Suric.indd 155 � AB STRA CT U-Th and 14C dating, and X-ray diffraction of parts of 16 submerged speleothems taken from depths of 1.5−41.5 m from 7 submarine caves and pits along the Eastern Adriatic coast, provided insight into the sea-level fl uctuations during the last 220 ka, and to the palaeogeographic changes caused by sea-level changes. Due to climate changes, palaeoenvironmental settings also varied, but not so abruptly and intensely as in the rest of Europe. As the Alps and Dinarides acted as orographic barriers, the Eastern Adriatic coast was the border region between periglacial Europe and the temperate Mediterranean region. It was also a refuge area for plant species from the north. This study showed that appropriate temperature, humidity and vegetation cover ensured favourable conditions for karstifi cation and speleothem formation even during the Last Glacial Maximum. Keywords: Palaeoenvironment, Late Pleistocene-Holocene, U-Th dating, 14C dating, sea-level change, sub- merged speleothems, Adriatic Sea, Croatia Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) � Maša Surić1 and Mladen Juračić2 1 Department of Geography, University of Zadar, Ulica dr. Franje Tuđmana 24, 23000 Zadar, Croatia; (msuric@unizd.hr) 2 Department of Geology, Faculty of Science, University of Zagreb, Horvatovac 102 a, 10000 Zagreb, Croatia; (mjuracic@geol.pmf.hr) doi: 104154/gc.2010.13 Geologia Croatica 63/2 155–169 3 Figs. 2 Tabs. 2 Pls. Zagreb 2010 Geologia CroaticaGeologia Croatica 1. INTRODUCTION Environmental conditions in the coastal zones almost com- pletely depend on sea-land distribution. Changes of this dis- tribution during the Late Pleistocene-Holocene period were mainly the result of the sea-level oscillations caused by global climate changes, typical for the entire Quaternary pe- riod. Other than on the spatial (palaeogeographic) settings, sea-land distribution had an indirect impact on climatic set- tings on the local and regional level, (therefore infl uencing animal and plant distribution), and on the hydrogeological settings of the coastal zones. Apparently, all of these changes can be recorded in the speleothems from the submerged caves. Calcite speleothems are secondary mineral deposits formed in caves by degassing of CO2 from supersaturated H2O-CO2-CaCO3 solutions that have entered the cave (DREY- BRODT, 2005). If these are typical subaerial features, their present positions under the sea, in submerged caves, are ir- refutable evidence of former lower sea stands. As they grow, they may trap trace quantities of other minerals, fl ood debris, dust, organic matter, pollen, etc. (FORD, 1997). If they con- tain remnants of marine organisms or any other indicator of a marine phase incorporated between the carbonate layers deposited in a continental phase, intervals of higher sea lev- els can be revealed. Furthermore, speleothems are poten- tially excellent subjects for the study of long-term changes of continental mean temperature and perhaps other climatic parameters (FORD & WILLIAMS, 1989). Geologia Croatica 63/2Geologia Croatica 156 & LENARDIĆ-FABIĆ, 1988; PAUNOVIĆ & RABEDER, 2000; ČEČUK & RADIĆ, 2005). In addition, geomorpho- logical analyses of areas that could have experienced Pleis- tocene glaciations, such as Velebit Mt., where glacial and periglacial relief (i.e., moraine material of Würmian glaciers) were studied (NIKLER, 1973; BELIJ, 1986; BOGNAR et al., 1991). Palaeoclimatological studies have covered much a wider region, and approximations of the LGM temperature vary geographically. According to PRENTICE et al. (1992), the LGM in the Mediterranean region was marked by tem- peratures 5–10 °C lower than today during the winter season, and 1–3 °C lower in summer. Approximations by PEYRON et al. (1998), in the region south of the line defi ned by the Pyrenees and Alps, suggest the mean-annual temperature was 10 ± 5 °C lower than today, with the temperature of the coldest months 15 ± 5 °C lower than present. Meanwhile, the shift of annual precipitation in Greece and Italy was es- timated to be –600 mm/a. Besides lower mean temperatures, MIRACLE (1995) suggests that the seasonal temperature variations during the LGM were larger than those of today. Additionally, seasonality of precipitation was also more pro- nounced, with relatively dry summers and rainy autumn- winter periods. Total precipitation was 10–20% lower than today, but, since the decreased temperatures reduced the evaporation potential, runoff from precipitation was even larger than that of today (MIRACLE, 1995). He also assumes that the area northwest of the Adriatic basin was consider- ably drier than that to the southeast. The