{238}U/

^{232}Th ratio, when adjusted according to NIST SRM-612, was 1:1. External calibration standards USGS MASS-1 [43] and UQAC FeS-1 were used to analyze every 7–13 spots to account for drifting of the laser and mass spectrometer. Mass contents of elements for NIST SRM-612 and USGS MASS-1 were taken from the GeoReM database. Data processing and calculation were carried out using the Iolite software package [44]. As internal standard (IS) for pyrite, we used

^{57}Fe measured by SEM-EMF. In some cases, normalization to 100% of the total components was performed according to standard techniques [45].

_{2}. The

^{34}S/

^{32}S isotope ratios were measured on a MAT-253 mass spectrometer (Thermo Scientific, Waltham, MA, USA) in continuous He flux mode. The measurements were performed against a standard laboratory gas SО

_{2}calibrated according to international standards IAEA-S-1, IAEA-S-2, IAEA-S-3, and NBS-127. The results of δ

^{34}S measurements are given in reference to the international VCDT standard.

## 4. Results

#### 4.1. Pyrite and Arsenopyrite Types and Textures

#### 4.1.1. Diagenetic Pyrite (Py1)

#### 4.1.2. Metamorphic Pyrite (Py2)

#### 4.1.3. Metasomatic Pyrite (Py3) and Arsenopyrite (Apy1)

#### 4.1.4. Vein Pyrite (Py4) and Arsenopyrite (Apy2)

#### 4.2. Composition of Pyrite and Arsenopyrite

#### 4.2.1. EPMA Results: Major and Minor Elements CAPS

_{Co}> C

_{Ni}, which are characterized by a strong correlation (r = 0.74). Copper constitutes 5–6% of the total amount of trace elements in Py1 and Py2 (0.02–0.11 wt.% Cu), and its content is variable, even within the same crystal. Another constant but quantitatively insignificant minor element in Py1 and Py2 is Sb (0.03–0.1 wt.% Sb). Correlation analysis revealed a Co–Ni–Pb geochemical association in Py1. The empirical formula of sedimentary and metamorphic pyrite is Fe

_{0.96–1.04}Ni

_{0.0–0.01}S

_{2.00}(Ni is present in 18% of the analyzed grains).

_{0.98–1.08}Ni

_{0.0–0.01}Co

_{0.0–0.01}S

_{1.95–2.00}As

_{0.01–0.05}.

_{0.98–1.07}S

_{1.96–1.99}As

_{0.01–0.04}.

_{0.93–1.04}As

_{0.86–1.01}S

_{0.99–1.14}.

#### 4.2.2. Gold and Trace Element Concentrations in Py3 and Apy1 According to LA-IСP-MS Data

#### 4.3. Gold Content of Sulfides from Proximal Metasomatites and in Veins

#### 4.4. Sulfur Isotopic Composition of Sulfides

^{34}S values close to 0 (−2.0 to 0.6‰) (Table 4), for gold-bearing Py3 it is δ

^{34}S = −0.6‰ (21.4 ppm Au, K-9-17), for Apy1 it is δ

^{34}S = −1.2‰ (12.3 ppm Au, K-4-17), and for Apy2 it is δ

^{34}S = −2.0 ‰ (KG-35-19).

## 5. Discussion

#### 5.1. Pyrite and Arsenopyrite Types and Textures

#### 5.2. Composition of Pyrite and Arsenopyrite

^{3−}or [Sb–Sb]

^{4−}dumbbells [62]. The negative correlation (r = 0.3–0.6) between antimony and iron indicates the possibility of isomorphic Fe → Sb substitution.

#### 5.3. Invisible Gold and Its Relationship with Other Elements in Py3 and Apy1 According to LA-ICP-MS Data

#### 5.3.1. Invisible Gold in Py3

^{2+}ionic radius r = 0.80 Å) and gold (atomic mass 196.96; Au

^{3+}ionic radius r = 0.85 Å; Au

^{+}r = 1.37 Å) also confirms the possibility of isomorphic incorporation of Au into pyrite [73,74]. Chouinard et al. [75] proposed a conjugate substitution mechanism of Au

^{3+}+ Cu

^{+}↔ 2Fe

^{2+}or Au

^{+}+ Cu

^{+}+ Co

^{2+}+ Ni

^{2+}↔ 3Fe

^{2+}types (Figure 13B,C). According to Wang et al. [61], the marked negative relationship between (Au + As) and Fe in Py3 (Figure 12D) suggests that Au and As entered the lattice through isomorphic substitution for Fe under conditions of high oxygen fugacity (fO

_{2}).

_{1.00}(S

_{1.98}As

_{0.02})

_{2.00}) to form, in some cases, arsenian pyrite (As > 1.7 %), which is typical for reducing conditions (see [60,77], etc.). Reich et al. [60] noted for epithermal and Carlin-type deposits increased Au solubility in the pyrite structure with increasing As content: C

_{Au}= 0.02 · C

_{As}+ 4 × 10

^{−5}.

^{+}is the dominant form of gold in the arsenian pyrite of the studied deposits. Analytical data [60] indicate that the Au solubility limit in arsenian pyrite of epithermal deposits is defined by an Au/As ratio of ~0.02. The solubility limit of Au in pyrite of orogenic deposits is lower (~0.004) [71].

^{+}). These results are confirmed by the rather low Au content in the analyzed Py3: in most samples, Au does not exceed 2.5 ppm (Table 2). Earlier, Tauson et al. [76] showed that the content of the Au

^{+}structural form in the studied pyrite samples from deposits of different genetic types in Russia (large Natalka and Degdekan orogenic gold-quartz deposits, Dukat volcanogenic-plutonogenic Au–Ag deposit, Dalnee and Oroch volcanic Au–Ag deposits, Sukhoi Log giant deposit with a debated genesis, Pokrovskoye epithermal Au–Ag deposit, Amur Dikes deposit with an unconventional type of mineralization, and Zun–Kholbinskoye deposit with a controversial genesis) and Uzbekistan (Kochbulak and Kyzylalmasay epithermal Au–Ag deposits) does not exceed ~5 ppm. Similar results were obtained by Deditius et al. [71] for pyrite from orogenic gold deposits, which, according to their data, contains less than 100 ppm Au. The higher Au content is mainly due to the presence of nano- and microparticles of native gold [78]. The occurrence of native superficially bound Au

^{0}in sulfides of metasomatites is reported from deposits of various genetic types [60,68,76,79].

#### 5.3.2. Invisible Gold in Apy1

^{+}structurally bound form in Apy1. This is confirmed by the low Au content (<6.1 ppm) in Apy1. At the same time, the results of atomic absorption analysis revealed high Au content in the bulk samples of Apy1 (Table 2), which indicates the presence of nano- and microparticles of native gold.

^{+}in the Py3 and Apy1 crystal lattices.

