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Article

Rare Metal (Li–Ta–Nb) Mineralization and Age of the Kvartsevoye Pegmatite Deposit (Eastern Kazakhstan)

by
Tatyana A. Oitseva
1,2,*,
Sergey V. Khromykh
3,
Anna V. Naryzhnova
3,
Pavel D. Kotler
3,
Marina A. Mizernaya
1,
Oxana N. Kuzmina
1 and
Artem K. Dremov
1
1
Faculty of Earth Sciences, D. Serikbayev East Kazakhstan Technical University, 19, Serikbayev str., Ust’-Kamenogorsk 070000, Kazakhstan
2
Geos LLP, 83, Protozanov str., Ust’-Kamenogorsk 070000, Kazakhstan
3
V.S. Sobolev Institute of Geology and Mineralogy Siberian Branch of the Russian Academy of Sciences, 3 Koptyug ave., Novosibirsk 630090, Russia
*
Author to whom correspondence should be addressed.
Minerals 2025, 15(7), 737; https://doi.org/10.3390/min15070737
Submission received: 5 May 2025 / Revised: 10 July 2025 / Accepted: 11 July 2025 / Published: 15 July 2025
(This article belongs to the Special Issue Pegmatites as Hosts of Critical Metals: From Petrogenesis to Mineral Exploration)
Browse Figures
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Abstract

The Kalba–Narym metallogenic belt is located in East Kazakhstan, which displays rare metal mineralization. The Kvartsevoye rare metal Li–Ta–Nb deposit is located in the north-western ore district. This study presents the results of geological, mineralogical, geochemical, and geochronological analyses of rare metal granite pegmatites. Rare metal mineralization belongs to a field of variably differentiated pegmatites, including barren, quartz–albite–muscovite, muscovite, and muscovite–quartz–albite microcline mineral associations. This study established that the rare metal mineralization is localized in the quartz–albite–muscovite zone. The main concentrator minerals of rare metals are spodumene for Li and tantalite–columbite for Ta and Nb. Ar/Ar dating of the muscovite allowed us to establish the age of mineralization during the period of 288–285 Ma. The present study enabled the linkage of rare metal mineralization with the differentiation processes of the granites of the Kalba complex.

1. Introduction

Rare metals (Li, Nb, Ta, Be, Cs, Sn) are currently the most popular high-tech raw materials in the global economy. Lithium (Li), niobium (Nb), and tantalum (Ta) are among the most sought-after materials for modern high-tech products. They are used in many strategic emerging industries, including electronics and aerospace, and are recognized worldwide as important strategic mineral resources [1,2,3,4]. Nowadays, there is a high need for the discovery of new or detailed additional exploration of already known deposits of rare metals. Nb deposits are frequently associated with alkaline–carbonatite igneous formations. In contrast, complex Li–Ta–Nb deposits are more commonly associated with rare metal granitic pegmatites [5,6]. The compositions and ages of coexisting rare metal pegmatites and granites have important petrogenetic implications for the formation mechanisms of mineralization.
The Kalba–Narym rare metal belt, which concentrates many deposits of rare metals associated with granites of the Kalba–Narym batholith, is located in East Kazakhstan. The best-known area is the Central Kalba ore district, which contains large deposits of Li, Cs, Ta, and Nb (Bakennoye, Yubileynoye, Belaya Gora) [7,8]. The majority of these deposits were developed for the extraction of metals such as tantalum, niobium, tin, and tungsten, which were in demand during the Soviet era. Other rare metals such as lithium, cesium, and beryllium were mined as by-products, and no detailed exploration of these components was carried out. In the early 1990s of the 20th century, mining stopped and these deposits were mothballed. Due to the emergence of interest in rare metals and new analytical possibilities for geological exploration, it is, therefore, timely to reassess the ore potential of rare metal deposits in East Kazakhstan. One of the poorly explored deposits is Kvartsevoye, located within the north-western ore district of the Kalba–Narym belt (Figure 1). According to the results of geological studies carried out in the 1970s and 1980s of the 20th century [9,10,11], the Kvartsevoye deposit is similar to the Yubileynoye and Belaya Gora deposits in the Central Kalba district. This suggests that the Kvartsevoye deposit has the potential to host substantial reserves of rare metals. In this paper, we present new data on the mineralogy, geochemistry, and age of the Kvartsevoye deposit, aiming to clarify the age of the deposit and the relationship between the formation of pegmatites and the differentiation processes of granitic magmas.

