Hydrothermally Altered Rocks of the Kommunar Gold Ore Field (Khakassia)
Abstract Generated abstract
This paper characterizes hydrothermally altered rocks in the Kommunar gold ore field of Khakassia and relates them to stages of postmagmatic and ore-forming activity. Using petrographic observations, chemical comparisons of altered and unaltered rocks, thermometric study of gas-liquid inclusions, aqueous extract analyses, and thermodynamic calculations, the authors distinguish skarns, amphibole metasomatites, and several types of near-ore alteration, including actinolitization, beresitization-listvenitization, and carbonatization. The study outlines mineral assemblages, component migration, inferred solution compositions, and approximate temperature ranges for these processes, from high-temperature skarn formation to lower-temperature carbonate alteration. It concludes that these alteration types can serve as guides for prospecting different forms of gold mineralization in comparable geological settings.
Full Text
Hydrothermally Altered Rocks of the Kommunar Gold Ore Field (Khakassia)
A. F. Korobeinikov, I. P. Shcherban (TPI, IG and G SO AN SSSR)
Within the ore field there are widespread rocks of the gabbro-diorite \((Pt_3—Cm?)\), granodiorite \((Cm_3—O)\), and gabbro-syenite \((D?)\) intrusive complexes, which cut through a diabase-porphyrite and volcanogenic-sedimentary sequence presumably of Upper Proterozoic age [1, 2, 5]. The emplacement of the granodiorite intrusion and its dike series was accompanied by the extensive development of postmagmatic processes, which led to the formation of contact hornfelses, skarns, and various hydrothermal formations. Among these, three principal types may be distinguished, sharply differing from one another in the conditions and time of their manifestation: skarns, amphibolized rocks, and beresite-listvenites.
Skarns
Endoskarns and exoskarns are clearly distinguished. The former arise in place of aluminosilicate rocks and are localized in the endocontact zones of the granodiorite intrusion, while the latter form at the expense of the rocks enclosing this intrusion. In both cases, the spatial distribution of the skarns was controlled by tectonic zones, which were most clearly manifested at the contacts of dissimilar rocks. Skarns most often form lens-shaped and vein-like bodies \((10—200 \times 5—40\ \text{m})\), extending as discontinuous chains along the contacts of the intrusion. The material composition of endo- and exoskarns is highly diverse. The former are usually composed of diopside-augite and grossular. Scapolite, albite, sphene, apatite, and zircon are present in them as accessory minerals. Skarns formed after limestones consist of salite-hedenbergite, diopside, wollastonite, and andradite. In smaller amounts there appear andesine, albite, vesuvianite, tourmaline, hornblende, sphene, and apatite. In separate parts of the endoskarns and especially the exoskarns, a later, in terms of the time of its manifestation, association of metasomatic and hydrothermal minerals is superimposed, represented by magnetite, pistacite, tremolite, actinolite, chlorite, prehnite, quartz, calcite, chabazite, pyrite, chalcopyrite, and gold. On the basis of the quantitative ratios of the principal rock-forming minerals, wollastonite, pyroxene, garnet, and garnet-pyroxene skarns may be distinguished.
A study of the chemical compositions of unaltered rocks and rocks skarned to varying degrees indicates significant migration of a number of components during this process. From aluminosilicate rocks there is removal of silica and aluminum and introduction of calcium into them, while from carbonate rocks there is removal of calcium and introduction of silica and aluminum [2]. In the subsequent ore stage, iron probably underwent considerable movements of a local nature, which may in some cases have caused the formation of small magnetite deposits. In general, the formation of skarns proceeded by infiltration, with a subordinate role of bimetasomatic phenomena.
In order to determine the temperatures of formation and the composition of the skarn-forming solutions, thermometric studies of gas–liquid inclusions in skarn minerals and chemical analyses of aqueous extracts from them were carried out. For analyses of aqueous extracts, samples of minerals and rocks with a volume of 70 cm³ were prepared. The samples were then ground in air in distilled water to a grain size of 0.08 mm and placed in flasks with 300 ml of bidistillate for 0.5–48 hours. At the same time, the pH of suspensions and aqueous extracts was measured on an LP-5 potentiometer with a glass electrode. The results obtained make it possible to conclude that the solutions contained appreciable amounts of Ca, Si, Mg, Fe, CO₂, and, to a lesser degree, Cl, F, H₂S; their temperature varied from 630 to 460° (Tables 1, 2). To judge the temperature conditions of formation of calcareous skarns, the reaction of wollastonite formation from calcite and quartz, which has been well studied by calculation and experimental methods, may also be used additionally [6]: CaCO₃ + SiO₂ ⇄ CaSiO₃ + CO₂ (1). According to calculations, reaction (1) may proceed from left to right in the temperature interval from 400 to 600°C, depending on the partial pressure of CO₂ in the mineral-forming system.
