Parallelization of Last Glacial loess-paleosol section of Red Hill with Heinrich events and ice core records 327 Hungarian Geographical Bulletin 61 (4) (2012) 327–341. Parallelization of Last Glacial loess-paleosol section of Red Hill with Heinrich events and ice core records Éva KIS1 Abstract In this paper, I would like to provide refi ned relative chronological data to loess-paleosol section situated on the IV. and V. terraces of Red Hill (Moravia), based on a comparison with Heirich events, North and South hemispheric ice core records. The last glacial–inter- glacial loess section is almost complete, all of the interstadial soils can be identifi ed in the series instead of the eroded upper part of the PK I complex. The onset of the formation of recent soil can be parallelized to H0 event (~12 000), the double structural soils to H1 and H2 events, the eroded soils of PK I to H3 and H4, while the lower part of the complex has been correlated with H5 and H6 events (~63 ka BP). The loess series above PK I has been classifi ed into Würm-3, the strata between PK I and PK II belong to the Würm-2. The lower part, under PK II is mostly clayey, cannot be regarded as a cold climate deposit. Aft er the Riss/Würm interglacial the climate has changed slowly, and the typical glacial climate has started only aft er 75 ka BP. Keywords: Heinrich events, ice cores, loess-paleosol series, chronology, δ18O values Introduction Main aim of this paper is to provide new, refi ned relative chronological data on the formation of loess-paleosol deposits in Southern Moravia (Photos 1–2). The section is located on Devonian red sandstone and pebbles, and Miocene sandstone at the IV–V. terraces of the Red Hill (Photo 3). This investigation was based on records of Heinrich events, North and South hemispheric ice core drillings, and on the comparison of these paleoenvironmental proxies with our former loess-studies in the region (Kis, É. et al. 2011). The stratigraphic investigations of the Red Hill section have been made by Kukla, G.J. (1975); Fink, J. and Kukla, G.J. (1977); Smolikova, L. (1982), Zeman, A. (1992) and Demek, J. et al. (2005). Loess deposits are important terres- 1 Geographical Institute, Research Centre for Astronomy and Earth Sciences (Hungarian Academy of Sciences) H-1112 Budapest, Budaörsi út 45. E-mail: kis.eva@csfk .mta.hu 328 Photo 1. The South Czech “Red Hill” (Photo: Kis, É.) Photo 2. Perspective view of the terrace system of Red Hill (source: GoogleEarthTM) 329 trial archives of climatic changes (Lóczy, D. and Szalay, L. 1995; Lóczy, D. 2008) and these aeolian dust deposits provide insight into the Plio-Pleistocene geo- morphological and environmental development of Central Europe (Frechen, M. et al. 1997, 2003; Fábián, Sz.Á. et al. 2004; Kovács, J. et al. 2011). During the last glacial period, the dust transportation was defi ned by three prevailing wind-directions: (1) westerlies in the east-west corridor along latitude 50°N, (2) northwesterly winds from the Fennoscandinavian ice sheet, and (3) according to Rozycki, S.Z. (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. (2011) and Varga, Gy. et al. (2012). Methods The sedimentary and stable isotopic parameters of the investigated, almost complete loess-paleosol section have been compared to the isotopic records of NGRIP (Greenland), EPICA Dome-C and Vostok (Antarctica) ice cores and to the North Atlantic Heinrich layers (Figures 1–2). I would like to correlate the Photo 3. Devonian red sandstone and pebbles underlying the loess-paleosol section at the IV. terrace (Photo: Kis, É.) 330 Fi g. 1 . P os si bl e co rr el at io n of th e la st g la ci al /in te rg la ci al lo es s- pa le os ol s er ie s of th e Re d H ill w ith H ei nr ic h ev en ts , A nt ar ct ic E PI C A an d Vo st ok δ D , a nd G re en la nd ic N G RI P δ1 8 O r ec or ds (K is , É .). S ed im en ta ry p ar am et er s: K is , É . S tr at ig ra ph ic a na ly si s: S ch w ei tz er , F. , K is , É ., Ba lo gh , J . a nd D i G lé ri a, M . O xy ge n is ot op e m ea su re m en ts : F ut ó, I. a nd V od il a, G . G ra in -s iz e an al ys is : D i G lé ri a, M . (D at a so ur ce s of ic e co re r ec or ds a nd H ei nr ic h ev en ts : P et it , J .R . e t a l. 19 99 ; E PI C A C om m un ity m em be rs 2 00 4; N G RI P C om m un ity m em be rs 2 00 4; H em m in g, S .R . 