2. Geological Background

The Kalba batholith is the main structural unit of the Kalba–Narym metallogenic belt (Figure 1). The granitoids were formed in the Early Permian at the post-collisional stage of geodynamic development of the region [13]. Two main associations are identified in the composition of the Kalba batholith [14]: (1) the Kalba granodiorite–granite complex, occupying about 80%–85% of the batholith volume and formed during the period of 295–285 Ma; (2) the Monastery granite–leucogranite complex, represented by several separate large intrusions (15%–20% of the batholith volume) formed during the period of 285–276 Ma. The host rocks for the granites of the Kalba batholith are terrigenous sedimentary formations of the Takyr formation (D3-C1), which are primarily comprised of siltstones, mudstones, and shales.
Most rare metal mineralization is associated with granites of the Kalba complex. Ore bodies are located in the dome part and endocontacts of granite intrusions. Mineralization occurs in pegmatite bodies and their clusters, in the form of greisen zones and halos of quartz veins.
There are four main ore districts (Figure 1)—Sh (Shulbinsk), NWK (North-Western Kalba), CK (Central Kalba), and N (Narym). The Central Kalba ore district is the most studied and contains most of the large commercially explored deposits (Yubileynoye, Belogorskoye, Bakennoye, etc.) [7,8,12].
The North-Western Kalba (NWK) area has been studied in less detail. The Kvartsevoye rare metal deposit is the most well-known in the area. It was discovered in the 1970s of the 20th century, after which a quarry was opened (the deposit will be mined for tantalum, niobium, beryllium, and lithium). Since the early 1990s, the development of the deposit has stopped. It is confined to the south-eastern part of the Alypkel intrusion.
The intrusion is mainly composed of medium-grained biotite granites. The granites are cut by bodies, which are represented by granites and microgranites. The granite bodies are up to 1 m thick and are composed of medium-grained muscovite granites. The microgranite bodies are up to 0.5 m thick and are composed of fine-grained muscovite granites with accessory garnet and tourmaline. All granites of the Alypkel intrusion are intruded by several pegmatite bodies (Figure 2). The general strike of the body is north-west (310–320°), and the bodies dip to the south-west over an angle range of 35–50°. Most of the pegmatite bodies are 5–10 m thick and range from 120 to 200 m in length. The pegmatite bodies exhibit a parallel arrangement. The largest body is known as the main body. Its thickness reaches 50 m and its length is 700 m. Granite xenoliths have been observed in the main body (Figure 3). The main body is composed of differentiated, internally zoned pegmatite. Several zones can be distinguished by their structural–textural features and distinct mineral assemblages, including blocky microcline, muscovite, muscovite–quartz–albite, muscovite–albite–quartz–microcline, and aplite. The greatest number of zones and mineral diversity can be observed in the central part of the body. The spodumene is localized predominantly in the muscovite–quartz–albite zone. The number of pegmatite zones decreases along the strike and dip of the body (according to drilling data [9,10,11]), and the content of useful components also decreases. The other pegmatite bodies are not zonal and do not contain rare metal mineralization; thus, we did not conduct a detailed study on them.

3. Methods

The scientific study included field and analytical work. Samples from ore-bearing rocks and rare metal pegmatites (more than 50 samples) were taken for laboratory research. Samples were taken directly from rock outcrops from the quarry walls. Several granite samples were taken from the core wells drilled in the frame of the quarry within granites of the Alypkel intrusion.
Analytical studies were performed in the VERITAS laboratory of the D. Serikbayev East-Kazakhstan Technical University (EKTU) (Ust-Kamenogorsk, Kazakhstan) and the V.S. Sobolev Institute of Geology and Mineralogy (IGM) of the Siberian Branch of the Russian Academy of Sciences (Novosibirsk, Russia). Petrographic studies on transparent thin sections were performed at IGM using a Carl Zeiss AxioScope.A1 (ZEISS, Oberkochen, Germany) polarizing light microscope equipped with a Canon EOS 650D camera (Canon, Tokyo, Japan). The backscattered electrons images of minerals were obtained using a scanning electron microscope (JEOL 100C, Tokyo, Japan) with an energy-dispersive attachment (Kevex Ray, Thermo Scientific, Waltham, MA, USA). For the analyses, the beam current was 1 nA, the beam diameter was 10 nm, and the analysis was carried out by scanning an area of 5 × 5 μm. The live spectrum acquisition time was 60 s. The stability of the survey parameters was controlled by periodically measuring the intensity of the K-line of pure cobalt. The correctness of the obtained results was controlled via periodic measurement of the standards used in the calibration.
The composition of mica was studied at IGM via an X-ray spectral microanalysis on a JEOL JXA-8230 microprobe (Jeol, Tokyo, Japan). The analyses were carried out at an accelerating voltage of 20 kV, with a beam current of about 30 nA and an electron beam diameter of 2 μm. A set of well-characterized intralaboratory standards (albite (Na, Al), orthoclase (K), fluoro-phlogopite (F), and diopside (Ca, Mg, Si)) were used to calibrate the instruments. The following are the limits of detection for impurity elements (wt.%): FeO 0.05, MnO 0.07, Na2O 0.14, MgO 0.07, Rb2O 0.27, K2O 0.03, CaO 0.02, TiO2 0.07, P2O5 0.13, Cs2O 0.06, F 0.2, and Cl 0.01. The main components, as well as the F and Cl concentrations, were analyzed. The Li2O contents were calculated according to the correlations between the established Li, F, and Mg concentrations [15]. The Li2O contents in the biotites were calculated using the formula Li2O (wt%) = [2.7/(0.35 + MgO(wt%)) − 0.13], and the Li2O contents in the muscovites using the formula Li2O (wt%) = 0.3935 × F(wt%)^1.326 [15]. The relationships have been shown to underestimate the Li content, in particular in situations when micas are rich in Fe [16].
The compositions of the rocks and minerals were determined via mass spectrometry with inductively coupled plasma (ICP-MS) on an Agilent 7500cx instrument (Agilent Technologies, Santa Clara, CA, USA), which determines 73 elements with high sensitivity. The contents of rare metals in pegmatite minerals and bulk rock samples were determined at EKTU. The samples were dried at a temperature of 105 °C and then ground to a fraction of less than 71 μm. Before the geochemical measurements, the samples were transferred into a solution using multi-acid digestion. During the acid digestion, at first standard samples of the composition of aqueous solutions of elements were used as calibration solutions and then the samples were analyzed. The calibration solutions were prepared by diluting standard samples (standards CMS-1, IV-Stock-21, and IV-Stock-29 made by Inorganic Ventures, USA) with a solution of nitric acid with a mass concentration of 2% or 5%, hydrochloric acid solution with a mass concentration of 10%, or distilled water. A solution of nitric acid with a mass concentration of 5% was used as an analytical background solution. The analyses were performed at the VERITAS Laboratory of EKTU.
The geochronological studies were carried out via the 40Ar/39Ar method [17] using the stepwise heating technique. The methodology is described in detail in [18]. The samples were irradiated in a nuclear BWR-reactor at the Tomsk Polytechnic University (Tomsk). A standard biotite sample MSA-11 (OSO No. 129-88) with an age of 311.0 ± 1.5 Ma, validated against the international standard samples Bern-4M (muscovite) and LP-6 (biotite), was used. The ages of the Bern 4M and LP-6 standard samples were assumed to be 18.51 and 128.1 Ma, respectively [17]. The Ar isotopic composition in the irradiated samples was measured using a Noble Gas 5400 (Micromass, Cheshire, UK) mass spectrometer. The separation of gas fractions and the isotopic analysis of argon were carried out over a temperature range of 500 to 1200 °C. The ages were calculated based on the measured 40Ar/39Ar ratios. The raw data were corrected for procedural blank mass discrimination via an analysis of atmospheric Ar; the decay of radioactive 37Ar and 39Ar isotopes produced by irradiation; and interferences of 36Ar, 39Ar, and 40Ar produced from 40Ca, 42Ca, and 40K, respectively. The corrections were applied using the following coefficients: (39Ar/37Ar)Ca = 0.001279 ± 0.000061, (36Ar/37Ar)Ca = 0.000613± 0.000084, (40Ar/39Ar)K = 0.0191 ± 0.0018. The amount of 40Ar in the blank did not exceed 0.5 ng. The plateau method is generally accepted for interpreting the results of 40Ar/39Ar step heating in the form of age spectra. According to this method, the average weighted age for several (at least three) successive temperature steps is considered reliable. The following conditions must be met for the steps included in the plateau: the difference in age values between any two steps must not be significant; they are characterized by consistent Ca/K ratios; at least 50% of the released 39Ar corresponds to them.