#### 5.4. Gold Content of Proximal Metasomatites and Their Sulfides

#### 5.5. Sources of Metals

#### 5.5.1. Pyrite Genesis as Evidenced by Co/Ni Ratio

_{Co}> C

_{Ni}(Co/Ni > 1.0). Increased Ni content (Co/Ni = 0.2–0.8) is characteristic of Py1 and Py2, and is recorded in the central part of zoned Py3 crystals. Variable correlations are observed between Co and Ni: a strong positive correlation (r = 0.64–0.73) in Py1 and Py2, a negative correlation (r = −0.6) in grains with elevated Ni content, and no correlation between Co and Ni in vein Py4 and Apy2. High concentrations of Ni in sulfides suggest, according to Lee et al. [58], that mafic and ultramafic components introduced into hydrothermal fluids were involved in the precipitation of sulfides (maximum 2230 ppm for Apy1, 1620 ppm for Apy2, 4830 ppm for Py3). Negative correlations between Co and Fe (r = −0.6) (Figure 15B) and Ni and Fe (r = −0.1, Figure 15C) in Py3 indicate the presence of Ni and Co in the crystal lattice through isomorphic substitution for Fe [61].

#### 5.5.2. Origin of Hydrothermal Sulfides According to Stable Sulfur Isotopes

^{34}S values for sulfide minerals from orogenic gold deposits range from −20‰ to + 25‰ [92]. As sulfur is an important complexing agent for gold, understanding the S source may be critical in identifying the source areas of gold. A number of researchers came to the conclusion that the δ

^{34}S composition in Phanerozoic deposits changes depending on the age of the host rock [92,95,96]. The sulfur isotopic composition of sulfides from the Khangalas deposit is in good agreement with these results (Figure 15B).

^{34}S ~ 0, it was determined that the ore-forming fluid had a felsic magmatic or mantle-level source of sulfur [98]. The sulfur isotopic composition (δ

^{34}S = 0.0 to −3.3‰) in a number of gold–sulfide deposits in Kazakhstan indicates that the ore matter had a mantle-level source of sulfur with some contribution from the crust [99,100].

^{34}S of accessory sulfides of host rocks with the δ

^{34}S of sulfides of gold deposits in the Upper Kolyma gold-bearing region, and suggested the involvement of sulfur mobilized from clastic strata in the hydrothermal process. It is believed that the most probable source of sulfur in sulfides (δ

^{34}S −6.3 to + 2.6) from the Natalka orogenic deposit, the largest in the region, is the host rocks of the Verkhoyansk clastic complex [101,102]. Sulfur and arsenic were mobilized as a result of phase transformations of iron sulfides from clastic strata during the transformation of pyrite to pyrrhotite in the course of metamorphism.

^{34}S values is established: from −2.1‰ to +2.4‰ (Apy), from −6.6 to +5.4‰ (Py), and from −6.1‰ to +4.2‰ (antimonite) (Figure 16) [8]. For example, the δ

^{34}S values in sulfides are close to zero: −0.2‰ to +2.4‰ for Malo-Tarynskoe, −2.9‰ to −1.5‰ for Avgustovskoe, −3.6‰ to 1.3‰ for Kinyas, −1.7‰ to −1.2‰ for Pil, and −4.4‰ to −0.7‰ for Elginskoe and other gold deposits. These data are interpreted by the authors as indicating a magmatic source of sulfur with some contribution from the host rocks of the Verkhoyansk clastic complex.

^{34}S values from −2.0‰ to −0.6‰ (Figure 16, Table 4). Similar sulfur isotopic compositions of arsenopyrite and pyrite of ore veins and disseminated mineralization of ore-hosting strata indicate their formation during a single hydrothermal event. The δ

^{34}S values of sulfides from the Khangalas deposit are close to those of the well-studied orogenic gold-sulfide deposits: Natalka (Upper Kolyma region) [103]; Suzdalskoe, Zhaima, Bolshevik, and Zherek (Kazakhstan) [99,100]; and deposits of the Adycha-Taryn metallogenic zone [8] (Figure 16A). For the large Nezhdaninskoe orogenic gold deposit in the Allakh–Yun metallogenic zone, deep magma chambers (−5‰ to +1‰ for vein ores) and sulfides of host rocks (Figure 16A) are considered as sulfur sources [104]. At the same time, the conclusions about the genesis of the fluid components here are ambiguous, as in the case of the Muruntau deposit [105]. Thus, mantle/magmatic sulfur was involved in the formation of the Khangalas deposit, but the participation of sulfur from the host rocks of the Verkhoyansk clastic complex cannot be ruled out. The small volume of the conducted isotope studies does not make it possible to represent the entire range of δ

^{34}S values for the Khangalas deposit. To obtain more information about the sources of ore matter, a comprehensive analysis of all generations of pyrite and arsenopyrite as well as thermobarometric and microelemental analysis of fluid inclusions are required.

## 6. Conclusions

^{+}. A low Au content in sulfides (Py3, avg. 1.5 ppm; Apy2, avg. 7.6 ppm) is interpreted by some researchers [76] as an indicator of the structurally bound form of Au. In addition, the negative correlation between Au and Fe established for Py3 and Apy1 indicates isomorphic Au ↔ Fe substitution [52,55,58]. The close correlation between Au and As indicates that they have a common genesis. Their distribution patterns relative to the line limiting the transition of the solid solution Au

^{+}to Au

^{0}[57,71] also indicate the development of Au

^{+}in Apy1 and Py3 from proximal metasomatites (Figure 13F,H). At the same time, a higher Au content was found in sulfides and proximal metasomatites (Py3: 39.32 ppm Au by atomic absorption; Apy1: 39.0 ppm by LA-ICP-MS). This may indicate the presence of micro- and nanoinclusions of native gold in sulfides, which is confirmed by the detection, with the use of a scanning electron microscope, of an Au

^{0}microinclusion in the Py3 and Apy1 intergrowth in 1 out of about 200 grains studied. Indirect evidence of the presence of native gold inclusions in sulfides may be the large number of dense phases detected by computed microtomography. Isotope characteristics of hydrothermal sulfides (δ

^{34}S = −2.0‰ to −0.6‰) indicate that mantle/magmatic sulfur was involved in the formation of the deposit, but the participation of sulfur from the host rocks of the Verkhoyansk clastic complex cannot be ruled out.

## Author Contributions

## Funding

## Data Availability Statement

## Acknowledgments

## Conflicts of Interest

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**Figure 1.**(

**A**,

**C**,

**D**) Regional location, (

**B**) geological structure, and (

**E**) cross-section of Khangalas deposit. Inset map: VFTB, Verkhoyansk fold-and-thrust belt; PDT, Polousny–Debin terrane; C-I, Charky–Indigirka fault; C-Y, Chai–Yureya failt; A-T, Adycha–Taryn fault. Mineralized crushed zones: S, Severnaya; P, Promezhutochnaya; C, Centralnaya; Yu, Yuzhnaya; Z, Zimnyaya.