2 00 4) 331 Fi g. 2 . V ar ia tio ns o f se di m en ta ry p ar am et er v al ue s in th e R ed H ill lo es s- pa le os ol s er ie s (s ou rc e: K is , É . e t al . 2 01 1) . S ed im en ta ry pa ra m et er s: K is , É . S tr at ig ra ph ic a na ly si s: S ch w ei tz er , F ., K is , É ., Ba lo gh , J . a nd D i G lé ri a, M . G ra in -s iz e an al ys is : D i G lé ri a, M . 332 δD and δ18O values of ice cores with the measured δ18O values of the analysed loess-paleosol deposits to refi ne the chronological framework of the section. The sedimentary parameters of the Red Hill section have been deter- mined by environmental-discrimination proxies (Kis, É. 2003; Schweitzer, F. and Kis, É. 2003; Kis, É. et al. 2011, 2012). These are traditional sedimentary parameters and our newly introduced indices (fi neness grade: Fg and degree of weathering: Kd), and δ18O-values. The detailed description of the applied methods can be found in Kis, É. et al. (2011). The NGRIP ice core (Greenland) The ice core provides information on the climatic changes and anomalies dur- ing the last glacial period of the North Atlantic domain (Figure 1). According to the North GRIP Community Members (2004), the analytical data represent 25 Dansgaard-Oeschger (D/O) events; abrupt, large amplitude climate fl uctua- tions (oft en within several decades). These events show us the rapid changes of cold and warm periods of the region. The D/O events can be correlated well with other North Atlantic paleotemperature proxies (e.g. benthic foraminiferal isotope records of VM23-0.81, DSDP 609, VM30-101k deep sea cores – Bond, G.C. et al. 1993; Ziegler, M. et al. 2008) or with terrestrial aeolian dust deposits (Varga, Gy. 2010). The stable isotope values and gas content of ice cores suggest the oc- currence of abrupt 8–16°C temperature fl uctuations during the last glacial period. EPICA Dome Concordia (DOME C) ice core (Antarctica) The EPICA DOME C ice core contains information on the climate changes of the last 800 kyr, the only one ice core which could have provide climate data on cyclic changes from the Brunhes/Matuyama Boundary (Figure 1). Beside the stable isotopes, the greenhouse gas content trapped in bubbles can be used as proxy of climatic fl uctuations. Based on the detailed analy- ses of the sequence, eight glacials and interglacials (and their durations) have been distinguished during the last 800 kyr. Earlier Antarctic ice cores provide data only on the climate of the last 400 kyr (e.g. Vostok – Petit, J.R. et al. 1999). The ice core records can be correlated with the benthic foraminiferal records and δ18O values of deep sea deposits (e.g. ODP 659 Tiedemann, R. et al. 1994; Lisiecki, L. and Raymo, M.E. 2005), confi rming the eight glacial cycles of the last 800 kyr. 333 Vostok ice core (Antarctica) The more than 3700 metres deep ice core represent the climatic cycles of the last 440 kyr (Figure 1). (The third deepest lake of the Earth, Lake Vostok sub- glacial lake can be found beneath the Vostok Station.) Various measurements provide data on local paleotemperature, humidity, wind speed, atmospheric O2, CO2 and CH4 content, lithic material of ancient volcanic eruptions. Based on the correlation of δD values of the ice core with