79 research outputs found
LATE MESOZOIC GRANITOIDS OF THE WESTERN TRANSBAIKALIA (RUSSIA) AND THEIR RELATION TO FORMATION OF METAMORPHIC CORE COMPLEXES
Early Cretaceous metamorphic core complexes (MCCs) are widespread in North-East Asia and indicate a large-scale crustal extension in this area [Wang et al., 2011, 2012]. Traditionally one of the formation mechanisms of MCCs is related to various magmatic activities including granitoid magmatism [Anderson et al., 1988, Hill et al., 1995; Lister, Baldwin, 1993]. Wang et al. [2012] have subdivided the intrusion associated with MCCs in NE Asia into pre-kinematic (~170β140 Ma), syn-kinematic (~150β125 Ma) and post-kinematic (~125β110 Ma). 40Ar/39Ar biotite and hornblende ages of 140β110 Ma are overlapping for all MCCs of NE Asia and represent the time of the final stage of the MCCs formation [Wang et al., 2012]. Here, we present overview of geochronological and geochemical data for Late Mesozoic granitoids of the Western Transbaikalia and our view on their role in formation of Transbaikalian MCCs.Early Cretaceous metamorphic core complexes (MCCs) are widespread in North-East Asia and indicate a large-scale crustal extension in this area [Wang et al., 2011, 2012]. Traditionally one of the formation mechanisms of MCCs is related to various magmatic activities including granitoid magmatism [Anderson et al., 1988, Hill et al., 1995; Lister, Baldwin, 1993]. Wang et al. [2012] have subdivided the intrusion associated with MCCs in NE Asia into pre-kinematic (~170β140 Ma), syn-kinematic (~150β125 Ma) and post-kinematic (~125β110 Ma). 40Ar/39Ar biotite and hornblende ages of 140β110 Ma are overlapping for all MCCs of NE Asia and represent the time of the final stage of the MCCs formation [Wang et al., 2012]. Here, we present overview of geochronological and geochemical data for Late Mesozoic granitoids of the Western Transbaikalia and our view on their role in formation of Transbaikalian MCCs
EARLY STAGE OF THE CENTRAL ASIAN OROGENIC BELT BUILDING: EVIDENCES FROM THE SOUTHERN SIBERIAN CRATON
The origin of the Central-Asian Orogenic Belt (CAOB), especially of its northern segment nearby the southern margin of the Siberian craton (SC) is directly related to development and closure of the Paleo-Asian Ocean (PAO). Signatures of early stages of the PAO evolution are recorded in the Late Precambrian sedimentary successions of the Sayan-Baikal-Patom Belt (SBPB) on the southern edge of SC. These successions are spread over 2000 km and can be traced along this edge from north-west (Sayan area) to south-east (Baikal area) and further to north-east (Patom area). Here we present the synthesis of all available and reliable LA-ICP-MS