**Figure 2.**(

**A**–

**C**) Mineral composition of vein-type ores, and (

**D**) morphology of native gold of Khangalas deposit. (

**A**) Banded quartz with inclusions of native gold (Au), galena (Gn), sphalerite (Sp), and arsenopyrite (Apy); (

**B**,

**C**) intergrowths of native gold (Au), galena (Gn), sphalerite (Sp), and chalcopyrite (Cсp) of the Au–polysulfide vein association and anhedral arsenopyrite (Apy) of quartz–pyrite–arsenopyrite vein association: (

**B**) in reflected light, (

**C**) in backscattered electrons. Hereafter, abbreviations for minerals are from [39].

**Figure 3.**Ore bodies of the Khangalas deposit: (

**A**) Yuzhnaya oxidized mineralized fault zone; (

**B**) quartz–carbonate vein. Photographs taken in underground mine workings: (

**C**) vein-type Au–quartz mineralization with native gold, Centralnaya zone, alt. 920 m a.s.l.; (

**D**) disseminated type of mineralization with invisible gold in quartz–sericite–carbonate metasomatites, Centralnaya zone, alt. 920 m a.s.l.; (

**E**) pyrite and quartz veinlets in sandstones, Centralnaya zone, alt. 920 m a.s.l.; (

**F**) oxidized pyrite in sandstones, alt. 945 m a.s.l.

**Figure 5.**(

**A**) Photo and (

**B**) photomicrographs of Py1 and Py2 of Khangalas deposit in reflected light

**,**and (

**C,D**) backscattered electrons: (

**A**) Py2 veinlets and Py1 bedding-plane dissemination in siltstone; (

**B**,

**C**) diagenetic Py1 and metamorphic Py2; (

**D**) metamorphic Py2.

**Figure 6.**(

**A**,

**B**) Photos and (

**C,D**) photomicrographs of Py3 and Apy1 of Khangalas deposit in reflected light and (

**E**–

**H**) backscattered electrons: (

**A**) disseminations of metasomatic Py3 in sandstone; (

**B**) vein-disseminated quartz-Py3-Apy1 mineralization; (

**C**) Py3 veinlets and bedded-plane Py1 dissemination in siltstone; (

**D**) euhedral Apy1; (

**E**) Apy1 aggregate; (

**F**) intergrowths of Py1, Py3, and Apy1 with galena inclusions (Gn); (

**G**) inclusions of native gold (Au) and galena (Gn) in Py3 and Apy1. (

**H**) inclusions of sulfides of gold–polysulfide association (Gn, galena; Ccp, chalcopyrite; Sp, sphalerite) in Py3. Insets: (

**A**, inset a) cubic Py3; (

**A**, inset b) pyritohedra Py3; (

**D**, inset) short prismatic Apy1; (

**E**, inset) pseudo-pyramidal Apy1.

**Figure 7.**Three-dimensional visualization of Py3 and Apy1 of Khangalas deposit. (

**A**) Apy1 grains with inclusions of dense minerals (galena, gold); (

**B**) Apy1 without inclusions of x-ray contrasting phases; (

**C**,

**D**) Py3 aggregate with included dense minerals (galena, gold).

**Figure 8.**(

**A**–

**C**) Photographs and (

**D**) photomicrograph of Py4 and Apy2 of Khangalas deposit (in backscattered electrons): (

**A**) nest-like clusters and individual idiomorphic Apy2 crystals in quartz; (

**B**) idiomorphic Py4 grains in quartz; (

**C**) gold–polysulfide association with Py4, Apy2 in banded quartz; (

**D**) Py4-Apy2 intergrowths with scattered galena (Gn) in quartz.

**Figure 9.**Trace element contents by EPMA: (

**A**) Py1; (

**B**) Py2; (

**C**) Py3; (

**D**) Py4; (

**E**) Apy1; (

**F**) Apy2. Box boundaries are first and third quartiles, and line in middle of box is median. Lower border of line shows minimum value, upper shows maximum value, cross shows average value.

**Figure 11.**Variations in total content of Co, Ni, Sb, Cu, and Pb (wt.%) in sulfides of different generations, Khangalas deposit. Box boundaries are first and third quartiles, and line in middle of box is median. Lower border of line shows minimum value, upper shows maximum value, cross shows average value.

**Figure 12.**Binary correlation diagrams for Ру3: (

**A**) Fe vs. Au; (

**B**) Fe vs. Au + Cu; (

**C**) Fe vs. Au + Cu + Co + Ni; (

**D**) Fe vs. Au + As; (

**E**) As vs. Au; (

**F**) Ag vs. Au, field of orogenic gold deposits (OGDs) and sedimentary Py after Large and Maslennikov [68]; (

**G**) As vs. Te; (

**H**) S vs. Te + As.

**Figure 14.**Correlation diagrams for Apy1: (

**A**) Au vs. Ag; (

**B**) Au vs. Pb; (

**C**) Au vs. Cu; (

**D**) Au vs. Ni; (

**E**) Au vs. Co; (

**F**) Au vs. Bi; (

**G**) Au vs. Sb; (

**H**) Au vs. Te; (

**I**) Ag vs. Pb. Distribution of some elements (

**K**) inside Apy1 grain (sample K-14-17) (

**J**).

**Figure 16.**(

**A**) S isotope composition of sulfides of Khangalas deposit [106,107,108]. Range of values of sulfur sources after Ohmoto [109] and Kryazhev [94]. (

**B**) Variation in δ

^{34}S values of sulfides in global sediment-hosted orogenic gold deposits after Goldfarb et al. [96]. Heavy line and blue error envelope indicate seawater sulfate evolution curve from Claypool et al. [110].

**Table 1.**Chemical composition of pyrites and arsenopyrites determined by EPMA (all values in wt.%.; nd, not detected).

No | Sample | Fe | S | As | Co | Ni | Cu | Sb | Pb |
---|---|---|---|---|---|---|---|---|---|

Diagenetic Py1 | |||||||||

1 | K-40-14; n = 11 | $\frac{47.48-45.99}{46.79}$ * | $\frac{55.82-51.78}{54.37}$ | $\frac{0.31-0.03}{0.15}$ | $\frac{0.13-0.05}{0.09}$ | $\frac{0.17-0.02}{0.06}$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.05-0.01}{0.03}$ | nd |

2 | K-55-14; n = 10 | $\frac{46.63-46.93}{46.45}$ | $\frac{53.89-52.77}{53.27}$ | $\frac{0.31-0.06}{0.22}$ | $\frac{0.18-0.06}{0.08}$ | $\frac{0.19-0.01}{0.07}$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.05-0.07}{0.03}$ | nd |

3 | K-61-14; n = 5 | $\frac{46.99-45.78}{46.66}$ | $\frac{54.44-52.93}{53.84}$ | $\frac{0.30-0.08}{0.18}$ | $\frac{0.11-0.05}{0.07}$ | $\frac{0.05-0.01}{0.02}$ | $\frac{0.02-0.01}{0.02}$ | $\frac{0.06-0.03}{0.04}$ | nd |

4 | K-23-14; n = 5 | $\frac{45.69-44.54}{45.04}$ | $\frac{52.41-51.17}{52.00}$ | $\frac{0.23-0.01}{0.07}$ | $\frac{0.07-0.05}{0.06}$ | $\frac{0.33-0.13}{0.03}$ | $\frac{0.03-0.01}{0.02}$ | $\frac{0.06-0.03}{0.05}$ | $\frac{0.10-0.05}{0.08}$ |

5 | Kpr2-4-14; n = 4 | $\frac{46.61-46.30}{46.44}$ | $\frac{51.76-50.96}{51.45}$ | $\frac{0.12-0.01}{0.06}$ | $\frac{0.05-0.03}{0.04}$ | 0.01 | nd | $\frac{0.04-0.02}{0.03}$ | $\frac{0.05-0.02}{0.04}$ |

6 | K-4-14; n = 6 | $\frac{46.51-45.73}{46.17}$ | $\frac{54.62-52.13}{53.18}$ | $\frac{0.23-0.09}{0.16}$ | $\frac{0.19-0.07}{0.10}$ | $\frac{0.03-0.01}{0.02}$ | 0.03 | $\frac{0.07-0.01}{0.03}$ | nd |

