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GEODYNAMICS & TECTONOPHYSICS
PUBLISHED BY THE INSTITUTE OF THE EARTH'S CRUST SIBERIAN BRANCH OF RUSSIAN ACADEMY OF SCIENCES
ISSN 2078-502X
2016 VOLUME 7 ISSUE 1 PAGES 105-118
http://dx.doi.org/10.5800/GT-2016-7-1-0199
Charoite. Experimental studies
M. V. Marchuk, V. Ya. Medvedev, L. A. Ivanova, T. S. Sokolova, B. S. Danilov, D. P. Gladkochub
Institute of the Earth's Crust, Siberian Branch of RAS, Irkutsk, Russia
Abstract: The article provides an overview of experimental studies of charoite and charoite-containing rock formation hypotheses. The authors conducted experiments to clarify charoite and host rocks interaction and study charoite transformation processes at high temperatures. A series of experiments was aimed at improving the substandard charoite samples. The experiments show the formation of polymineral reaction zones due to the contact interaction between charoite and microcline-arfvedsonite lamprophyre. By studying the newly formed phases, the authors reveal the distribution of elements by phases and establish their compositions. It is shown that thermal decomposition of charoite leads to the formation of wollastonite, which amount increases with the temperature increase from 800 to 1000 °C, and heating above 1200 °C leads to the formation of pseudowollastonite. The physicochemical simulation of charoite decomposition under the specified temperatures and pressure shows the following paragenesis: quartz, wollastonite, alkaline pyroxene (aegerine), microcline, rhodonite, and sphene.
The experiments prove the formation of charoite at low temperatures and the lack of silicate melt in the systems studied. The calculated values are consistent with the results of experiments conducted to study the charoite and host rocks interaction, which allows identifying phases potentially co-existing with wollastonite.
Special studies using by the coloring technique were conducted to improve the decorative properties of charoite. The color close to natural high-grade charoite coloration was achieved by keeping the rock samples in the active bright purple dye 4KT solution for 72 hours at a temperature of 70 to 90 °C.
Key words: charoite; Murun alkaline massif; experiment; fluid systems; physicochemical simulation; treatment
Recommended by E.V. Sklyarov
For citation: Marchuk M.V., Medvedev V.Ya., Ivanova L.A., Sokolova T.S., Danilov B.S., Gladkochub D.P. 2016. Charoite. Experimental studies. Geodynamics & Tectonophysics 7 (1), 105-118. doi:10.5800/GT-2016-7-1-0199.
Чароит. Экспериментальные исследования
М. В. Марчук, В. Я. Медведев, Л. А. Иванова, Т. С. Соколова, Б. С. Данилов, Д. П. Гладкочуб
Институт земной коры СО РАН, Иркутск, Россия
Аннотация: Приведен обзор экспериментальных исследований чароита в России и в мире. Рассмотрены гипотезы формирования чароитовых пород. Для выяснения характера взаимодействия чароитового субстрата с вмещающими породами и исследования процессов преобразования чароита при повышенных температурах проведен ряд экспериментов. Кроме того, изучены возможности повышения сортности некондиционных
чароититов. При экспериментальном исследовании контактового взаимодействия чароитового субстрата с лампрофиром микроклин-арфведсонитового состава установлено образование реакционных полиминеральных зон. Исследование новообразованных фаз позволило изучить распределение элементов по фазам и получить их составы. Показано, что при термическом разложении чароита происходит его преобразование в вол-ластонит, количество которого увеличивается с ростом температуры от 800 до 1000 °С, при нагревании выше 1200 °С образуется псевдоволластонит. Согласно проведенному физико-химическому моделированию разложения чароита, из различных составов минерала при заданных температурах и давлении образуется следующий парагенезис: кварц, волластонит, щелочной пироксен (эгирин), микроклин, родонит и сфен.
Проведенные эксперименты подчеркивают низкотемпературный характер чароитообразования и показывают отсутствие силикатного расплава в исследованных системах. Результаты расчетов согласуются с проведенными экспериментами по взаимодействию чароита с вмещающими породами и его отжигу и позволяют определить возможные сосуществующие с волластонитом фазы.
Исследования по улучшению декоративно-художественных свойств чароититов методом окрашивания показали, что для получения окраски чароититов, близкой к окраске высокосортных природных образцов, требуется выдержка образцов в растворе активного ярко-фиолетового красителя 4КТ при длительности 72 ч и температуре 70-90 °С.
Ключевые слова: чароит; Мурунский щелочной массив; эксперимент; флюидные системы; физико-химическое моделирование; облагораживание
1. Introduction
Charoite is a unique mineral called "the lilac miracle of Siberia" [Rogova et al., 2013]. It is considered "the main mineralogical discovery of the second half of the 20th century" [Solyanik et al., 2008]. This rare gemstone has become widely known and recognized in the global market of ornamental stones due to its aesthetic and processing properties, such as unique lilac to purple coloration, structural features and high strength. The only currently known charoite deposit is Sirenevyi Kamen' (Lilac Stone) located in the Murun alkaline massifs in the northwestern part of the Aldan Shield at the border of the Irkutsk region and Yakutia (Russian Federation) (Fig. 1). Reportedly, charoite has been recently discovered in the marine sediment of Kalpak-kam, the southeast coast of India [Deepthi et al., 2015].
The Sirenevyi Kamen' deposit includes both cha-roite and charoite-containing rocks, as well as eluvial boulders of charoite [Bondarenko, 2009]. The charoite composition is (K, Sr, Ba, Mn)i5-i6(Ca, Na)32[(Si7o(O, OH)i8o)](OH, F)4-nH2O, and its structure is highly complex [Rozhdestvenskaya et al., 2010]. The main charoite chemical components are K, Na, Ca, Si, and H2O; the secondary components are Ba, Sr and Mn; the presence of traceable amounts of Fe, Mg Al, Ti, Zr and Th is noted. Charoite is an alkaline calcium silicate with tubular Si-O-radicals. Its crystalline structure is quite specific, like that of other minerals of this group (kanasite, tinaksite, frankamenite, mizerite etc.) discovered in the Murun charoite mineralization field. Over 50 minerals are closely associated with charoite, and the latter does not occur in nature in its "pure" form [Konev et al., 1996; Solyanik, 2004; Vorobjev, 2008].