U-Pb geochronological studies of detrital zircons from these sedimentary successions.The origin of the Central-Asian Orogenic Belt (CAOB), especially of its northern segment nearby the southern margin of the Siberian craton (SC) is directly related to development and closure of the Paleo-Asian Ocean (PAO). Signatures of early stages of the PAO evolution are recorded in the Late Precambrian sedimentary successions of the Sayan-Baikal-Patom Belt (SBPB) on the southern edge of SC. These successions are spread over 2000 km and can be traced along this edge from north-west (Sayan area) to south-east (Baikal area) and further to north-east (Patom area). Here we present the synthesis of all available and reliable LA-ICP-MS U-Pb geochronological studies of detrital zircons from these sedimentary successions
Paleomagnetism of Cryogenian Kitoi mafic dykes in South Siberia: Implications for Neoproterozoic paleogeography
We present a new paleomagnetic pole of 1.1Β°N, 22.4Β°E, A95 = 7.4Β° from the 760 Ma gabbro-dolerite Kitoi dykes located in the southern part of the Siberian Craton. The pole is supported by contact tests and suggests closer position of Siberia relative to Laurentia at 760 Ma than in Mesoproterozoic. We propose that this closer configuration was achieved by dextral transpressive motion of Siberia relative to Laurentia between 780 and 760 Ma. This motion was probably initiated at the first stage of the Rodinia breakup and is coeval with the 780 Ma Gunbarrel magmatic event of the western Canadian shield
MARBLE MΓLANGE: COMPOSITION VARIATIONS AND FORMATION MECHANISMS
The Olkhon terrane in the Western Baikal area accommodates four types of carbonate-silicate mixtures: injection (protrusion), metamorphic-boudinated, mingling, and tectonite marble mΓ©lange. The outcrops of injection mΓ©lange consist of a carbonate matrix with inclusions of native silicic rocks found in the immediate vicinities, commonly cover large areas and lack any distinct linearity in the map view. MΓ©lange of the metamorphic boudinage type comprises diopsidite and tremilote-diopsidite fragments in a dolomitic or calcite-dolomitic matrix. Its origin is apparently due to tectonism and related metamorphism of quartz sandstones in Neoproterozoic strata on the passive margin of the Siberian craton. Mingling mΓ©lange appears as calcite marble or carbonate-silicate (calciphyre) veins with metadolerite and granite inclusions of different sizes. The veins formed by intrusion of carbonate and silicate melt batches and subsequent fragmentation of silicate rocks that crystallized earlier. Marble tectonites localized in narrow zones record the late phase of ductile marble injection
