Special paleogeographic characteristics and changes in δ18O values in Upper Pleistocene deposits of the Moravian Plateau 247 Hungarian Geographical Bulletin 60 (3) (2011) 247–259. Special paleogeographic characteristics and changes in δ18O values in Upper Pleistocene deposits of the Moravian Plateau Éva KIS1, Ferenc SCHWEITZER1, István FUTÓ2, Gergely VODILA2 János BALOGH1 and Mária di GLERIA1 Abstract Our own new environment-discrimination proxies, which include beyond the traditional sedimentary parameters our newly introduced indices (fi neness grade: Fg and degree of weathering: Kd), δ18O values and stratigraphic data were used in our study to compare loess-paleosol sequences with the data of mid-latitude deep-sea sediments and ice cores from Greenland. By our data from the Červený kopec section completed with other sur- rounding sequences, we came to the conclusion that the section consists of the last glacial (Würm) and last interglacial (Riss/Würm) deposits. The double paleosols equivalent with the MF1 soils (according to the Hungarian loess terminology) can be found together only in some places. In most of the sections only some part of the complex remained (e.g. the chernozem soil in Dolní Vĕstonice with an age of 30.9 ky BP; the forest soil in Červený kopec – Bohunice-type culture: 40.2 ky BP). The MF2 paleosol is situated in the lower part of the section and it was formed during the MIS 5 (Marine Isotope Stage). Keywords: Quaternary, loess-paleosol series, paleoclimate, δ18O, granulometric parameters, demarcation of the layers, warming and cooling peaks, erosional gaps. Introduction The variations of the paleogeographic environment were investigated using sedimentological parameter values of samples from the northwestern fringe of the Carpathian Basin. 1 Geographical Research Institute Hungarian Academy of Sciences, H-1112 Budaörsi út 45. Budapest, Hungary. E-mail: for Eva Kis: csapkam@sparc.core.hu, schweitf@mtafk i.hu, baloghj@ helka.iif.hu, digleria@freemail.hu 2 Institute of Nuclear Research of the Hungarian Academy of Sciences, H-4026 Bem tér 18/C, Debrecen, Hungary. E-mail: futo@atomki.hu, gvodila@atomki.hu 248 We would like to contribute to the scientifi c studies of the environ- mental changes during the last 2 million years and to the understanding of the cooling and warming stages of the last major glaciation. The Červený kopec (Red Hill) section (photos 1 and 2) was investigated in this paper due to its location in the so called “Moravian Gate”. All of the variations of the North European and the Alpine glaciations could be examined in the outcrop. It is situated at the southeastern fringe of the Bohemian Massif, 50 kilometers to the one-time southernmost limit of the Pleistocene inland ice sheet and also close to the Danube and to the foreland of the glaciated Alps. The uplift of the area was caused by postglacial gradual crustal movements, so the height of the uppermost, fi ft h (V) river terrace is 280 m above sea level. The loess-covered terraces are the most reliable evidence of the uplift ing. The outcrop is situated on the uppermost two terraces of the terrace- system along the Svratka River (photos 3, 4, 5). The hiatuses are scarce, the loca- tion of the Brunhes/Matuyama paleomagnetic boundary and of the Jaramillo event is known in the series. It is important because the upper part of the long section of Krems is missing, and it consists almost only of loess-paleosol series older than B/M. In the course of the crustal movements in the last 700 thousand years vast amount of sediments were eroded. The generalized section from the series of the Krems site combined with the series of Červený kopec can be regarded the most complete loess-paleosol sequence in Central Europe. The stratigraphic investigations of the Červený