The geological structure of the Murun massif and a wide variety of rare and unique formations are factors contributing to the inconsistency of scientific views on the charoite mineralization origin. Today opinions differ on the conditions and mechanisms of the formation of charoite rocks [Bulakh, 1984; Biryukov, Berdnikov, 1993; Evdokimov, 1995; Konev et al., 1996; Mitchell, 1996; Vladykin, 2000, 2009; Reguir, 2002; Vorobjev, 2008]. It is assumed that the Murun massif was formed in the unstable tectonic conditions [Konev et al., 1996], as evidenced by numerous dykes of varied composition and strong foliation of igneous rocks. At the same time, there was a lack of tectonic control during the formation of the charoite field, and the charoite bodies intruded and dissected other rocks. However, conformable bedding of charoite veins and veinlets is also common. Probably, the intrusion of fluidized melt may be accompanied by shock decompression of the melt [Medvedev et al., 2014] and the formation of structures typical for torgolite disintergration. Some researchers support the hypothesis of the metasomatic origin of charoite in the exocontact halo of the Malomurun alkaline massif under the influence of fluids enriched with Sr, Ba, Mn, F, CO2, and alkalis [Biryukov, Berdnikov, 1993; Vorobjev, 2008; Bondarenko, 2009]. The metaso-matic origin is viewed as a result of the interaction between the fluidized melt and the host rocks of different compositions, or the interaction between hydrothermal solutions and the host rocks, or the interaction between alkaline intrusions and carbonate host rocks. There is a hypothesis about the initial fluidized melts [Konev et al., 1996], which assumes that charoite is similar to pegmatites in the morphology of the veins, mineralogical diversity, large- and giant-grain struc-
Fig. 1. The Sirenevyi Kamen' deposit location map (marked by the lilac circle).
Рис. 1. Схема района расположения месторождения «Сиреневый камень» (отмечено сиреневым кружком).
ture, and relationships with the host rocks. According to [Vladykin, 2000] charoite is formed by the fractionation of the alkali melt. In [Vorobjev, 2008], the genesis of charoite is also considered as a combination of magmatic and metasomatic processes. Some researchers propose charoite and its paragenetic minerals can be classified as late-stage hydrothermal minerals. It is assumed that charoite, being formed in potassium-rich environments, is an equivalent of high-sodium silicates of late-stage mineral associations [Bulakh, 1984; Bori-sov, 1985; Evdokimov et al., 1985].
So, the challenge of the charoite formation involves a number of genetic problems, such as initial magma composition determining, magma crystallization and differentiation mechanisms, features of certain rocks types genesis in Murun alkaline complex and others. The wide complex of geochemical, mineralogical and other methods is employed in studies aimed at solving these problems, and an important component of such studies is thermodynamic simulation using experimental methods.
2. Experimental studies review
Systematic experimental studies of charoite have been limited recently both in Russia and abroad due to a number of reasons, including the fact that the genesis of charoite mineralization remains unclear, and the
charoite rocks chemical composition and structure are unique. The concretion and intergrowth of pheno-cryst minerals [including quartz, microcline, aegerine, tinaksite, frankamenite, arfvedsonite, apophyllite etc.) are common in charoite, and experiments with a pure charoite material are thus challenging.
Termobarogeochemical studies conducted in the 1980s suggested the charoite rock crystallization from the residual melt fluid at temperatures ranging from 400 to 750 °C [Lazebnik et al, 1977]. The study of inclusions in charoite rocks was conducted by A.A. Bo-rovikov at the Institute of Geology and Mineralogy, SB RAS, and revealed the charoite crystallization from the melt fluid at a temperature of about 800 °C. However, these results require confirmation by studies engaging the most typical charoitite morphological varieties in the system.
The temperature of the dehydration reaction of charoite was established by the thermogravimetric analyses reported in [Lazebnik et al., 1977; Matesanz et al., 2008; Foldvári, 2011] - thermograms clearly show two endothermal effects in the temperature ranges from 210 to 480 °C and 940 to 960 °C, when charoite loses water [the water content may amount to 5 wt. %) [Foldvári, 2011]. The first temperature range is typical of the samples with high water contents, the second is the same for all the samples. According to [Lazebnik et al., 1977], these effects are due to the fact that the charoite samples contain water of three types: molecular water with strong intermolecular bonds, molecular water with weak intermolecular bonds, and loosely bound hydroxyl groups. Molecular water with weak intermolecular bonds is removed from charoite when it is heated to 300 °C, and the remaining water is removed in the temperature range from 900 to 1000 °C during the structural destruction of the mineral [Konev et al, 1996].
According to [Janeczek, 1991], the charoite structure was destroyed at a temperature of 970 °C, and only a crystalline phase - wollastonite - was diagnosed by the high-temperature X-ray method at 1000 °C. The formation of charoite was simulated in the experiments described in [Zaraisky, 2007] - the rock samples from the Malomurun massif [quartzite sandstone, dolomite, quartzite-richterite, and aegerine-K-feldspar fenite) were treated by alkaline solutions of potassium at T=550 °C and P=1 kbar. The experiments show that charoite does not form in dolomites, quartzite-richterite rocks and fenites. A mineral similar to charoite was obtained in the paragenesis with aegirine and potassium feldspar due to the experiment with the host quartzite sandstone in the alkaline solution containing K, Na, Ca, Ba, Sr, Fe, Al, Fe, Mn, F, and CO2.
Charoite stability conditions depending on the chemical composition of the mineral-forming environment were studied by D.S. Glyuck [Vorobjev, 2008] in expe-
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Irkutsk
Fig. 2. The charoite melt and lamprophyre interaction contact zone. The sample was mined from the Staryi site.
Thin section; parallel nicols; the viewing field size is 7.2x4.8 mm. 1 - lamprophyre (arfvedsonite + microcline); 2 - aegerine; 3 - micro-dine; 4 - charoite interbedded with apophyllite; 5 - charoite.
Рис. 2. Контактовая зона взаимодействия чароитового расплава с лампрофиром в образце с участка «Старый».
Шлиф, николи параллельны, поле зрения 7.2x4.8 мм. 1 - лампрофир (арфведсонит + микроклин); 2 - эгирин; 3 - микроклин; 4 - чароит с прослоями апофиллита; 5 - чароит.
riments conducted in specific isothermal-isobaric conditions (T=550 °C; P=1 kbar). In all the experiments, silicate melt was formed. However, neither the alkali concentration nor the composition of the mixture used in the experiments were published, and a description of the silicate melt composition was not provided.