The relative time of skarn formation is determined by the fact that they are superimposed on hornfelses, alkaline metasomatites, and rocks of the dike series of the granodiorite complex, and are themselves subjected to later processes of magnetite mineralization, amphibolization, and carbonatization [2, 3]. These facts indicate that, among the metasomatic formations, the skarns are among the earliest in the time of their manifestation, apart from the early albitites and scapolitites [2].
Amphibole Metasomatites
The appearance of amphibolized rocks is associated with the next stage of postmagmatic mineral formation (the stage of magnetite ore formation). They form sheet-like, lens-shaped bodies that fringe skarn–magnetite lenses, or nest-like deposits in the skarns. The extent of zones of amphibolized rocks is several tens, more rarely hundreds, of meters. The thickness of such bodies rarely exceeds several tens of meters. Like the skarns, the amphibole metasomatites are controlled by longitudinal fractures with associated fine fracturing of the rocks of the exocontact aureole of the granodiorite intrusion. The process of amphibolization develops both in limestones and in aluminosilicate rocks (plagioclase–pyroxene hornfelses and pyroxene skarns). In the first case, tremolite is formed predominantly, and in the second, actinolite.
Amphibolized hornfelses differ from the original rocks by lower density and a darker color, with greenish tones predominating. Initially the amphiboles replace pyroxenes, and then corrode feldspars, this process being accompanied by the formation of-
by magnetite, sphene, calcite, and epidote. After actinolite, in turn, pennine sometimes develops, with needles of rutile and accumulations of sphene. Along with secondary amphibole, one or another amount of secondary quartz is recorded in the rocks. During amphibolization of skarns, actinolite develops after pyroxenes and also often replaces aggregates of garnet and magnetite, in the form of nests and lens-shaped bodies. In amphibolized limestones, tremolite occurs in the form of radiating and matted-fibrous aggregates, sometimes composing rather extensive lens-shaped deposits.
Comparison of chemical analyses of the original and amphibolized aluminosilicate rocks showed that, as a result of this process, there is an introduction of magnesium and calcium and removal of aluminum, iron, and sodium [2].
Decrepitometric data and chemical analyses of aqueous extracts of gas–liquid inclusions in amphiboles give grounds to suppose that their formation proceeded from solutions containing Ca, Mg, Fe, Cl, F, CO₂, and Al, at temperatures of 480–270°C (Tables 1, 2).
To judge the thermodynamic conditions of the amphibolization process, the results of calculations of the reactions of tremolitization of diopside and silicified dolomite may additionally be used:
$$ \mathrm{CaMgSi_2O_6 + 3CO_2 + H_2O \rightarrow Ca_2Mg_5Si_8O_{22}(OH)_2 + CaCO_3 + 2SiO_2} \tag{2} $$
$$ \mathrm{CaMg(CO_3)_2 + 8SiO_2 + H_2O \rightleftarrows Ca_2Mg_5Si_8O_{22}(OH)_2 + 3CaCO_3 + 2SiO_2} \tag{3} $$
The method for calculating reactions of this kind is considered in detail in special works [6, 9]. The calculation results showed that the process of tremolitization proceeded in a fairly narrow temperature interval, which was 150–275°C at a partial pressure of CO₂ approaching 0, and 400–525°C at 1000 atm, etc. (Figs. 1, 2). On the whole, taking into account existing concepts regarding pressures in hydrothermal solutions and the concentrations of CO₂ in them, the temperature interval of 350–450°C may be considered the most probable for the process under consideration.
In terms of the time of its manifestation, the process of formation of amphibolized rocks is later than skarn formation, which is confirmed by the facts that skarns are cut by zones of metasomatic amphibolites and by the replacement of skarn minerals by actinolite and tremolite.
Near-Ore Altered Rocks
Among them, three different-temperature types are distinguished: 1) high-temperature veinlet–actinolite, accompanying stockwork gold–quartz ores; 2) medium-temperature beresite–listvenite, accompanying quartz–gold–scheelite and quartz–gold–sulfide veins; and 3) low-temperature carbonate, accompanying calcite–quartz–gold–chlorite ores.