δ18O values of GRIP core (Jouzel, J. et al. 1997), all of the 25 D/O events of the last glacial periods can be found in the sequence. However, the relationship between the two re- gions is asynchronous; the warming phases had been occurring earlier in the Vostok cores compared to the Greenland ice cores. The northern ice cores have ~1,500 years lag behind the southern hemispheric climatic variations, but the global changes can be well correlated with statistical analyses of the phase-lag relationships. Oxygen isotope values of the ice cores Dansgaard, W. has established that the isotope ratio of H2 18O/H2 16O of precipi- tation is constantly decreasing into the direction of higher latitudes, implying a strong relationship between temperature and stable isotope content. The temporal changes of isotopic composition of the precipitation provide informa- tion on the temperature changes. This relationship can be used to determine the paleotemperature from the ice cores oxygen isotope values. The values have been diff erent during glacial and interglacial periods (Dansgaard, W. et al. 1983). Oeschger, H. measured similar diff erences between cold and warm phases in the sequence of the Grenzensee deposits in Switzerland (Dansgaard, W. et al. 1993). These climatic fl uctuations are not only typical for Greenland and Switzerland, however represent the whole northern hemispheric changes. The early measurements were confi rmed by the recent NGRIP drillings and measurements (NGRIP Community Members 2004). The abrupt warming epi- sodes and the longer cooling phases have determined the last glacial period. Heinrich events Heinrich events provide valuable information to recognition of paleoenviron- mental, paleoclimatic and principally global climate changes. These events caused relatively rapid changes on a global paleoclimatic temporal scale. To recognize the causes of climate changes, the complex eff ects of terrestrial, 334 oceanic and atmospheric components should be investigated together. The deep sea deposits and ice cores provide the most comprehensive and complex picture on climate changes. These proxies refl ect the variability of climatic stages and the variations of components on various temporal scales, even the seasonal changes. Heinrich events correlate with the destruction of the Arctic ice-sheets, and with the consequent release of vast volume of icebergs to North Atlantic. Signs of the events can be observed in the deep sea deposits aft er periodic major, mainly longer cold episodes. These last glacial events were fi rst reported by Heinrich, H. (1988) and by Bond, G.C. et al. (1992). The deep sea sediments of North Atlantic consist several layers rich in ice raft ed terrestrial material and with decreased foraminiferal abundance. These, so called Heinrich layers can be correlated with cooling periods of marine and terrestrial environments, and also with decreased oceanic salinity. Investigations have confi rmed that the cooling events can be connected to the presence and drift ing of freshwater reservoir icebergs even at lower latitudes. The trails of the icebergs could be tracked trough 3000 km, following the melted detrital carbonate deposits. The deep sea sediments prove the abrupt cooling episodes in the last glacial period and the presence of vast volume of drift ing icebergs. Heinrich layers provide important sedimentary information on the short term, abrupt climate fl uctuations by the repeated occurrence of ice raft ed debris. The terrestrial material was eroded by glaciers and the calving icebergs transported it to the Atlantic Ocean. The melting and drift ing icebergs dropped the embedded material onto the sea fl oor. The freshwater content of melted ice has changed signifi cantly the oceanic and atmospheric circulation patt