MARBLE DIKES IN THE OLKHON COMPOSITE TERRANE (WEST BAIKAL AREA)
Linear or lens-like carbonate (marble) and carbonate-silicate bodies among gabbro and amphibolites within the Krestovsky subterrane of the Olkhon composite terrane (West Baikal Area) are identified as dikes. The dikes commonly dip almost vertically, range in thickness from 20 cm to a few meters, and are up to 100 m long. The Olkhon marble dikes quite often coexist with dolerite dikes and/or granite veins and show signatures of emplacement synchronously with the igneous bodies. The marble dikes differ from mantle carbonatites in mineralogy and chemistry and thus may be derived from sedimentary carbonate rocks molten during collisional events.The origin of the Olkhon carbonate and carbonate-silicate dikes may be explained with two possible geodynamic scenarios. They may be derived either from Neoproterozoic carbonate sediments upon the Early Precambrian basement of a cratonic block which was involved in collisional events, or from abundant carbonate sedimentary material in an island-arc terrane. Large-scale melting of silicate and carbonate rocks was maintained by heat released from mantle mafic magma intruding into the lower crust. The batches of both crustal (carbonate and granitic) and mantle (mafic) melts intruded late during the collision in a strike-slip tectonic setting
Π‘Π’Π Π£ΠΠ’Π£Π Π ΠΠΠΠΠ’ΠΠ Π£ΠΠΠΠΠ ΠΠΠ‘Π’ΠΠ ΠΠΠΠΠΠΠ― ΠΠΠΠΠ¦ ΠΠ«Π‘ΠΠ§ΠΠΠ¨ΠΠ (Π‘ΠΠΠΠ ΠΠΠ ΠΠΠΠΠΠΠΠΠ¬Π)
The article describes the fold-thrust structure of the Golets Vysochaishy deposit located at the Baikal-Patom Upland in the Marakan-Tunguska megasyncline. The latter is composed of terrigenous-carbonate carbonaceous rocks metamorphosed in greenschist facies conditions. The deposit is detected in the hanging wing of the asymmetric Kamenskaya anticline. In a cross section, the anticline is an S-shaped structure extending in the latitudinal direction. The main feature of the Golets Vysochaishy deposit is the development of interlayer sulfidization zones (pyrite, pyrrhotite), including gold-bearing ones. Its gold-ore zones tend to occur in layered areas of interlayer sliding in the rocks of the Khomolkhinskaya suite.Four structural markers revealed within the deposit area are indicative of repeated deformation processes: (1) sublatitudinal folding, cleavage of the axial surface and its subsequent transformation into schistosity; (2) crenulation cleavage; (3) interlayer sliding and rock breakdown with interlayer drag folds, parallel microfractures and polished slickensides; (4) large quartz veins and veinlets that cross cut the main structural elements in plan.ΠΡΠΈΠ²ΠΎΠ΄ΠΈΡΡΡ ΠΎΠΏΠΈΡΠ°Π½ΠΈΠ΅ ΡΠΊΠ»Π°Π΄ΡΠ°ΡΠΎ-Π½Π°Π΄Π²ΠΈΠ³ΠΎΠ²ΠΎΠΉ ΡΡΡΡΠΊΡΡΡΡ ΠΌΠ΅ΡΡΠΎΡΠΎΠΆΠ΄Π΅Π½ΠΈΡ ΠΠΎΠ»Π΅Ρ ΠΡΡΠΎΡΠ°ΠΉΡΠΈΠΉ, ΡΠ°ΡΠΏΠΎΠ»ΠΎΠΆΠ΅Π½Π½ΠΎΠ³ΠΎ Π½Π° ΡΠ΅ΡΡΠΈΡΠΎΡΠΈΠΈ ΠΠ°ΠΉΠΊΠ°Π»ΠΎ-ΠΠ°ΡΠΎΠΌΡΠΊΠΎΠ³ΠΎ Π½Π°Π³ΠΎΡΡΡ Π² ΠΏΡΠ΅Π΄Π΅Π»Π°Ρ