kopec section were conducted by Kukla, G.J. (1975); Fink, J. and Kukla, G.J. (1977); Smolíková, L. (1982); Zeman, A. (1992) and others. The loess-paleosol series is underlain by Lower Devonian red sandstone with high quartz-content, conglomerate and arcose (Photo 6, Demek, J. et al. 2005). The arcose was formed from the weathering of the granite of the Lower Devonian Caledonian Mountains with high feldspar content (>25%), its thick- ness varies between 100 m to few thousand meters. The conglomerate is lo- cally overlain by Miocene limestone (Smolíková, L. and Zeman, A. 1982). Above the pre-Quaternary strata fl uvial river terraces (covered by Younger and Older Gravel) and loess-paleosol series can be found (Photo 7). The Younger and Older Gravel covers are gravelly sand layers, and ferrett o-like soils were formed on them (Smolíková, L. and Zeman, A. 1982). These soils can be catego- rized in the same group as the terra rossae, the diff erence is only the bedrock, which is siliceous (e.g. gravel and sand) in the case of the ferrett o soils. The soils directly superimposing the gravel and sand layers were formed in situ, its position is autochthonous. Our sample from the uppermost paleosol is also of this kind and above it recent chernozem-like soil has formed (Photo 8). We have investigated the sediment series of the upper two steps of the Červený kopec section (Photo 1). The signifi cant thickness of the section is due to its location between the Alpine and Fennoscandinavian glaciated 249 Photo 1. The outcrop of Červený kopec exposed on the V and IV terraces of the Svratka River (Photo by Kis, É.) Photo 2. The environment of the outcrop at the eastern fringe of the Bohemian Massif (Source: Google Earth™) 250 Photo 3. Loess-paleosol series on the V terrace (the recent soil formed on a fossil pedogene horizon) (Photo by Kis, É.) Photo 4. The location of the terrace system (Photo by Kis, É.) 251 Photo 6. The underlying conglomer- ate derived from Devonian sandstone (Photo by Kis, É.) Photo 7. The gravel and sand material of the V terrace (Photo by Kis, É.) Photo 8. The uppermost loess layer of the outcrop (Photo by Kis, É.) Photo 5. The view from the III terrace to the river valley. The B/M paleomagnetic boundary is located in the lower part of the terrace (Photo by Kis, É.) 252 zones. During the glacial periods in the environs of the section three main wind directions have defi ned the eolian sedimentation: the westerlies in the east-west corridor along latitude 50°N, the north-westerly winds from the Fennoscandinavian ice sheet, and according to Rozycki, Sz. (1991) and Rousseau, D.D. et al. (2007) the Saharan dust from south was also relevant. This last conception about the role of the Saharan dust was confi rmed by the studies of Varga, Gy. (2007, 2010, 2011). The dust deposition was dominant under the cold continental climate of the glacial periods, while during the warm and moist interglacials pedogene processes played primary role. The section covers the last glacial-interglacial cycle (~125 ky; OXY Stage 5 – Kukla, G.J. and Cílek, V. 1996, ODP-677 record – Shackleton, N.J. et al. 1990, benthic δ18O, the B loess/paleosol cycle – Kukla, G.J. 1975). The B subcycle contains three soil series (PK-I, PK-II., PK-III.; Demek, J. and Kukla, G.J. 1969). The investigated section comprises the uppermost strata of the sediments covering the V and IV terraces of the Svratka River. The study was especially important, because the section is almost complete and made up from in situ sediments. The surrounding deposits with the same age were formed from redeposited material. The section can be used as the upper part (B cycle) of the Central European general section. From the results of our studies, we can get a fairly good overview of the paleogeographic