4. Results

4.1. Lithology

4.1.1. Granites

The biotite granites are uniformly grained or weakly porphyritic fine- to medium-grained rocks with a hypidiomorphic structure (Figure 4a,b). The early minerals (relatively idiomorphic grains) are albite and potassium feldspar (total of 40–50 vol.%). The total amount of early minerals is in the range of approximately 40–50 vol.%. Potassium feldspar slightly predominates over plagioclase. The quartz is represented by xenomorphic grains (35–50 vol.%). The biotite is represented by subidiomorphic flakes, the quantity of which reaches 10–12 vol.%. Muscovite is rare in interstices between the earlier minerals. The mineral formation sequence was Ab + Kfs + Bt → Otz → Ms.
The muscovite granites are medium-grained or fine-grained rocks with a hypidiomorphic structure. The earliest mineral (sub-idiomorphic grains) is albite, which forms elongated laths, amounting for 55–65 vol.%. Less idiomorphic is the potassium feldspar, which forms weakly elongated grains comprising 15–20 vol.%. The xenomorphic quartz grains occupy no more than 20–25 vol.%. Muscovite is present everywhere in interstices as a late magmatic mineral (Figure 4c,d). The amounts vary from 5 to 10 vol.%. Biotite was not found in any variety of muscovite granites. In some samples, there were single idiomorphic small grains of garnet (not more than 2 vol.%), and in some other samples there were single idiomorphic grains of tourmaline (less than 1 vol.%). The mineral formation sequence was Ab (± Grt ± Turm) → Kfs + Qtz → Ms

4.1.2. Pegmatites of the Main Body

The rare metal mineralization is hosted by the main body, which is part of a field (or swarm) of variably differentiated pegmatite dikes, with distinct mineral assemblages (barren, muscovite–quartz–albite, and muscovite–quartz–albite–microcline). The barren quartz–feldspar bodies are composed of quartz and microcline, with minor amounts of albite and small grains of muscovite (Figure 5).
The muscovite–quartz–albite–microcline zone of the main body consists of predominantly albite, muscovite, microcline, and quartz. It contains accessory minerals such as garnet, apatite, tourmaline, topaz, zircon, monazite, allanite, tantalite–columbite, and Fe and Mn phosphates.
The quartz–albite–muscovite zone is composed mainly of these minerals, and contains important ore minerals such as beryl and spodumene (Figure 6).
Within the main vein, there are local zones with a predominance of light green muscovite (more than 70%) in paragenesis with quartz and albite. These local zones are most similar to greisens, and were named exactly as such. They are not independent bodies.