Manifestations of a distinctive actinolitization are observed among uralitized gabbro-diorites, porphyrites, dike lamprophyres, skarn–magnetite lenses, and accompany veinlet gold–quartz ores. Usually, actinolitized rocks form linear bodies bordering gold-ore veins, or, at the intersections of such veins, compose stockworks or nest-like deposits. Initially, amphibole replaces the dark-colored components of the rock, and then begins to corrode the feldspars, which ultimately leads to the appearance of nearly monomineralic actinolite aggregates. In addition to actinolite, quartz, magnetite, albite, apatite, and sphene sporadically appear in the altered rock. The distribution of hydrothermal
Fig. 1. Equilibrium curves for the tremolitization reaction of diopside in temperature–pressure coordinates (according to thermodynamic calculations)
Fig. 2. Equilibrium curves for the tremolitization reaction of silicified carbonate rocks in temperature–pressure coordinates (according to thermodynamic calculations; thermochemical constants are taken from the books by V. A. Nikolaev and V. V. Dolivo-Dobrovolsky, 1961)
the amphibole in space, like the gold-ore mineralization, is controlled by the predominant fracturing in the rock. The relationships between the gold–quartz veinlets and the actinolitized rocks show that the near-ore amphibolization precedes the formation of the gold–quartz veins [4].
The study of the material balance during hydrothermal metasomatism
showed that the formation of actinolitized rocks took place from solutions of chloride–magnesium–sodium composition. At the same time, Al, Na, and K were initially removed from the wall rocks, while Mg, Ca, and Fe were introduced [2, 4]. In the final period of near-fracture metasomatism, alkalis and especially sodium probably accumulated in the solutions, which ultimately led to locally manifested albitization of the rocks.
Thermometric data on vein quartz and actinolite, and the composition of aqueous extracts from them (Table 2), make it possible to assume that the temperature of the hydrotherms varied from 380 to 240°C, and that the solutions carried Si, Mg, Al, Fe, Cu, Au, Ag, Na, Cl, F, and, in part, CO₂ and H₂S. Evidently, the high potential of magnesium, iron, and chlorine in the early portions of the solutions caused intense actinolitization of the wall rocks.
A review of the literature data showed that the processes of pre-ore amphibolization of ore-hosting rocks may have a rather wide distribution, although due attention has not yet been paid to the near-ore character of these transformations. This circumstance prompted us to consider the actinolitization of gold-bearing rocks as a special high-temperature type of near-ore alteration [4].
Berezites, like actinolitized rocks, form near-vein halos in zolbands of quartz veins composed of quartz–gold–scheelite and quartz–gold–sulfide material. Zones of beresitization affect the near-ore actinolitization in gabbro-diorites and diorites and, at the same time, are themselves cut by quartz–gold–sulfide veinlets. On this basis, the process of beresitization is assigned to the next stage of hydrothermal metamorphism, preceding the formation of quartz–gold–scheelite and quartz–gold–sulfide ores [2]. Petrographic observations show that, in the process of beresitization, the original rocks undergo deep transformations, as a result of which the primary minerals are almost completely replaced by muscovite, carbonate, pyrite, quartz, and chlorite. Muscovite usually develops after plagioclases; in cases of the deepest transformation of the rocks it also replaces the mafic components. The amount of muscovite in the rock reaches 15–35%. The second most important mineral of the beresites (up to 45–60%) is carbonate, which, in association with quartz and chlorite, replaces both feldspars and mafic minerals. By optical properties, dolomite, calcite, and ankerite are determined rather clearly. Heating curves of carbonate fractions preliminarily separated from the beresites indicate that the carbonates included in these rocks are a mixture of dolomite and calcite (endothermic effects at temperatures of 850–880° and 900–925°C). Pyrite is also widespread; its cubic crystals not infrequently make up 6–17% of the total volume of the rock, and sometimes more.
Chemical analyses of the original and beresitized rocks indicate that, during the process of beresitization, there is an introduction of Si, K, CO₂, to a lesser degree Na, and removal of the remaining petrogenic elements, with their partial redistribution in the mineral-forming system [2, 3]. During this period, the hydrotherms were probably characterized by an alkaline–hydrocarbonate–hydrogen-sulfide–chloride composition.