last glacial cycle is divided into fi ve marine isotope stages (MIS), from MIS 5 to MIS 1, and includes the high- est sea-level stand during the last interglacial (MIS 5e), the lowest sea-level during the LGM within MIS 2, and the se- ries of oscillations of the stadials and interstadials between MIS 5e and MIS 2. The last period, MIS 1, corresponds to the Holocene, and is characterized by rapid ice decay (LAM- BECK et al., 2002a). In tectonically stable regions, MIS 5e (~128–118 ka BP) sea-level records are found consistently at an elevation of several metres above present sea level (POTTER & LAMBECK, 2004). Unlike MIS 5e, records of sea-levels for the MIS 5a (~80 ka BP), range from –30 to +10 m (see COYNE et al., 2007; references therein and Fig. 18), which is explained by the effects of glacio-hydro-iso- stasy (POTTER & LAMBECK, 2004). Within the MIS 5a, two distinct sea-level highstands (double peak) have been identifi ed, at ~84 and ~77 ka BP (POTTER et al., 2004; POT- TER & LAMBECK, 2004; RADTKE & SCHELLMANN, 2005). An oft-cited timing of the LGM is 21 ka BP, with sea level 121±5 m below present (FAIRBANKS, 1989). If the LGM is considered to coincide with maximum global ice volumes, this period covers more than 10 ka with a rapid sea-level fall about 30 ka BP down to the LGM lowstand, and the onset of the global ice melting at about 19 ka BP (LAMBECK & CHAPPELL, 2001; LAMBECK et al., 2002a). The lowest sea-level stand appears to be at 26 ka BP, and it could have been as low as –135 m relative to present sea level (PELTIER & FAIRBANKS, 2006). A rapid rise started around 19.6 cal ka BP and reached some 10 m within 800 years (HANEBUTH et al., 2009). Further ice melting at During their growth, speleothems incorporate stable and radioactive isotopes of various elements that can be used to reconstruct environmental settings. Variations of the ratio of stable oxygen isotopes 18O and 16O are the key for revealing changes of palaeotemperature, whilst the ratio of stable car- bon isotopes 13C and 12C resolves the origin of the carbon i.e. condition of the vegetation at the surface during speleothem growth. Additionally, to date the onset of the changes that are recorded in speleothems (growth cessation or recom- mencement, shifts in stable isotope ratios, etc.), radioactive isotopes such as 14C or the U-Th series are the most useful. The eastern Adriatic coast, a young ingressional karstic coast, offers a good potential for studying these phenomena as it has numerous submerged caves with speleothems from a wide range of depths. Palaeoenvironmental changes recorded in speleothems primarily result in their deposition/non-deposition, depend- ing on environmental conditions. Generally, during the Last Glacial Maximum (LGM) speleothem deposition ceased in most of Europe, and began again ~15 ka BP (GASCOYNE, 1992; LOWE & WALKER, 1998; MIHEVC, 2001). At the same time, in southern Europe, speleothem deposition was uninterrupted from 20 to 15 ka BP along the Tyrrhenian coast of Italy (ALESSIO et al., 1992) and during the last 60 ka in Israel (Soreq Cave) (BAR-MATHEWS et al., 1999) as it was infl uenced by the Mediterranean Sea. In addition, the pal- aeoclimatic signal (δ18O oscillations) in this region differs markedly from Northern European terrestrial records. It shifts to more negative values during the warm periods and increases during glaciations due to the prevailing infl uence of the Mediterranean Sea (McGARRY et al., 2004). In order to constrain the timing of sea-level oscillations by analysis of submerged speleothems, the youngest parts of the speleothems are usually dated to provide the maximum age of marine transgression, while the oldest parts provide the minimum age of continental conditions (note that cessa- tion of speleothem growth can be caused by numerous other factors, RICHARDS & DORALE, 2003). The most reliable data for the minimum age of transgression is provided by the age of the marine overgrowth that usually covers the spele- othems. Stalagmites with remnants of marine organisms in- corporated between layers of continental origin are very pe- culiar, clearly distinguishing continental-marine-continental transitions (e.g. GASCOYNE et al., 1979; DUTTON et al., 2009). With the intention of reconstructing global and rela- tive sea-level changes, submerged speleothems have been studied on Tyrrhenian coast (ALLESIO et al., 1992; BARD et al., 2002; ANTONIOLI et al., 2001; 2004; 2007; DUT- TON et al., 2009), Bahamas (SPALDING & MATHEWS, 1972; GASCOYNE et al., 1979; LUNDBERG & FORD, 1994; RICHARDS et al., 1994), Bermuda (HARMON et al., 1978), Majorca (FORNÓS et al., 2002; VESICA et al., 2000), and