4.2. Mineralogy

The mica in the granites is represented by biotite and muscovite. The mica in the greisen and pegmatites is represented by muscovite. The mica composition is given in Table 1. The biotite in the granites of the 1s phase of the Alypkel intrusion is represented by Fe–biotite, containing up to 3.6 wt% TiO2 and up to 0.36 wt% MnO, as well as 0.03–0.05 wt% Cl, 0.32–0.74 wt% F, and 0.16–0.17 wt% Li2O. The muscovite in the microgranite bodies, greisens, and pegmatites has a similar composition. It corresponds to Fe–muscovite, with composition points located near the Li–Fe field of muscovite and Li–siderophyllite (Figure 7a).
The muscovite from the muscovite microgranites contains the highest concentrations of F (up to 2.2 wt%) and Li2O (up to 1.49 wt%). The muscovite from the greisens and pegmatites has a similar composition, characterized by low Cl contents of up to 0.02 wt% (Figure 7b), increased aluminosity (Al2O3/(Al2O3 + SiO2 + MgO + FeO) from ranging 0.41 to 0.45, Figure 7c,d), and decreased F and Li2O contents (Figure 7c,d).
Beryl occurs in all mineral assemblages in association with veins of grey and dark grey quartz. It forms prismatic crystals of white, pale green, and yellowish-grey colors. It contains tantalite phenocrysts of up to 3 × 4 mm in size. Small inclusions of beryl are characteristic of the quartz–albite–muscovite zone.
Garnet occurs in assemblages of up to 2 mm in size or as clusters of grains. Sometimes garnet grains are embedded in beryl crystals (Figure 8a–c). Apatite can be observed as clusters of thickened prisms (Figure 9d).
Zircon can be encountered in microscopic examinations of ores. The grain shape is square or irregular, measuring 0.1 mm or less (Figure 8e–g).
Spodumene occurs mainly in the quartz–albite–muscovite assemblage, sometimes reaching 10% of the rock volume. It forms rather large, well-cut crystals up to 40 cm long. It is cut by veins of quartz and replaced by albite and muscovite. Galena, magnetite, cassiterite, and hematite were found as inclusions in the spodumene (Figure 8h–l).
The tantalite distribution within the albitized zones is non-uniform, forming thick tabular grains measuring up to 8 × 10 mm and tabular grains up to 1 mm thick (Figure 9). The Ta2O5/Nb2O5 ratios vary from 1:1 to 2:1. The Ta-rich samples contain large grains (up to 1.5 cm in size) of tantalite evenly distributed in the quartz–albite–muscovite zone (with green muscovite), traced to a depth of 30–40 m. The Ta2O5 contents in this zone range from 0.05 to 0.23 wt.%. The ore-bearing assemblages in the pegmatites include thin phenocrysts of tantalite–columbite in association with fine crystalline albite. The average value of Ta2O5 is about 0.017 wt.%.

4.3. Geochemistry

According to the results of the mass spectrometric analysis, the distribution of geochemical elements in the host rocks (granites) and rare metal pegmatites was studied. Table 2 shows the contents of rare elements in the granites and quartz, while Table 3 shows the pegmatites of the main body of the Kvartsevoye deposit.
The contents of rare elements in the quartz core are insignificant. In the granites, elevated values of Li (243 ppm) and Rb (204 ppm) can be observed. In the muscovite–quartz–albite–microcline, high contents of Li (up to 12,079 ppm), associated mainly with spodumene, were determined. High Li (707 ppm) and Rb (1591 ppm) contents due to muscovite and Sn (421 ppm) were noted in the greisenized pegmatite varieties, associated with small inclusions of cassiterite.

4.4. Ar/Ar Age

To determine the age of formation of the Kvartsevoye deposit, Ar/Ar dating of muscovite from a body of medium-grained muscovite granite (sample Kv-13-3) and the pegmatite main body (sample Kv-13-4) was carried out. In the muscovite granites, muscovite occupies interstices between quartz and feldspar grains and is late magmatic. In the main pegmatite, muscovite forms idiomorphic crystals located among quartz and albite grains. The morphology of muscovite commonly indicates its primary origin from hydrous melts.
The age of the muscovite from the muscovite granite (sample Kv-13-3) is 288.1 ± 7.2 Ma for 98% cumulative 39Ar. The age of the muscovite from the pegmatite body (sample Kv-13-4) is 285.2 ± 6 Ma for 99% cumulative 39Ar (Figure 10).