7 | K-7-17; n = 19 | $\frac{47.40-45.06}{46.04}$ | $\frac{53.89-51.41}{52.74}$ | $\frac{0.28-0.02}{0.17}$ | $\frac{0.20-0.02}{0.11}$ | $\frac{0.14-0.01}{0.07}$ | $\frac{0.04-0.01}{0.01}$ | $\frac{0.11-0.01}{0.05}$ | nd |

8 | KG-32-19, n = 1 | 46.80 | 53.66 | 0.18 | nd | 0.02 | nd | 0.06 | nd |

9 | KG-7-19, n = 1 | 46.50 | 52.31 | 0.01 | nd | 0.01 | nd | 0.05 | nd |

Metamorphic Py2 | |||||||||

10 | K-40-14; n = 4 | $\frac{46.97-45.91}{46.65}$ | $\frac{54.89-50.60}{53.73}$ | $\frac{0.15-0.09}{0.13}$ | $\frac{0.15-0.08}{0.10}$ | $\frac{0.06-0.03}{0.05}$ | $\frac{0.04-0.02}{0.03}$ | $\frac{0.03-0.01}{0.02}$ | nd |

11 | K-55-14; n = 3 | $\frac{46.74-45.53}{46.60}$ | $\frac{52.97-52.67}{52.67}$ | $\frac{0.27-0.20}{0.24}$ | $\frac{0.09-0.07}{0.09}$ | $\frac{0.32-0.01}{0.13}$ | $\frac{0.03-0.01}{0.02}$ | $\frac{0.05-0.03}{0.04}$ | nd |

12 | K-4-14; n = 4 | $\frac{46.70-46.13}{46.50}$ | $\frac{52.88-51.71}{52.14}$ | $\frac{0.25-0.03}{0.16}$ | $\frac{0.07-0.05}{0.06}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.03-0.01}{0.02}$ | $\frac{0.03-0.02}{0.03}$ | nd |

13 | K-23-14; n = 7 | $\frac{45.93-45.31}{45.67}$ | $\frac{53.14-51.35}{51.88}$ | $\frac{0.23-0.02}{0.08}$ | $\frac{0.10-0.06}{0.08}$ | $\frac{0.23-0.04}{0.15}$ | $\frac{0.12-0.01}{0.04}$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.13-0.03}{0.08}$ |

14 | KG-29-19; n = 4 | $\frac{46.98-46.48}{46.74}$ | $\frac{53.95-52.66}{53.32}$ | $\frac{0.14-0.01}{0.06}$ | $\frac{0.05-0.03}{0.04}$ | $0.01$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.03-0.01}{0.02}$ | $\frac{0.11-0.02}{0.07}$ |

Hydrothermal-metasomatic Py3 | |||||||||

15 | K-32-14; n = 16 | $\frac{46.17-45.14}{45.50}$ | $\frac{51.95-50.37}{50.94}$ | $\frac{2.14-1.01}{1.57}$ | $\frac{0.08-0.04}{0.05}$ | $\frac{0.07-0.01}{0.02}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.05-0.01}{0.02}$ | nd |

16 | K-51-14; n = 27 | $\frac{46.91-44.91}{46.00}$ | $\frac{53.59-50.25}{51.84}$ | $\frac{2.22-0.56}{1.31}$ | $\frac{0.17-0.05}{0.09}$ | $\frac{0.25-0.01}{0.04}$ | $\frac{0.05-0.01}{0.03}$ | $\frac{0.04-0.01}{0.02}$ | nd |

17 | K-52-14; n = 24 | $\frac{47.01-45.98}{46.59}$ | $\frac{55.10-50.93}{53.71}$ | $\frac{2.49-0.97}{1.58}$ | $\frac{0.11-0.03}{0.05}$ | $\frac{0.14-0.01}{0.03}$ | $\frac{0.03-0.01}{0.01}$ | $\frac{0.04-0.01}{0.02}$ | nd |

18 | K-55-14; n = 6 | $\frac{46.59-46.02}{46.36}$ | $\frac{53.32-51.30}{52.24}$ | $\frac{1.03-0.31}{0.67}$ | $\frac{0.21-0.07}{0.12}$ | $\frac{0.10-0.01}{0.06}$ | $\frac{0.04-0.01}{0.03}$ | $\frac{0.06-0.02}{0.04}$ | nd |

19 | K-61-14; n = 17 | $\frac{47.15-45.24}{46.45}$ | $\frac{55.48-50.89}{52.63}$ | $\frac{1.86-0.34}{0.98}$ | $\frac{0.08-0.05}{0.06}$ | $\frac{0.07-0.01}{0.02}$ | $\frac{0.12-0.01}{0.03}$ | $\frac{0.12-0.02}{0.05}$ | nd |

20 | K-9-17/1; n = 18 | $\frac{46.63-44.87}{45.98}$ | $\frac{54.16-51.04}{52.81}$ | $\frac{1.71-0.31}{0.95}$ | $\frac{0.12-0.06}{0.08}$ | $\frac{0.11-0.01}{0.03}$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.10-0.01}{0.03}$ | nd |

21 | K-4-17; n = 13 | $\frac{46.53-45.58}{46.15}$ | $\frac{52.60-50.76}{51.98}$ | $\frac{1.28-0.40}{0.77}$ | $\frac{0.13-0.04}{0.06}$ | $\frac{0.38-0.01}{0.16}$ | $\frac{0.03-0.01}{0.02}$ | $\frac{0.08-0.01}{0.02}$ | nd |

22 | K-14-17; n = 19 | $\frac{46.85-45.36}{46.22}$ | $\frac{54.28-52.82}{53.63}$ | $\frac{1.59-0.38}{0.81}$ | $\frac{0.50-0.05}{0.11}$ | $\frac{0.48-0.01}{0.16}$ | $\frac{0.03-0.01}{0.01}$ | $\frac{0.04-0.01}{0.02}$ | $0.01$ |

23 | K-35-17; n = 24 | $\frac{46.98-45.59}{46.43}$ | $\frac{53.39-50.31}{51.56}$ | $\frac{1.81-0.45}{1.03}$ | $\frac{0.13-0.04}{0.06}$ | $\frac{0.24-0.01}{0.06}$ | $\frac{0.06-0.01}{0.02}$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.13-0.01}{0.07}$ |

24 | KG-12-19; n = 25 | $\frac{47.39-45.33}{46.60}$ | $\frac{55.27-52.25}{53.93}$ | $\frac{1.45-0.32}{0.82}$ | $\frac{0.10-0.03}{0.05}$ | $\frac{0.09-0.01}{0.02}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.08-0.01}{0.04}$ | $\frac{0.12-0.01}{0.06}$ |

25 | KG-13-19; n = 39 | $\frac{46.95-45.50}{46.35}$ | $\frac{54.02-51.59}{53.04}$ | $\frac{2.23-0.33}{0.93}$ | $\frac{0.54-0.04}{0.08}$ | $\frac{0.15-0.01}{0.03}$ | $\frac{0.05-0.01}{0.02}$ | $\frac{0.05-0.01}{0.02}$ | $\frac{0.06-0.01}{0.02}$ |