A number of studies [Konev et al., 1996; Vorobiev, 2008] considered the successive transformation of host rocks xenoliths in charoitites. It was assumed this interaction has an effect on charoite rocks. It was noted at a temperature of 500 °C and a pressure of 1 kbar, a reaction rim was formed only in high alkalinity conditions. Such a transformation is evidenced by a sample from the Staryi (Old) site of the Sirenevyi Kamen' deposit. The sample shows charoite and lamprophyre contact and the reaction zone of the rocks. The contact zone looks as follows: lamprophyre (arfvedsonite + microcline) - aegerine - microcline - charoite interbedded with apophyllite - charoite (Fig. 2).
Such interactions raise a number of questions: what was the range of temperatures and pressures when the process was carried out, what was the fluid regime, and whether there was a charoite melt or melts of other compositions in this case.
3. Experimental study of the charoite stability in various T-P conditions and the charoite and host rocks interaction
Our study is focused on the high temperature cha-roite transformation, and the charoite and host rocks interaction. Our experiments are conducted using samples of charoite (with microcline and quartz impurities) and potassium K-feldspar-amphibole lampro-phyre from the Staryi site of the Sirenevyi Kamen' deposit. Average chemical compositions of the initial samples are specified in Table 1.
Charoite transformation at high temperatures is studied in the experiments by heating the samples to temperatures from 800 to 1200 °C (at intervals of 50 °C) at the atmospheric pressure. The charoite samples (length up to 15 mm, and thickness from 2 to 5 mm) are put into microcrucibles made of aluminum oxide (or zirconium oxide in high-temperature experiments above 1200 °C), placed in the high-temperature furnace to be heated to the specified temperature, and kept for one hour in the specified conditions. Afterwards, the samples are tempered in air, for three minutes from 1200 to 400 °C, and for seven minutes from 400 to 100 °C.
Table 1. Average compositions of original samples
Таблица 1. Средний состав исходных образцов
Charoite substance Lamprophyre Charoite substance Lamprophyre
wt. % wt. % ppm ppm
SiO2 73.22 60.51 V 40 506.7
TiO2 0.02 0.52 Cr 7 219
AI2O3 0.54 6.32 Ni 7 158.8
Fetotal 0.17 4.78 Cu 160 690.6
MnO 0.13 0.18 Zn 53 94.3
MgO 1.84 11.22 As 21 105.5
CaO 16.10 3.88 Y 60 15.7
SrO 0.47 0.13 Zr 55 6.9
BaO 2.02 0.04 La 231 34.7
Na2O 3.90 1.91 Ce 394 41.1
K2O 8.14 8.57 Nd 307 6.6
P2O5 0.02 1.25 W 8 2.2
F 1.10 0.67 Pb 110 574.3
S 0.05 0.05
Cl 0.004 0.008
On exposure at the samples for one hour at 800 °C, a charoite with reduced interplanar spacings is identified. When the sample is heated to 850-900 °C, two phases - charoite and wollastonite - are observed, and the charoite content is gradually decreasing from 90 to 80 %. At a temperature of 950 °C, the content of charoite drops abruptly to trace values. This experiment confirms the destruction of the charoite structure at temperatures above 900 °C and supports the research results published in [Janeczek, 1991]. Above 1000 °C, both the triclinic and monoclinic modifications of wol-lastonite are observed. When the samples are heated to 1100 °C, wollastonite and its high-temperature modification called pseudo-wollastonite are formed. When the charoite sample is subject to heating above 1200 °C for one hour, charoite is completely transformed into pseudo-wollastonite (Fig. 3). The charoite structure is similar to tinaksite or kanasite, while its silicon-oxygen framework corresponds to calcium silicates, and the charoite structure transformation into the lattice of triclinic wollastonite can be thus explained [Janeczek, 1991]. In our experiments, no charoite melt was formed.
Сharoite and host rocks interaction. We studied the charoite and microcline-arfvedsonite lamprophyre interaction as a model of the natural transformation of host rock xenoliths in the charoite substance [Vorobjev, 2008].
In the experiments, a three-gram charoite sample (with microcline and quartz impurities) is crushed down to powder. The powder is put into a platinum capsule (9-10 mm in diameter; volume of 7-9 cm3). A lamprophyre sample (0.3-0.5 g) is added into the same capsule. The fluid composition in the capsule changes from pure ^О to 85 % (NaHCO3 + KOH) or (NaOH +
KOH) solution. The K/Na ratio in the system is 1.375 as calculated from the average ratio of these elements in charoite from the Staryi site. In the experiments at temperatures in the range from 500 to 800 °C and pressures from 0.5 to 1 kbar, the alkali content varies from 0 to 5 % in the (KOH + NaOH, KOH + NaHCO3) solution. The initial charoite substance is bleached, and a recrystallized charoite (with traces of calcite) is observed on the lamprophyre surface. When the solution concentration reaches 10 %, no interaction takes place at the charoite powder and lamprophyre contact at 500 °C; however, charoite is partially transformed into wollastonite. When the solution alkalinity is raised to 50 % (KOH + NaOH), lamprophyre is transformed, and
CHAROITE r OMT.RSION HIGH TEMPERATURES
120
1 1
800 850 900 950 1000 1050 1100 1150 1200 1250 Temperature. °C
■ Charoite M Wollastonite ■ Pseudowollastonite
Fig. 3. The sample composition changing as a function of temperature.
Рис. 3. Изменение состава образца в зависимости от температуры.
sodium-containing phlogopite is formed, while charoite remains stable, even though its recrystallization takes place at the contact with lamprophyre. Increasing the (NaOH + KOH) alkalinity to 85 % results in the partial assimilation of lamprophyre to form fluorphlogopite, while charoite remains stable. This series of high-alkalinity experiments show a dense opaque (translucent in some cases) reaction zone formed at the lamprophyre and charoite substance contact. The zone contains microcline, calcite, and dolomite with traces of amphibole, and its widths amounts to 1.6 mm.
With the temperature increase up to 800 °C, the pressure of 1 kbar, and 10 % (KOH + NaHCOs) solution, charoite is transformed in areas located at a distance from the contact with lamprophyre, and the recrystallization zone composed of wollastonite, mica phase and microcline is formed. At the charoite and lamprophyre contact, we observed the reaction zone containing wol-lastonite in the form of transparent columnar crystals (0.40-1.20 mm x 0.15 mm), microcline and recrystal-lized charoite with calcite traces, amphibole and afvil-lite, Ca3(SiO3-OH)2-2H2O. The reaction metasomatic column (Fig. 4, a, b) is quite similar to the natural one (see Fig. 2). We identified compositions of the newly formed phases and analyzed the distribution of elements. Various barium- and strontium-containing phases occur in some areas (Table 2).