erns. Based on deep sea drillings, the Heinrich events were dated as the fol- lowing: H0: ~12 ka (Hemming, S.R. 2004); H1: ~16.8 ka (Hemming, S.R. 2004), ~14 ka (Vidal, L. et al. 1999); H2: ~24 ka (Hemming, S.R. 2004), ~22 ka (Bond, G.C. and Lotti, R. 1995; Vidal, L. et al. 1999); H3: ~31 ka (Hemming, S.R. 2004), ~29 ka (Bond, G.C. and Lotti, R. 1995); H4: ~38 ka (Hemming, S.R. 2004), ~37 ka (Bond, G.C. and Lotti, R. 1995), ~35 ka (Vidal, L. et al. 1999); H5: ~45 ka (Hemming, S.R. 2004; Vidal, L. et al. 1999); H6: ~60 ka (Figure 1). The orientation of the H1, H2, H4 and H5 layers on the sea fl oor is north- south (from Labrador Sea into southern direction), while H3 and H6 deposits has west-east orientation (from North America into the direction of Europe, around the 40° northern latitude). The main causes of Heinrich events are still a matt er of scientifi c debate and there are several competing explanations about the processes leading to abrupt climatic fl uctuations. The calving icebergs of the Laurentide ice sheet and the huge freshwater input could have major eff ect on the thermohaline circulation of the ocean, and causing southward (and westward) migration of North Atlantic Current. Consequently, the northward heat transport de- 335 creases, leading to the increase of Laurentide ice sheet. According to the EPICA Community Members (2004), the main causes can be traced back to changes of greenhouse gas concentration of the atmosphere. Even small-scale fl uctuations of oceanic circulations (especially at Arctic regions) have major impact on the atmospheric CO2 concentrations. The most important reservoir of CO2 is the ocean, where fi ft yfold of the atmospheric CO2 can be stored. (The natural CO2 concentration of the atmosphere was 200 ppm during the cold and 280ppm during the warm episodes). Other investigations suggest various explanations on the causes; e.g. instability of West Arctic ice sheet; intensifying iceberg calving aft er cold win- ters; collapses of ice sheets due to backward erosion (Tiedemann, R. et al. 1994). The abrupt and large sea-level rises could have eroded the ice sheets leading to collapses. These explanations were also confi rmed by model calculations (Arz, H.W. et al. 2007). Generally, the Heinrich events occurred aft er a longer (7–10 kyr) cold period, which was terminated a massive release of calving and drift ing ice- bergs. The H-events have been followed by an abrupt warming climatic phase. These cold-warm fl uctuations of oceanic-atmospheric system between 20 and 80 ka BP were confi rmed by the pioneering works of Bond, G.C. et al. (1993). Typical global environmental consequences of the Heinrich events are: de- creased δ18O content of deep sea deposits and decreased oceanic salinity re- lated to the colder climate and to the increased infl ux of freshwater; increased grain-size of loess deposits indicating stronger winds due to the changing patt erns of oceanic currents; increased sedimentation rate of lithic terrestrial fragments at the sea fl oor; palynological records show the replacement of oak by pines; and decreased foraminiferal abundance. Results This research is dealing with the last glacial period’s (~100 kyr) stratigraphic features in a South Czech loess-paleosol section. I would like to compare the almost complete series of Moravian aeolian dust deposits to North and South hemispheric ice core records, Heinrich events and sea level changes. The aim of this paper is to complete the chronological framework of the investigated strata, based on the data contributed by Kis, É. et al. (2011). The newest ice core and deep sea drillings provide new insight into dynamics of Plio-Pleistocene paleoenvironmental and paleoclimatic changes. These new databases of ice cores and deep sea sediments allow