ΠΠ°ΡΠ°ΠΊΠ°Π½ΠΎ-Π’ΡΠ½Π³ΡΡΡΠΊΠΎΠΉ ΠΌΠ΅Π³Π°ΡΠΈΠ½ΠΊΠ»ΠΈΠ½Π°Π»ΠΈ. ΠΠΎΡΠ»Π΅Π΄Π½ΡΡ ΡΠ»ΠΎΠΆΠ΅Π½Π° ΡΠ΅ΡΡΠΈΠ³Π΅Π½Π½ΠΎ-ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΡΠΌΠΈ ΡΠ³Π»Π΅ΡΠΎΠ΄ΠΈΡΡΡΠΌΠΈ ΠΏΠΎΡΠΎΠ΄Π°ΠΌΠΈ, ΠΌΠ΅ΡΠ°ΠΌΠΎΡΡΠΈΠ·ΠΎΠ²Π°Π½Π½ΡΠΌΠΈ Π² ΡΡΠ»ΠΎΠ²ΠΈΡΡ
Π·Π΅Π»Π΅Π½ΠΎΡΠ»Π°Π½ΡΠ΅Π²ΠΎΠΉ ΡΠ°ΡΠΈΠΈ. ΠΠ΅ΡΡΠΎΡΠΎΠΆΠ΄Π΅Π½ΠΈΠ΅ Π»ΠΎΠΊΠ°Π»ΠΈΠ·ΠΎΠ²Π°Π½ΠΎ Π² Π²ΠΈΡΡΡΠ΅ΠΌ ΠΊΡΡΠ»Π΅ Π°ΡΠΈΠΌΠΌΠ΅ΡΡΠΈΡΠ½ΠΎΠΉ ΠΠ°ΠΌΠ΅Π½ΡΠΊΠΎΠΉ Π°Π½ΡΠΈΠΊΠ»ΠΈΠ½Π°Π»ΠΈ S-ΠΎΠ±ΡΠ°Π·Π½ΠΎΠΉ ΡΠΎΡΠΌΡ Π² ΠΏΠΎΠΏΠ΅ΡΠ΅ΡΠ½ΠΎΠΌ ΡΠ΅ΡΠ΅Π½ΠΈΠΈ, ΠΏΡΠΎΡΡΠ³ΠΈΠ²Π°ΡΡΠ΅ΠΉΡΡ Π² ΡΠΈΡΠΎΡΠ½ΠΎΠΌ Π½Π°ΠΏΡΠ°Π²Π»Π΅Π½ΠΈΠΈ. ΠΠ»Π°Π²Π½ΠΎΠΉ ΠΎΡΠΎΠ±Π΅Π½Π½ΠΎΡΡΡΡ ΠΌΠ΅ΡΡΠΎΡΠΎΠΆΠ΄Π΅Π½ΠΈΡ ΠΠΎΠ»Π΅Ρ ΠΡΡΠΎΡΠ°ΠΉΡΠΈΠΉ ΡΠ²Π»ΡΠ΅ΡΡΡ ΡΠ°Π·Π²ΠΈΡΠΈΠ΅ ΠΌΠ΅ΠΆΡΠ»ΠΎΠ΅Π²ΡΡ
Π·ΠΎΠ½ ΡΡΠ»ΡΡΠΈΠ΄ΠΈΠ·Π°ΡΠΈΠΈ (ΠΏΠΈΡΠΈΡ, ΠΏΠΈΡΡΠΎΡΠΈΠ½), Π² ΡΠΎΠΌ ΡΠΈΡΠ»Π΅ ΠΈ Π·ΠΎΠ»ΠΎΡΠΎΠ½ΠΎΡΠ½ΡΡ
. ΠΠΎΠ»ΠΎΡΠΎΡΡΠ΄Π½ΡΠ΅ ΡΠ΅Π»Π° ΡΡΠ³ΠΎΡΠ΅ΡΡ ΠΊ ΠΏΠΎΡΠ»ΠΎΠΉΠ½ΡΠΌ Π·ΠΎΠ½Π°ΠΌ ΠΌΠ΅ΠΆΡΠ»ΠΎΠ΅Π²ΠΎΠ³ΠΎ ΡΠΊΠΎΠ»ΡΠΆΠ΅Π½ΠΈΡ Π² ΠΏΠΎΡΠΎΠ΄Π°Ρ
Π₯ΠΎΠΌΠΎΠ»Ρ
ΠΈΠ½ΡΠΊΠΎΠΉ ΡΠ²ΠΈΡΡ.Π ΠΏΡΠ΅Π΄Π΅Π»Π°Ρ
ΠΌΠ΅ΡΡΠΎΡΠΎΠΆΠ΄Π΅Π½ΠΈΡ ΡΡΡΠ°Π½ΠΎΠ²Π»Π΅Π½Ρ ΡΠ΅ΡΡΡΠ΅ ΡΡΡΡΠΊΡΡΡΠ½ΡΡ
ΠΌΠ°ΡΠΊΠ΅ΡΠ°, ΡΠΊΠ°Π·ΡΠ²Π°ΡΡΠΈΡ
Π½Π° Π½Π΅ΠΎΠ΄Π½ΠΎΠΊΡΠ°ΡΠ½ΠΎΡΡΡ Π΄Π΅ΡΠΎΡΠΌΠ°ΡΠΈΠΎΠ½Π½ΡΡ
ΠΏΡΠΎΡΠ΅ΡΡΠΎΠ²: 1) ΡΠΎΡΠΌΠΈΡΠΎΠ²Π°Π½ΠΈΠ΅ ΡΠΊΠ»Π°Π΄ΡΠ°ΡΠΎΡΡΠΈ ΡΡΠ±ΡΠΈΡΠΎΡΠ½ΠΎΠΉ ΠΎΡΠΈΠ΅Π½ΡΠΈΡΠΎΠ²ΠΊΠΈ, ΠΊΠ»ΠΈΠ²Π°ΠΆΠ° ΠΎΡΠ΅Π²ΠΎΠΉ ΠΏΠΎΠ²Π΅ΡΡ
Π½ΠΎΡΡΠΈ ΠΈ ΠΏΠΎΡΠ»Π΅Π΄ΡΡΡΠ΅Π΅ Π΅Π³ΠΎ ΡΡΠ°Π½ΡΡΠΎΡΠΌΠΈΡΠΎΠ²Π°Π½ΠΈΠ΅ Π² ΡΠ»Π°Π½ΡΠ΅Π²Π°ΡΠΎΡΡΡ; 2) ΡΠΎΡΠΌΠΈΡΠΎΠ²Π°Π½ΠΈΠ΅ ΠΊΡΠ΅Π½ΡΠ»ΡΡΠΈΠΎΠ½Π½ΠΎΠ³ΠΎ ΠΊΠ»ΠΈΠ²Π°ΠΆΠ°; 3) ΠΌΠ΅ΠΆΡΠ»ΠΎΠ΅Π²ΡΠ΅ ΠΏΠΎΠ΄Π²ΠΈΠΆΠΊΠΈ (ΡΡΡΠ²Ρ), ΡΠΎΠΏΡΠΎΠ²ΠΎΠΆΠ΄Π°ΡΡΠΈΠ΅ΡΡ ΠΌΠ΅ΠΆΡΠ»ΠΎΠ΅Π²ΡΠΌΠΈ ΡΠΊΠ»Π°Π΄ΠΊΠ°ΠΌΠΈ Π²ΠΎΠ»ΠΎΡΠ΅Π½ΠΈΡ, ΠΏΠ°ΡΠ°Π»Π»Π΅Π»ΡΠ½ΡΠΌΠΈ ΠΌΠΈΠΊΡΠΎΡΡΠ΅ΡΠΈΠ½Π°ΠΌΠΈ, Π° ΡΠ°ΠΊΠΆΠ΅ ΠΎΡΠΏΠΎΠ»ΠΈΡΠΎΠ²Π°Π½Π½ΡΠΌΠΈ Π·Π΅ΡΠΊΠ°Π»Π°ΠΌΠΈ ΡΠΊΠΎΠ»ΡΠΆΠ΅Π½ΠΈΡ; 4) ΡΠΎΡΠΌΠΈΡΠΎΠ²Π°Π½ΠΈΠ΅ ΠΊΡΡΠΏΠ½ΡΡ
ΠΊΠ²Π°ΡΡΠ΅Π²ΡΡ
ΠΆΠΈΠ» ΠΈ ΠΏΡΠΎΠΆΠΈΠ»ΠΊΠΎΠ², Π·Π°Π½ΠΈΠΌΠ°ΡΡΠΈΡ
ΡΠ΅ΠΊΡΡΠ΅Π΅ ΠΏΠΎΠ»ΠΎΠΆΠ΅Π½ΠΈΠ΅ ΠΏΠΎ ΠΎΡΠ½ΠΎΡΠ΅Π½ΠΈΡ ΠΊ ΠΎΡΠ½ΠΎΠ²Π½ΡΠΌ ΠΏΠ»ΠΎΡΠΊΠΎΡΡΠ½ΡΠΌ ΡΡΡΡΠΊΡΡΡΠ½ΡΠΌ ΡΠ»Π΅ΠΌΠ΅Π½ΡΠ°ΠΌ
Microfossils of the late proterozoic debengdinskaya formation of the olenekskiy uplift
Microfossils from the Middle Riphean Debengdinskaya formation of the Olenekskiy uplift have been studied. Various stenoorganic forms of acritarchs and cyanobacteries are described. Morphological groups which are preliminary compared with large flora taxons are allocated among acritarchs : brown and green seaweed, mushrooms, seaweed located in symbiotic relations (?) with cyanobionts. The prematurity of radical conclusions about age of the deposit based on majority of Proterozoic microfossils is underline