4. Thermodynamic simulation
Analyses of the experiment results failed to determine the phase composition of the fine-grained reaction rim, and we attempt to employ the physicochemi-cal simulation in order to establish a possible mineral association formed during the high-temperature decomposition of charoite. In order to identify the mineral phases formed under charoite annealing and coexisting with wollastonite, we use the Selector software [Chudnenko, 2010]. A model of charoite decomposition reaction is constructed for the temperature range from 700 to 900 °C at the pressure of 1 kbar. The 18-component model system (K, Na, Ca, Fe, Mg, Al, Si, Ti, Mn, Sr, Ba, P, F, Cl, S, C, O, and H) corresponding to the charoite chemical composition is used as a basis for calculations covering 116 potentially possible phases, including solids (minerals), gas and an aqueous solution. We used the thermodynamics databases from [Holland, Powell, 2011] and [Yokokawa, 1998] in calculations for minerals and simple substances. The gas phase data are from [Reid et al., 1977]. The aqueous phase data are from SUPCRT98 electronic database. The published chemical analysis data for charoite (Table 3) are used to construct the model. In the simulation, an excessive amount of H2O (55.51 mol) is added to the charoite composition, which ensures the
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Fig. 4. The reaction rim resulting from the charoite substance and lamprophyre interaction in experimental conditions (T=500°C; P=1 kbar; 10 % concentration (NaHCOs+KOH)).
a - the viewing field size is 7.5x5.1 mm; b - the image is taken in the backscattered electrons (zoom 40 x). 1 - lamprophyre (arfvedsonite + microcline); 2 - wollastonite; 3 - wollastonite with microcline and charoite; 4 - charoite.
Рис. 4. Реакционная кайма, образовавшаяся при взаимодействии чароитового субстрата и лампрофира в экспериментах при Т=500 °С, Р=1 кбар, 10%-концен-трации (NaHCO3+KOH).
а - поле зрения 7.5x5.1 мм; b - снимок сделан в обратно рассеянных электронах, увеличение x40. 1 - лампрофир (арфведсонит + микроклин); 2 - волластонит; 3 - воллас-тонит с микроклином и чароитом; 4 - чароит.
permanent presence of the liquid phase, and a small amount of CO 2 (0.01 mol) is added to provide the conditions for potential formation of carbonates.
Our calculations show (Table 4) that at the given temperature and pressure, the following paragenesis is
Table 2. Composition of newly-formed phases (wt. %)
Таблица 2. Состав новообразованных фаз (вес. %)
Wallastonite Microcline Amphibole Apatite
SiO2 52.719 Na2O 0.952 Na2O 5.703 F 7.769
CaO 47.281 MgO 1.335 MgO 18.074 CaO 42.591
M2O3 14.421 M2O3 0.000 SrO 11.243
SiO2 61.754 SiO2 57.408 P2O5 38.397
K2O 13.026 K2O 4.914
CaO 1.073 CaO 3.261
TiO2 0.064 TiO2 0.334
MnO 0.681 MnO 0.079
FeO 5.292 FeO 10.227
formed from charoite of various compositions: quartz, wollastonite, alkaline pyroxene (aegerine), microcline, rhodonite, and sphene. Besides, manganese oxide, barium carbonate and hydroxide, BaTiO3, as well as BaSiO3 and SrSiO3 may be present in small amounts.
According to the simulation results, in the entire temperature range from 700 to 900 °C, the main stabile products of the charoite decomposition reaction are quartz and wollastonite. In case of the charoite decomposition at 900 °C, the content of wollastonite can reach 40 mol. % (Fig. 5, a). Quantities of other mineral phases are insignificant and variable depending on the initial composition of charoite: pyroxene - up to 4.5 mol. %; microcline - up to 1 mol. %; rhodonite - up to 0.17 mol. %; sphene - up to 0.02 mol. %; and manganese oxide, barium carbonate and hydroxide, BaTiO3, BaSiO3 and SrSiO3 - 3.5 mol. % in total. Figure 5, b,
shows the ratio of minerals (mol. %) formed from the charoite substance used in the experiments aimed to studying the charoite and host rock xenoliths interaction [Marchuk et al., 2014]. It should be noted that the presence of the diopside component in pyroxene is typical of the given composition (column 4 in Table 3) as the content of MgO is higher than that in the composition of pure charoite (columns 1 to 3 in Table 3). Sphene and BaSiO3 are also stable phases under the simulation conditions for this composition.
In the study of the charoite substance and lampro-phyre xenoliths interaction, the experiments show that, in addition to wollastonite, traces of microcline and alkali phases of different compositions are contained in the reaction zone. Thus, the calculation results are consistent with the results obtained in the experiments aimed at studying the charoite and host rocks interac-
Table 3. Chemical composition of charoite (wt. %)
Таблица 3. Химический состав чароита (вес. %)
Component 1 2 3 4
SiO2 58.50 57.31 58.94 73.22
TiO2 0.02 0.02 0.14 0.02
Al2O3 0.03 0.01 - 0.54
Fe2O3 0.14 - - -
FeO - 0.02 0.01 0.17
MgO - - - 1.84
MnO 0.10 0.35 0.23 0.13
CaO 21.90 21.01 21.12 16.10
SrO - 1.43 0.64 0.47
BaO 2.53 0.65 3.22 2.02
Na2O 2.26 2.29 2.62 3.90
K2O 10.01 8.35 9.48 8.00
P2O5 0.03 - - 0.02
F 0.33 0.53 0.49 0.11
Cl2 0.02 - - -
Note. 1 - composition of charoite according to [Matesanz et al., 2008]; 2 - composition of charoite according to [Rozhdestvenskaya et al., 2010]; 3 - average composition of charoite according to five analyses in [Wang et al., 2014]; 4 - composition of the charoite substance in Table 1.
Примечание. 1,2 - состав чароита из работ [Matesanz et al., 2008] и [Rozhdestvenskaya et al., 2010] соответственно, 3 - средний состав чароита по пяти анализам из работы [Wang et al., 2014], 4 - состав чароитового субстрата из табл. 1.