us to correlate the climatic fl uctuations and the terrestrial, oceanic and at- mospheric relationships with various proxies from diff erent environments (e.g. loess deposits). In this case, the almost complete South Czech “Red 336 Hill” loess-paleosol sequence has been compared with the last glacial oscil- lations. With this comparison, the main aim is to refi ne the chronological properties of the section. The known intensity, duration and absolute age data of deep sea Heinrich events provide ground for relative dating and correlation of the investigated deposits. Based on these parallelization, the controversial stratigraphic position and 14C data of thin, humic horizons above (and between) thick, well-developed paleosoils (e.g. in the Hungarian Tápiósüly–Dunaújváros loess series) can also be explained. The sedimentary parameters and oxygen isotope data of the series have been used during this comparison. The investigated 120–130 kyr comprise the paleoenvironmental properties of the last glacial and interglacial periods. During the last inter- glacial the arctic summers were warmer by 5°C than the later epochs. All of the glaciers have been melted, only the inner part of Greenland remained covered by ice. As a result of the huge amount of melted ice, the sea level has been increased by 5 metres. The temperature of the last glacial maximum (21 ka BP) was colder by 20°C than present conditions (Miler, G.H. et al. 2010). The Heinrich events had various intensity and duration. Based on the deep sea records, the H3 and H6 events were fairly diff erent than the others; the spatial distribution of the ice-raft ed debris of these events is also diff erent. The investigated section consist of loess and intercalated soils of the last 100 kyr, however the lower part (between 100 and 80 ka BP) cannot be regarded as typical loess, these layers are sandy loess deposits (Figure 1.; Photos 1 and 4–6.). The loess section is generally intercalated by interstadial soils instead of the PK III., which is the last interglacial soil-series. The up- permost pedogenic complex consists of the recent (upper) and a redeposited paleosoil (lower). The onset of the soil-formation can be dated from 12 ka BP (preboreal oscillation), the preceding colder period is represented by the underlying loess layer. The next thick soil is a double, weakly developed humic soil or struc- tural paleosoil and can be correlated with the H1 and H2 events. The age of the upper pedogenic horizon is ~16.8 ka BP (Hemming, S.R. 2004), similarly to other loess sections in Central Europe (e.g. Paks: 16730±400 years; Dolní Vestonice). Loess between the two soil horizons cannot be found at the Red Hill, it was eroded or redeposited. The lower structural soil has been formed ~22–24 ka BP. The thick Würm-3 loess series (Photo 4) represents well the cold glacial climate; while the upper part of the underlying PK I soil-complex is eroded. These missing horizons could be parallelized to the H3 and H4 events. The middle part of the PK I complex is related to the H5 and H6 events, the ages of these events are 45 and 60 ka BP (Vidal, L. et al. 1999; Hemming, S.R. 2004). The hiatus at the top of PK I is ~10 kyr. 337 Photo 4. Würm-3 loess series in the upper part of the section (Photo: Kis, É.) Similarly to Dolní Vestonice, the Würm-2 loess stratum is well-devel- oped and fairly thick. Beneath the PK II soil-complex the section shows us that the climate has changed slowly aft er the last interglacial, the Würm-1 period was not a real cold stadial and cannot identifi ed in the loess series; the tempera- ture has decreased and the typical steppe environment was formed slowly. This interpretation of the Red Hill loess section could also be con- fi rmed by several evidences from the discussed ice core and deep sea records (Figure 1). Acknowledgement: The study and the measurements were supported by Hungarian Scientifi c Research Fund (OTKA K63814). 