Thermometric data on gas–liquid inclusions in minerals from gold-ore bodies accompanied by beresitization, and analyses of aqueous extracts from them, indicate that the temperature of the solutions
Table 1.
Results of analyses of aqueous extracts, decrepitation and homogenization temperatures of gas–liquid inclusions in minerals of the Kommunar ore field
| Mineral name | pH of suspension | pH of aqueous extract | Cl | S (sulfide) | CO₂ | SO₄ | HCO₃ | Ca + Mg | Fe²⁺ | Decrepitation T, °C | Homogenization T, °C |
|---|---|---|---|---|---|---|---|---|---|---|---|
| Contact-metasomatic formations: | |||||||||||
| Diopside from endoskarns | 9.5 | 7.1 | 10.1 | — | 1.60 | 0.30 | 22.0 | 8 | — | 560 | |
| Grossular No. 23—25 from endoskarns | 8.0 | 7.0 | 8.5 | — | 1.58 | — | 29.28 | 4 | — | 460—530 | |
| Magnetite from a skarn–magnetite lens | 9.2 | 7.1 | 4.2 | — | 1.62 | — | 29.0 | 6 | — | 410—520 | |
| Epidote from nests in garnet endoskarns | 8.7 | 7.4 | tr. | — | 1.78 | — | 36.6 | 6 | — | 370—510 | |
| Tremolite from amphibole metasomatites | 9.7 | 7.5 | 1.8 | — | 1.60 | 4.8 | 36.9 | 7 | — | 300—500 | |
| Metasomatic chlorite | 9.2 | 7.2 | 6.4 | — | 1.50 | — | 21.96 | 4 | — | 270—430 | |
| Hydrothermal formations: | |||||||||||
| Quartz I from quartz–pyrrhotite veins | 8.3 | 6.6 | 1.3 | — | 1.50 | — | 19.2 | 6.0 | — | 420—460 | 340 |
| Quartz II from gold–quartz veins | 8.7 | 6.9 | 4.26 | — | 1.55 | — | 6.2 | — | 240—380 | 300—360 | |
| Quartz III from quartz–gold–sulfide veins | 7.8 | 6.7 | 2.13 | tr. | 1.50 | — | 0.6 | 4.8 | — | 240—310 | 210—310 |
| Quartz IV from barren quartz–sulfide veins | 9.1 | 7.4 | 6.4 | — | 1.60 | — | 22.0 | 0.4 | — | 300—320 | 220—280 |
| Quartz–calcite–ankerite aggregate | 9.4 | 7.4 | 0.5 | — | 1.50 | — | 36.1 | 0.3 | 120—220 | 120—200 | |
| Quartz–prehnite aggregate | 9.0 | 7.2 | tr. | tr. | 1.53 | 3.1 | 35.1 | 0.8 | — | 110—140 | |
| Barite | 8.4 | 7.3 | tr. | — | 1.58 | 1.28 | 22.0 | tr. | 0.3 | 140 | |
| Actinolitized gabbro-diorite | 8.8 | 6.9 | 14.4 | — | 5.0 | — | — | 20.0 | — | ||
| Albitized gabbro-diorite | 8.8 | 7.1 | 11.6 | — | 5.0 | — | — | 16.3 | — | ||
| Beresitized gabbro-diorite | 9.4 | 7.6 | 3.6 | — | 5.3 | 6.9 | 29.2 | 31.7 | — | ||
| Carbonatized gabbro-diorite | 9.1 | 7.2 | 3.2 | — | 7.8 | — | — | 24.2 | — | ||
| Unaltered gabbro-diorite | 8.9 | 7.3 | 1.3 | — | 1.5 | — | — | 4.8 | — |
Measurements of the pH of mineral suspensions and chemical analyses of aqueous extracts were carried out in the hydrogeochemical laboratory of the Tomsk Polytechnic Institute. The pH of the distilled water in the experiments was 6.5.