ΠΠΠΠ₯ΠΠΠΠ― Π ΠΠΠΠ ΠΠ‘Π’ ΠΠΠ ΠΠ ΠΠΠΠΠΠ₯ ΠΠΠΠ‘Π’ΠΠ ΠΠ£Π’Π£ΠΠΠΠ-ΠΠ£Π Π‘ΠΠΠΠ Π ΠΠΠΠΠΠ‘ΠΠΠΠ ΠΠΠΠΠΠΠΠ‘ΠΠ ΠΠΠ’ΠΠΠΠ Π€ΠΠ§ΠΠ‘ΠΠΠ₯ Π―ΠΠΠ (Π‘ΠΠΠΠ ΠΠΠ― ΠΠΠΠΠΠΠΠ― β ΠΠΠΠΠΠΠΠ ΠΠΠΠΠΠΠΠΠ¬Π)
This article reviews data on ages of rocks in the footwall of the Butuliyn-Nur and Zagan metamorphic core complexes (MCC) and provides new data on the geochemistry of the rock complexes. It is noted that the oldest rocks are mylonitized gneisses on rhyolites (554 Ma) in the footwall of the Butuliyn-Nur MCC. The Late Permian β Triassic (249β211 Ma) igneous rocks are ubiquitous in the footwall of the Butuliyn-Nur and Zagan MCC. The youngest rocks in the studied MCC are the Jurassic granitoids (178β152 Ma) of the Naushki and Verhnemangirtui massifs. In the footwall of the Butuliyn-Nur and Zagan MCC, the most common are granitoids and felsic volcanic rocks (249β211 Ma) with many similar geochemical characteristics, such as high alkalinity, high contents of Sr and Ba, moderate and low concentrations of Nb and Y. Considering the contents of trace elements and REE, the granitoids and the felsic volcanic rocks are similar to I-type granites. Specific compositions of these rocks suggest that they might have formed in conditions of the active continental margin of the Siberian continent over the subducting oceanic plate of the Mongol-Okhotsk Ocean. The granitoids of the Naushki and Verhnemangirtui massifs, which are the youngest of the studied rocks (178β152 Ma), also have similar geochemical characteristics. In both massif, granitoids are ferriferous, mostly alkaline rocks. By contents of both major and trace elements, they are comparable to A-type granites. Such granitoids formed in conditions of intracontinental extension while subduction was replaced by collision. Based on ages and geochemical characteristics of the rocks in the footwall of the Butuliyn-Nur and Zagan MCC, a good correlation is revealed between the studied rocksΒ and the rock complexes of the Transbaikalian and North-Mongolian segments of the Central Asian fold belt (CAFB), and it can thus be suggested that the regions under study may have a common evolutionary history.Π ΡΡΠ°ΡΡΠ΅ ΠΏΡΠΈΠ²ΠΎΠ΄ΠΈΡΡΡ ΠΎΠ±Π·ΠΎΡ Π΄Π°Π½Π½ΡΡ
ΠΏΠΎ Π²ΠΎΠ·ΡΠ°ΡΡΡ ΠΏΠΎΡΠΎΠ΄ Π½ΠΈΠΆΠ½ΠΈΡ
ΠΏΠ»Π°ΡΡΠΈΠ½ ΠΡΡΡΠ»ΠΈΠΉΠ½-ΠΡΡΡΠΊΠΎΠ³ΠΎ ΠΈ ΠΠ°Π³Π°Π½ΡΠΊΠΎΠ³ΠΎ ΠΊΠΎΠΌΠΏΠ»Π΅ΠΊΡΠΎΠ² ΠΌΠ΅ΡΠ°ΠΌΠΎΡΡΠΈΡΠ΅ΡΠΊΠΈΡ
ΡΠ΄Π΅Ρ (ΠΠΠ―), Π° ΡΠ°ΠΊΠΆΠ΅ Π½ΠΎΠ²ΡΠ΅ Π΄Π°Π½Π½ΡΠ΅ ΠΏΠΎ Π³Π΅ΠΎΡ
ΠΈΠΌΠΈΠΈ ΡΡΠΈΡ
ΠΏΠΎΡΠΎΠ΄Π½ΡΡ
ΠΊΠΎΠΌΠΏΠ»Π΅ΠΊΡΠΎΠ². ΠΡΠΌΠ΅ΡΠ΅Π½ΠΎ, ΡΡΠΎ ΡΠ°ΠΌΡΠΌΠΈ Π΄ΡΠ΅Π²Π½ΠΈΠΌΠΈ ΠΏΠΎΡΠΎΠ΄Π°ΠΌΠΈ ΡΠ²Π»ΡΡΡΡΡ ΠΌΠΈΠ»ΠΎΠ½ΠΈΡΠΈΠ·ΠΈΡΠΎΠ²Π°Π½Π½ΡΠ΅ Π³Π½Π΅ΠΉΡΡ ΠΏΠΎ ΡΠΈΠΎΠ»ΠΈΡΠ°ΠΌ (554 ΠΌΠ»Π½ Π»Π΅Ρ) Π½ΠΈΠΆΠ½Π΅ΠΉ ΠΏΠ»Π°ΡΡΠΈΠ½Ρ ΠΡΡΡΠ»ΠΈΠΉΠ½-ΠΡΡΡΠΊΠΎΠ³ΠΎ ΠΠΠ―. ΠΠ°ΠΊΡΠΈΠΌΠ°Π»ΡΠ½ΠΎΠ΅ ΡΠ°ΡΠΏΡΠΎΡΡΡΠ°Π½Π΅Π½ΠΈΠ΅ ΡΡΠ΅Π΄ΠΈ ΠΎΠ±ΡΠ°Π·ΠΎΠ²Π°Π½ΠΈΠΉ Π½ΠΈΠΆΠ½ΠΈΡ