Table 4. Products of high-temperature decomposition of charoite (mol. quantity) Таблица 4. Продукты высокотемпературного разложения чароита (мол. кол-во)
Mineral phases Temperature, °С
700 800 900 700 800 900 700 800 900 700 800 900
1 2 3 4
Quartz 0.4942 0.5476 0.5550 0.4837 0.5343 0.5408 0.5122 0.564 0.5715 0.6517 0.7072 0.7224
(SiO2)
Wollastonite 0.3905 0.3905 0.3905 0.3746 0.3746 0.3746 0.3766 0.3766 0.3766 0.2267 0.2267 0.2267
(CaSiO3)
Aegirine 0.0017 0.0017 0.0017 0.0003 0.0003 0.0003 0.0001 0.0001 0.0001 0.0022 0.0022 0.0022
(NaFeSi2O6)
Diopside - - - - - - - - - 0.0428 0.0428 0.0428
(CaMgSi2O6)
Microcline 0.0006 0.0006 0.0006 0.0002 0.0002 0.0002 - - - 0.0096 0.0096 0.0095
(KAlSi3O8)
Rhodonite - 0.0014 0.0014 - 0.0049 0.0049 - 0.0032 0.0032 0.0017 0.0017 0.0017
(MnSiO3)
Sphene - - - - - - - - - 0.0002 0.0002 0.0002
(CaTiSiO5)
Bixbite 0.0007 - - 0.0025 - - 0.0016 - - - - -
(Mn2O3)
BaCO3 0.0008 - - 0.0040 - - 0.0008 - - - - -
Ba(OH)2 0.0154 0.0162 0.0162 - 0.0040 0.0040 0.0184 0.0193 0.0193 - - -
BaTiO3 0.0002 0.0002 0.0002 0.0002 0.0002 0.0002 0.0017 0.0017 0.0017 - - -
BaSiO3 - - - - - - - - - 0.0123 0.0123 0.0123
SrSiO3 - - - 0.0138 0.0138 0.0138 0.0062 0.0062 0.0062 0.0042 0.0042 0.0042
Note. Columns 1, 2,3, and 4 according to Table 3.
Примечание. Колонки 1,2, 3, 4 - аналогичны Табл. 3.
tion and charoite annealing, which suggests that there are phases coexisting with wollastonite in the reaction rim during the charoite decomposition.
5. Charoite treatment
The specific natural lilac to purple charoite coloration is due to impurity ions Mn2+ h Mn3+ in the mineral structure [Nikolskaya et al., 1976]. In this respect, Mn3+ has the main role. Besides, low concentrations of electron-hole centers put a slight effect on the color. The mineral is fluorescent in ultra-violet and green spectra in the photographic and X-ray excitation [Yarovoy, 1983]. According to [Nikolskaya et al., 1976], the charoite sample can be completely discolored by annealing in the reducing conditions at a temperature of 700 °C for three hours. The coloration can be restored by gamma irradiation, but become less intensive. After annealing in oxidizing conditions, coloration does not change. Subsequent gamma irradiation does not lead to any significant change in coloration. The methods of artificial mineral color changing in different redox environments [Medvedev, 1983] have provided a unique opportunity to track changes in the charoite chromo-phore and fluorescent characteristics [Yarovoy et al., 1987] in a variety redox conditions.
Charoite with high contents of impurity minerals looks less colourful, while its monomineral samples are recognized as highly decorative in terms of colors and patterns. Color shades depend on impurity minerals: honeylike (tinaksite), yellow (tokkoite), brown (titan-ite), black (aegirine), greenish (pectolite and micro-cline), and whitish (calcite and apofillite). Colouring with chemical agents is one of the techniques proposed to improve the colour-related characteristics of charoite [Ivicheva et al., 1998; Aleksandrova, Ivanova, 2015]. In this technique, charoite is impregnated with a selected colorant, and this process is accompanied by chemical reactions in the pore space of the rock sample. Options of using inorganic chromophores and synthetic dyes have been also studied. The technique ensures the color stability that is confirmed by corrosion tests and sufficient depths of the coloured matter, from the surface staining (for massive variations) to complete penetration of the dye (in samples with fiber and puckered structures).
Methods aimed at strengthening of charoitites are based on the use of high- and low-concentration dispersions and inorganic adhesives [Ivicheva et al., 1998]. Two types of inorganic adhesives can be used - soluble 'liquid' glass and silica sol obtained by the hydrolysis of tetraethoxysilane. Strengthening of porous samples is ensured by gradual (and, in some cases, repeated)
QUARTZ
57.47 %
AEGIRINE 0.18 %
MICROCLINE
0.06 %
RHODONITE
0.15 %
Ba(OH)2, ВаТЮз 1.71 %
WOLLASTONITE
40.44 %
MICROCLINE
0.94 %
BaSi03, SrSi03 1.63 %
RHODONITE
0.17 %
SPHENE
0.02 %
Fig. 5. Charoite high-temperature decomposition products (mol. %). The figure shows results of the phisicochemical simulation by the Selector software. The simulation conditions are given in the figure. Chemical compositions of charoite 1 (a) and 4 (b) are given in Table 1.
Рис. 5. Продукты высокотемпературного разложения чароита (мол. %) при физико-химическом моделировании с помощью ПК «Селектор». Условия моделирования приведены на рисунке. Химический состав чароита 1 (а) и 4 (Ь) приведен в Табл. 1.
soaking of the sample rock with organosilicon, which is followed by heating, and modifying and hardening agents may also be used.
6. Improving decorative properties of substandard
charoite samples
Coloring of charoitites samples is a complex multistage process, including sample preparation for coloring, coloring itself, fixing the result and testing the color stability against effects of water, alkaline solutions, sunlight and mechanical processing. The process cycle is 480-960 hours. The experiments are carried out in a temperature range from 20 to 100 °C. Charoitite samples preparation includes cleaning and surface degreas-ing by a soap-alcohol solution or acetone to provide for deeper penetration of the dye into the sample and to ensure the coloration uniformity.
Charoitites with different tones, structures, textures and mineral composition have been studied. Charoite contents in the samples varies from 20 to 70 %. Results of our experiments shows an optimal dye for charoite-containing rocks is synthetic - active bright purple dye 4KT, C20Hi4N3Oi5S4Na3Cu. By the type of the chromo-phore system, this dye is classified in the group of azo-dyes characterized by the presence in the molecule of -N=N- azogroup, connecting aromatic and heterocyclic compounds residues with each other and with the residues of compounds having active CH2-group. Preliminary experimental studies have shown unacceptability of acetic acid as a reaction accelerator, as the coloring becomes unstable to any impact. In the experiments
with the sample treatment in the dye solution for 12-24 hours, only the near-surface layer (maximum 10 mm thick) is colored. To achieve optimal coloration (Fig. 6), the samples are kept in the dye solution for 72 hours, the temperature is raised to 70-90 °C, and NaCl is added to the 3-7 % aqueous solution of active bright purple dye 4KT as electrolyte in order to accelerate the diffusion.