Croatia (MALEZ et al., 1979; VRHOVEC et al., 2001; SURIĆ et al., 2005a; 2009). Palaeoenvironmental studies of the eastern Adriatic re- gion have been based mostly on the spatial distribution of habitats of Pleistocene fauna, (TEŠIĆ, 1958; MALEZ & BOŽIČEVIĆ, 1965; MALEZ & RABEDER, 1984; MALEZ Surić and Juračić: Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) Geologia Croatica 157 According to Köppen’s climatic classifi cation, the north- ern part of the investigated area (including Krk, Lošinj and Pag islands, and the Vrulja Zečica region) belongs to the contemporary Cfa-type of temperate humid climate with hot summers. The middle and southern part (Rogoznica and the islands of Iž and Brač) belong to the Csa-type, which is a Mediterranean climate characterized by temperate and rainy winters and hot, dry summers (ŠEGOTA & FILIPČIĆ, 2003). Mean-annual temperatures are between 13.2 and 16.2 °C, with winter temperatures between 5.4 and 9.4 °C, and pre- cipitation ranging from 690 to 1561 mm/a. 3. SITE DESCRIPTIONS This survey encompassed four pits, two caves, and one sub- marine spring, all located along the eastern Adriatic coast (Fig. 1). All of the surveyed features were formed within heavily fractured Upper Cretaceous rudist limestones with the exception of Vrulja Zečica, which was developed in Ter- tiary limestone. Medvjeđa spilja Cave (Lošinj Island) is an anchialine cave with the entrance 17.5 m above mean sea level (a.m.s.l.), 55 m from the coast (Fig. 2a). Connection with the open sea, with distinct tidal oscillations, is established through chan- nels and fractures in karstifi ed bedrock. According to the fi ndings of Ursus speleaus remnants (MALEZ et al., 1979), there might have originally been a horizontal entrance that is presumably now 8 m below mean sea level (b.m.s.l.), but which has been fi lled with collapsed material. The cave is well decorated with speleothems of varied age and genesis. Cave in Tihovac Bay (Pag Island), with its entrance at 12 m b.m.s.l. (Fig. 2b), ca 100 m off-shore, is completely within the marine environment. Two massive stalagmites below the entrance indicate the existence of a major fi ssure at the loca- an irregular rate lasted until 7 ka BP, when the oceans ap- proached their present volumes (LAMBECK & CHAPPELL, 2001). Instrumental records today show global sea-level rise to be ~1.8 ± 0.3 mm/a (CHURCH et al., 2004). In order to reconstruct palaeoenvironmental changes forced by climatic and sea-level changes on the Eastern Adri- atic coast, this paper provides results from a variety of pre- vious studies. These are based on the 14C dating of spele- othems from three submerged caves (SURIĆ et al., 2005a), their stable isotope composition (SURIĆ et al., 2005b), and new results from extensive 14C and U-Th measurements from old and new speleothem samples from seven submerged caves. In addition, thanks to colleagues, cavers, and speleo- divers, a list of all presently known submerged speleological features along the Croatian Adriatic coast has been compiled (SURIĆ, 2006). 2. GEOLOGICAL AND ENVIRONMENTAL SETTINGS The Eastern Adriatic coast is an ingressive karstic coast form ed during the last Late Pleistocene-Holocene transgres- sion. It is characterized by the parallel extension of geological structures (folds, normal and reverse faults, overthrusts), geomorphological features, coast, channels and island chains, presenting a so-called Dalmatian type coast (VON RICH- THOFEN, 1901). Such a parallel characteristic of the Dina- ridic trend (NW-SE) is the result of collision of the Adria mic- ro plate and Eurasian plate from the Alpine orogeny to the present, with maximal stress oriented SW-NE (VLAHOVIĆ et al., 2002; 2005; KORBAR, 2009). A thick carbonate suc- cession (more than 8000 m) was deposited in several phases from the Middle Permian (or even Upper Carboniferous) to the Eocene (VLAHOVIĆ et al., 2005). This was intensively tectonically disturbed, periodically emergent, and exposed to exogenous processes resulting in karstifi cation. Karstifi - cation took place down to the contemporary erosional base level (sea level), while in some places it extended below sea level (SURIĆ, 2005). According to the LGM low sea-level stand, karst features may be found down to depths of 120–130 m (LAMBECK et al., 2002b), but if we take into consideration the Messinian Salinity Crisis (~6 Ma BP), with sea level ~1500 m lower than today (MURPHY et al., 2009), evidence for karstifi cation could be expected throughout the entire Adri- atic region. Currently the deepest speleothems found within submerged Croatian caves are those from Brač Island at –71 m (GARAŠIĆ, 2006). The