ΠΏΠ»Π°ΡΡΠΈΠ½ ΠΡΡΡΠ»ΠΈΠΉΠ½-ΠΡΡΡΠΊΠΎΠ³ΠΎ ΠΈ ΠΠ°Π³Π°Π½ΡΠΊΠΎΠ³ΠΎ ΠΠΠ― ΠΈΠΌΠ΅ΡΡ ΠΏΠΎΠ·Π΄Π½Π΅ΠΏΠ΅ΡΠΌΡΠΊΠΈΠ΅ β ΡΡΠΈΠ°ΡΠΎΠ²ΡΠ΅ (249β211 ΠΌΠ»Π½ Π»Π΅Ρ) ΠΌΠ°Π³ΠΌΠ°ΡΠΈΡΠ΅ΡΠΊΠΈΠ΅ ΠΏΠΎΡΠΎΠ΄Ρ. Π‘Π°ΠΌΡΠΌΠΈ ΠΌΠΎΠ»ΠΎΠ΄ΡΠΌΠΈ ΠΏΠΎΡΠΎΠ΄Π°ΠΌΠΈ Π² ΠΈΠ·ΡΡΠ΅Π½Π½ΡΡ
ΠΠΠ― ΡΠ²Π»ΡΡΡΡΡ Π³ΡΠ°Π½ΠΈΡΠΎΠΈΠ΄Ρ ΡΡΡΠΊΠΎΠ³ΠΎ Π²ΠΎΠ·ΡΠ°ΡΡΠ° (178β152 ΠΌΠ»Π½ Π»Π΅Ρ) ΠΠ°ΡΡΠΊΠΈΠ½ΡΠΊΠΎΠ³ΠΎ ΠΈ ΠΠ΅ΡΡ
Π½Π΅ΠΌΠ°Π½Π³ΠΈΡΡΡΠΉΡΠΊΠΎΠ³ΠΎ ΠΌΠ°ΡΡΠΈΠ²ΠΎΠ². ΠΠ°ΠΈΠ±ΠΎΠ»Π΅Π΅ ΡΠ°ΡΠΏΡΠΎΡΡΡΠ°Π½Π΅Π½Π½ΡΠ΅ ΡΡΠ΅Π΄ΠΈ Π½ΠΈΠΆΠ½ΠΈΡ
ΠΏΠ»Π°ΡΡΠΈΠ½ ΠΡΡΡΠ»ΠΈΠΉΠ½-ΠΡΡΡΠΊΠΎΠ³ΠΎ ΠΈ ΠΠ°Π³Π°Π½ΡΠΊΠΎΠ³ΠΎ ΠΠΠ― Π³ΡΠ°Π½ΠΈΡΠΎΠΈΠ΄Ρ ΠΈ Π²ΡΠ»ΠΊΠ°Π½ΠΈΡΡ ΠΊΠΈΡΠ»ΠΎΠ³ΠΎ ΡΠΎΡΡΠ°Π²Π° Ρ Π²ΠΎΠ·ΡΠ°ΡΡΠΎΠΌ 249β211 ΠΌΠ»Π½ Π»Π΅Ρ ΠΎΠ±Π½Π°ΡΡΠΆΠΈΠ²Π°ΡΡ Π²ΠΎ ΠΌΠ½ΠΎΠ³ΠΎΠΌ ΡΡ
ΠΎΠ΄Π½ΡΠ΅ Π³Π΅ΠΎΡ
ΠΈΠΌΠΈΡΠ΅ΡΠΊΠΈΠ΅ Ρ
Π°ΡΠ°ΠΊΡΠ΅ΡΠΈΡΡΠΈΠΊΠΈ (ΠΏΠΎΠ²ΡΡΠ΅Π½Π½Π°Ρ ΡΠ΅Π»ΠΎΡΠ½ΠΎΡΡΡ, Π²ΡΡΠΎΠΊΠΈΠ΅ ΡΠΎΠ΄Π΅ΡΠΆΠ°Π½ΠΈΡ Sr ΠΈ Ba, ΡΠΌΠ΅ΡΠ΅Π½Π½ΡΠ΅ ΠΈ Π½ΠΈΠ·ΠΊΠΈΠ΅ ΠΊΠΎΠ½ΡΠ΅Π½ΡΡΠ°ΡΠΈΠΈ Nb, Y). ΠΠΎ ΡΠΎΠ΄Π΅ΡΠΆΠ°Π½ΠΈΡΠΌ ΡΠ΅Π΄ΠΊΠΈΡ
ΠΈ ΡΠ΅Π΄ΠΊΠΎΠ·Π΅ΠΌΠ΅Π»ΡΠ½ΡΡ
ΡΠ»Π΅ΠΌΠ΅Π½ΡΠΎΠ² Π΄Π°Π½Π½ΡΠ΅ Π³ΡΠ°Π½ΠΈΡΠΎΠΈΠ΄Ρ ΠΈ Π²ΡΠ»ΠΊΠ°Π½ΠΈΡΡ ΠΊΠΈΡΠ»ΠΎΠ³ΠΎ ΡΠΎΡΡΠ°Π²Π° ΠΎΠ±Π½Π°ΡΡΠΆΠΈΠ²Π°ΡΡ ΡΡ
ΠΎΠ΄ΡΡΠ²ΠΎ Ρ Π³ΡΠ°Π½ΠΈΡΠ°ΠΌΠΈ I-ΡΠΈΠΏΠ°. ΠΡΠΎΠ±Π΅Π½Π½ΠΎΡΡΠΈ ΡΠΎΡΡΠ°Π²ΠΎΠ² ΡΡΠΈΡ
ΠΏΠΎΡΠΎΠ΄ ΠΏΠΎΠ·Π²ΠΎΠ»ΡΡΡ Π΄ΠΎΠΏΡΡΠΊΠ°ΡΡ ΠΈΡ
ΡΠΎΡΠΌΠΈΡΠΎΠ²Π°Π½ΠΈΠ΅ Π² ΠΎΠ±ΡΡΠ°Π½ΠΎΠ²ΠΊΠ΅ Π°ΠΊΡΠΈΠ²Π½ΠΎΠΉ ΠΊΠΎΠ½ΡΠΈΠ½Π΅Π½ΡΠ°Π»ΡΠ½ΠΎΠΉ ΠΎΠΊΡΠ°ΠΈΠ½Ρ Π‘ΠΈΠ±ΠΈΡΡΠΊΠΎΠ³ΠΎ ΠΊΠΎΠ½ΡΠΈΠ½Π΅Π½ΡΠ° Π½Π°Π΄ ΠΏΠΎΠ³ΡΡΠΆΠ°ΡΡΠ΅ΠΉΡΡ ΠΎΠΊΠ΅Π°Π½ΠΈΡΠ΅ΡΠΊΠΎΠΉ ΠΏΠ»ΠΈΡΠΎΠΉ ΠΠΎΠ½Π³ΠΎΠ»ΠΎ-ΠΡ
ΠΎΡΡΠΊΠΎΠ³ΠΎ ΠΎΠΊΠ΅Π°Π½Π°. ΠΠ°ΠΈΠ±ΠΎΠ»Π΅Π΅ ΠΌΠΎΠ»ΠΎΠ΄ΡΠ΅ ΠΈΠ· ΠΈΠ·ΡΡΠ΅Π½Π½ΡΡ
ΠΏΠΎΡΠΎΠ΄ Π³ΡΠ°Π½ΠΈΡΠΎΠΈΠ΄Ρ ΠΠ°ΡΡΠΊΠΈΠ½ΡΠΊΠΎΠ³ΠΎ ΠΈ ΠΠ΅ΡΡ
Π½Π΅ΠΌΠ°Π½Π³ΠΈΡΡΡΠΉΡΠΊΠΎΠ³ΠΎ ΠΌΠ°ΡΡΠΈΠ²ΠΎΠ² Ρ Π²ΠΎΠ·ΡΠ°ΡΡΠΎΠΌ 178β152 ΠΌΠ»Π½ Π»Π΅Ρ ΡΠ°ΠΊΠΆΠ΅ ΠΎΠ±Π»Π°Π΄Π°ΡΡ ΡΡ
ΠΎΠ΄Π½ΡΠΌΠΈ Π³Π΅ΠΎΡ
ΠΈΠΌΠΈΡΠ΅ΡΠΊΠΈΠΌΠΈ Ρ
Π°ΡΠ°ΠΊΡΠ΅ΡΠΈΡΡΠΈΠΊΠ°ΠΌΠΈ. ΠΡΠ°Π½ΠΈΡΠΎΠΈΠ΄Ρ ΠΎΠ±ΠΎΠΈΡ
ΠΌΠ°ΡΡΠΈΠ²ΠΎΠ² ΡΠ²Π»ΡΡΡΡΡ ΠΆΠ΅Π»Π΅Π·ΠΈΡΡΡΠΌΠΈ, ΠΏΡΠ΅ΠΈΠΌΡΡΠ΅ΡΡΠ²Π΅Π½Π½ΠΎ ΡΠ΅Π»ΠΎΡΠ½ΡΠΌΠΈ ΠΎΠ±ΡΠ°Π·ΠΎΠ²Π°Π½ΠΈΡΠΌΠΈ. ΠΠΎ ΡΠΎΠ΄Π΅ΡΠΆΠ°Π½ΠΈΡΠΌ ΠΊΠ°ΠΊ ΠΏΠ΅ΡΡΠΎΠ³Π΅Π½Π½ΡΡ
, ΡΠ°ΠΊ ΠΈ ΡΠ΅Π΄ΠΊΠΈΡ
ΡΠ»Π΅ΠΌΠ΅Π½ΡΠΎΠ² ΠΎΠ½ΠΈ ΡΠΎΠΏΠΎΡΡΠ°Π²ΠΈΠΌΡ Ρ Π³ΡΠ°Π½ΠΈΡΠ°ΠΌΠΈ Π-ΡΠΈΠΏΠ°. Π€ΠΎΡΠΌΠΈΡΠΎΠ²Π°Π½ΠΈΠ΅ ΡΡΠΈΡ
Π³ΡΠ°Π½ΠΈΡΠΎΠΈΠ΄ΠΎΠ² ΠΈΠΌΠ΅Π»ΠΎ ΠΌΠ΅ΡΡΠΎ Π² ΡΡΠ»ΠΎΠ²ΠΈΡΡ
Π²Π½ΡΡΡΠΈΠΊΠΎΠ½ΡΠΈΠ½Π΅Π½ΡΠ°Π»ΡΠ½ΠΎΠ³ΠΎ ΡΠ°ΡΡΡΠΆΠ΅Π½ΠΈΡ Π½Π° ΡΠΎΠ½Π΅ ΡΠΌΠ΅Π½Ρ ΡΡΠ±Π΄ΡΠΊΡΠΈΠΎΠ½Π½ΠΎΠ³ΠΎ ΡΠ΅ΠΆΠΈΠΌΠ° Π½Π° ΠΊΠΎΠ»Π»ΠΈΠ·ΠΈΠΎΠ½Π½ΡΠΉ. Π Π°ΡΡΠΌΠΎΡΡΠ΅Π½Π½ΡΠ΅ Π² ΡΡΠ°ΡΡΠ΅ ΠΌΠ°ΡΠ΅ΡΠΈΠ°Π»Ρ ΠΏΠΎ Π²ΠΎΠ·ΡΠ°ΡΡΡ ΠΈ Π³Π΅ΠΎΡ
ΠΈΠΌΠΈΠΈ ΠΏΠΎΡΠΎΠ΄ Π½ΠΈΠΆΠ½ΠΈΡ
ΠΏΠ»Π°ΡΡΠΈΠ½ ΠΡΡΡΠ»ΠΈΠΉΠ½-ΠΡΡΡΠΊΠΎΠ³ΠΎ ΠΈ ΠΠ°Π³Π°Π½ΡΠΊΠΎΠ³ΠΎ ΠΠΠ― ΠΏΠΎΠΊΠ°Π·ΡΠ²Π°ΡΡ, ΡΡΠΎ ΡΡΠΈ ΠΏΠΎΡΠΎΠ΄Ρ Ρ
ΠΎΡΠΎΡΠΎ ΠΊΠΎΡΡΠ΅Π»ΠΈΡΡΡΡΡΡ Ρ ΠΏΠΎΡΠΎΠ΄Π½ΡΠΌΠΈ ΠΊΠΎΠΌΠΏΠ»Π΅ΠΊΡΠ°ΠΌΠΈ Π·Π°Π±Π°ΠΉΠΊΠ°Π»ΡΡΠΊΠΎΠ³ΠΎ ΠΈ ΡΠ΅Π²Π΅ΡΠΎ-ΠΌΠΎΠ½Π³ΠΎΠ»ΡΡΠΊΠΎΠ³ΠΎ ΡΠ΅Π³ΠΌΠ΅Π½ΡΠΎΠ² Π¦ΠΠ‘Π, ΡΠ²ΠΈΠ΄Π΅ΡΠ΅Π»ΡΡΡΠ²ΡΡ ΠΎ Π΅Π΄ΠΈΠ½ΠΎΠΉ ΠΈΡΡΠΎΡΠΈΠΈ ΡΠ²ΠΎΠ»ΡΡΠΈΠΈ Π²ΡΠ΅Π³ΠΎ ΡΡΠΎΠ³ΠΎ ΡΠ΅Π³ΠΈΠΎΠ½Π°.
