A New Stratigraphic Scale for the Precambrian of the Ussr

Семихатов, М. А.; Shurkin, Kathleen; Aksenov, Ye. M.; Bekker, Yu. R.; Bibikova, Ye. V.; Duk, V. L.; Yesipchuk, K. Ye.; Karsakov, L. P.; Kiselev, V. V.; Kozlov, V. L.; Лобач-Жученко, С. Б.; Negrutsa, V. Z.; Robonen, V. I.; Sez'ko, A. I.; Filatova, L. I.; Khomentovskiy, V. V.; Shemyakin, V. M.; diner, V. I. Shul'

doi:10.1080/00206819109465699

Cited by 12 publications

(9 citation statements)

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“…Traces of the Dalslandian orogen are recognised in western Norway, southern Sweden and possibly also in the Dobrogea (Garetsky, 1990). Angular unconformities between Middle and Late Riphean series are also evident in the Uralian domain from which low-grade metamorphic and plutonic rocks have been reported (Keller and Chumakov, 1983;Semikhatov et al, 1991). Also in the interior rifts, a major break in sedimentation straddles the Middle-Late Riphean boundary (Fig.…”

Section: Middle Riphean (1350-1050 Ma)mentioning

confidence: 82%

“…3) indicates that towards the end of the Early Riphean the entire craton was uplifted, perhaps in response to compressional deformation of its western and eastern margins. Occurrences of metamorphic rocks and granitic plutons, yielding radiometric ages in the 1.4-1.2 Ga range, have been reported from eastern Poland, the Trans-Scandinavian magmatic belt, and the Urals (Pozaryski, 1977;Semikhatov et al, 1991;Milanovsky et al, 1994).…”

Section: Early Riphean (1650-1350 Ma)mentioning

confidence: 99%

“…4, are more reliable. For the Precambrian, the time scale of Semikhatov et al (1991) and for the Phanerozoic, the Harland et al (1990) scale were adopted. Our analysis of the Riphean to early Mesozoic evolution of the EEC is based on regional compilations and syntheses of stratigraphical and structural data, an inventory of magmatic activity, and the construction of a set of regional, interpretative palaeogeographic-palaeotectonic maps.…”

Section: L%4mentioning

confidence: 99%

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Late Precambrian to Triassic history of the East European Craton: dynamics of sedimentary basin evolution

et al. 1996

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During its Riphean to Palaeozoic evolution, the East European Craton was affected by rift phases during Early, Middle and Late Riphean, early Vendian, early Palaeozoic, Early Devonian and Middle-Late Devonian times and again at the transition from the Carboniferous to the Permian and the Permian to the Triassic. These main rifting cycles were separated by phases of intraplate compressional tectonics at the transition from the Early to the Middle Riphean, the Middle to the Late Riphean, the Late Riphean to the Vendian, during the mid-Early Cambrian, at the transition from the Cambrian to the Ordovician, the Silurian to the Early Devonian, the Early to the Middle Devonian, the Carboniferous to Permian and the Triassic to the Jurassic. Main rift cycles axe dynamically related to the separation of continental terranes from the margins of the East European Craton and the opening of Atlantic-type palaeo-oceans and/or back-arc basins. Phases of intraplate compression, causing inversion of extensional basins, coincide with the development of collisional belts along the margins of the East European Craton. The origin and evolution of sedimentary basins on the East European Craton was governed by repeatedly changing regional stress fields. Periods of stress field changes coincide with changes in the drift direction, velocity and rotation of the East European plate and its interaction with adjacent plates. Intraplate magmatism was controlled by changes in stress fields and by mantle hot-spot activity. Geodynamieally speaking, different types of magmatism occurred simultaneously.

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Section: Middle Riphean (1350-1050 Ma)mentioning

confidence: 82%

Section: Early Riphean (1650-1350 Ma)mentioning

confidence: 99%

Section: L%4mentioning

confidence: 99%

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Late Precambrian to Triassic history of the East European Craton: dynamics of sedimentary basin evolution

et al. 1996

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“…This succession is one of the most complete Lower Proterozoic sections and embraces a significant geological time interval from 2.55 to 1.65 Ga (Sokolov et al, 1970;Salop, 1973;Semikhatov et al, 1991). Terrigenous-carbonatevolcanic complexes are exposed in different parts of the Baltic Shield: in the north (Pechenga-ImandraVarzuga belt), northwest (Kemi-Perapohja, Kuusamo, and Kainuu belts), southwest (Kiihtelys vaara area), and southeast (Karelian Craton).…”

Section: Geological Overview and Setting Of The Zaonega Formationmentioning

confidence: 97%

Strontium isotope composition of the lower proterozoic carbonate concretions: The Zaonega Formation, Southeast Karelia

Кузнецов

Горохов

Melezhik

et al. 2012

Lithol Miner Resour

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The middle part of the volcanosedimentary Zaonega Formation of the Ludikovian Suprahorizon (approximately 2.0 Ga) includes large carbonates concretions and lenses in shungite layers. Carbonate lenses and concretions are primarily elongated and flattened, and their thickness varies from tens of centimeters to a few meters. Some lenses retain relicts of lamination. Concretions are composed of calcite or dolomite. They contain abundant organic matter, as well as mica, talc, chlorite, quartz, and pyrite crystals. The calcite con cretions contain some dolomite admixture (Mg/Ca = 0.011-0.045) and differ from sedimentary limestones by a low Fe/Mn value (0.3-2.1). The Sr content is as much as 385-505 μg/g in most samples and is low (86 μg/g) only in one sample. The Rb-Sr systematics of carbonate concretions was studied with the stepwise dissolution procedure, which included processing with the ammonium acetate solution (AMA fraction) to partially remove the secondary carbonate material, with dissolution of the residue in acetic acid (ACA frac tion). In individual calcite samples, discrepancy between the measured 87 Sr/ 86 Sr values in the AMA and ACA calcite fractions shows a variation range of 0.0008-0.0033. The initial 87 Sr/ 86 Sr ratio in the ACA fractions of the studied samples varies from 0.7053 to 0.7162. The ratio shows a positive correlation with Mg/Ca and the proportion of siliciclastic admixture and negative correlation with the Mn content. The concretions were formed when the sediments subsided, probably, during the transition from a zone with "mild" reductive con ditions to zones with active sulfate reduction and methanogenesis. In the sulfate reduction zone, where most pyrite bearing concretions were formed, the sediment was not geochemically exchaged with the bottom water and was evolved into a closed or semiclosed system. Processes of diagenesis in this zone promoted the release of the radiogenic 87 Sr from the associated siliciclastic minerals, resulting in growth of the initial 87 Sr/ 86 Sr in concretions up to 0.7108-0.7162. Some calcite concretions, which lacked pyrite (or contained its minimal amount) were likely formed in a thin surficial sediment layer located above the sulfate reduction zone. There fore, they precipitated Sr in isotope equilibrium with Sr of the bottom water. However, large concretions and carbonate lenses with an insignificant siliciclastic admixture could retain the signature of early diagenesis or even sedimentation. The initial 87 Sr/ 86 Sr ratio in one of such samples with the siliciclastic admixture of 6.2% makes it possible to estimate the maximal value of this ratio (0.7053) in the Ludikovian paleobasin.

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“…These include the IUGS International Stratigraphic Chart (2000), the older International Stratigraphic Chart of Plumb (1991), as well as the Russian timescale (Semikhatov et al, 1991) in which Riphean and Vendian subdivide parts of the Precambrian. For the convenience of the reader, the various timescales are summarized (Fig.…”

Section: Introductionmentioning

confidence: 99%