Adriatic basin is characterized by a relatively shallow northern part with a low gradient (0.02°) down to –100 m. Such morphology makes this region very sensitive to eu static sea-level changes, and consequently, it experienced consi- derable environmental changes throughout the Quaternary Period. During the LGM with sea-level 120–130 m lower than today, the entire northern part, down to the Zadar-Pescara line, was emergent as a wide fl uvio-lacustrine plain with a coastline located at the northern edge of the Meso-Adriatic depression (PIRAZZOLI, 2000). Fi gu re 1: Studied localities: a – Medvjeđa spilja Cave (Lošinj Island), b – Cave in Tihovac Bay (Pag Island), c – the Vrulja Zečica submarine spring (near Starigrad), d – Pit near Iški Mrtovnjak Islet, e – U vode Pit (Krk Island), f – Zmajevo uho Pit (near Rogoznica), g – Pit in Lučice Bay (Brač Island). Geologia Croatica 63/2Geologia Croatica 158 tion of the present-day entrance that was opened by roof col- lapse. Two passages were explored down to 30 m b.m.s.l. Vrulja Zečica, near Starigrad, is a periodically active submarine spring with its outlet 20 m off the coast at 9 m b.m.s.l. (Fig. 2c). Speleothems at 41.5 m b.m.s.l. indicate a former vadose phase. Due to sea-level rise, it was subse- quently transformed to a coastal spring and fi nally to a sub- marine one. Unlike some other dispersed fresh-water outlets, Vrulja Zečica has a wide funnel-like shape. The Pit near Iški Mrtovnjak Islet lies entirely in the marine environment and is rich in speleothems completely covered with marine biogenic overgrowths. The entrance is 12 m off-shore at 5 m b.m.s.l., and the pit has been explored down to 25 m b.m.s.l., where it continues as a narrow pas- sage (Fig. 2d). U vode Pit (Krk Island) is a vertical speleological fea- ture with the entrance at 5.5 m a.m.s.l. (Fig. 2e). Although free circulation between the cave and the open sea is present, there is a thin brackish water lens of 0.5 m. The deepest part of the cave is within the marine environment, with marine organisms (serpulids) covering the rock and speleothem sur- faces. The bottom of the pit is at 24 m b.m.s.l. The Zmajevo uho Pit, near Rogoznica, was originally located in a shallow bay 40 m from the coast, but after the construction of an artifi cial island, its entrance is now within the pool connected to the open sea by the pipe. The opening was formed by roof collapse and is presently at 2.5 m b.m.s.l., while collapse debris covers the bottom of the pit (Fig. 2f). Rich marine biogenic overgrowths indicate the absence of a fresh-water infl uence. The Pit in Lučice Bay (Brač Island) has two entrances formed by roof collapses at a depth of 5 m b.m.s.l. some 10 m off-shore, on a horizontal rock ledge (Fig. 2g). The max- imum explored depth is 40 m. Marine conditions prevail in the whole pit and marine overgrowth is quite abundant. 4. SAMPLING Sampling of submerged speleothems was conducted accord- ing to the National Speleological Society (USA) Code of Conduct, suggesting that ‘the scientifi c collection should be professional, selective, and minimal’. Seventeen speleo thems were collected by SCUBA divers from 1.5 to 41.5 m b.m.s.l. from 7 submerged caves, as follows: – U vode Pit: two stalagmites from 14.5 m (K-14) and 18.8 m b.m.s.l. (K-18) (Pl. 1) – Medvjeđa spilja Cave: ‘fallen stalactite’ from 1.5 m b.m.s.l. (L-1) and stalagmite from 10 m b.m.s.l. (L-10) (Pl. 1) – Cave in Tihovac Bay: stalactite from 23 m b.m.s.l. (P-23) (Pl. 2) – Vrulja Zečica: stalagmite from 41.5 m b.m.s.l. (Z-41) (Pl. 1) – Pit near Iški Mrtovnjak Islet: three stalactites from 14 m (M-14), 19 m (M-19) and from 23 m b.m.s.l. (M-23) (Pl. 1), and ‘fallen stalactite’ from 25 m b.m.s.l. (M-25) – Zmajevo uho Pit: two stalactites from 17 m (R-17) and 21.4 m b.m.s.l. (R-21) (Pl. 2) – Pit in Lučice Bay: stalactite from 26 m b.m.s.l. (B-26) and four stalagmites from 28 (B-28), 34 (B-34), 36 (B-36) and 38.5 m b.m.s.l. (B-38) (Pl. 2). Fi gu re 2: Cross sections of studied caves with marked po- sitions of sampled speleothems: a – Medvjeđa spilja Cave (Lošinj Island); b – Cave in Tihovac Bay (Pag Island); c – the Vrulja Zečica submarine spring (near Starigrad); d – Pit near Iški Mrtovnjak Islet; e – U vode Pit (Krk Island); f – Zma- jevo uho Pit (near Rogoznica); g – Pit in Lučice Bay (Brač Island) (note the diff erent scale). Surić and Juračić: Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) Geologia Croatica 159 Plate 1: Longitudinal sections of speleothems K-14, K-18, L-1, L-10, M-14, M-19, M-23 and Z-41, with marked locations of subsamples for U-Th and 14C dating (white squares and dotted lines) and XRD (yellow lines). White arrows (K-14 and K-18) mark hiatuses where the white substance apeared (see text). Scale bar 10 cm, except for M-23, which is 5 cm. Geologia Croatica 63/2Geologia Croatica 160 We use the expression ‘fallen stalactite’ for speleothems that were collected from the cave fl oor in the growth posi- tion of stalagmites, but whose origin was primarily stalactitic (reported in SURIĆ et al., 2007) Since stalagmites provide better stratigraphic resolution than stalactites and generally have less ionic mobility, sta- lagmites are preferred for palaeoenvironmental reconstruc- tions and geochronological studies (RICHARDS & DO- RALE, 2003). Yet, in submarine caves, it is not possible to follow this sampling strategy thoroughly, since the bottoms of the caves, together with stalagmites, are sometimes cov- ered with marine sediments and fallen rock debris. Hence, some stalactites were also collected and analysed. After collecting speleothems from the sea, and prior to any mechanical modifi cation, biological species covering the samples were determined. Afterwards, speleothems were longitudinally cut and polished to provide a view of their growth layers. Samples for measurement and analysis were taken from the youngest and the oldest parts of the spele- othems and along distinct hiatuses, in order to constrain the timing of cessation/recommencement or where distinct changes in morphology and mineralogy that affected spele- othem deposition occurred. Speleothem carbonate samples for measurement were separated by micro-drill and diamond saw: 250–450 mg for the U-Th analyses, and for 14C dating ca 30 g for the measurements on a gas proportional counter (GPC) and ca 20 g for a liquid scintillation counter (LSC). The aim of mineralogical analyses on two speleothems from U vode Pit (K-14 and K-18; Pl.1) was to qualitatively determine the composition of the material associated with presumed hiatuses. In fresh cuts the hiatuses were high- lighted by a thin red layer, but after several days of exposure to air, a white substance appeared along the discontinuities. Speleothems from Medvjeđa spilja Cave were also minera- logically analysed in order to resolve the composition of the needle-like surface of L-1 that resembled aragonite, and the inhomogeneous material from the base of stalagmite L-10 which might have been of marine origin (Pl. 1). For stable isotope measurements reported earlier (SURIĆ et al., 2005b), samples of 5–10 mg of speleothem carbonate were drilled from the successive growth layers every 5–10 mm. 5. METHODS The main goal of this study was the dating of certain events recorded in speleothems. Therefore, three different dating tech niques were employed: U-Th Multi Collector Inductively Coupled Mass Spectrometry (MC-ICPMS), and conventional β-spectrometry 14C dating using gas proportional counting (GPC) and liquid scintillation counting (LSC) methods. U-Th measurements were undertaken in the Bristol Iso- tope Group facilities at University of Bristol, UK, using a ThermoFinnigan Neptune MC-ICPMS. Carbonate samples were dissolved in HNO3, spiked with 229Th/236U, and proc- essed through ion exchange columns for the separation of U and Th. The instrumental procedure with the mass spectrom- eter is reported in full in HOFFMANN et al. (2007) and briefl y in SURIĆ et al. (2009). The 14C dating was undertaken in the Radiocarbon and Tritium Laboratory of Ruđer Bošković Institute in Zagreb, Croatia, using a liquid scintillation counter Quantulus 1220 and conventional gas proportional counter. Carbonate sam- ples were treated with dilute HCl to obtain CO2 which was subsequently converted to benzene for LSC measurements (HORVATINČIĆ et al., 2004), and to methane for GPC (SRDOČ et al., 1971). The conventional protocol for calcu- lation of 14C value was followed (OBELIĆ, 1989; MOOK & VAN DER PLICHT, 1999). The 14C activity is expressed as percent of modern carbon (pMC), which relates the 14C content of a sample to the 14C content of a modern standard. The 14C age is expressed in conventional 14C years BP, ad- justed to initial 14C activity (A0 = 85%), and measured δ13C (or –8‰ when not measured). Calibrated ages for 14C age <22000 BP were obtained as a mean of the range obtained by OxCal v.3.10 calibration software (BRONK RAMSEY, 2005), and for 14C age >22000 BP by the extension of the calibration curve proposed by BARD et al. (2004). Qualitative mineralogical composition of the samples was determined by the X-ray diffraction method (XRD). Measurements were made in the Faculty of Natural Science, University of Zagreb, using a PANalytical X’pert Pro theta-theta diffractometer equipped with multilayer parabolic mono- chromator