338 Photo 5. Periglacial features in young loess (Photo: Kis, É.) Photo 6. The PK I soil series with notable hiatus in the upper part (Photo: Kis, É.) 339 REFERENCES Arz, H.W., Lamy, F., Ganopolski, A., Nowaczyk, N. and Pätzold, J. 2007. Dominant Northern Hemisphere climate control over millennial-scale glacial sea-level variability. Quaternary Science Reviews 26. 312–321. Bond, G., Broecker, W., Johnson, S., McManus, J., Labeyrie, L., Jouzel, J. and Bonani, G. 1993. Correlation between climate records from North Atlantic sediments and Greenland ice. Nature 365. 507–508. Bond, G., Heinrich, H., Broecker,W., Labeyrie, L., McManus, J., Andrews, J., Huon, S., Jantschik, R., Clasen, S., Simet, C., Tedesco, K., Klas, M., Bonani, G. and Ivy, S. 1992. Evidence for massive discharges of icebergs into the North Atlantic ocean during the last glacial period. Nature 360. 245–249. Bond, G.C. and Lotti, R. 1995. Iceberg discharges into the North Atlantic on millennial time scales during the last glaciation. Science 267. 1005–1010. Dansgaard, W., Johnsen, S.J., Clausen, H.B., Dahl-Jensen, D., Gundestrup, N.S., Hammer, C.U., Hvidberg, C.S., Steffensen, J.P., Sveinbjörnsdottir, A.E., Jouzel, J. and Bond, G. 1993. Evidence for general instability of past climate from a 250-kyr ice-core record. Nature 364. 218–220. Dansgaard, W., Oeschger, H. and Langway, C.C., Jr. 1983. Ice core indications of abrubt cli- mate changes. In Palaeoclimatic Research and Models. Proceedings of Workshop, Brussels, Dec. 1982. Dordrecht–Boston–Lancaster, D. Reidel Publishing Company, 72–73. Demek, J., Havliček, M., Kirchner, K., Nehyba, S., Petrová, P., Bubík, M. and Gilíkova, H. 2005. Příspěvek k poznání geologické situace na JV svahu Červeného kopce v Brně. Brno, Geol. výzk. Mor. Slez. v. r. Brno, 162 p. EPICA community members, 2004. Eight glacial cycles from an Antarctic ice core. Nature 429. 623–628. Fábián, Sz.Á., Kovács, J., Nagyváradi, L. and Varga, G. 2004. Was There Desert Climate in the Carpathian Basin, or Not? Studia Geomorphologica Carpatho Balcanica 38. 49–58. Fink, J. and Kukla, G.J. 1977. Pleistocene climate in Central Europe at least 17 interglacials aft er Olduvai event. Quaternary Research 7. 363–371. Frechen, M., Horváth, E. and Gábris, Gy. 1997. Geochronology of Middle and Upper Pleistocene loess sections in Hungary. Quaternary Research 48. (3): 391–312. Frechen, M., Oches, E.A. and Kohfeld, K.E. 2003. Loess in Europe – mass accumulation rates during the Last Glacial Period. Quaternary Science Reviews 22. (18–19): 1835–1857. Heinrich, H., 1988. Origin and consequences of cyclic ice raft ing in the northeast Atlantic Ocean during the past 130,000 years. Quaternary Research 29. 142–152. Hemming, S.R., 2004. Heinrich Events: Massive Late Pleistocene detritus layers of the North Atlantic and their global climate imprint. Reviews in Geophysics 42. 1–43. Jouzel, J., Froehlich, K. and Schotterer, U. 1997. Deuterium and oxygen-18 in present-day precipitation: data and modelling. Hydrological Sciences 42. (5): 747–763. Kis, É. 2003. The sequence of the Susak loess profi le. In Susak – environmental reconstruction of a loess island in the Adriatic. Eds. Bognár, A., Schweitzer, F. and Szöőr, Gy. Budapest, Geographical Research Institute HAS, 51–66. Kis, É., Schweitzer, F., Palcsu, L., Futó, I., Balogh, J. and Di Gléria, M. 2012. Investigations of paleogeographic variations on the basis of the stratotype section of Viatovo at the Lower Danube. Hungarian Geographical Bulletin / Földrajzi Értesítő 61. (2): 93–111. Kis, É., Schweitzer, F., Vodila, G., Futó, I., Balogh, J. and di Gléria, M. 2011. Special paleo- geographic characteristics of environs of the Moravian Plateau. Hungarian Geographical Bulletin 60 (3): 247–259. 