7. Results and conclusions
The charoite system experimental study overview emphasizes the need to develop more comprehensive and detailed experimental techniques for studying the conditions of the fluid-melt formation associated with the formation of charoite rocks.
It is established that in case of thermal decomposition, charoite is transformed into wollastonite which amount gradually increases with the temperature increase to 900 °C and, once the temperature is raised to 950 °C, grows dramatically to 95 % of the original sample weight. From the temperature of 1000 °C, both triclinic and monoclinic wollastonite modifications are observed. Further temperature increasing leads to the pseudo-wollastonite formation. Polymineral reaction zones of complex compositions are formed in case of the interaction between charoite and K-feldspar-am-phibole lamprophyre, as revealed in the experiments using the samples from the Murun massif. Possibly, the difference in compositions of the natural and experimental interaction zones is due to discrepancy between the temperature parameters in the experimental and
Fig. 6. Charoitite samples: initial view (top row]; the same samples after coloring (bottom row].
Рис. 6. Общий вид исходных образцов чароититов (верхний ряд], общий вид образцов после окрашивания (нижний ряд].
natural conditions and differences in the fluid composition, wherein the K/Na ratio may change at lower temperatures (about 500 °C). According to [Bondarenko, 2009], variations in the charoite compositions are fully similar to features of the alkaline trend of the Murun alkaline complex. For the early-stage charoite (meta-somatic stage, high temperatures), K-component of the mineral-forming environment is considerable. The chemical activity of Na is enhanced with the decreasing charoite formation temperature. In nature, wollaston-ite is commonly associated with pectolite and charoite. Therefore, we can consider wollastonite is a typical rock associated with charoite, which crystallization conditions are similar. There is an opinion about the charoite formation by substituting wollastonite [Lazeb-nik et al., 1977]. The mineralogical and petrographic studies of charoitites show the possibility for the assimilation of lamprophyre xenoliths in the charoite substance with a specific distribution of pyroxene and K-feldspar [Vorobjev, 2008]. Based on the analysis of the charoitites and host rocks interaction in the natural and experimental conditions, it becomes possible to clarify the T-P conditions for the charoite formation. In particular, the experiments emphasize the low-temperature character of charoite formation and show a lack of silicate melt in the systems studied. The results obtained by the physicochemical simulation of the char-oite decomposition reaction give grounds for the following conclusions: wollastonite and quartz together make up more than 97 mol. % of the total mass of
charoite; alkali mainly occur in the solution and, in small amounts, are present in aegirine and microcline; after the charoite decomposition is complete, manganese, strontium and barium form their own phases, which quantities are insignificant and would be even less if the model would take into account more complex schemes of isomorphism in minerals.
Charoite coloring by an active dye can be applied as a modern treatment method for the off-grade samples coloration and improving the colorimetry parameters of the material being processed, and can enhance the operational capabilities of the deposit. In our experiments, most of the samples acquired richer and attractive lilac and purple coloring, close to the natural cha-roite raw material.
8. Acknowledgements
The study was conducted using facilities of Centre for Geodynamics and Geochronology at the Institute of the Earth's Crust, SB RAS, Irkutsk, Russia by analysts Z.F. Ushchapovskaya and T.Yu. Cherkashina. The electronic probe X-ray analyses were performed in Vinogradov Institute of Geochemistry SB RAS by analyst L.A. Pavlova
The study was supported by the Russian Foundation for Basic Research (Grant Baikal No. 14-45-04108) and the Government of the Irkutsk Region.
9. References
Aleksandrova A.Yu, Ivanovo L.A, 2015. Refining of ornamental charoite. Proceedings of Siberian Branch, Earth Sciences Section, the Russian Academy of Natural Sciences. Geology and Exploration of Mineral Deposits (3 (52)), 86-94 (in Russian) [Александрова А.Ю, Иванова Л.А. Облагораживание поделочного чароита. Известия Сибирского отделения Секции наук о Земле РАЕН. Геология, поиски и разведка рудных месторождений. 2015. № 3 (52). С. 86-94].
Biryukov V.M., Berdnikov N.V., 1993. The paragenetic relation between charoite mineralization and alkali metasomatism. International Geology Review 35(7), 585-602. http://dx.doi.org/10.1080/00206819309465544.
Bondarenko N.V., 2009. The Geological and Structural Position and Genesis of the Sirenevyi Kamen' Charoite Deposit. PhD Thesis (Geology and Mineralogy). Moscow, 150 p. (in Russian) [Бондаренко Н.В. Геолого-структурная позиция и генезис чароититов месторождения «Сиреневый камень»: Дис. ... канд. геол.-мин. наук. М., 2009. 150 с.].
Borisov A.B, 1985. On the time and conditions for the formation of charoite rocks of different textures. Zapiski Vseso-yuznogo Mineralogicheskogo Obshchestva 113 (4), 455-463 (in Russian) [Борисов А.Б. О времени и условиях образования чароитовых пород разной текстуры // Записки Всесоюзного минералогического общества. 1985. Т. 113. № 4. С. 455-463].
Bulakh A.G., 1984. On the genesis of charoite. Zapiski Vsesoyuznogo Mineralogicheskogo Obshchestva 113 (2), 226-228 (in Russian) [Булах А.Г. К генезису чароита // Записки Всесоюзного минералогического общества. 1984. Т. 113. № 2. С. 226-228].
Chudnenko K.V., 2010. Thermodynamic Modeling in Geochemistry: Theory, Algorithms, Software, and Applications. GEO Publishing House, Novosibirsk, 287 p. (in Russian) [Чудненко К.В. Термодинамическое моделирование в геохимии: теория, алгоритмы, программное обеспечение, приложения. Новосибирск: Изд-во «ГЕО», 2010. 287 с.].
Deepthi K., Natesan U., Muthulakshmi A.L., Ferrer V.A., Venugopalan V.P., Narasimhan S.V., 2015. Mineralogical characterization in the marine environment of Kalpakkam, Southeast coast of India. Marine Georesources & Geotechno-logy 33 (6), 496-503. http://dx.doi.org/10.1080/1064119X.2014.954176.
