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Luminescence chronostratigraphy for the loess deposits in Złota, Poland

where the loess cover is preserved and its thickness rarely exceeds a few meters. In south-western Poland, several independent loess cover forms can be seen. Each form can be characterized by different sediment thickness, stratigraphy or physical properties. Such a large variety of loess deposits depending on their east-west geographical location is explained by the influence of continental climate in the eastern part of Poland and more oceanic in the western part ( Cegła, 1972 ; Jersak, 1973 ; Jary, 2007 ). Investigations showing the distribution of loess cover in

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Historical metallurgical activities and environment pollution at the substratum level of the Main Market Square in Krakow

can be avoided); – stratum — spatially defined entity of homogenous content, distinguished by stratigraphic context, physical features and cultural content of illegible, primary character. Thus in this article, when describing the anthropogenic origin of the substrata of the Main Market Square in Kra-kow, the terms ‘deposit’, ‘strata’ and ‘stratum’ will be used — when we have in mind their successive formation as a consequence of their self-accumulation, or intention-al accumulation of matter (including waste) as a consequnce of the functioning of the town

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Regional Conditions for Maximum Probable Discharge in Poland’s Rivers

REFERENCES Acreman M.C., Sinclair C.D., 1986, Classification of drainage basins according to their physical characteristics; an application for flood frequency analysis in Scotland, Journal of Hydrology , 84, 365-380. Bartniak A., Jokiel P., 2008, Odpływy maksymalne i indeksy powodziowości rzeki półkuli północnej [Maximum flows and river flood indexes on the North Hemisphere], Przegląd Geograficzny , 80, 3, 361-383. Bayliss A.C., Reed D.W., 2001, The use of historical data in flood frequency estimation . Report to MAFF. Centre for Ecology and

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Paleoenvironments during the Rhaetian transgression and the colonization history of marine biota in the Fatric Unit (Western Carpathians)

Abstract

Terminal Triassic environmental changes are characterized by an integrated study of lithology, litho- and cyclostratigraphy, paleontology, mineralogy, geochemistry and rock magnetism in the Tatra Mts. The Carpathian Keuper sequence was deposited in an arid environment with only seasonal rivers, temporal lakes and swamps with scarce vegetation. Combination of a wide range of δ18O values (-0.7 to + 2.7) with negative δ13C values documents dolomite precipitation either from brackish or hypersaline lake water, or its derivation from pore water comparably to the Recent Coorong B-dolostone. Negative δ13C values indicate microbial C productivity. Rhaetian transgressive deposits with restricted Rhaetavicula fauna accumulated in nearshore swamps and lagoons. Associations of foraminifers, bivalves and sharks in the Zliechov Basin were controlled by physical factors. Bivalve mollusc biostromes were repetitively destroyed by storms, and temporary firm bottoms were colonized by oysters and burrowers. Subsequent black shale deposition recorded input of eolian dust. Bottom colonization by pachyodont bivalves, brachiopod and corals started much later, during highstand conditions. Facies evolution also revealed by geochemical data, C and O isotope curves reflect eustatic and climatic changes and help reconstruct the evolution of Rhaetian marine carbonate ramp. The Fatra Formation consists of 100 kyr eccentricity and 40 kyr obliquity cycles; much finer rhythmicity may record monsoonlike climatic fluctuations. Fluvial and eolian events were indicated by analysis of grain size and content of clastic quartz, concentrations of foraminiferal (Agathammina) tests in thin laminae indicates marine ingression events. Magnetic susceptibility (MS) variations reflect the distribution of authigenic and detrital constituents in the sequence. Increasing trend of MS correlates with the regressive Carpathian Keuper sequence and culminates within the bottom part of the Fatra Formation. Decreasing trend of MS is observed upwards the transgressive deposits of the Fatra Formation.