340 Kovács, J., Fábián, Sz.Á., Varga, G., Újvári, G., Varga, Gy. and Dezső, J. 2011. Plio-Pleistocene red clay deposits in the Pannonian Basin: A review. Quaternary International 240. (1–2): 35–43. 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. Lisiecki, L. and Raymo, M.E. 2005. A Pliocene–Pleistocene stack of 57 globally distributed benthic δ18O records. Paleoceanography 20. PA1003. 17 p. Lóczy, D. 2008. A löszvidékek formakincse (Geomorphology of loess terrains). In Geomorfológia II. Földfelszíni folyamatok és formák. Ed. Lóczy, D. Budapest–Pécs, Dialóg Campus Kiadó, 55–58. Lóczy, D. and Szalay, L. 1995. Assessment of loess as parent material for agro-ecological potential. GeoJournal 36. (2–3): 275–280. Miller, G.H., Brigham-Grette, J., Alley, R.B., Anderson, L., Bauch, H.A., Douglas, M.S.V., Edwards, M.E., Elias, S.A., Finney, B.P., Fitzpatrick, J.J., Funder, S.V., Herbert, T.D., Hinzman, L.D., Kaufman, D.S., MacDonald, G.M., Polyak, L., Robock, A., Serreze, M.C., Smol, J.P., Spielhagen, R., White, J.W.C., Wolfe, A.P., and Wolff, E.W. 2010. Temperature and precipitation history of the Arctic. Quaternary Science Reviews 29. (15–16): 1679–1715. North Greenland Ice Core Project members, 2004. High-resolution record of Northern Hemisphere climate extending into the last interglacial period. Nature 431. 147–151. Petit, J.R., Jouzel, J., Raynaud, D., Barkov, N.I., Barnola, J.M., Basile, I., Bender, M., Chappellaz, J., Davis, J., Delaygue, G., Delmotte, M., Kotlyakov, V.M., Legrand, M., Lipenkov, V., Lorius, C., Pépin, L., Ritz, C., Saltzman, E. and Stievenard, M. 1999. Climate and Atmospheric History of the Past 420,000 years from the Vostok Ice Core, Antarctica. Nature 399. 429–436. Richter, D., Tostevin, G., Skrdla, P. and Davies, W. 2009. New radiometric ages for the Early Upper Paleolithic type locallity of Brno-Bohunice (Czech Republic): comparison of OSL, IRSL, TL and 14C dating results. Journal of Archeological Science 36. 708–720. Rousseau, D.D., Derbyshire, E., Antoine, P. and Hatte, C. 2007. Loess records. Europa. Elsevier: 1440–1457. Rozycki, Sz. 1991. Loess and loess-like deposits. Wroclaw, Ossolineum, Polish Acadamy of Sciences. 187 p. Schweitzer, F. and Kis, É. 2003. Formation of loess and loess-like sediments. In Susak – envi- ronmental reconstruction of a loess island in the Adriatic. Eds. Bognár, A., Schweitzer, F. and Szöőr, Gy. Budapest, Geographical Research Institute HAS, 45–65. Smolíková, L. and Zeman, A. 1982. Bedeutung der Ferrett o-Böden für die Quartärstratigraphie. Praha, Sbor. geol. věd. Antropozoikum 14. 57–93. Tiedemann, R., Sarnthein, M. and Shackleton, N.J. 1994. Astronomic timescale for the Pliocene Atlantic δ18O and dust fl ux records of Ocean Drilling Program Site 659. Paleoceanography 9. (4): 619–638. Varga, Gy. 2010. Gondolatok a porviharok és a klimatikus, környezeti folyamatok összefüggéseiről. (On the relationships between duststorms and climatic processes.) Földrajzi Közlemények 134. (1): 1–14. Varga, Gy. 2011. Similarities among the Plio-Pleistocene terrestrial aeolian dust depositsinthe world and in Hungary. Quaternary International 234. (1–2): 98–108. Varga, Gy., Kovács, J. and Újvári, G. 2012. Late Pleistocene variations of the background aeolian dust concentration in the Carpathian Basin: an estimate using decomposition of grain-size distribution curves of loess deposits. Netherlands Journal of Geosciences – Geologie en Mij nbouw 91. (1–2): 159–171. 341 Vidal, L., Schneider, R.R., Marchal, O., Bickert, T., Stocker, T.F. and Wefer, G. 1999. Link between the North and South Atlantic during the Heinrich events of the last glacial period. Climate Dynamics 15. 