Optical and chemical properties of metasomatic minerals of the Kommunar ore field
Table 2.
| Mineral name | Ng | Nm | Np | Ng − Np | 2V | cNg | Chemical composition and other properties |
|---|---|---|---|---|---|---|---|
| Diopside-augite from endoskarns | 1.710 | 1.686 | 1.678 | 0.032 | +59 | 41° | \((Ca_{0.85}Mn_{0.03}Fe^{+2}_{0.16})_{1.02}(Mg_{0.67}Fe^{+3}_{0.17}Al_{0.05})_{0.89}(Si_{1.88}Ti_{0.02}Al_{0.10})_{2}O_{6}\). |
| Diopside-augite from endoskarns | 1.715 | 1.689 | 1.682 | 0.033 | |||
| Diopside from exoskarns | 1.693 | 1.668 | 0.025 | +48 | 38–41° | \((Ca_{0.94}Na_{0.02}K_{0.01}Fe^{+2}_{0.04})_{1.01}(Mg_{0.89}Fe^{+3}_{0.14})_{1.03}(Si_{1.96}Al_{0.04})_{2}O_{6}\). | |
| Diopside from exoskarns | 1.701 | 1.674 | 0.027 | +57 | 39 | ||
| Salite from exoskarns | 1.730 | 1.697 | 0.035 | +60 | 45 | Up to 55% hedenbergite molecule. | |
| Hedenbergite from exoskarns | 1.748 | 1.728 | 1.720 | 0.028 | +60 | 45 | Up to 80% hedenbergite molecule. |
| Wollastonite from exoskarns | 1.752 | 1.730 | 1.721 | 0.031 | \(Y = c = 3.56\) (determined goniometrically). | ||
| Light-green garnet from endoskarns | 1.633 | 1.620 | 0.013 | −38 | 43 | Up to 6% hedenbergite molecule. | |
| Light-green garnet from endoskarns | 1.744 | \((Ca_{2.7}Na_{0.05}K_{0.04}Mn_{0.03}Fe^{+2}_{0.03})_{2.85}(Al_{1.62}Fe^{+3}_{0.38}Ti_{0.01})_{2.01}Si_{3.02}O_{12}\). | |||||
| Red-brown garnet from endoskarns | 1.787 | \((Ca_{2.8}Na_{0.02}K_{0.02}Mn_{0.03}Fe^{+2}_{0.04})_{2.91}(Al_{1.38}Fe^{+3}_{0.67})_{2.05}Si_{3}O_{12}\). | |||||
| Light-brown garnet from exoskarns | 1.780 | \(a_{0}=11.898 \pm 0.007\ \mathrm{kX}\). | |||||
| Epidote metasomatic | 1.767 | 1.725 | 0.042 | −79 | 2–8 | \((Ca_{2.88}Mn_{0.66}Mg_{0.02})_{2.96}(Al_{1.3}Fe^{3}_{0.76})_{2.06}(Si_{2.98}Ti_{0.01})_{2.99}O_{12}\). | |
| Tremolite metasomatic | 1.627 | 1.612 | 0.015 | −82 | 16 | \((Ca_{1.88}Mn_{0.01}Na_{0.02}K_{0.01})_{1.92}(Al_{0.61}Mg_{0.08}Fe^{+2}_{0.21}Fe^{+3}_{0.75})_{2.65}(Si_{2.8}Ti_{0.04}Al_{0.09})_{3}O_{12}(OH)_{0.84}\). | |
| Actinolite from nests in endoskarns | 1.667 | 1.646 | 0.021 | −78 | 15 | \((Ca_{2.18}Na_{0.03}K_{0.02}Mn_{0.05}Fe^{+2}_{0.16}Fe^{+3}_{0.19}H_{3}O_{0.42})_{3}Mg_{5.05}Si_{7.93}Al_{0.07})_{8}O_{22}(OH)_{0.57}O_{1.43}\). | |
| Ferroactinolite from exoskarns | 1.714 | 1.692 | 0.022 | −64 | 15 | Sp. gr. 3.23; FeO 50% of the hedenbergite molecule. | |
| Actinolite, hydrothermal, from near-ore amphibolized rocks | 1.670 | 1.665 | 1.655 | 0.015 | −62 | 14 | Pleochroism: \(Ng\)—bluish green, \(Np\)—pale yellow-green. |
| Actinolite, hydrothermal, from near-ore amphibolized rocks | 1.673 | 1.667 | 1.657 | \((Ca_{2.2}H_{3}O_{0.8})_{3}(Mg_{1.38}Fe^{+2}_{3.18}Fe^{+3}_{0.21}Ti_{0.01}Al_{0.23})_{5}(Si_{7.92}Al_{0.08})_{8}O_{22}\cdot(OH)_{1.5}Cl_{0.04}F_{0.03})_{1.4}O_{0.6/2.0}\). | |||
| Chlorite metasomatic | 1.585 | 1.580 | 0.005 | −3–7 | \((Si_{3.38}Al_{0.41}Fe^{3}_{0.21})[Al_{1.13}(Fe^{2}_{0.59}Mg_{3.21}Ca_{0.34})]_{5.27}(OHCl)_{8}O_{10}\cdot0.35H_{2}O\). | ||
| Muscovite from beresites | 1.587 | 1.557 | 0.040 | −3–5 | Up to 10–25% hedenbergite molecule. | ||
| Muscovite from beresites | 1.608 | 1.565 | 0.043 | ||||
| Calcite from beresites | 1.666 | 1.491 | 0.175 | Up to 5% molecule. | |||
| Ankerite from beresites | 1.722 | 1.520 | 0.202 | Up to 25–27% molecule. | |||
| Dolomite from beresites | 1.678 | 1.502 | 0.176 | Magnesiodolomite. | |||
| Calcite from the carbonation zone | 1.660 | 1.485 | 0.175 | Up to 5% molecule. |
varied from 280 to 180°C. The hydrothermal solutions contained Ca, Si, Mn, Sr, Au, Ag, Cu, CO₂, HCO₃, and, to a lesser extent, H₂S (Tables 1, 2).