26 | KG-9-19; n = 5 | $\frac{46.95-45.97}{46.43}$ | $\frac{54.02-52.58}{53.47}$ | $\frac{1.27-0.42}{0.78}$ | $\frac{0.10-0.04}{0.06}$ | $\frac{0.15-0.01}{0.05}$ | $\frac{0.05-0.01}{0.02}$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.03-0.01}{0.01}$ |

27 | KG-18-19; n = 26 | $\frac{46.86-45.82}{46.48}$ | $\frac{53.61-50.76}{52.89}$ | $\frac{2.29-0.56}{1.27}$ | $\frac{0.13-0.04}{0.07}$ | $\frac{0.27-0.01}{0.04}$ | $\frac{0.04-0.01}{0.01}$ | $\frac{0.08-0.01}{0.02}$ | $\frac{0.05-0.01}{0.02}$ |

28 | KG-24-19; n = 21 | $\frac{46.32-46.76}{45.99}$ | $\frac{54.78-52.66}{53.97}$ | $\frac{2.40-0.36}{1.28}$ | $\frac{0.08-0.04}{0.06}$ | $\frac{0.04-0.01}{0.02}$ | $\frac{0.03-0.01}{0.01}$ | $\frac{0.04-0.01}{0.02}$ | $\frac{0.07-0.01}{0.03}$ |

29 | KG-29-19; n = 20 | $\frac{47.17-45.78}{46.51}$ | $\frac{53.62-58.88}{52.51}$ | $\frac{1.88-0.42}{1.08}$ | $\frac{0.62-0.03}{0.08}$ | $\frac{0.23-0.01}{0.04}$ | $\frac{0.06-0.01}{0.02}$ | $\frac{0.05-0.01}{0.02}$ | $\frac{0.13-0.01}{0.05}$ |

30 | KG-30-19/1; n = 21 | $\frac{47.18-45.86}{45.81}$ | $\frac{53.93-51.92}{53.00}$ | $\frac{1.05-0.32}{0.58}$ | $\frac{0.08-0.02}{0.05}$ | $\frac{0.33-0.01}{0.10}$ | $\frac{0.04-0.01}{0.02}$ | $\frac{0.04-0.01}{0.02}$ | $\frac{0.14-0.01}{0.05}$ |

31 | Kpr-4-14; n = 9 | $\frac{46.84-44.87}{46.52}$ | $\frac{51.87-48.88}{51.38}$ | $\frac{0.97-0.31}{0.75}$ | $\frac{0.08-0.02}{0.05}$ | $\frac{0.04-0.01}{0.02}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.07-0.01}{0.03}$ | $0.03$ |

32 | KG-30-19/2; n = 9 | $\frac{46.29-45.86}{45.86}$ | $\frac{53.64-52.10}{53.06}$ | $\frac{0.81-0.32}{0.53}$ | $\frac{0.08-0.03}{0.05}$ | $\frac{0.33-0.01}{0.12}$ | $\frac{0.04-0.01}{0.01}$ | $\frac{0.04-0.01}{0.02}$ | nd |

33 | K-7-17; n = 10 | $\frac{46.99-45.44}{46.08}$ | $\frac{53.88-49.99}{52.44}$ | $\frac{1.96-0.98}{1.37}$ | $0.02$ | $\frac{0.04-0.01}{0.01}$ | $\frac{0.02-0.01}{0.01}$ | $0.01$ | nd |

34 | K-5-14/1; n = 27 | $\frac{50.61-44.99}{45.89}$ | $\frac{55.31-52.48}{52.48}$ | $\frac{1.52-0.45}{1.09}$ | $\frac{0.17-0.04}{0.09}$ | $\frac{0.15-0.01}{0.08}$ | $\frac{0.02-0.01}{0.01}$ | $0.03$ | nd |

Hydrothermal vein Py4 | |||||||||

35 | KG-1-19; n = 14 | $\frac{47.56-46.30}{46.88}$ | $\frac{54.41-52.86}{53.65}$ | $\frac{1.14-0.35}{0.85}$ | $\frac{0.08-0.05}{0.06}$ | $\frac{0.04-0.01}{0.02}$ | $\frac{0.05-0.01}{0.02}$ | $\frac{0.05-0.01}{0.03}$ | nd |

36 | K-45-14; n = 9 | $\frac{46.71-41.62}{45.42}$ | $\frac{52.63-43.86}{49.70}$ | $\frac{2.50-0.45}{1.21}$ | $\frac{0.06-0.03}{0.04}$ | $\frac{0.05-0.01}{0.02}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.07-0.01}{0.03}$ | nd |

Hydrothermal-metasomatic Apy1 | |||||||||

37 | K-32-14; n = 10 | $\frac{33.60-32.12}{33.00}$ | $\frac{20.78-18.88}{19.98}$ | $\frac{44.83-40.40}{42.36}$ | $\frac{0.05-0.03}{0.04}$ | $\frac{0.10-0.01}{0.03}$ | $\frac{0.03-0.01}{0.01}$ | $\frac{0.10-0.02}{0.05}$ | nd |

38 | K-51-14; n = 4 | $\frac{33.85-33.16}{33.60}$ | $\frac{21.46-20.34}{20.72}$ | $\frac{48.45-46.61}{47.57}$ | $\frac{0.11-0.07}{0.09}$ | $\frac{0.05-0.01}{0.03}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.03-0.01}{0.01}$ | nd |

39 | K-52-14; n = 5 | $\frac{35.24-34.36}{34.69}$ | $\frac{23.70-21.77}{22.37}$ | $\frac{44.21-41.93}{43.52}$ | $\frac{0.04-0.02}{0.03}$ | $\frac{0.05-0.01}{0.03}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.13-0.05}{0.09}$ | nd |

40 | K-4-17; n = 5 | $\frac{33.96-33.16}{33.56}$ | $\frac{20.83-19.93}{21.30}$ | $\frac{44.51-43.22}{43.80}$ | $\frac{0.15-0.03}{0.08}$ | $\frac{0.69-0.04}{0.27}$ | $\frac{0.06-0.01}{0.03}$ | $\frac{0.09-0.03}{0.07}$ | nd |

41 | KG-9-19; n = 5 | $\frac{34.29-33.53}{34.02}$ | $\frac{21.90-20.64}{21.30}$ | $\frac{45.06-43.05}{43.81}$ | $\frac{0.07-0.04}{0.06}$ | $\frac{0.02-0.01}{0.02}$ | 0.01 | $\frac{0.05-0.03}{0.04}$ | nd |

42 | KG-30-19/1; n = 5 | $\frac{34.51-33.96}{34.10}$ | $\frac{22.25-20.55}{21.33}$ | $\frac{44.16-42.02}{43.21}$ | $\frac{0.08-0.04}{0.05}$ | $\frac{0.12-0.05}{0.08}$ | nd | $\frac{0.15-0.02}{0.08}$ | nd |

43 | K-7-17; n = 15 | $\frac{36.96-33.77}{34.58}$ | $\frac{35.80-20.96}{23.12}$ | $\frac{43.92-4.99}{42.23}$ | $\frac{0.10-0.03}{0.06}$ | $\frac{0.22-0.01}{0.03}$ | nd | $\frac{0.16-0.01}{0.06}$ | nd |

Hydrothermal vein Apy2 | |||||||||

44 | KG-11-19; n = 43 | $\frac{35.66-31.59}{33.02}$ | $\frac{22.62-19.03}{20.50}$ | $\frac{49.97-41.76}{47.52}$ | $\frac{0.07-0.02}{0.03}$ | $\frac{0.16-0.01}{0.04}$ | $0.002$ | $\frac{0.22-0.01}{0.06}$ | nd |

45 | K-21-14; n = 24 | $\frac{35.57-33.24}{34.58}$ | $\frac{23.09-19.18}{21.70}$ | $\frac{47.53-41.11}{43.46}$ | $\frac{0.07-0.03}{0.05}$ | $\frac{0.04-0.01}{0.01}$ | $\frac{0.02-0.01}{0.01}$ | $\frac{0.16-0.03}{0.08}$ | nd |

**Table 2.**Data of LA-ICP-MS trace element analysis of Py3 and Apy1 of Khangalas gold deposit (all values in ppm; bdl, below detection limit; nd, not detected).