5. Discussion

Rare metal granitic pegmatites usually form as a result of the differentiation of granitic magmas in crustal magmatic chambers [5,6,20,21,22]. In the majority of cases, rare metal granite pegmatites are associated with granite intrusions [7,23,24,25,26]. However, in some cases, rare metal pegmatites are located outside of granite intrusions and can form extensive fields of multiple pegmatite bodies [27].
At the Kvartsevoye deposit, pegmatite bodies cut the biotite granites of the Alypkel intrusion; therefore, they are more recent. Nevertheless, here, as in the entire Kalba rare metal belt, the pegmatite bodies are closely spatially associated with granites [7,8,12], and there are no cases described where bodies of rare metal granite pegmatites are located far from granites.
The next pieces of evidence of the connection of rare metal pegmatite mineralization with the Kalba granite are geochronological data. Figure 11 shows a comparison of the ages for granite intrusions and rare metal pegmatite deposits in the Kalba–Narym metallogenic belt. The pegmatite deposits of the Central Kalba district (Asubulak ore district) show age values determined from muscovite and lepidolite in the range of 295–281 Ma [7]. The majority of the obtained age values are located in the period of 295–286 Ma. The youngest age values obtained here (282–281 Ma) can be caused by the disturbance of the Ar–isotope system in mica. For the Tochka deposit, also located in the Central Kalba district, age values of 293–290 Ma were obtained [28]. The age values obtained from the mica of the Kvartsevoye deposit (288 ± 7 and 285 ± 6 Ma) are comparable to those of the deposits in the Central Kalba district.
Although we do not have a geochronological definition of the age of the Alypkel granites, we can make the following assumptions about their age. Firstly, the terrigenous rocks of Kalba–Narym terrain were formed in the Late Devonian–Early Carboniferous, and the most ancient magmatic complexes have a Late Carboniferous age range (308–304 Ma); magmatic complexes older than 308 Ma have not been found in this terrane. The age of the granites of the Kalba complex, as determined by U–Pb dating of magmatic zircons, falls within the range of 297–286 Ma [14]. The age of the mica from the biotite Kalba granites, as determined using the Ar/Ar method, falls within the range of 288–275 Ma [28], which coincides with the Ar/Ar age of mica samples from similar pegmatite deposits in the region. The closing temperature of the K–Ar isotope system in the micas is lower than the closing temperature of the U–Pb isotope system in the zircons, which is why the mica ages are younger. The age difference between the U–Pb zircon and Ar/Ar mica ages may reach 10–15 Ma [7]. Secondly, the Alypkel granites are very similar to the granites of the Kalba complex, both in their petrographic and geochemical features. This suggests their age as being in the Early Permian, as well as the granites of the Kalba complex. The muscovite granites from the body that intrude the Alypkel granites are 288 million years old (see Figure 10). Consequently, the age of the biotite granites from the Alypkel intrusion were determined to be in the range between 297 (the oldest age of the Kalba granites) and 288 Ma. Thus, it can be assumed that both the biotite granites and rare metal pegmatites were formed as a result of a single endogenous event in the Early Permian.
According to the U–Pb dating of magmatic zircons, the granites of the Monastery complex show age values of 283–276 Ma, generally younger than the ages of rare metal pegmatites (Figure 11). Moreover, according to geological data, only barren quartz–feldspar pegmatites are associated with the intrusions of the Monastery complex. Consequently, it stands to reason that the rare metal pegmatite deposits of the Kalba–Narym belt are associated with granitic intrusions of the Kalba complex.
Thus, the first hypothesis, according to which rare metal granite pegmatites are associated with granite intrusions, seems more preferable. It assumes that the formation of rare metal pegmatites was a result of the differentiation of granitic magma within the chamber, during which the accumulation of volatile components and rare metals (Ta, Nb, Be, Li) compatible with them occurred in the residual melts. The composition of the micas, which concentrate these components, may be an indicator. As shown in Figure 7, the muscovites can be divided into two groups according to their concentrations of F and Li. These concentrations are highest in the muscovite from the microgranites, which indicates its crystallization from differentiated aluminosilicate melts. In the muscovites from greisen and rare metal pegmatites, the concentrations of F and Li are significantly lower. Once Li saturation was reached in the more fractionated aluminosilicate melt, the Li preferentially partitioned in spodumene rather than mica, which explains the lower Li concentrations in these muscovites. At the same time, the differences between the F and Li concentrations may be explained by fluid–melt immiscibility. As shown by the results of the study of rare metal pegmatite systems [21,29,30,31], during this process, F prefers to concentrate in the early aluminosilicate melt, while Li prefers to concentrate in the most differentiated hydrous melt phase.
Based on geological, geochemical, and geochronological data, the following model of the Kvartsevoye deposit formation can be proposed. The biotite granites of the Alypkel intrusion, body granites, greisen, and pegmatites may be genetically related. This is supported by their spatial proximity and age. All of these rocks most likely occurred as a result of the differentiation of a parental granite magma in the deep chamber. The biotite granites are the rocks closest in composition to the parental magma and are the least differentiated. Their intrusion took place in the first stage. While the biotite granites of the Alypkel intrusion crystallized at the upper levels of the crust, fractional crystallization also occurred in the deep granite magma chamber, as a result of which the residual melts were enriched with volatile components and rare metals. These residual melts intruded into the upper levels of the crust after cooling of the Alypkel intrusion through the faults, which formed the bodies of muscovite microgranites. Further differentiation of these residual melts could occur both at depth and in some intermediate chambers. The most advanced differentiation occurred in the largest main pegmatite body, where zones with rare metal ore mineralization were formed. Thus, the formation of ore-bearing rare metal pegmatites is a consequence of complex multi-stage processes, involving the differentiation of granite magma in deep chambers, followed by the differentiation of potentially ore-bearing F-enriched magmas in shallower or hypabyssal chambers in a closed system. Similar models have been described for the formation of many rare metal pegmatites in the Central Kalba ore region [8], northwestern China [24], and Thailand [25].

6. Conclusions

This investigation enabled the clarification of the geological structures, mineralogical and geochemical compositions, and ages of rare metal pegmatites of the Kvartsevoye deposit. The rare metal mineralization is concentrated in the largest main body, within which differentiation processes took place. The study allowed us to establish that the rare metal mineralization is localized in the quartz–albite–muscovite zone, where the Li concentrations can reach 12,000 ppm, the Ta concentrations 87 ppm, the Nb concentrations 152 ppm, and the Sn concentrations 421 ppm. The main rare metal concentrator minerals are spodumene for Li, tantalite–columbite for Ta and Nb, and cassiterite represented as microinclusions in spodumene for Sn.
Geological, geochemical, and geochronological data testify to the great potential of granites of the Kalba complex to reveal the associated rare metal mineralization of pegmatite and greisen types. Further detailed studies of the internal structures of granite intrusions of the Kalba complex may facilitate the identification of promising rare metal pegmatite targets in their upper parts. The north-western and Shulbinsk ore districts of the Kalba–Narym belt are considered to be promising districts for the identification of mineralization.

Author Contributions

Conceptualization, T.A.O. and S.V.K.; methodology, S.V.K., A.V.N., P.D.K. and M.A.M.; software, A.K.D.; validation T.A.O., S.V.K., A.V.N. and O.N.K.; formal analysis, A.V.N., P.D.K. and M.A.M.; investigation, T.A.O.; resources, T.A.O.; data curation, S.V.K.; writing—original draft preparation, S.V.K. and T.A.O.; writing—review and editing, S.V.K. and T.A.O.; visualization, T.A.O., S.V.K. and A.K.D.; supervision, T.A.O.; project administration, T.A.O.; funding T.A.O. and S.V.K. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the Science Committee of the Ministry of Science and Higher Education of the Republic of Kazakhstan (Grant No. AP19676805) and by the State Assignment of IGM SB RAS (Project No 122041400044-2).

Data Availability Statement

The data presented in this study are available on request from the corresponding author.