Thermodynamic calculations of some listvenitization reactions, which are an analogue of the beresitization process developing, in contrast to the latter, in ultrabasic rocks, indicate that the upper temperature limit of these processes may be taken as 200–300°C. Experimental data confirm the results of the calculations [7, 8].
Summarizing the data presented, it may be concluded that the beresitization process proceeded at temperatures of about 220–300°C.
The final process in the hydrothermal alteration of the rocks was carbonatization, which was most widely manifested in gabbro-diorites containing calcite–quartz–chlorite gold-bearing mineralization. Carbonates (calcite and, more rarely, ankerite) usually develop after plagioclases and dark-colored minerals of the rock, in places almost completely replacing them, and contain only chlorite, sericite, albite, and pyrite as impurities. In the character of its manifestation, carbonatization approaches the process of beresitization and, considering that it completes the hydrothermal process in the ore field, the temperatures at which this process occurred may be assumed to lie within 180–220°C.
In addition to the named processes of hydrothermal mineral formation, products of albitization, epidotization, and chloritization of the ore-hosting rocks have been established in the ore field. These processes, however, were very poorly developed and therefore are not considered separately here.
In conclusion, it should be noted that the identified types of hydrothermally altered rocks may be used in prospecting for a certain type of gold mineralization both in the area described and in other gold-bearing areas similar in geological-structural setting.
REFERENCES
-
G. A. Ivankin, I. I. Koptev, V. E. Nomokonov, V. A. Shipitsyn. On the stratigraphy of the ancient strata of the eastern slope of the Kuznetsk Alatau. Materials on Mineralogy, Petrography, and Useful Minerals of Western Siberia and Krasnoyarsk Krai. TSU Press, 1965.
-
A. F. Korobeinikov. Contact-metasomatic and hydrothermal formations of the Kommunar gold-ore field. In: Problems of the Geology of Gold Deposits of Siberia. Tomsk University Press, 1968.
-
A. F. Korobeinikov. Postmagmatic alteration of rocks of the dike complex of the Kommunar gold-ore field (Khakassia). Izvestiya of the Tomsk Polytechnic Institute, vol. 135, 1965.
-
A. F. Korobeinikov. A new type of near-ore alteration of rocks in the Kommunar gold-ore field. Doklady of the Academy of Sciences of the USSR, vol. 182, no. 4, 1968.
-
A. A. Mossakovskii. Tectonic Development of the Minusinsk Depressions and Their Mountain Framing in the Precambrian and Paleozoic. Gosgeoltekhizdat, 1963.
-
V. A. Nikolaev, V. V. Dolivo-Dobrovolskii. Fundamentals of the Theory of Processes of Magmatism and Metamorphism. Moscow, Gosgeoltekhizdat, 1961.
-
B. I. Omelyanenko. Physicochemical conditions of the processes of near-ore alteration of the beresitization type. In: Metasomatism and Other Problems of Physicochemical Petrology. Moscow, Nauka, 1968.
-
I. P. Shcherban. On the temperatures of formation of quartz-dolomite and quartz-magnesite rocks. In: Mineralogical Thermometry and Barometry, vol. II. Moscow, Nauka, 1968.