using CuKα radiation. Analyses of the white sub- stance from the hiatuses were preformed by in situ measure- ments directly on the speleothems, then on the powder removed from the polished surface, and fi nally, samples of 2–5 mg were drilled out. Moreover, speleothem carbonate was also analysed both along the discontinuity and at a dis- tance from it. Stable isotope measurements of the speleothem carbo nate were undertaken by continuous-fl ow isotope ratio mass spec- trometry (CF-IRMS), using a Finnigan GasBench and Delta-S mass spectrometer located in Datierungen und Isotopenhy- drologie Sektion, Institut für Geowissenschaftliche Gemein- schaftsaufgaben in Hannover, Germany. The procedure re- ported in SURIĆ et al. (2005b) was followed. d13C and d18O values in carbonate are expressed in ‰ deviations from the international standard PDB. The analytical error ranges from ±0.05‰ to ±0.2‰ depending on the type of sample. 6. RESULTS 6.1. Marine biogenic overgrowth determination Marine biogenic overgrowths can be regarded as a proxy re- cord of prevailing environmental conditions in submerged caves, so in completely marine conditions as in the Cave in Tihovac Bay, the Pit near Iški Mrtovnjak, Zmajevo uho Pit, and the Pit in Lučice Bay, submarine speleothems are cov- ered with a marine overgrowth, in places more than 1 cm thick. In contrast, within the caves with fresh water input, as in the U vode Pit, Medvjeđa spilja Cave, and Vrulja Zečica, marine organisms, mostly Polychaeta (serpulids), have scar- cely settled on the speleothems. Marine overgrowths include various species of Foraminifera, Porifera, Polychaeta, Bival- via, Gastropoda and Bryozoa. However, certain organisms Surić and Juračić: Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) Geologia Croatica 161 Plate 2: Longitudinal sections of speleothems B-38, B-36, B-34, B-28, B-26, R-17, R-21 and P-23, with marked locations of the subsamples for the U-Th and 14C dating (bracketed with black lines) and for stable isotope analyses (white lines). Scale bar 5 cm. Geologia Croatica 63/2Geologia Croatica 162 were identifi ed only to generic level and for some it was not possible to identify even the genus. Identifi ed organisms be- long to the biocenosis of caves and ducts in complete dark- ness (JURAČIĆ et al., 2002) that consists exclusively of animal species adapted to complete darkness, limited sea- water circulation and nutrient infl ow, and stable sea-water temperature. 6.2. Mineralogical composition The mineralogical composition of samples analysed from U vode Pit stalagmites was determined as follows: (i) the main components of the white material measured directly on the speleothems were halite, gypsum and calcite; (ii) the same material scratched from the surface showed the presence of halite and calcite (and possibly dolomite); (iii) in the samples drilled from the discontinuities only calcite and halite were determined; (iv) calcite was the only mineral determined far from the discontinuities (SURIĆ et al., 2009). The needle-like surface of the speleothem L-1 from Medvjeđa spilja Cave was determined to be calcite, with only one peak that could be ascribed to aragonite. Probably metastable aragonite changed its crystal structure to stable calcite preserving the external habit of aragonite (ONAC, 2005). In porous and inhomogeneous material from the base of the stalagmite L-10 from the same cave, apatite and cal- cite were determined. This eliminates the possibility that it was of marine origin, because marine biogenic deposits con- sist mostly of calcite, high-magnesium calcite, aragonite and quartz (SURIĆ et al., 2005a). 6.3. U-Th and 14C ages The results of U-Th MC-ICPMS and 14C measurements are given in Tables 1 and 2, respectively. Locations of samples are shown in Plates 1 and 2. A total of 36 U-Th measurements were made on 32 spe- leothem subsamples and one sample of the marine biogenic overgrowth (no. 29). Some samples were measured twice in order to check or confi rm the results. Concentrations of 238U were in the range 29–437 ng/g (ppb), and for 232Th the range was 0.08–427 ng/g, except for values of 1260 ng/g for 238U and 1217 ng/g for 232Th that were recorded in the sample of marine overgrowth. An extremely high 232Th concentration of 427 ng/g in speleothem carbonate was also measured at the contaminated surface part of the K-18 speleothem. Such surface parts were usually avoided during sampling. Initial contamination by 230Th from the detritus was estimated from the 230Th/232Th activity ratio, so when necessary, corrections were made using the bulk Earth value of Th/U=3.8. Three samples (MS-08, MS-12, MS-13) that had an activity