909–919. Zeman, A. 1992. New data on the Quaternary at Červený kopec Hill in Brno. Scripta, Geology 22. 123–131. Ziegler, M., Nürnberg, D., Karas, C., Tiedemann, R. and Lourens, L.J. 2008. Persistent sum- mer expansion of the Atlantic Warm Pool during glacial abrupt cold events. Nature Geoscience 1. 601–605. 342 AVAILABLE! Ethnic map of Hungary 1941 + Ethnic map of present territory of Hungary 2001 Scale 1:500 000 Authors: KOCSIS, K. and BOTTLIK, ZS. Geographical Research Institute, Hungarian Academy of Sciences, Budapest, 2009 The latest (eighth) piece of ethnic map series of the Carpathian Basin was an att empt to draft the changes that have taken place in the ethnic structure during the past fi ve hun- dred years as well as to display its present state with the help of ethnic maps and a chart - in our case referring to the present-day territory of Hungary. On the front pages of our work consist- ing of two sheets ethnic maps of the present-day territory of Hungary are displayed with the help of pie-charts, based on ethnic ( 2 0 0 1 ) a n d mother tongue (1941) data. Population-proportional p ie - char t s provide information on the territorial distribu- tion of the major ethnic groups and on the contemporary admin- istrative division. T h e nine supplementary maps on the re- verse show the lingual-ethnic com- position of the present-day ter- ritory of Hungary in 1495, 1715, 1784, 1880, 1910, 1930, 1941, 1990 and 2001 respectively. The chart here explores the quantitative and proportional changes of the main ethnic groups’ population between 1495 and 2001. The series of maps displays absolute or relative ethnic majorities only in the inhabited areas of the sett lements which had been mentioned in the source referred. Uninhabited areas with no permanent sett lements are shown as blank spots. Price: EUR 10.00 – For sale only in pairs! O r d e r : G e o g r a p h i c a l I n s t i t u t e R C A E S H A S Library. H-1112 Budapest, Budaörsi út 45. E-mail: magyar.arpad@csfk .mta.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. Stvoreni PDF dokumenti mogu se otvoriti Acrobat i Adobe Reader 5.0 i kasnijim verzijama.) /ITA /JPN /KOR /LTH /LVI /NLD (Gebruik deze instellingen om Adobe PDF-documenten te maken die zijn geoptimaliseerd voor prepress-afdrukken van hoge kwaliteit. De gemaakte PDF-documenten kunnen worden geopend met Acrobat en Adobe Reader 5.0 en hoger.) /NOR /POL /PTB /RUM /RUS /SKY /SLV /SUO /SVE /TUR /UKR /ENU (Use these settings to create Adobe PDF documents best suited for high-quality prepress printing. Created PDF documents can be opened with Acrobat and Adobe Reader 5.0 and later.) /HUN >> /Namespace [ (Adobe) (Common) (1.0) ] /OtherNamespaces [ << /AsReaderSpreads false /CropImagesToFrames true /ErrorControl /WarnAndContinue /FlattenerIgnoreSpreadOverrides false /IncludeGuidesGrids false /IncludeNonPrinting false /IncludeSlug false /Namespace [ (Adobe) (InDesign) (4.0) ] /OmitPlacedBitmaps false /OmitPlacedEPS false /OmitPlacedPDF false /SimulateOverprint /Legacy >> << /AddBleedMarks false /AddColorBars false /AddCropMarks false /AddPageInfo false /AddRegMarks false /ConvertColors /ConvertToCMYK /DestinationProfileName () /DestinationProfileSelector /DocumentCMYK /Downsample16BitImages true /FlattenerPreset << /PresetSelector /MediumResolution >> /FormElements false /GenerateStructure false /IncludeBookmarks false /IncludeHyperlinks false /IncludeInteractive false /IncludeLayers false /IncludeProfiles false /MultimediaHandling /UseObjectSettings /Namespace [ (Adobe) (CreativeSuite) (2.0) ] /PDFXOutputIntentProfileSelector /DocumentCMYK /PreserveEditing true /UntaggedCMYKHandling /LeaveUntagged /UntaggedRGBHandling /UseDocumentProfile /UseDocumentBleed false >> ] >> setdistillerparams << /HWResolution [2400 2400] /PageSize [612.000 792.000] >> setpagedevice