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Fluid Inclusion Evidences for the P-T Conditions of Quartz Veins Formation in the Black Shale-Hosted Gold Deposits, Bodaybo Ore Region, Russia

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Fluid Inclusion Evidences for the P-T Conditions of Quartz Veins Formation in the Black Shale-Hosted Gold Deposits, Bodaybo Ore Region, Russia Journal of Earth Science, Vol. 31, No. 3, p. 514–522, June 2020 ISSN 1674-487X Printed in China https://doi.org/10.1007/s12583-019-1024-4 Fluid Inclusion Evidences for the P-T Conditions of Quartz Veins Formation in the Black Shale-Hosted Gold Deposits, Bodaybo Ore Region, Russia Natalia N. Ankusheva *1, 2, Ekaterina E. Palenova1, Svetlana N. Shanina3 1. Institute of Mineralogy, South-Urals Federal Research Center of Mineralogy and Geoecology, Urals Branch, Russian Academy of Sciences, Miass 456 317, Russia 2. Geological Department, South-Urals State University, Miass 456 300, Russia 3. Institute of Geology of the Komi Science Center, Urals Branch, Russian Academy of Sciences, Syktyvkar 167 982, Russia Natalia N. Ankusheva: https://orcid.org/0000-0003-4142-5606 ABSTRACT: The P-T conditions of auriferous and barren quartz veins from Kopylovsky, Kavkaz and Krasnoye gold deposits in Proterozoic black shales of Bodaybo ore region are presented the first time in this study. Fluid inclusions trapped in auriferous quartz are aqueous Na±K-Mg chloride with salinity of 6 wt.%–8.8 wt.% NaCleqv. Homogenization temperatures vary from 260 to 350 ºС, and calculated trapping pressures are 1.2–1.6 kbar. The fluids trapped in barren quartz have more complicated compositions with Na, K, Mg and Fe chlorides, salinity up to 13 wt.% NaCleqv, and homogenization temperatures ranging between 140 and 280 ºС. The volatiles in fluids are dominated by H2O, followed by CO2 with minor amounts of CH4 and N2. We suppose that auriferous and barren quartz veins have been formed due to the basic metamorphogenic fluid as evidenced by the close slat and gas fluid composition. KEY WORDS: Bodaybo, black shales, gold deposits, gold-bearing quartz, barren veins, fluid inclusions, P-T conditions. 0 INTRODUCTION whereas smaller gold occurrences in the Bodaybo region are The Bodaybo gold-bearing region is one of the largest studied poorly. But many features to understand the genesis of gold provinces in Russia. Situated in the eastern part of Russia gold mineralization could be better defined by small deposits in the Lena River Basin, this region belongs to the Baikal oro- rather than the giant deposits, which are characterized by poly- genic belt. It hosts the well-known giant Sukhoi Log Deposit genic and polychronic ore-forming processes (Rundqvist, 1997). (2 956 t Au and 1 541 t Ag, Migachev et al., 2008) as well as Therefore, the small-scaled deposits Kopylovsky, Kavkaz, and several smaller deposits (Verninskoye, Golets Vysochayshiy, Krasnoye were studied in this work. etc.). All gold deposits of the Bodaybo region are hosted by The study focuses on characterizing P-T conditions of the Upper Proterozoic black shales. formation of the gold-bearing and barren quartz veins and fluid There are two major hypotheses for the formation of the volatile composition of the Kopylovsky, Kavkaz, and Krasnoye deposits in the Bodaybo region: magmatic hydrothermal and deposits, on the basis of previous studies of our colleagues whi- metamorphic hydrothermal. According to the first hypothesis, the ch aimed to describe mineralogical-geochemical features of main stage of gold concentration in the ore is related to post- these deposits and host rocks (Palenova et al., 2015a, b, 2013). metamorphic intrusions, including granitoid and hypothetical deep-seated mafic complexes (Yudovskaya et al., 2011; Laverov 1 GEOLOGICAL SETTING et al., 2007; Distler et al., 2004). According to the metamorphic The Bodaybo region is the part of the Mamsko-Bodaybinsky hydrothermal hypothesis, ore-forming fluids result from the re- District and composed of Upper Proterozoic carbonaceous- gional metamorphism of initially metalliferous carbonaceous terrigenous sediments folded and intruded by Late Paleozoic sequences (Large et al., 2007; Buryak and Bakulin, 1998). granitoids (Fig. 1). Granitoid stocks and large batholiths of the Many papers have been focused on the Sukhoi Log Deposit, Mamsko-Oronsky (about 420 Ma, Gerasimov et al., 2007) and which is the typical of the aforementioned genetic models, Konkudera-Mamakan (2 phases, 325 and 270 Ma, Bukharov et al., 1992) complexes intrude terrigenous sequences in the southern *Corresponding author: [email protected] part of the region. Also there are Late Paleozoic thin lamprophyre © China University of Geosciences (Wuhan) and Springer-Verlag dykes. The sedimentary rocks are greenschist facies metamor- GmbH Germany, Part of Springer Nature 2020 phosed with increasing grade from chlorite-muscovite subfacies in the central part to biotite subfacies at the margins (Ivanov, 2008). Manuscript received February 13, 2019. The gold deposits in the Bodaybo region consist of two Manuscript accepted May 30, 2019. large ore clusters: Kholmolkhyn, with the largest known deposits Ankusheva, N. N., Palenova, E. E., Shanina, S. N., 2020. Fluid Inclusion Evidences