Sample | Spot Position | As | Ti | V | Cr | Mn | Co | Ni | Cu | Zn | Ga | Ge | Se | Mo | Ag | Cd | In | Sn | Sb | Te | W | Tl | Pb | Bi | Au | Pd | Ba | Pt | Hg | Au/Ag |
---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|

K-4-17 | Asp10-6 | - | 218 | 1.23 | 6.3 | 1.04 | 521 | 565 | 15.9 | 15 | 0.036 | 1.99 | 323 | 1.53 | 0.9 | nd | 0.048 | 0.09 | 890 | 5.9 | 2.44 | 0.045 | 9.7 | 0.71 | 3.31 | 0.025 | 2.25 | 0.051 | 1.26 | 3.68 |

K-4-17 | Asp11-11 | - | 2060 | 5.07 | 3.4 | 1.45 | 57.5 | 93 | 7 | 4.2 | 0.035 | 2.36 | 104 | 0.56 | 0.55 | 0.57 | 0.122 | 0.68 | 385 | 0.5 | 0.83 | 0.01 | 7.41 | 0.417 | 2 | 0.012 | 2.49 | 0.033 | 0.41 | 3.64 |

K-4-17 | Asp12-14 | - | 37.5 | 0.204 | 2.6 | 1.16 | 524 | 534 | 14 | 3.7 | 0.055 | 1.8 | 268 | 21.6 | 0.6 | 0.16 | 0.119 | 0.18 | 721 | 1.97 | 0.129 | 0.11 | 13.5 | 0.99 | 0.574 | 0.003 | 0.29 | 0.006 | 0.3 | 0.96 |

K-4-17 | Asp13-15 | - | 0.8 | 0.077 | 3.3 | 1.09 | 3.24 | 6.3 | 4.6 | 5.7 | 0.019 | 1.86 | 156 | 7.16 | 0.186 | 0.07 | 0.076 | 0.22 | 416 | 0.35 | 0.016 | 0.026 | 1.95 | 0.466 | 0.255 | bdl | 0.28 | bdl | 0.42 | 1.37 |

K-4-17 | Asp14-15 | - | 8 | 0.132 | 2.3 | 0.3 | 7.2 | 50 | 7.9 | 3.3 | 0.085 | 1.95 | 66.9 | 7.72 | 0.47 | nd | 0.119 | bdl | 883 | 6.2 | 0.22 | 0.03 | 38.9 | 0.402 | 0.352 | 0.002 | 0.33 | 0.028 | 0.82 | 0.75 |

K-4-17 | Asp15-25 | - | 0.97 | 0.194 | 2.9 | 1.71 | 4.22 | 13.6 | 19 | 10 | 0.013 | 2.01 | 187 | 1.38 | 0.41 | 0.043 | 0.133 | 0.13 | 778 | bdl | bdl | 0.012 | 5.49 | 0.89 | 6.13 | 0.001 | 0.08 | 0.057 | 0.98 | 14.95 |

K-4-17 | Asp16-26 | - | 1.06 | 0.069 | 0.59 | 1.35 | 1070 | 1680 | 7.8 | 3.6 | 0.021 | 2.17 | 329 | 9.9 | 0.55 | 0.036 | 0.114 | 0.07 | 1414 | 8 | 0.19 | 0.043 | 7.83 | 1.42 | 0.7 | 0.017 | 0.34 | 0.01 | 1.95 | 1.27 |

K-4-17 | Asp17-33 | - | 21.7 | 0.29 | 2.7 | 1.29 | 35.7 | 76 | 9.8 | 2.55 | 0.059 | 2.01 | 107 | 20 | 0.5 | nd | 0.097 | bdl | 926 | 0.01 | 0.082 | 0.019 | 7.12 | 0.77 | 0.88 | bdl | 0.11 | 0.018 | 0.63 | 1.76 |

K-4-17 | LineA1-1 | - | 295 | 0.62 | 1.15 | nd | 65 | 122.1 | 8 | 2 | 0.014 | 3.82 | 126.2 | 9.22 | 0.57 | nd | 0.062 | 0.126 | 550 | 0.74 | 1.68 | 0.0239 | 9.18 | 0.641 | 0.488 | bdl | 3.1 | bdl | 0.51 | 0.86 |

K-4-17 | LineA1-2 | - | 242 | 0.42 | 0.71 | nd | 3.7 | 8.9 | 3.44 | 0.69 | bdl | 4.19 | 98 | 3.05 | 0.35 | 0.1 | 0.06 | 0.3 | 378 | bdl | 1.17 | 0.0038 | 5.43 | 0.56 | 0.44 | bdl | 2.2 | bdl | 1.03 | 1.26 |

K-4-17 | LineA1-3 | - | 32 | 0.111 | 0.27 | nd | 728 | 1182 | 4.57 | 1.63 | 0.0079 | 3.88 | 145.7 | 6.03 | 0.388 | nd | 0.059 | 0.1 | 429 | 0.7 | 0.27 | 0.0049 | 5.79 | 0.636 | 0.715 | bdl | 0.29 | 0.004 | 0.64 | 1.84 |

K-4-17 | LineA2 | - | 3.1 | 0.089 | 89 | nd | 56.5 | 184 | 6.5 | 4.3 | 0.058 | 4.06 | 48.9 | 0.156 | 0.341 | nd | 0.035 | 0.12 | 193.8 | 2.34 | 0.035 | 0.044 | 36.3 | 0.113 | 2.7 | bdl | 4.2 | 0.012 | 0.43 | 7.92 |

K-4-17 | LineA2 | - | 2.93 | 0.025 | 5.6 | nd | 10.32 | 26.1 | 2.46 | 2.47 | 0.0086 | 3.8 | 93.1 | 2.34 | 0.698 | nd | 0.062 | 0.091 | 208.8 | 0.24 | 0.026 | 0.0176 | 76 | 0.226 | 3.16 | bdl | 2.61 | 0.02 | 0.95 | 4.53 |

K-4-17 | LineA2 | - | 399 | 0.945 | 1.89 | nd | 401 | 874 | 2.27 | 2.3 | 0.051 | 3.89 | 118.5 | 1.5 | 0.54 | nd | 0.0534 | 0.262 | 328.3 | 0.28 | 0.93 | 0.0297 | 11.4 | 0.454 | 0.715 | bdl | 2.82 | 0.033 | 0.72 | 1.32 |

K-4-17 | LineA2 | - | 72 | 0.201 | 2.2 | nd | 109.7 | 250.8 | 2.05 | 1.69 | 0.022 | 4.09 | 71.2 | 8.68 | 0.448 | nd | 0.052 | 0.184 | 495 | bdl | 0.13 | 0.0178 | 6.16 | 0.712 | 0.833 | 0.016 | 0.54 | 0.008 | 0.46 | 1.86 |