ratio 230Th/234U >1 gave unreliable or indeterminable ages. The U-Th ages that we consider reliable cover the period from ~210 to ~20 ka BP. 6.4. Stable isotope records Stable isotope ratios from measured speleothems (B-28, B-34, B-36, B-38, R-17 and R-21) were given in detail in SURIĆ et al. (2005b). In the speleothem samples the d13C ranges from –10.4‰ to –6.2‰ and the d18O from –6.7‰ to –4.1‰. However, a weak correlation between d13C and d18O indi- cates that kinetic isotope fractionation probably occurred during calcite precipitation. According to theory and the early suggestions of HENDY (1971), d18O values are di- rectly related to the cave temperature only when calcite de- position takes place under equilibrium conditions. In the sampled speleothems deposited during the LGM, the d18O values range from –6.7‰ to –4.1‰, being very similar to the –6‰ to –3.5‰ range recorded within the Holocene con- tinental speleothems from the marine-infl uenced regions (Mediterranean) (HORVATINČIĆ et al., 2003). 6.5. Submerged speleological features So far, 235 submerged voids have been discovered, and par- tially explored, in the Croatian part of the Adriatic Sea. Among them, 163 are on or along island coasts, and 72 are along the mainland coast. This distribution matches the pro- portion of the lengths of island coastline (4398 km; DUP- LANČIĆ et al., 2004) and mainland coastline (1777.3 km; STATISTICAL YEARBOOK 2008, 2009). According to their inclination, 60% are caves and 40% are pits, although in many cases only the entrance parts were explored, and more remote channels may have a different morphology. In the continental part of the Dinaric karst, 29% are caves, 60% are pits, and 2% are combined features (GARAŠIĆ, 1991). Among the 235 features, 126 have completely marine con- ditions, 75 are anchialine (mostly) pits, 13 are submarine springs (vruljas), and 21 features are not determined by hy- drological or environmental conditions. Detailed analysis is given in SURIĆ et al. (2010), and the list of the submerged caves is available in SURIĆ (2006). Speleothems, as the ma- terial for these investigations, were discovered in more than 140 submerged caves. 7. DISCUSSION 7.1. Sea level changes during the last 220 ka Sea-level changes are the result of vertical readjustment of the ocean-bordering landmasses at locally varying rates (hydro-isostasy) in addition to the global (eustatic) meltwa- ter-related sea-level fl uctuations (HANEBUTH et al., 2009). Global sea-level changes with amplitudes of several hundred metres are generally induced by plate tectonics and they oc- cur on a time scale of millions of years, while Quaternary sea-level changes are primarily induced by cyclic growth and decay of ice sheets, i.e. by climatically induced periodic exchange of mass between ice sheets and oceans (LAM- BECK & CHAPPELL, 2001). Three different approaches are generally used for the reconstruction of Late Pleistocene- Holocene sea-level changes: (i) fi eld observations using datable sea-level markers, (ii) simulation of global sea level based on the water-equivalent ice volume on the continents, (iii) use of proxy data, such as stable oxygen isotopes, to defi ne temperature minima that correspond to sea-level minima (e.g., HANEBUTH et al., 2009). Surić and Juračić: Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) Geologia Croatica 163 Eustatic sea-level changes are worldwide changes which can be reconstructed only in tectonically stable areas. In tec- tonically unstable regions sea-level changes take place through movement of both the land and/or sea, and they are referred to as relative sea-level changes (changes in the position of the sea relative to the land) (LOWE & WALKER, 1998). Since the eastern Adriatic coast is considered tectonically active (PRELOGOVIĆ et al., 2003) only the relative sea-level curve can be reconstructed. Taking into account known eustatic sea- level changes, regional or local tectonics could be revealed. Table 1: U-Th ages of speleothems K-14, K-18, L-1, L-10, Z–41, P-23, M-14, M-19 and M–23 and of marine overgrowth of speleothem P-23. Numbers in the fi rst column correspond to the sample locations indicated in Plates 1 and 2. Sample No. Lab. no. Sample 238U (ng g–1) 232Th (ng g–1) Measured Corrected Uncorr. age (ka) Corrected age (ka) (230Th/232Th) activity (232Th/238U) activity (230Th/238U) activity (234U/238U) activity (230Th/238U) activity (234U/238U) activity 1 MS-43 K-14-B-50d 60.9 57.11 2.3 3.07E-01 0.7184 1.1221 0.6348 1.1584 108.7 84.7 ± 12.3 2 MS-44 K-14-B-45 67.1 7.16 18.4 3.49E-02 0.6416 1.1250 0.6320 1.1287 90.3 87.8 ± 1.3 3 MS-42 K-14-B-1d 44.9 1.39 62.2 1.01E-02 0.6296 1.1655 