variations in the last 125 ky. The lowest deposits (overlying the Miocene terrace gravels) are rather old; their formion could precede the Matuyama/Gauss paleomagnetic bound- ary. The B/M boundary and the Jaramillo event were reached by several drills (e.g. 830 and 831 by Zeman, A. 1992). The B/M can be found in the loess be- tween the PC-Xa and the PC-X paleosols. The relatively complete sequence can be correlated well with other mid-latitude sections situated on terrace- systems uplift ed by crustal movements in the foreground of large mountains (e.g. Tibet). In the case of Červený kopec fi ve, while at Lanzhou six terraces build up the terrace system (Kukla, G.J. and Cílek, V. 1996). Methods In the course of the studies, we have compared the section of Červený kopec along the Middle Danube with the paleoclimatic data of the ice core GISP2 from Greenland. We have studied how to establish the cold-warm periods of the ice cores (estimated by isotope-stratigraphic methods) in the terrestrial sediments, and how to determine the limit of the Pleistocene glaciations. The section was characterized by our own new environment-discrimi- nation proxies, which include beyond the traditional sedimentary parameters 253 our newly introduced indices (fi neness grade: Fg and degree of weathering: Kd), and δ18O-values, which were not used in previous studies. The curves of the measured and calculated values were plott ed next to the section, so the data of each horizon can be promptly determined. The grain-size of the samples was measured using a Fritsch Analysett e Microtec 22 laser grain-size analyzer in the Laboratory for Sediment and Soil Analysis in the Geographical Research Institute of the Hungarian Academy of Sciences (HAS). The oxygen-isotope (δ18O) values were determined in the Laboratory of Environmental Studies in the Institute of Nuclear Research (HAS) using a Thermo Finnigan DeltaPLUS XP stable isotope mass spectrometer. Results On the evaluation fi gure of the Červený kopec outcrop next to the section the following parameters were plott ed: CaCO3 content, δ18O values, MIS values, sedimentary cycles, clay content, the diff erent new and traditional sedimentary parameters and grain-size distribution values. With the comparison of these parameters with the δ18O values of the ice cores from Greenland (GRIP/GISP2) we can make conclusions about the characteristics of the sediments and fairly reliable estimations about their age. All values of a given depth can be easily determined from the fi gure. The following stratigraphic units were determined in the outcrop (Figure 1, Photo 1): I. 9 soil horizons − 1 B horizon of the recent soil (Photo 3, 8) − 2 redeposited soils − 6 paleosols – “Stillfried B” (Photo 9, 10) and “Stillfried A” (photos 11 and 12) pedocomplexes and the chernozem soil between them II. 5 loess layers (Kiss, É. 2004, photos 8, 9, 10, and 12). The stratigraphic column of the Červený kopec section consist of loess and paleosol horizons of the last glacial-interglacial cycles (Würm glacial and Riss/Würm interglacial) from ~125 ky onward. The units based on its param- eter values can be correlated with the similar sediments of the Stillfried (Photos 13, 14, 15) and the Dolní Vĕstonice (Photos 16, 17) sections. The section of the last interglacial/glacial period lying on one of the most beautiful terrace-system of Central Europe is almost complete. The δ18O values and sedimentary parameters of our own available loess-paleosol sec- tions can be compared with the data of deep-sea sediments and ice cores. The δ18O values of the carbonates are refl ecting the paleotemperature conditions during their formation. These were also aff ected by the waters from diff erent sources (e.g. precipitation, the water removal due to desiccation 254 Fi g. 1 . G ra nu lo m et ri c pa ra m et er v al ue s b y sa m pl es fr om th e Č er ve ný k op ec se ct io n (K is , É .). S tr at ig ra ph ic al a na ly si s: S ch w ei tz er , F ., K is , É ., Ba lo gh , J . a nd d i G le ri a, M . O xy ge n is ot op e m ea su re m en ts : F ut ó, J. a nd V od il a, G . G ra nu lo m et ri c an al ys es in 9 g ra in -s iz e ca te go ri es : d i G le ri a, M . 