Acknowledgments

We wish to thank the VERITAS Engineering Laboratory (EKTU) and the Analytical Center (IGM) for the analytical work. We are very thankful to Sergey Z. Smirnov for the useful discussion about fluorine and lithium behaviors in granitic melts and related fluids. Our thanks are extended to Alexey Volosov for their aid in the manuscript’s preparation.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Scheme of the geological structure of the Kalba–Narym metallogenic belt. The main ore districts are shown: Sh—Shulbinsk; NWK—North-Western Kalba; CK—Central Kalba; N—Narym. Rare metal deposits: 1—Mokhnatukha; 2—Malo-Kaindy; 3—Kvartsevoye; 4—Zelenoye; 5—Novo-Saryozek; 6—Kanaika; 7—Medvedka, 8—Ognevka; 9—Bakennoye; 10—Yubileinoye; 11—Belaya Gora; 12—Karagoin; 13—Komarovskoye; 14—Kozlovskoye; 15—Shebuntai; 16—Komsomolskoye; 17—Palatsy; 18—Kasatkinskoye; 19—Cherdoyak; 20—Burabai; 21—Karasu. The inset shows the position of the Kalba–Narym belt (red star) on the scheme of terranes of the western part of the Central Asian Fold Belt (CAOB), according to [12]. The terranes are separated by large regional faults: ChSZ—Char shear zone; ISZ—Irtysh shear zone; NESZ—north-eastern shear zone.
Figure 1. Scheme of the geological structure of the Kalba–Narym metallogenic belt. The main ore districts are shown: Sh—Shulbinsk; NWK—North-Western Kalba; CK—Central Kalba; N—Narym. Rare metal deposits: 1—Mokhnatukha; 2—Malo-Kaindy; 3—Kvartsevoye; 4—Zelenoye; 5—Novo-Saryozek; 6—Kanaika; 7—Medvedka, 8—Ognevka; 9—Bakennoye; 10—Yubileinoye; 11—Belaya Gora; 12—Karagoin; 13—Komarovskoye; 14—Kozlovskoye; 15—Shebuntai; 16—Komsomolskoye; 17—Palatsy; 18—Kasatkinskoye; 19—Cherdoyak; 20—Burabai; 21—Karasu. The inset shows the position of the Kalba–Narym belt (red star) on the scheme of terranes of the western part of the Central Asian Fold Belt (CAOB), according to [12]. The terranes are separated by large regional faults: ChSZ—Char shear zone; ISZ—Irtysh shear zone; NESZ—north-eastern shear zone.
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Figure 2. Geological map (a) and cross-section (b) of the Kvartsevoye deposit [11].
Figure 2. Geological map (a) and cross-section (b) of the Kvartsevoye deposit [11].
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Figure 3. Xenoliths of Kalba biotite granites in the main pegmatite body of the Kvartsevoye deposit.
Figure 3. Xenoliths of Kalba biotite granites in the main pegmatite body of the Kvartsevoye deposit.
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Figure 4. Petrography of granites of the Kvartsevoye deposit: (a) medium-grained biotite granites; (b) fine-grained biotite granite with muscovite; (c) muscovite microgranite; (d) muscovite granite.
Figure 4. Petrography of granites of the Kvartsevoye deposit: (a) medium-grained biotite granites; (b) fine-grained biotite granite with muscovite; (c) muscovite microgranite; (d) muscovite granite.
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Figure 5. Quartz core with a rim of blocky microcline in the Kvartsevoye deposit.
Figure 5. Quartz core with a rim of blocky microcline in the Kvartsevoye deposit.
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Figure 6. Pegmatite of the Kvartsevoye deposit: (a) spodumene pegmatite on outcrop and in sample (b); (c) garnet–muscovite pegmatite with beryl. Abbreviations used in the figure: spd—spodumene; grt—garnet; ta—tantalite.
Figure 6. Pegmatite of the Kvartsevoye deposit: (a) spodumene pegmatite on outcrop and in sample (b); (c) garnet–muscovite pegmatite with beryl. Abbreviations used in the figure: spd—spodumene; grt—garnet; ta—tantalite.
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Figure 7. Mica composition from the Kvartsevoye deposit [19]: (a) micas on the Mg–Li (apfu) vs. VIFeTot + Mn + Ti–VIAl (apfu) diagram; (b) micas on the Cl vs. F diagram; (c) micas on the Al2O3/(Al2O3 + SiO2 + FeO + MgO) vs. Li2O diagram; (c,d) micas on the Al2O3/(Al2O3 + SiO2 + FeO + MgO) vs. F diagram. Please see the text for details about the marked trends.
Figure 7. Mica composition from the Kvartsevoye deposit [19]: (a) micas on the Mg–Li (apfu) vs. VIFeTot + Mn + Ti–VIAl (apfu) diagram; (b) micas on the Cl vs. F diagram; (c) micas on the Al2O3/(Al2O3 + SiO2 + FeO + MgO) vs. Li2O diagram; (c,d) micas on the Al2O3/(Al2O3 + SiO2 + FeO + MgO) vs. F diagram. Please see the text for details about the marked trends.
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Figure 8. Microinclusions of minerals in pegmatites samples of the main body of the Kvartsevoye deposit (BSE images): (a) garnet grains in quartz; (b) microgarnet inclusion in muscovite; (c) garnet in spodumene; (d) apatite inclusions in albite; (e,f) zircon micrograins in albite; (g) zircon and ilmenite inclusion in biotite; (h) prismatic inclusion of hematite in spodumene; (i) cassiterite grains in albite; (j) galena micrograins in albite; (k,l) cassiterite and magnetite grains in albite.
Figure 8. Microinclusions of minerals in pegmatites samples of the main body of the Kvartsevoye deposit (BSE images): (a) garnet grains in quartz; (b) microgarnet inclusion in muscovite; (c) garnet in spodumene; (d) apatite inclusions in albite; (e,f) zircon micrograins in albite; (g) zircon and ilmenite inclusion in biotite; (h) prismatic inclusion of hematite in spodumene; (i) cassiterite grains in albite; (j) galena micrograins in albite; (k,l) cassiterite and magnetite grains in albite.
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Figure 9. Microinclusions of tantalite and columbite in pegmatites samples of the main body from the Kvartsevoye deposit: (a) massive inclusions of tantalite and columbite grains; (b) tantalite inclusions in albite; (c) contact of tantalite and columbite; (d,e) columbite micrograins in albite; (f) tantalite inclusions in albite.
Figure 9. Microinclusions of tantalite and columbite in pegmatites samples of the main body from the Kvartsevoye deposit: (a) massive inclusions of tantalite and columbite grains; (b) tantalite inclusions in albite; (c) contact of tantalite and columbite; (d,e) columbite micrograins in albite; (f) tantalite inclusions in albite.
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Figure 10. 40Ar/39Ar age spectra of muscovites from the Kvartsevoye deposit.
Figure 10. 40Ar/39Ar age spectra of muscovites from the Kvartsevoye deposit.