for the P-T Conditions of Quartz Veins Forma- tion in the Black Shale-Hosted Gold Deposits, Bodaybo Ore Region, Russia. Journal of Earth Science, 31(3): 514–522. https://doi.org/10.1007/s12583-019-1024-4. http://en.earth-science.net Fluid Inclusion Evidences for the P-T Conditions of Quartz Veins Formation in the Black Shale-Hosted Gold Deposits 515 Figure 1. Simplified geological scheme of Bodaybo ore region (after Ivanov, 2008). (Sukhoi Log, Verninskoe) located in the north and Artemovsky in the Vasilievsky anticline, Kavkaz Deposit is located. the south (Ivanov, 2008); Kopylovsky and Kavkaz (Dogaldyn The Krasnoye Deposit is situated in 75 km north from Formation (Vdg3) and Krasnoye (Vacha Formation) deposits Bodaybo Town at the watershed of Krasny and Tjoply streams (Palenova et al., 2015b). and confined to the complicated anticline upper bend (Kuz- The Kopylovsky Deposit is located 45 km NE from Bo- menko, 2013). The deposit is hosted by carbonaceous quartz daybo Town and confined to the homonymous near-latitudinal and quartzitic metamorphosed sandstones and siltstones, and anticline—a tight asymmetric fold with gently dipping northern less, interbedded carbonaceous shales. Gold mineralization is (42º–50º) and near-vertical southern limbs. The curved hinge of confined to the dispersed and lens-shaped pyrite dissemination the fold dips gently to the southwest and east. Quartz veins, zones, and fewer quartz veins with sulfide mineralization. Gold stockworks and NE-trending strike-slip-normal faults are devel- has formed inclusions and growths in pyrite (Ankusheva et al., oped at the hinge curvature (Palenova et al., 2015b). The host 2019; Palenova et al., 2013). rocks are sandstones and siltstones, and carbonaceous shales of All studied deposits are characterized by sulfide mineraliza- the Dogaldyn Formation metamorphosed to sericite-chlorite tion in the form of layers and disseminations in carbonaceous greenschist facies (Palenova et al., 2013). In addition, rare thin shales and metamorphosed sandstones and siltstones; quartz- lamprophyre dykes are developed at Kopylovsky Deposit. The pyrite veinlets in stockwork zones; nest-shaped and poor dis- nearest granite pluton is located 40 km east (Aksenov, 2004). semination in quartz veins (Fig. 2) (Palenova et al., 2015a, b). Gold ores are located in the core and north limb of the Kopy- Gold formed inclusions and growths with pyrite and native grains lovsky anticline and predominantly hosted in carbonaceous shale in quartz veins. At the deposits, ores are divided into gold- intercalated with metamorphosed sandstones and siltstones. sulfide-quartz (quartz veins and stockwork zones in anticlinal The Kavkaz Deposit is located 35 km north from Bodaybo fold core) and Au-sulfide (mineralized zones in host rocks) types. Town in the central part of the Vasilievsky ore field which con- Quartz veins are divided into 3 types: (1) thick (1–8 m) selli- tains a 200 to 800 m wide ‘belt’ of quartz veins. This belt is con- form in curves of folds and flexures; (2) concordant thin quartz- trolled by the Millionny and Korolkovsky oblique-slip faults pyrite veinlets (from several millimeters to 5 cm thick); (3) the which are complicated by the northern limb of the Kairo-Lenin youngest veins of different thicknesses (from 1 cm to tens of cm). anticline and conjugated with higher order folds, in one of which, Quartz (rare quartz-carbonate) veins at Kopylovsky Deposit 516 Natalia N. Ankusheva, Ekaterina E. Palenova and Svetlana N. Shanina Figure 2. Photographs showing the quartz veins of deposits. (a) Sample 358-2 with Au, and (b) sample 504-80.2, barren from Kopylovsky; (c) sample 258-2, squares are visible Au from Kavkaz; (d) sample 141425-135.6, galena-quartz vein with Au from Krasnoye. include galena and chalcopyrite. At Kavkaz Deposit, quartz veins 514 nm emission line (10 mW); the lateral resolution was better contain chalcopyrite, sphalerite, galena, chalcocite, secondary than 2 μm; acquisition time was equal to 30 s; accumulation covellite, and visible gold. And at Krasnoye Deposit, quartz veins number was equal to 10 (Pankrushina et al., 2019). The nitro- contain galena, chalcopyrite, and tennantite. gen peak area from the inclusions was calculated by subtracting atmospheric N2 peak area from the measured one when focused 2 ANALYTICAL METHODS in the gas phase. Microthermometric studies were performed using double- polished sections on TMS-600 (Linkam) stage at the Thermo- 3 RESULTS barogeochemistry Laboratory of the South-Urals State University 3.1 Characteristics of Fluid Inclusions (Miass). The temperatures within -20 to +80 ºC range are meas- At Kopylovsky Deposit, quartz was sampled in gold- ured with a precision of ±0.1 ºC and out of this range, ±1 ºC. The bearing vein from a trench (sample 358-2). According to the fluid composition was determined according to Davis et al. (1990) atomic adsorption analysis, Au content in this vein is 0.73 ppm and Spencer et al. (1990). Salinities were calculated using the (after acid dissociation) and 1.40 ppm (after alkali dissociation). temperatures of final ice melting of fluid inclusions according to Quartz formed non-zoned anhedral grains up to 3 mm size.
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