255 Photo 10. The fossil soil of the II step (Photo by Kis, É.) Photo 9. The II step on the IV terrace (Photo by Kis, É.) Photo 11. Loess layers between paleosols in the substrate of the I step (Photo by Kis, É.) 256 Photo 13. The Stillfried B pedocomplex (under the sample 22) in the Stillfried section (Photo by Kis, É.) Photo 12. Fossil soil in the middle part of the I step (Photo by Kis, É.) Photo 14. The triple PK-III pedocomplex in the Stillfried section (Photo by Kis, É.) Photo 15. The lowest brown forest soil of the PK-III pedocomplex with krotovinas and traces of soli-fl uctional processes in its lowermost part in the Stillfried sec- tion (Photo by Kis, É.) 257 Photo 16. The brown forest soil (low- er) and the chernozem soil (upper) of the PK-III pedocomplex in the Dolní Vĕstonice section (Photo by Kis, É.) Photo 17. The lowest part (R/W inter- glacial) of the PK-III pedocomplex and the underlying Riss loess in the Dolní Vĕstonice section (Photo by Kis, É.) under warm climates – Demény, A. et al. 2010). According to Kis, É. (2010) the series of Červený kopec consist of the last glacial (Würm) and last interglacial (Riss/Würm) deposits, based on their values. The maxima of the isotope curves represent the coldest climate (full glaciations), while the minimum values mean the warmest phases of the interglacial periods. Our oxygen-isotope curves agree especially well with the Kd index (degree of weathering), with the clay-content, with the CaCO3 content, with the data of deep-sea sediments and ice cores. The concordant values of the ca. 10 parameters of the stratigraphic column allow to separate and compare the units, also those which were not visible to the naked eye. By these parameters, the diff erentiation of forest and chernozem soils is quite good. We can affi rm the opinion of Valoch, K. (1996) who has stated that the two parts (the upper chernozem and lower forest soil) of paleosols equivalent with our MF1 soils can be found together only in some places (e.g. Stillfried). In most of the sections only one part of the complex remained (e.g. the chernozem soil in Dolní Vĕstonice with an age of 30,9 ky BP; the forest soil in Červený kopec – Bohunice-type culture: 40,2 ky BP). According to Valoch, 258 K. (1996), the lack of the lower part of the “Stillfried B” soils is peculiar in fl at terrains, while the absence of the upper part is typical on the more diff erenti- ated areas, where the chernozem soil was eroded during the uplift . Richter, D. et al. 2009 have explained the ~10 ky hiatus within the MF1 soil also with erosion, and the TL age of the lower soil is 48.2±1.9 ky, its OSL age is 58.7±5.8 ky (EVA-LUM-07/02), the OSL age of the loess above the upper soil is 30.9±3.1 ka (EVA-LUM-07/01). The MF2 soil in the Červený kopec section is similar; its upper chernozem soil was formed during the glacial, while the lower forest soil belongs to the R/W interglacial. According to Gábris, Gy. (2006), the MF2 soils in Hungary were formed in the last interglacial. Based on our results, the Červený kopec section represents nobly the regional characteristics of the Late Pleistocene loess deposits. Acknowledgements: The research (measurements and publication) was supported by the K63814 OTKA project (Hungarian Scientifi c Research Fund). REFERENCES Demek, J. and Kukla, J. 1969. Periglazialzone, Löss und Paläolithicum der Tschechoslowakei. Brno, Tschechoslowakische Akademie