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Figure 11. Comparison of ages of granite intrusions and rare metal pegmatite deposits in the Kalba–Narym belt [7,14,22].
Figure 11. Comparison of ages of granite intrusions and rare metal pegmatite deposits in the Kalba–Narym belt [7,14,22].
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Table 1. Table with mineral compositions of micas of the Kvartsevoye deposit (ppm).
Table 1. Table with mineral compositions of micas of the Kvartsevoye deposit (ppm).
Rock TypeComponent, wt. %a.p.f.u.
SiO2TiO2Al2O3Cr2O3FeOMnOMgONa2OK2OLi2OFClSumTSiTAlTFe3+MAlMMgMFe2+MTiMCrMMnMLiAKANa
Bt granite
(splAL23-08)		36.673.1417.620.0717.800.338.940.049.450.160.650.0496.712.831.120.050.481.061.130.190.0040.020.050.920.01
36.663.1218.060.0517.940.329.020.169.370.160.600.0497.302.821.150.040.491.061.120.180.0030.020.050.910.02
36.533.3217.630.0617.900.318.890.109.580.160.580.0396.882.821.130.040.471.051.140.200.0040.020.050.930.02
36.463.2217.950.0617.510.348.600.029.410.170.650.0596.172.831.140.040.501.031.140.190.0040.020.050.920.00
36.403.5817.780.0617.460.318.580.119.480.170.570.0396.252.831.150.020.481.031.140.210.0030.020.050.930.02
36.453.2518.100.0717.590.348.860.099.460.160.500.0496.642.811.160.030.491.051.120.190.0040.020.050.920.01
36.643.1017.960.0617.790.348.960.059.540.160.690.0597.122.821.140.040.491.061.130.180.0040.020.050.930.01
36.343.2517.480.0618.090.348.860.079.460.160.320.0496.302.821.120.060.481.061.120.190.0040.020.050.930.01
36.433.0217.960.0717.720.368.960.109.490.160.500.0396.562.811.150.040.481.061.120.180.0040.020.050.930.01
36.033.1417.800.0617.580.368.730.109.560.170.740.0496.092.811.160.030.481.061.150.190.0040.020.050.940.01
Ms mircogranite body
(spl K23-01)		46.790.5231.750.015.340.411.380.168.311.431.660.0097.103.251.300.001.300.001.200.060.0010.020.400.740.02
46.610.4932.490.005.140.371.580.108.541.271.610.0297.713.221.350.001.300.001.200.050.0000.020.350.750.01
46.970.4632.300.015.390.401.320.048.281.481.810.0197.783.241.320.001.310.001.230.050.0000.020.410.730.00
46.070.5332.360.014.610.341.370.228.321.442.100.0196.753.221.370.001.300.001.230.060.0000.020.400.740.03
46.860.4233.250.014.920.371.620.008.481.241.740.0098.423.211.390.001.290.001.210.050.0010.020.340.740.00
46.220.5034.350.004.710.411.630.168.601.241.590.0198.893.161.490.001.280.001.220.050.0000.020.340.740.02
43.870.5034.220.015.050.381.630.008.561.232.240.0197.303.071.600.001.230.021.320.050.0000.020.350.770.00
43.880.4534.370.004.750.381.550.008.501.291.800.0196.473.071.590.001.250.021.290.050.0000.020.360.770.00
44.010.4734.170.015.020.381.540.008.561.302.080.0197.093.081.580.001.240.011.310.050.0000.020.370.770.00
44.760.4533.450.004.960.411.320.048.651.491.840.0096.633.131.490.001.270.001.300.050.0000.020.420.780.01
Greisen (spl AK23-01)48.060.0337.900.011.140.010.460.538.660.070.260.0297.453.221.520.001.480.000.990.030.0000.000.020.710.07
47.200.0337.770.010.970.030.260.458.800.080.290.0196.123.201.540.001.470.001.020.030.0000.000.020.740.06
48.290.0938.150.030.930.050.400.618.770.000.010.0197.563.231.530.001.480.000.960.030.0010.000.000.710.08
47.980.0537.470.001.170.040.440.468.620.070.260.0096.723.231.510.001.470.000.990.030.0000.000.020.720.06
46.980.0639.110.021.040.010.470.458.340.040.160.0096.993.151.650.001.440.001.010.030.0010.000.010.690.06
47.670.0336.720.021.640.070.420.408.210.140.450.0095.873.231.480.001.460.001.000.030.0010.000.040.700.05
47.720.0636.430.001.080.030.580.328.120.150.490.0295.063.251.450.001.470.000.970.040.0000.000.040.690.04
47.270.0539.210.021.250.080.450.448.580.070.280.0197.853.151.650.001.440.001.030.030.0010.000.020.700.06
48.570.0437.940.011.310.040.260.618.560.060.230.0097.823.241.510.001.480.000.980.030.0010.000.020.700.08
Pegmatite of main body (spl Kv23-03)47.440.2037.250.022.060.100.250.449.210.230.660.0198.013.211.530.001.440.001.100.040.0010.010.060.770.06
48.930.1938.100.022.110.090.240.358.770.220.640.0099.853.241.520.001.450.001.070.030.0010.010.060.710.04
46.990.2136.810.012.140.100.320.4310.100.220.650.0198.153.201.520.001.430.001.150.040.0010.010.060.850.06
47.500.1837.230.021.960.080.230.379.450.150.470.0097.853.211.520.001.450.001.100.040.0010.000.040.790.05
47.730.2736.790.022.170.110.300.329.060.190.590.0197.743.231.490.001.450.001.080.040.0010.010.050.760.04
47.260.2136.140.022.490.090.210.449.330.150.480.0197.113.231.460.001.450.001.090.040.0010.010.040.790.06
48.220.1637.570.032.540.150.150.409.380.090.330.0199.393.221.510.001.450.001.080.030.0020.010.020.770.05
47.880.2835.770.012.450.120.330.329.200.180.560.0197.393.261.420.001.450.001.080.040.0010.010.050.770.04
47.920.2137.200.022.070.090.280.369.530.130.420.0198.463.231.500.001.450.001.090.040.0010.000.030.790.05
47.920.2336.510.032.790.110.350.369.290.160.500.0098.583.231.470.001.430.001.090.040.0020.010.040.770.05
Table 2. Contents of rare elements in granites and quartz of Kvartsevoye deposit (ppm).
Table 2. Contents of rare elements in granites and quartz of Kvartsevoye deposit (ppm).
SampleTaNbBeLiRbCsSnWMo
1Kv23-0145.975.265.6150.220425.138.51.66.9
2Kv23-0238.446.58.627.9366.425.81.37.5
3Kv23-057.62.95.831.6111.34.11.16.7
4Q6-243.310.10.69.0746.115.62.47.8
5Q5-245.452.53.88.4475.711.84.24.6
6Kv23-075.37.810.1243.516781.832.72.49.3
7Kv23-083.87.83.2170.98911.226.31.87.6
Note: Results of ICP-MS analyses: 1—microgranite with muscovite; 2—muscovite leucogranite; 3–5—quartz; 6—unaltered medium-grained granite; 7—altered medium-grained granite.
Table 3. Contents of rare elements in pegmatites of the Kvartsevoye deposit (ppm).
Table 3. Contents of rare elements in pegmatites of the Kvartsevoye deposit (ppm).
SampleTaNbBeLiRbCsSnWMo
1Kv23-0328.247.237.1274.748768.8117.02.926.7
2Q5-2472.57.94.3163.461.55.979.250.95.2
3Kv23-048.39.941.71207953.512.679.51.116.7
4Q8-2431.15.41.2910053.56.957.966.95.3
5Kv23-0687.5152.421.37071591209.8421.88.24.8
6Q5-24M59.590.86.74520.1176.7299.152.96.2
7Q1-2435.82.40.88.50.1107.85.138.77.2
8Q2-2434.44.7255.851.20.137.619.341.77.6
Note: Results of ICP-MS analyses: 1–2—garnet–muscovite pegmatite; 3–4—spodumene pegmatite; 5–6—greisen; 7—quartz–albite–microcline pegmatite; 8—beryl-bearing pegmatite.
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Oitseva, T.A.; Khromykh, S.V.; Naryzhnova, A.V.; Kotler, P.D.; Mizernaya, M.A.; Kuzmina, O.N.; Dremov, A.K. Rare Metal (Li–Ta–Nb) Mineralization and Age of the Kvartsevoye Pegmatite Deposit (Eastern Kazakhstan). Minerals 2025, 15, 737. https://doi.org/10.3390/min15070737