ΠΠΠΠΠ ΠΠ ΠΠΠΠ ΠΠ Π ΠΠΠΠ¬Π¦ΠΠ€ΠΠ ΠΠ ΠΠΠ¬Π₯ΠΠΠ‘ΠΠΠΠ ΠΠΠΠΠΠΠΠ’ΠΠΠΠ Π’ΠΠ Π ΠΠΠΠ (ΠΠΠΠΠΠΠΠ ΠΠ ΠΠΠΠΠΠΠΠ¬Π, Π ΠΠ‘Π‘ΠΠ―)
Linear or lens-like carbonate (marble) and carbonate-silicate bodies among gabbro and amphibolites within the Krestovsky subterrane of the Olkhon composite terrane (West Baikal Area) are identified as dikes. The dikes commonly dip almost vertically, range in thickness from 20 cm to a few meters, and are up to 100 m long. The Olkhon marble dikes quite often coexist with dolerite dikes and/or granite veins and show signatures of emplacement synchronously with the igneous bodies. The marble dikes differ from mantle carbonatites in mineralogy and chemistry and thus may be derived from sedimentary carbonate rocks molten during collisional events.The origin of the Olkhon carbonate and carbonate-silicate dikes may be explained with two possible geodynamic scenarios. They may be derived either from Neoproterozoic carbonate sediments upon the Early Precambrian basement of a cratonic block which was involved in collisional events, or from abundant carbonate sedimentary material in an island-arc terrane. Large-scale melting of silicate and carbonate rocks was maintained by heat released from mantle mafic magma intruding into the lower crust. The batches of both crustal (carbonate and granitic) and mantle (mafic) melts intruded late during the collision in a strike-slip tectonic setting.Π ΡΡΠ°ΡΡΠ΅ Π΄Π°Π΅ΡΡΡ Ρ
Π°ΡΠ°ΠΊΡΠ΅ΡΠΈΡΡΠΈΠΊΠ° Π΄Π°Π΅ΠΊ ΠΌΡΠ°ΠΌΠΎΡΠΎΠ² ΠΈ ΠΊΠ°Π»ΡΡΠΈΡΠΈΡΠΎΠ² Π² ΠΏΡΠ΅Π΄Π΅Π»Π°Ρ
ΠΠ»ΡΡ
ΠΎΠ½ΡΠΊΠΎΠ³ΠΎ ΠΊΠΎΠΌΠΏΠΎΠ·ΠΈΡΠ½ΠΎΠ³ΠΎ ΡΠ΅ΡΡΠ΅ΠΉΠ½Π° (ΠΠ°ΠΏΠ°Π΄Π½ΠΎΠ΅ ΠΡΠΈΠ±Π°ΠΉΠΊΠ°Π»ΡΠ΅). ΠΠ°Π΄Π΅ΠΆΠ½ΠΎ ΠΎΠ±ΠΎΡΠ½ΠΎΠ²Π°Π½Π° Π΄Π°ΠΉΠΊΠΎΠ²Π°Ρ ΠΏΡΠΈΡΠΎΠ΄Π° Π»ΠΈΠ½Π΅ΠΉΠ½ΡΡ
ΠΈ Π»ΠΈΠ½Π·ΠΎΠ²ΠΈΠ΄Π½ΡΡ
ΡΠ΅Π» ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΡΡ
ΠΏΠΎΡΠΎΠ΄ Π² ΠΌΠ°ΡΡΠΈΠ²Π°Ρ
Π³Π°Π±Π±ΡΠΎ ΠΈ ΠΎΡΡΠΎΠ°ΠΌΡΠΈΠ±ΠΎΠ»ΠΈΡΠ°Ρ
ΠΡΠ΅ΡΡΠΎΠ²ΡΠΊΠΎΠ³ΠΎ ΡΡΠ±ΡΠ΅ΡΡΠ΅ΠΉΠ½Π°. ΠΡΠ΅ΠΎΠ±Π»Π°Π΄Π°ΡΡ ΡΡΠ±Π²Π΅ΡΡΠΈΠΊΠ°Π»ΡΠ½ΡΠ΅ Π΄Π°ΠΉΠΊΠΈ ΠΌΠΎΡΠ½ΠΎΡΡΡΡ ΠΎΡ 20 ΡΠΌ Π΄ΠΎ Π½Π΅ΡΠΊΠΎΠ»ΡΠΊΠΈΡ