der Wissenschaft en, Geographisches Institut 158 p. Demek, J., Havlíček, M., Kirchner, K., Petrová, P., Bubík, M. and Gilíková, H. 2005. Příspěvek k poznání geologické situace na JV svahu Červeného kopce v Brně. Geologické výzkumy na Moravě a ve Slezsku v roce 2004 12, srpen, 8–11. Demény, A., Schöll-Barna, G., Siklósy, Z., Bodnár, M., Sümegi, P., Serlegi, G., Fábián, Sz. and Fórizs, I. 2010. Az elmúlt ötezer év éghajlat-változási eseményei a Kárpát-medencében és társadalmi hatásaik (Climate change events in the Carpathian Basin in the last fi ve thousand years, and their eff ects on society). Klíma-21 Füzetek 59. 82–94. Fink, J. and Kukla, G.J. 1977. Pleistocene climate in Central Europe at least 17 interglacials aft er Olduvai event. New York, Quaternary Research 7, C7, 36, 3. 371. Gábris, Gy. 2006. A magyarországi folyóteraszok kialakulásának és korbeosztásának magyarázata az oxigénizotóp-sztratigráfi a tükrében (Explanation of river terrace formation and chronology in Hungary in the light of oxygen isotope stratigraphy). Földrajzi Közlemények 130. (3–4): 123–133. Kis, É. 2004. Őskörnyezet-változások vizsgálata a dolní-věstonicei feltárás környezetében. (Studies on paleoenvironmental changes in the vicinity of the exposure at Dolní Věstonice) In Táj és környezet. Tiszteletkötet a 75 éves Marosi Sándornak. Eds. Dövényi, Z. and Schweitzer, F. Budapest, Geographical Research Institute of HAS 121–138. Kukla, G.J. 1975. Loess stratigraphy of Central Europe. In Aft er the Australopithecines. Eds. Butzer, K.W. and Isaac, G.L. The Hague–Paris, Mouton Publishers, 99–188. Kukla, G.J. 1977. Pleistocene land-sea correlations. 1. Europe. Earth Sci. Rev. 13. 307–374. Kukla, G.J. and Cílek, V. 1996. Plio-Pleistocene megacycles: record of climate and tectonics. Palaeogeography, Palaeoclimatology, Palaeoecology. 120. 171–194. Richter, D., Tostevin, G., Skrdla, P. and Davies, W. 2009. New radiometric ages for the Early Upper Paleolithic type locallity of Brno-Bohunice (Czeh Republic): comparison of OSL, IRSL, TL and 14C dating results. Journal of Archeological Science 36. 708–720. 259 Rousseau, D.D., Derbyshire, E., Antoine, P. and Hatte, C. 2007. European loess records. In Encyclopedia of Quaternary Science. Ed. Elias, S.A. Amsterdam, Elsevier publisher, 2. 1440–1456 Rozycki, Sz. 1991. Loess and loess-like deposits. Wroclaw, Ossolineum, Polish Academy of Sciences. 187 p. Shackleton, N.J., van Andel, T., Boyle, E.A., Jansen, E., Labeyrie, L.D., Leinen, M., McKenzie, J., Mayer, L.A. and Sundquist, E. 1990. Contributions from the oce- anic record to the study of global change on three time scales. Palaeogeography, Palaeoclimatology, Palaeoecology (Global and Planetary Change Section). 82. 5–37. Smolíková, L. 1982. Fosilí půdy ve sprašových sériích. Brno, Studia Geographica, 80. 107–134. Smolíková, L. and Zeman, A. 1982. Bedeutung der Ferreto – Böden für die Quartärstratigraphie. Praha, Sborník geologických věd, Antropozoikum. Series A 14. 57–93. Valoch, K. 1996. Das Mitt elwürm in den Lössen Südmährens und seine paläolitischen Kulturen. Hannover, Eiszeitalter und Gegenwart 46. 54–64. Varga, Gy. 2007. Hasonlóságok a világ legidősebb löszfeltárásai és a Kárpát-medence idős löszei között (Similarities of the oldest loesses in the World and Hungary). Modern Geográfi a 2. 19 p. Varga, Gy. 2010. Gondolatok a porviharok és a klimatikus, környezeti folyamatok össze- függéseiről (On the relationships between dust storms and climatic processes). Földrajzi Közlemények 134. (1): 1–14. Varga, Gy. 2011. Similarities among the Plio-Pleistocene terrestrial aeolian dust deposits in the world and in Hungary. Quaternary International 234. (1–2): 98–108. Zeman, A. 1992. New data on the Quaternary at Červený kopec Hill in Brno. Scripta Geology, 22. 123–127. 