AMA Style

Oitseva TA, Khromykh SV, Naryzhnova AV, Kotler PD, Mizernaya MA, Kuzmina ON, Dremov AK. Rare Metal (Li–Ta–Nb) Mineralization and Age of the Kvartsevoye Pegmatite Deposit (Eastern Kazakhstan). Minerals. 2025; 15(7):737. https://doi.org/10.3390/min15070737

Chicago/Turabian Style

Oitseva, Tatyana A., Sergey V. Khromykh, Anna V. Naryzhnova, Pavel D. Kotler, Marina A. Mizernaya, Oxana N. Kuzmina, and Artem K. Dremov. 2025. "Rare Metal (Li–Ta–Nb) Mineralization and Age of the Kvartsevoye Pegmatite Deposit (Eastern Kazakhstan)" Minerals 15, no. 7: 737. https://doi.org/10.3390/min15070737

APA Style

Oitseva, T. A., Khromykh, S. V., Naryzhnova, A. V., Kotler, P. D., Mizernaya, M. A., Kuzmina, O. N., & Dremov, A. K. (2025). Rare Metal (Li–Ta–Nb) Mineralization and Age of the Kvartsevoye Pegmatite Deposit (Eastern Kazakhstan). Minerals, 15(7), 737. https://doi.org/10.3390/min15070737

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