ΠΌΠ΅ΡΡΠΎΠ² ΠΏΡΠΈ ΠΏΡΠΎΡΠ»Π΅ΠΆΠ΅Π½Π½ΠΎΠΉ ΠΏΡΠΎΡΡΠΆΠ΅Π½Π½ΠΎΡΡΠΈ, ΠΈΠ½ΠΎΠ³Π΄Π° ΠΏΡΠ΅Π²ΡΡΠ°ΡΡΠ΅ΠΉ 100 ΠΌ. ΠΠ΅ΡΠ΅Π΄ΠΊΠΎ ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΡΠ΅ Π΄Π°ΠΉΠΊΠΈ Π°ΡΡΠΎΡΠΈΠΈΡΡΡΡ Ρ Π΄Π°ΠΉΠΊΠ°ΠΌΠΈ Π΄ΠΎΠ»Π΅ΡΠΈΡΠΎΠ² ΠΈ/ΠΈΠ»ΠΈ ΠΆΠΈΠ»Π°ΠΌΠΈ Π³ΡΠ°Π½ΠΈΡΠΎΠ² Ρ ΠΏΡΠΈΠ·Π½Π°ΠΊΠ°ΠΌΠΈ ΡΡΠ±ΡΠΈΠ½Ρ
ΡΠΎΠ½Π½ΠΎΠ³ΠΎ Π²Π½Π΅Π΄ΡΠ΅Π½ΠΈΡ. ΠΠΎ ΠΌΠΈΠ½Π΅ΡΠ°Π»ΠΎΠ³ΠΎ-Π³Π΅ΠΎΡ
ΠΈΠΌΠΈΡΠ΅ΡΠΊΠΈΠΌ ΠΎΡΠΎΠ±Π΅Π½Π½ΠΎΡΡΡΠΌ ΠΈΠ·ΡΡΠ΅Π½Π½ΡΠ΅ Π΄Π°ΠΉΠΊΠΈ ΡΠ΅Π·ΠΊΠΎ ΠΎΡΠ»ΠΈΡΠ°ΡΡΡΡ ΠΎΡ ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠΈΡΠΎΠ² ΠΌΠ°Π½ΡΠΈΠΉΠ½ΠΎΠ³ΠΎ Π³Π΅Π½Π΅Π·ΠΈΡΠ° ΠΈ, ΠΏΡΠ΅Π΄ΠΏΠΎΠ»ΠΎΠΆΠΈΡΠ΅Π»ΡΠ½ΠΎ, ΡΠ²Π»ΡΡΡΡΡ ΠΏΡΠΎΠ΄ΡΠΊΡΠ°ΠΌΠΈ ΠΏΠ»Π°Π²Π»Π΅Π½ΠΈΡ ΠΏΠ΅ΡΠ²ΠΈΡΠ½ΠΎ-ΠΎΡΠ°Π΄ΠΎΡΠ½ΡΡ
ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΡΡ
ΡΠΎΠ»Ρ Π² ΡΠ΅Π·ΡΠ»ΡΡΠ°ΡΠ΅ ΠΊΠΎΠ»Π»ΠΈΠ·ΠΈΠΎΠ½Π½ΡΡ
ΠΏΡΠΎΡΠ΅ΡΡΠΎΠ².ΠΡΠ΅Π΄Π»Π°Π³Π°Π΅ΠΌΠ°Ρ ΠΌΠΎΠ΄Π΅Π»Ρ ΠΎΠ±ΡΠ°Π·ΠΎΠ²Π°Π½ΠΈΡ ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΡΡ
Π΄Π°Π΅ΠΊ Π²ΠΊΠ»ΡΡΠ°Π΅Ρ Π²ΠΎΠ²Π»Π΅ΡΠ΅Π½ΠΈΠ΅ ΡΡΠ°Π³ΠΌΠ΅Π½ΡΠ° ΡΠ°Π½Π½Π΅Π΄ΠΎΠΊΠ΅ΠΌΠ±ΡΠΈΠΉΡΠΊΠΎΠ³ΠΎ Π±Π»ΠΎΠΊΠ° Ρ ΠΏΠ΅ΡΠ΅ΠΊΡΡΠ²Π°ΡΡΠΈΠΌΠΈ Π½Π΅ΠΎΠΏΡΠΎΡΠ΅ΡΠΎΠ·ΠΎΠΉΡΠΊΠΈΠΌΠΈ ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΡΠΌΠΈ ΠΎΡΠ°Π΄ΠΊΠ°ΠΌΠΈ Π² ΠΏΡΠΎΡΠ΅ΡΡΠ΅ ΠΊΠΎΠ»Π»ΠΈΠ·ΠΈΠΈ ΠΊΠΎΠΌΠΏΠΎΠ·ΠΈΡΠ½ΠΎΠ³ΠΎ ΡΠ΅ΡΡΠ΅ΠΉΠ½Π° Ρ Π‘ΠΈΠ±ΠΈΡΡΠΊΠΈΠΌ ΠΊΡΠ°ΡΠΎΠ½ΠΎΠΌ. ΠΠ»ΡΡΠ΅ΡΠ½Π°ΡΠΈΠ²Π½ΡΠΌ Π²Π°ΡΠΈΠ°Π½ΡΠΎΠΌ ΡΠ²Π»ΡΠ΅ΡΡΡ ΠΏΡΠΈΡΡΡΡΡΠ²ΠΈΠ΅ Π·Π½Π°ΡΠΈΡΠ΅Π»ΡΠ½ΠΎΠ³ΠΎ ΠΊΠΎΠ»ΠΈΡΠ΅ΡΡΠ²Π° ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΡΡ
ΡΠΎΠ»Ρ Π² ΠΎΡΡΡΠΎΠ²ΠΎΠ΄ΡΠΆΠ½ΠΎΠΌ ΡΠ°Π·ΡΠ΅Π·Π΅. ΠΠΎΠ²ΡΡΠ΅Π½ΠΈΠ΅ ΡΠ΅ΠΌΠΏΠ΅ΡΠ°ΡΡΡΡ, ΡΠ²ΡΠ·Π°Π½Π½ΠΎΠ΅ Ρ Π²Π½Π΅Π΄ΡΠ΅Π½ΠΈΠ΅ΠΌ ΠΌΠ°Π½ΡΠΈΠΉΠ½ΡΡ
ΠΌΠ°Π³ΠΌ Π±Π°Π·ΠΈΡΠΎΠ²ΠΎΠ³ΠΎ ΡΠΎΡΡΠ°Π²Π° Π² Π½ΠΈΠΆΠ½ΠΈΠ΅ ΡΠ°ΡΡΠΈ ΠΊΠΎΡΡ, Π½Π°ΡΡΠ΄Ρ Ρ ΡΡΠΎΠ»ΡΠ΅Π½ΠΈΠ΅ΠΌ ΠΏΠΎΡΠ»Π΅Π΄Π½Π΅ΠΉ, ΠΎΠ±ΡΡΠ»ΠΎΠ²ΠΈΠ»ΠΎ ΠΌΠ°ΡΡΠΎΠ²ΠΎΠ΅ ΠΏΠ»Π°Π²Π»Π΅Π½ΠΈΠ΅ ΡΠΈΠ»ΠΈΠΊΠ°ΡΠ½ΡΡ
ΠΏΠΎΡΠΎΠ΄ Π°Π½Ρ
ΠΈΠ³ΡΠ°Π½ΠΈΡΠ½ΠΎΠ³ΠΎ ΡΠΎΡΡΠ°Π²Π° ΠΈ ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠΎΠ². Π ΠΏΡΠΎΡΠ΅ΡΡΠ΅ Π½Π°ΠΈΠ±ΠΎΠ»Π΅Π΅ ΠΌΠΎΡΠ½ΠΎ ΠΏΡΠΎΡΠ²Π»Π΅Π½Π½ΠΎΠ³ΠΎ ΡΠ΄Π²ΠΈΠ³ΠΎΠ²ΠΎΠ³ΠΎ ΡΠ΅ΠΊΡΠΎΠ³Π΅Π½Π΅Π·Π° ΠΏΡΠΎΠΈΡΡ
ΠΎΠ΄ΠΈΠ»ΠΎ Π²Π½Π΅Π΄ΡΠ΅Π½ΠΈΠ΅ ΠΏΠΎΡΡΠΈΠΉ Π³ΡΠ°Π½ΠΈΡΠ½ΠΎΠ³ΠΎ ΠΈ ΠΊΠ°ΡΠ±ΠΎΠ½Π°ΡΠ½ΠΎΠ³ΠΎ ΡΠΎΡΡΠ°Π²Π°, Π° ΡΠ°ΠΊΠΆΠ΅ ΠΌΠ°Π½ΡΠΈΠΉΠ½ΡΡ
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