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Mineral stability of Fe-rich bentonite in the Mock-Up-CZ experiment

References Amman L., Bergaya F. & Lagaly G. 2005: Determination of the cation exchange capacity of clays with copper complexes revisited. Clay Miner. 40, 441-453. Bujdák J., Iyi N., Kaneko Y., Czimerová A. & Sasai R. 2003: Molecular arrangement of rhodamine 6G cations in the films of layered silicates: the effect of the layer charge. Physical Chemistry Chemical Physics 5, 4680-4685. Czimerová A., Bujdák J. & Dohrmann R. 2006: Traditional and novel methods for estimating the

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Soil as the landscape balance indicator

, Izd. Moskowskogo Uniwersiteta, Moskwa. Kostrzewski, A (ed.) 1995, Zintegrowany monitoring środowiska przyrodniczego. Stan geosystemów Polski w 1994 roku [Integrated monitoring of the natural environment. The state of geosystems in Poland in 1994]. Environmental Monitoring Library, PIOŚ, Warsaw (In Polish). Lemercier, B, Gaudin, L, Walter, C, Auroussean, P, Arrouays, D, Schvartz, C, Saby, NPA PA , Follain, S & Abrassart, J 2008, ‘Soil phosphorus monitoring at the regional level by means of a soil test database’, Soil Use and

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Reconsidering Zipf’s law for regional development: The case of settlements and cities in Croatia

, ‘Pareto versus lognormal: a Maximum entropy test’, Physical Review E , vol. 84, no. 2, 10.1103/PhysRevE.84.026104 . Bee M Riccaboni M Schiavo S 2011 ‘Pareto versus lognormal: a Maximum entropy testPhysical Review E 84 2 10.1103/PhysRevE.84.026104 Bee, M, Riccaboni M & Schiavo, S 2013, ‘The size distribution of U.S. cities: Not Pareto, even in the tail’, Economics Letters , vol. 120, pp. 233-237. Bee M Riccaboni M Schiavo S 2013 ‘The size distribution of U.S. cities: Not Pareto, even in the tail’ Economics Letters 120 233 237 Borozan, D 2017, ‘Internal migration

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Does Zipf’s law hold for Polish cities?

References Alperovich, G & Deutsch, J 1995, ‘The size distribution of urban areas: Testing for the appropriateness of the Pareto distribution using a generalized Box-Cox transformation function’, Journal of Regional Science , vol. 35, pp. 267–276. Auerbach, F 1913, ‘Das Gesetz der Bevölkerungskonzentration’, Petermann’s Geographische Mitteilungen , vol. 59, pp. 74–76. Bee, M, Riccaboni, M & Schiavo, S 2013, ‘The size distribution of US cities: Not Pareto, even in the tail’, Economics Letters , vol. 120, no. 2, pp. 232–237. Berry, BJL

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Lichenometry and Schmidt hammer tests in the Kaunertal glacier foreland (Ötztal Alps) during the AMADEE-15 Mars Mission Simulation

conditions on the ISS’, International Journal of Astrobiology, vol 14, no. 3, pp. 411‑425. DOI: https://doi.org/10.1017/S1473550414000214. Burga, CA, Frauenfelder, R, Ruffet, J, Hoelzle, M & Kääb, A 2004, ‘Vegetation on Alpine rock glacier surfaces: a contribution to abundance and dynamics on extreme plant habitats’, Flora, vol. 199, pp. 505-515. Day, MJ & Goudie, AS 1977, ‘Field assessment of rock hardness using the Schmidt test hammer’, British Geomorphological Research Group Technical Bulletin, vol. 18, pp. 19‑29. Dąbski

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Bentonite from the Central Slovakia Volcanic Field – A Prospective Raw Material for Polish Industry

.E. & Marantos, I. (2016). Mineralogy, geochemistry and physical properties of bentonites from the Western Thrace Region and the islands of Samos and Chios, East Aegean, Greece. Clay Minerals, 51, 563-588. DOI: 10.1180/claymin.2016.051.4.03. Kraus, I., Čičel, B. & Machajdik, D. (1982). Origin and genesis of the clays resulting from alteration of rhyolite volcanic rocks in Central Slovakia. Geologica Carpathica, 33, 269-275. Kraus, I., Hroncová, Z., Horský, S. & Mihalič, A. (1989). Ložiská a výskyty bentonitov SSR. Deposits and occurrence of

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