K-4-17 | LineA2 | - | 99 | 0.334 | 1.98 | nd | 140 | 276 | 2.07 | 2.28 | 0.0314 | 3.76 | 118.5 | 11.85 | 0.376 | 0.0031 | 0.0544 | 0.182 | 512.6 | 0.255 | 0.451 | 0.0087 | 7.46 | 0.659 | 0.319 | bdl | 1.08 | 0.011 | 0.57 | 0.85 |

K-4-17 | LineA2 | - | 278 | 0.61 | 3.1 | nd | 14.84 | 37.5 | 6.3 | 2.29 | 0.0114 | 3.67 | 130.3 | 11.07 | 0.732 | nd | 0.051 | 0.218 | 550.6 | 0.35 | 0.76 | 0.0067 | 60.2 | 0.759 | 0.562 | 0.024 | 1.16 | 0.010 | 0.61 | 0.77 |

K-4-17 | LineA2 | - | 7790 | 15 | 14.8 | nd | 32.6 | 50 | 7.91 | 2.08 | 0.16 | 3.92 | 112.9 | 11.18 | 1.49 | nd | 0.037 | 0.8 | 534.3 | 0.21 | 22.6 | 0.0071 | 27.4 | 0.693 | 2.43 | 0.011 | 30.5 | 0.017 | 0.25 | 1.63 |

Minimum | 0.8 | 0.0 | 0.3 | 0.3 | 3.2 | 6.3 | 2.1 | 0.7 | 0.0079 | 1.8 | 48.9 | 0.2 | 0.2 | 0.0 | 0.04 | 0.07 | 193.8 | 0.01 | 0.02 | 0.004 | 2.0 | 0.1 | 0.3 | 0.001 | 0.08 | 0.004 | 0.25 | 0.75 | ||

Maximum | 7790.0 | 15.0 | 89.0 | 1.7 | 1070.0 | 1680.0 | 19.0 | 15.0 | 0.16 | 4.2 | 329.0 | 21.6 | 1.5 | 0.6 | 0.13 | 0.80 | 1414.0 | 8.00 | 22.60 | 0.110 | 76.0 | 1.4 | 6.1 | 0.025 | 30.5 | 0.057 | 1.95 | 14.95 | ||

Average | 642.3 | 1.4 | 8.0 | 1.2 | 210.3 | 335.0 | 7.3 | 3.9 | 0.040 | 3.1 | 144.7 | 7.5 | 0.6 | 0.1 | 0.08 | 0.23 | 588.5 | 1.87 | 1.88 | 0.026 | 18.7 | 0.6 | 1.5 | 0.012 | 3.04 | 0.021 | 0.72 | 2.84 | ||

Std dev | 1846.3 | 3.6 | 20.5 | 0.4 | 309.8 | 471.4 | 4.8 | 3.5 | 0.038 | 1.0 | 82.0 | 6.3 | 0.3 | 0.2 | 0.0 | 0.2 | 302.5 | 2.5 | 5.2 | 0.025 | 21.0 | 0.3 | 1.6 | 0.009 | 6.97 | 0.017 | 0.41 | 3.52 | ||

CV | 287% | 252% | 254% | 35% | 147% | 141% | 66% | 89% | 94% | 32% | 57% | 84% | 51% | 140% | 43% | 89% | 51% | 133% | 279% | 98% | 112% | 46% | 105% | 74% | 229% | 79% | 57% | |||

K-4-17 | Py1-1 | 4890 | 2470 | 7.16 | 10.3 | 0.85 | 1.13 | 14.4 | 3.96 | 3.51 | 0.197 | 2.49 | 4.4 | 0.079 | 0.92 | nd | 0.005 | 0.23 | 10.19 | 0.056 | 9.71 | 0.0076 | 66 | 0.243 | 0.955 | 0.008 | 3.88 | 0.062 | bdl | 1.04 |

K-4-17 | Py2-3 | 7110 | 0.7 | 0.028 | 0.38 | 0.57 | 0.233 | 8.2 | 0.54 | 3.62 | 0.055 | 2.67 | 6.2 | 0.21 | 0.0076 | nd | 0.0021 | 0.11 | 0.25 | 0.21 | 0.067 | 0.018 | 0.479 | 0.048 | 0.502 | bdl | 0.008 | 0.0073 | 0.02 | 66.05 |

K-4-17 | Py3-4 | 4390 | 8.6 | 0.116 | 0.39 | 0.82 | 17.5 | 13.4 | 1.58 | 3.8 | 0.056 | 2.59 | 2.6 | 0.64 | 0.196 | nd | 0.021 | 0.059 | 2 | 0.13 | 0.055 | 0.0074 | 3.71 | 0.084 | 0.236 | 0.01 | 0.16 | 0.034 | 0.01 | 1.20 |

K-9-17 | Py4-7 | 4220 | 0.78 | 0.058 | 0.52 | 0.41 | 1.15 | 74.9 | 3 | 4.2 | 0.018 | 2.46 | 7.2 | 0.059 | 0.85 | 0.024 | 0.0033 | 0.033 | 407 | 0.083 | 0.019 | 0.065 | 860 | 0.93 | 0.507 | 0.0036 | 0.008 | 0.029 | 0.2 | 0.60 |

K-9-17 | Py5-8 | 17480 | 36.1 | 0.35 | 0.98 | 0.4 | 7.05 | 39 | 19 | 4.7 | 0.19 | 2.71 | 3.5 | 0.047 | 0.055 | 0.036 | 0.017 | 0.07 | 6.19 | bdl | 0.08 | 0.047 | 3.35 | 0.09 | 8.83 | 0.01 | 1.83 | 0.037 | 0.33 | 160.55 |

K-9-17 | Py6-10 | 17260 | 2390 | 8.42 | 7.9 | 1.53 | 21.3 | 56.9 | 18 | 5.3 | 0.191 | 2.66 | 4.5 | 0.71 | 0.8 | 0.065 | 0.0105 | 0.31 | 40.1 | 0.06 | 8.66 | 0.089 | 26.7 | 0.446 | 15.85 | 0.013 | 4.68 | 0.064 | 0.36 | 19.81 |

K-14-17 | Py7-11 | 10280 | 77 | 0.235 | 0.58 | 7.55 | 505 | 690 | 7.3 | 6.4 | 0.009 | 2.69 | 52.1 | 1.04 | 1.01 | 0.027 | 0.0012 | 0.07 | 8.42 | 0.31 | 0.112 | 0.03 | 23.3 | 0.457 | 2.5 | 0.0027 | 0.151 | 0.044 | 0.33 | 2.48 |

K-14-17 | Py8-13 | 6820 | 79 | 0.105 | 1.09 | 0.74 | 41.6 | 1298 | 1.4 | 4.65 | 0.036 | 2.7 | 40.3 | 0.29 | 0.062 | nd | bdl | 0.1 | 1.05 | 0.21 | 0.096 | 0.0028 | 2.75 | 0.043 | 0.143 | 0.0028 | 0.05 | 0.013 | bdl | 2.31 |