Evdokimov M.D., 1995. Charoite - a unique mineral from a unique deposit. Mir Kamnya (The World of Stone) 7-8, 1-7 (in Russian) [Евдокимов М.Д. Чароит - уникальный минерал уникального месторождения // Мир камня. 1985. № 7-8. С. 1-7].
Evdokimov M.D., Bulakh A.G., Borisov A.B., 1985. Morphological types of charoite and their jewelry properties. Mine-ralogicheskii Zhurnal (Mineralogical Journal) 7 (5), 24-31 (in Russian) [Евдокимов М.Д., Булах А.Г., Борисов А.Б. Морфологические типы чароита и их ювелирные качества // Минералогический журнал. 1985. № 5. С. 24-31].
Foldvári M., 2011. Handbook of Thermogravimetric System of Minerals and Its Use in Geological Practice. Occasional Papers of the Geological Institute of Hungary, vol. 213. Geological Institute of Hungary, Budapest, 180 p.
Holland T.J.B., Powell R., 2011. An improved and extended internally consistent thermodynamic dataset for phases of petrological interest, involving a new equation of state for solids. Metamorphic Geology 29 (3), 333-383. http://dx.doi.org/10.1111/j.1525-1314.2010.00923.x.
lsaev V.A., Prasolov D.S., 2012. The justification of synthetic wollastonite production from a mixture of chalk and quartz sand at the Stoilensky Mining and Processing Combine. Mining Informational and Analytical Bulletin (9), 158-166 (in Russian) [Исаев В.А., Прасолов Д.С. Обоснование получения синтетического волластонита на стойленском ГОКе из смеси мела и кварцевого песка. Горный информационно-аналитический бюллетень. 2012. № 9. C. 158-166].
Ivicheva S.N., Yakhontova L.K., Soboleva T.V., 1998. Mineralogical prerequisites and methods for charoite refining. In: Synthesis of minerals and study methods. Proceedings of VNIISIMS. V. XV. P. 206-217 (in Russian) [Ивичева С.Н., Яхонтова Л.К., Соболева Т.В. Минералогические предпосылки и методы облагораживания чароита. Синтез минералов и методы их исследования. Труды ВНИИСИМС. 1998. Т. XV. С. 206-217].
JaneczekJ., 1991. Thermal decomposition of charoite. Mineralogia Polonica 22 (2), 21-27.
Konev A.A., Vorobjev E.l., Lazebnik K.A, 1996. Mineralogy of the Murunsky Alkaline Massif. SIC UIGGM, Publishing House of SB RAS, Novosibirsk, 221 p. (in Russian) [Конев А.А., Воробьев Е.И., Лазебник К.А. Минералогия Мурунского щелочного массива. Новосибирск: Изд-во СО РАН, НИЦ ОИГГМ, 1996. 221 с.].
Lazebnik K.A., Zayakina N.V., Lazebnik Yu.D., Suknev V.S., 1977. New data on charoite from metasomatic rocks of the Murunsky massif. In: Minerals of endogenous formation of Yakutia. Yakutsk, p. 123-153 (in Russian) [Лазебник К.А., Заякина Н.В., Лазебник Ю.Д., Сукнев В.С. Новые данные о чароите из метасоматических пород района Мурунского массива // Минералы эндогенных образований Якутии. Якутск, 1977. С. 123-153].
Marchuk M.V., Ivanova L.A., Medvedev V.Ya., 2014. Experimental studies of charoite transformations in case of interaction with host rocks. In: Reports of the Third All-Russia scientific conference. Institute of Geology and Use of Natural Resources of FEB RAS, Blagoveshchensk, p. 124-126 (in Russian) [Марчук М.В., Иванова Л.А., Медведев В.Я. Экспериментальные исследования преобразования чароита при взаимодействии с вмещающими породами // Третья Всероссийская научная конференция: сборник докладов. Благовещенск: ИГиП ДВО РАН, 2014. С. 124-126].
Matesanz E., Garcia-Guinea J., Crespo-Feo E., Lopez-Arce P., Valle-Fuentes F. J., Correcher V., 2008. The high-temperature behavior of charoite. Canadian Mineralogist 46 (5), 1207-1213. http://dx.doi.org/10.3749/canmin.46.5.1207.
Medvedev V.Ya., Ivanova L.A., 1983. The Natural Stones Processing Method and Products. Authors Certificate 1033584 USSR. Published in Bulletin of Inventions No. 29 (in Russian) [Медведев В.Я., Иванова Л.А. Способ обработки природных камней и изделий из них. Авторское свидетельство 1033584 СССР. Опубл. в Б. И. 1983, № 29].
Medvedev V.Ya., Ivanova LA, Lysov B.А., Ruzhich V.V., Marchuk М. V., 2014. Experimental study of decompression, permeability and healing of silicate rocks in fault zones. Geodynamics & Tectonophysics 5 (4), 905-917 (in Russian) [Медведев В.Я., Иванова Л.А., Лысов Б.А., Ружич В.В., Марчук М.В. Экспериментальное изучение декомпрессии, проницаемости и залечивания силикатных пород в зонах разломов // Геодинамика и тектонофизика. 2014. Т. 5. № 4. С. 905-917]. http://dx.doi.org/10.5800/GT-2014-5-4-0162.
Mitchell R.H., Vladykin N.V., 1996. Compositional variation of pyroxene and mica from the Little Murun Ultrapotassic Complex, Aldan Shield, Russia. Mineralogical Magazine 60 (6), 907-925. http://dx.doi.org/10.1180/minmag.1996. 060.403.06.
Nikolskaya L.V., Novozhilov A.l., Samoilovich M.l., 1976. On the nature of colours of the new alkaline calcium silicate from the Eastern Transbaikalia. Izvestiya AN SSSR, seriya geologicheskaya (10), 116-120 (in Russian) [Никольская Л.В., Новожилов А.И., Самойлович М.И. О природе окраски нового щелочного кальциевого силиката из Восточного Забайкалья // Известия АН СССР, серия геологическая. 1976. № 10. С. 116-120].
Reguir E., 2002. Aspects of the Mineralogy of the Muran Alkaline Complex, Yakutia, Russia, 193 p.
Reid R., Prausnitz J., Sherwood T., 1977. The Properties of Gases and Liquids. McGrawHill Book Company, New York, 3d edition, 592 p.