260 NOW AVAILABLE! Ethnic map of Hungary 1941 + Ethnic map of present territory of Hungary 2001 Scale 1:500 000 Authors: KOCSIS, K. and BOTTLIK, ZS. 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E-mail: magyar@sparc.core.hu << /ASCII85EncodePages false /AllowTransparency false /AutoPositionEPSFiles true /AutoRotatePages /None /Binding /Left /CalGrayProfile (Dot Gain 20%) /CalRGBProfile (sRGB IEC61966-2.1) /CalCMYKProfile (U.S. Web Coated \050SWOP\051 v2) /sRGBProfile (sRGB IEC61966-2.1) /CannotEmbedFontPolicy /Error /CompatibilityLevel 1.3 /CompressObjects /Tags /CompressPages true /ConvertImagesToIndexed true /PassThroughJPEGImages true /CreateJobTicket false /DefaultRenderingIntent /Default /DetectBlends true /DetectCurves 0.0000 /ColorConversionStrategy /LeaveColorUnchanged /DoThumbnails false /EmbedAllFonts true /EmbedOpenType false /ParseICCProfilesInComments true /EmbedJobOptions true /DSCReportingLevel 0 /EmitDSCWarnings false /EndPage -1 /ImageMemory 1048576 /LockDistillerParams false /MaxSubsetPct 100 /Optimize false /OPM 1 /ParseDSCComments true /ParseDSCCommentsForDocInfo true /PreserveCopyPage true /PreserveDICMYKValues true /PreserveEPSInfo true /PreserveFlatness true /PreserveHalftoneInfo false /PreserveOPIComments true /PreserveOverprintSettings true /StartPage 1 /SubsetFonts true /TransferFunctionInfo /Apply /UCRandBGInfo /Preserve /UsePrologue false /ColorSettingsFile () /AlwaysEmbed [ true ] /NeverEmbed [ true ] /AntiAliasColorImages false /CropColorImages true /ColorImageMinResolution 300 /ColorImageMinResolutionPolicy /OK /DownsampleColorImages true /ColorImageDownsampleType /Bicubic /ColorImageResolution 300 /ColorImageDepth -1 /ColorImageMinDownsampleDepth 1 /ColorImageDownsampleThreshold 1.50000 /EncodeColorImages true /ColorImageFilter /DCTEncode /AutoFilterColorImages true /ColorImageAutoFilterStrategy /JPEG /ColorACSImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /ColorImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /JPEG2000ColorACSImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /JPEG2000ColorImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /AntiAliasGrayImages false /CropGrayImages true /GrayImageMinResolution 300 /GrayImageMinResolutionPolicy /OK /DownsampleGrayImages true /GrayImageDownsampleType /Bicubic /GrayImageResolution 300 /GrayImageDepth -1 /GrayImageMinDownsampleDepth 2 /GrayImageDownsampleThreshold 1.50000 /EncodeGrayImages true /GrayImageFilter /DCTEncode /AutoFilterGrayImages true /GrayImageAutoFilterStrategy /JPEG /GrayACSImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /GrayImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /JPEG2000GrayACSImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /JPEG2000GrayImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /AntiAliasMonoImages false /CropMonoImages true /MonoImageMinResolution 1200 /MonoImageMinResolutionPolicy /OK /DownsampleMonoImages true /MonoImageDownsampleType /Bicubic /MonoImageResolution 1200 /MonoImageDepth -1 /MonoImageDownsampleThreshold 1.50000 /EncodeMonoImages true /MonoImageFilter /CCITTFaxEncode /MonoImageDict << /K -1 >> /AllowPSXObjects false /CheckCompliance [ /None ] /PDFX1aCheck false /PDFX3Check false /PDFXCompliantPDFOnly false /PDFXNoTrimBoxError true /PDFXTrimBoxToMediaBoxOffset [ 0.00000 0.00000 0.00000 0.00000 ] /PDFXSetBleedBoxToMediaBox true /PDFXBleedBoxToTrimBoxOffset [ 0.00000 0.00000 0.00000 0.00000 ] /PDFXOutputIntentProfile (None) /PDFXOutputConditionIdentifier () /PDFXOutputCondition () /PDFXRegistryName () /PDFXTrapped /False /CreateJDFFile false /Description << /ARA /BGR /CHS /CHT /CZE /DAN /DEU /ESP /ETI /FRA /GRE /HEB /HRV (Za stvaranje Adobe PDF dokumenata najpogodnijih za visokokvalitetni ispis prije tiskanja koristite ove postavke. 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