K-42-17 | Py9-18 | 8030 | 208 | 0.274 | 0.77 | 0.73 | 43.5 | 64.9 | 1.29 | 4.22 | 0.018 | 2.63 | 73.6 | bdl | 0.128 | nd | 0.0031 | 0.03 | 1 | bdl | 0.56 | bdl | 3.34 | 0.024 | 1.028 | 0.007 | 0.008 | 0.01 | bdl | 304.69 |

Minimum | 4220.0 | 0.7 | 0.028 | 0.38 | 0.40 | 0.23 | 8.2 | 0.5 | 3.5 | 0.0 | 2.5 | 2.6 | 0.05 | 0.01 | 0.024 | 0.001 | 0.03 | 0.3 | 0.1 | 0.0 | 0.003 | 0.5 | 0.02 | 0.1 | 0.003 | 0.01 | 0.01 | 0.01 | 0.6 | |

Maximum | 17480.0 | 2470.0 | 8.42 | 10.30 | 7.55 | 505.0 | 1298.0 | 19.0 | 6.4 | 0.2 | 2.7 | 73.6 | 1.04 | 1.01 | 0.065 | 0.021 | 0.31 | 407.0 | 0.3 | 9.7 | 0.089 | 860.0 | 0.93 | 39.0 | 0.013 | 4.68 | 0.06 | 0.36 | 304.7 | |

Average | 8942.2 | 585.6 | 1.86 | 2.55 | 1.51 | 70.9 | 251.1 | 6.2 | 4.5 | 0.1 | 2.6 | 21.6 | 0.38 | 0.45 | 0.038 | 0.008 | 0.11 | 52.9 | 0.2 | 2.2 | 0.033 | 110.0 | 0.26 | 7.6 | 0.007 | 1.20 | 0.03 | 0.21 | 62.1 | |

Std dev | 5147.9 | 1047.8 | 3.38 | 3.77 | 2.29 | 163.6 | 448.4 | 7.2 | 0.9 | 0.1 | 0.1 | 26.7 | 0.37 | 0.43 | 0.023 | 0.007 | 0.10 | 133.4 | 0.1 | 4.0 | 0.031 | 282.1 | 0.30 | 12.9 | 0.004 | 1.85 | 0.02 | 0.16 | 105.3 | |

CV | 58% | 179% | 182% | 148% | 151% | 231% | 179% | 116% | 20% | 96% | 3% | 124% | 96% | 96% | 61% | 95% | 85% | 252% | 70% | 186% | 94% | 257% | 115% | 170% | 60% | 155% | 63% | 79% |

**Table 3.**Results of atomic absorption analysis of proximal metasomatites, their sulfides, and sulfides in quartz veins.

Sample | Mineral/Rock | Content | Au/Ag | |
---|---|---|---|---|

Au, ppm | Ag, ppm | |||

K-4-17 | Ру3 | 7.39 | 8.73 | 0.8 |

K-9-17 | Ру3 | 21.4 | 5.64 | 3.8 |

K-9-17 | Ру3 | 22.37 | 7.8 | 2.9 |

K-14-17 | Ру3 | 3.54 | 1.31 | 2.7 |

K-14-17 | Ру3 | 0.76 | 1.15 | 0.7 |

KG-9-19 | Ру3 | 4.89 | 2.74 | 1.8 |

KG-32-19 | Ру3 | 10.06 | 5.44 | 1.8 |

KG-20-19 | Ру3 | 11.87 | 6.54 | 1.8 |

K-13-18 | Ру3 | 3.67 | 6.95 | 0.5 |

KG-8-19 | Ру3 | 39.32 | 17.38 | 2.3 |

KG-30-19 | Ру3 | 12.36 | 1.13 | 10.9 |

Average | 12.51 | 5.89 | ||

Std dev | 11.32 | 4.71 | ||

CV | 91% | 80% | ||

K-4-17 | Ару1 | 12.3 | 0.43 | 28.6 |

KG-26-19 | Ару1 | 16.44 | 11.83 | 1.4 |

KG-29-19 | Ару1 | 23.8 | 7.2 | 3.3 |

Average | 17.51 | 6.49 | ||

Std dev | 5.82 | 5.73 | ||

CV | 33% | 88% | ||

KG-23-19 | Ру4 | 27.07 | 4.46 | 6.1 |

K-5-17 | Ру4 | 9.42 | 3.47 | 2.7 |

KG-34-19 | Ру4 | 51.42 | 11.13 | 4.6 |

Average | 29.30 | 6.35 | ||

Std dev | 21.09 | 4.17 | ||

CV | 72% | 66% | ||

KG-35-19 | Ару2 | 20.49 | 2.06 | 9.9 |

K-4-17 | Sandstone with sulfides and quartz veinlets | 0.084 | 0.088 | 1.0 |

K-9-17 | Sandstone with sulfides and quartz veinlets | 0.740 | 0.084 | 8.8 |

K-14-17 | Sandstone with sulfides | 0.001 | 0.032 | 0.0 |

K-25-17 | Sandstone with sulfides | 0.240 | 0.042 | 5.7 |

K-27-17 | Sandstone with sulfides | 0.059 | 0.007 | 8.4 |

K-28-17 | Sandstone with sulfides | 0.064 | 0.097 | 0.7 |

K-40-17 | Sandstone with sulfides | 5.29 | 0.142 | 37.3 |

K-41-17 | Siltstone with pyrite | 0.006 | 0.041 | 0.1 |

Average | 0.81 | 0.07 | ||

Std dev | 1.83 | 0.04 | ||

CV | 225% | 66% |

№ | Sample | Generation | δ^{34}S_{VCDT} (‰) |
---|---|---|---|

1 | K-4-17 | Apy1 | −1.2 |

2 | KG-9-19 | Apy1 | −1.4 |

3 | K-9-17 | Py3 | −0.6 |

4 | KG-32-19 | Py3 | −1.3 |

5 | KG-35-19 | Apy2 | −2.0 |

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**MDPI and ACS Style**

Kudrin, M.V.; Fridovsky, V.Y.; Polufuntikova, L.I.; Kryuchkova, L.Y.
Disseminated Gold–Sulfide Mineralization in Metasomatites of the Khangalas Deposit, Yana–Kolyma Metallogenic Belt (Northeast Russia): Analysis of the Texture, Geochemistry, and S Isotopic Composition of Pyrite and Arsenopyrite. *Minerals* **2021**, *11*, 403.
https://doi.org/10.3390/min11040403

**AMA Style**

Kudrin MV, Fridovsky VY, Polufuntikova LI, Kryuchkova LY.
Disseminated Gold–Sulfide Mineralization in Metasomatites of the Khangalas Deposit, Yana–Kolyma Metallogenic Belt (Northeast Russia): Analysis of the Texture, Geochemistry, and S Isotopic Composition of Pyrite and Arsenopyrite. *Minerals*. 2021; 11(4):403.
https://doi.org/10.3390/min11040403

**Chicago/Turabian Style**

Kudrin, Maxim V., Valery Yu. Fridovsky, Lena I. Polufuntikova, and Lyudmila Yu. Kryuchkova.
2021. "Disseminated Gold–Sulfide Mineralization in Metasomatites of the Khangalas Deposit, Yana–Kolyma Metallogenic Belt (Northeast Russia): Analysis of the Texture, Geochemistry, and S Isotopic Composition of Pyrite and Arsenopyrite" *Minerals* 11, no. 4: 403.
https://doi.org/10.3390/min11040403