Rogova V.P., Rozhdestvenskaya l.V., Vorobjov E.l., Gladkochub D.P., Smirnov A.N., Spiridonov A.M., Antipin V.S., Kuz'-min M.l. Charoit. The Lilac Miracle of Siberia. Illustrated popular science book. Petrografika Publishing House, Irkutsk, 192 p. (in Russian) [Рогова В.П., Рождественская И.В., Воробьев Е.И., Гладкочуб Д.П., Смирнов А.Н., Спиридонов А.М., Антипин В.С., Кузьмин М.И. Чароит. Сиреневое чудо Сибири. Иллюстрированное научно-популярное издание. Иркутск: Изд-во «Петрографика», 2013. 192 с.].
Rozhdestvenskaya I., Mugnaioli E, Czank M., Depmeier W., Kolb U., Reinholdt A., Weirich T., 2010. The structure of cha-roite, (K, Sr, Ba, Mn)i5-i6 (Ca, Na)32[(Si70(O,OH)180)](OH,F)4.0*nH2O, solved by conventional and automated electron diffraction. Mineralogical Magazine 74 (1), 159-177. http://dx.doi.org/10.1180/minmag.2010.074.1.159.
Solyanik V.A., 2004. Charoit - a discovery of the second half of the 20th century. Vestnik DVO RAN (4), 152-156 (in Russian) [Соляник В.А. Чароит - открытие второй половины XX в. // Вестник ДВО РАН. 2004. № 4. С. 152-156].
Solyanik V.A., Pakhomova V.A., Ushkova M.A, 2008. Charoite - a champion among mineralogical discoveries in the second half of the 20th century. The Journal of the Gemmological Association of Hong Kong 29, 77-80.
Vladykin N.V, 2000. The Malyi Murun volcano-plutonic complex: an example of differentiated mantle magmas of lamproitic type. Geochemistry International 38 (1), S73-S83.
Vladykin N.V., 2009. Potassium alkaline lamproite-carbonatite complexes: petrology, genesis, and ore reserves. Russian Geology and Geophysics 50 (12), 1119-1128. http://dx.doi.org/10.1016Zj.rgg.2009.11.010.
Vorobjev E.I., 2008. Charoite. Geo Publishing House, Novosibirsk, 140 p. (in Russian) [Воробьев Е.И. Чароит. Новосибирск: Академическое изд-во «Гео», 2008. 140 с.].
Wang Y., He H., IvanovA.V., Zhu R., Lo C., 2014. Age and origin of charoitite, Malyy Murun massif, Siberia, Russia. International Geology Review 56 (8), 1007-1019. http://dx.doi.org/10.1080/00206814.2014.914860.
Yarovoy P.N., 1983. Spectral and kinetic characteristics of charoite. Journal of Applied Spectroscopy 39 (3), 486-498 (in Russian) [Яровой П.Н. Спектрально-кинетические характеристики минерала чароит // Журнал прикладной спектроскопии. 1983. Т. 39. № 3. С. 486-498].
Yarovoy P.N., Medvedev V.Y., Ivanova L.A., Serykh S.V., 1987. Color and luminescent properties of minerals in various redox conditions. Journal of Applied Spectroscopy 46 (6), 586-590. http://dx.doi.org/10.1007/BF00661233.
Yokokawa H., 1988. Tables of thermodynamic properties of inorganic compounds. Journal of the National Chemical Laboratory for Industry 83, 27-118.
Zaraisky G.P., 2007. The Experiment in Solving the Problems of Metasomatism. GEOS, Moscow, 136 p. (in Russian) [Зарайский Г.П. Эксперимент в решении проблем метасоматизма. М.: ГЕОС, 2007. 136 с.].
Marchuk, Marina V., Candidate of Geology and Mineralogy, Junior Researcher Institute of the Earth's Crust, Siberian Branch of RAS 128 Lermontov street, Irkutsk 664033, Russia H e-mail: marin@crust.irk.ru
Марчук Марина Валерьевна, канд. геол.-мин. наук, м.н.с. Институт земной коры СО РАН 664033, Иркутск, ул. Лермонтова, 128, Россия H e-mail: marin@crust.irk.ru
Medvedev, Vladimir Ya., Candidate of Geology and Mineralogy, Senior Researcher Institute of the Earth's Crust, Siberian Branch of RAS 128 Lermontov street, Irkutsk 664033, Russia e-mail: med@crust.irk.ru
Медведев Владимир Яковлевич, канд. геол.-мин. наук, с.н.с. Институт земной коры СО РАН 664033, Иркутск, ул. Лермонтова, 128, Россия e-mail: med@crust.irk.ru
Ivanova Larisa A., Candidate of Geology and Mineralogy, Senior Researcher Institute of the Earth's Crust, Siberian Branch of RAS 128 Lermontov street, Irkutsk 664033, Russia e-mail: liva@crust.irk.ru
Иванова Лариса Александровна, канд. геол.-мин. наук, с.н.с., Институт земной коры СО РАН 664033, Иркутск, ул. Лермонтова, 128, Россия e-mail: liva@crust.irk.ru
Sokolova, Tatyana S., Candidate of Geology and Mineralogy, Researcher
Institute of the Earth's Crust, Siberian Branch of RAS
128 Lermontov street, Irkutsk 664033, Russia
Tel.: 8(3952)511680, e-mail: sokolovats@crust.irk.ru
Соколова Татьяна Сергеевна, канд. геол.-мин. наук, н.с. Институт земной коры СО РАН 664033, Иркутск, ул. Лермонтова, 128, Россия Тел.: 8(3952)511680, e-mail: sokolovats@crust.irk.ru
Danilov, Boris S., Candidate of Geology and Mineralogy, Researcher Institute of the Earth's Crust, Siberian Branch of RAS 128 Lermontov street, Irkutsk 664033, Russia Tel.: 8(3952)511680; e-mail: boris@crust.irk.ru
Данилов Борис Станиславович, канд. геол.-мин. наук, н.с. Институт земной коры СО РАН 664033, Иркутск, ул. Лермонтова, 128, Россия Тел.: 8(3952)511680; e-mail: boris@crust.irk.ru
Gladkochub, Dmitry P., Doctor of Geology and Mineralogy, Professor of RAS, Director of the Institute Institute of the Earth's Crust, Siberian Branch of RAS 128 Lermontov street, Irkutsk 664033, Russia e-mail: dima@crust.irk.ru
Гладкочуб Дмитрий Петрович, докт. геол.-мин. наук, профессор РАН, директор института
Институт земной коры СО РАН
664033, Иркутск, ул. Лермонтова, 128, Россия
e-mail: dima@crust.irk.ru