0.6268 1.1668 82.9 82.2 ± 1.1 4 MS-41 K-14-A-172d 69.6 15.53 8.6 7.30E-02 0.6314 1.0888 0.6102 1.0939 93.2 87.7 ± 3.7 5 MS-25 K-14-A-10 100.3 21.11 9.3 6.89E-02 0.6383 1.0825 0.6187 1.0870 95.7 90.6 ± 2.9 6 MS-08 K-18-S 212.3 426.56 1.5 6.57E-01 1.0116 1.2062 1.0228 1.4045 183.1 131.4 ± 28.4 7 MS-05 K-18-C-14L 33.4 3.25 17.2 3.19E-02 0.5506 1.3515 0.5396 1.3601 55.7 53.8 ± 2.1 8 MS-06 K-18-C-14R 38.8 4.00 17.1 3.37E-02 0.5749 1.3818 0.5639 1.3916 57.2 55.2 ± 1.4 9 MS-06 K-18-C-14R 34.4 3.46 17.6 3.29E-02 0.5806 1.4917 0.5700 1.5041 52.3 50.5 ± 5.3 10 MS-17 K-18-C-14M 34.8 3.16 18.5 2.97E-02 0.5483 1.3687 0.5381 1.3770 54.5 52.8 ± 1.1 11 MS-04 K-18-C-11 35.8 1.05 61.3 9.65E-03 0.5910 1.3911 0.5880 1.3939 58.7 58.1 ± 1.4 12 MS-03 K-18-C-2 66.5 2.03 59.3 1.00E-02 0.5933 1.2951 0.5902 1.2973 65.2 64.5 ± 1.2 13 MS-02 K-18-B-40 65.4 0.94 138.6 4.68E-03 0.6491 1.2464 0.6479 1.2472 78.1 77.7 ± 1.4 14 MS-45 K-18-B-10 48.7 1.03 96.9 6.91E-03 0.6694 1.2290 0.6677 1.2300 83.3 82.9 ± 0.6 15 MS-46 K-18-A-95L 90.2 10.69 17.6 3.88E-02 0.6833 1.1240 0.6739 1.1273 99.9 97.2 ± 1.4 16 MS-47 K-18-A-95R 80.6 10.79 15.3 4.38E-02 0.6694 1.1430 0.6582 1.1479 93.9 90.8 ± 1.5 17 MS-01 K-18-A-5 48.3 4.25 25.0 2.88E-02 0.7199 1.2167 0.7137 1.2214 94.7 93.7 ± 3.4 18 MS-23 L-1-2 205.1 36.77 12.5 5.87E-02 0.7352 1.0681 0.7231 1.0712 124.9 120.4 ± 3.2 19 MS-24 L-10-T1 254.7 6.63 37.0 8.51E-03 0.3153 1.1731 0.3110 1.1742 33.8 33.2 ± 0.5 20 MS-24 L-10-T1 253.3 6.59 37.1 8.51E-03 0.3155 1.1618 0.3112 1.1629 34.2 33.7 ± 0.6 21 MS-30 L-10-T2 259.1 4.32 35.4 5.45E-03 0.1929 1.1147 0.1896 1.1152 20.6 20.2 ± 0.5 22 MS-29 L-10-25 265.8 4.88 156.2 6.01E-03 0.9383 1.0713 0.9380 1.0716 217.3 216.8 ± 10.5 23 MS-18 M-14-T 437.1 74.85 6.3 5.60E-02 0.3531 1.0651 0.3249 1.0679 43.6 39.3 ± 2.0 24 MS-19 M-19-T1A 359.7 1.33 350.5 1.21E-03 0.4231 1.0560 0.4226 1.0561 55.4 55.3 ± 1.9 25 MS-20 M-19-T1B 388.6 5.78 74.4 4.86E-03 0.3620 1.0622 0.3597 1.0624 45.2 44.8 ± 1.0 26 MS-21 M-19-T2 222.8 0.08 4198.2 1.16E-04 0.4865 1.0418 0.4865 1.0418 68.1 68.1 ± 0.7 27 MS-22 M-23-T 231.1 7.99 77.7 1.13E-02 0.8793 1.0350 0.8782 1.0353 202.2 201.3 ± 5.5 28 MS-22 M-23-T 230.8 7.93 77.6 1.12E-02 0.8717 1.0264 0.8707 1.0266 202.9 202.0 ± 7.4 29 MS-09 P-23-MO 1259.9 1217.40 1.4 3.16E-01 0.4490 1.1510 0.2789 1.1976 53.2 28.7 ± 11.2 30 MS-10 P-23-T1 148.1 57.07 3.1 1.26E-01 0.3867 1.0987 0.3230 1.1090 46.9 37.3 ± 4.2 31 MS-11 P-23-T2 363.6 1.36 233.6 1.22E-03 0.2857 1.0812 0.2850 1.0813 33.3 33.2 ± 0.7 32 MS-31 P-23-T3 91.5 4.21 18.5 1.50E-02 0.2789 1.0609 0.2708 1.0616 33.1 31.9 ± 0.9 33 MS-12 Z-41-B-40 76.3 265.54 1.5 1.14E+00 1.6677 1.1141 5.4493 1.7603 – – 34 MS-13 Z-41-B-28 50.0 124.82 1.4 8.17E-01 1.1845 1.1765 1.4726 1.4521 371.2 308.1 ± 53.8 35 MS-28 Z-41-B-26 28.6 15.59 2.3 1.78E-01 0.4078 1.2585 0.3169 1.2982 42.1 30.2 ± 5.2 36 MS-27 Z-41-A3 60.1 48.02 1.5 2.61E-01 0.3843 1.2277 0.2351 1.2829 40.4 21.9 ± 8.2 * Data 1–5 and 7–17 were presented in SURIĆ et al. (2009) Geologia Croatica 63/2Geologia Croatica 164 On the basis of the U-Th and 14C ages of particular parts of sub merged speleothems, a partial sea-level curve can be reconstructed for the eastern Croatian coast for the last 220 ka (Fig. 3). MIS 7 (245–190 ka BP) was the earliest interglacial re- corded in the sampled speleothems. This stage was marked with three high sea-level stands at ~238 ka BP (MIS 7e), ~216 ka BP (MIS 7c) and ~195 ka BP (MIS 7a) (BARD et al., 2002). Deposition of speleothem L-10 probably started right after the MIS 7c peak, while the growth of speleothem M-23 had ceased by the subsequent MIS 7a sea-level rise. MIS 6 (190–130 ka BP) was the glacial event with a sea level probably as low as during the LGM (BARD et al., 2002), and from that period, no speleothems have been Table 2: 14C ages of speleothems L-1 and L-10 measured by a liquid scintillation counter, and of speleothems Z-41, B-38, B-36, B-34, B-28, P-23 and R-21 measured by a gas proportional counter. The youngest parts are marked with A and S, while B regards the oldest parts. 14C ages are expressed as conven- tional 14C corrected for A0 = 85% and measured δ13C (–8‰ when not measured), and as calibrated ages. Numbers in the fi rst column correspond to the sample locations on Plates 1 and 2. Sample No. Lab. no. Sample 14C activity (pMC)1 d13C (PDB ‰) 14C conventional age corrected for A0 (BP) Calibrated range (cal BP)2 Calibrated age (cal BP)3 37 Z-3495 L-1-S 57.4 ± 0.9 –8.0 3150 ± 125 3490 – 3210 3350 38 Z-3661 L-10-S 35.5 ± 0.7 –8.0 7015 ± 170 7990 – 7670 7830 39 Z-3660 Z-41-S 25.2± 0.8 –8.0 9760 ± 280 9700 – 8750 9225 40 Z-3032 B-38-A 2.7 ± 0.5 –7.4 27 550 ± 1600 32 200 41 Z-3033 B-38-B 0.0 ± 0.5 –9.5 > 37 000 42 Z-3036 B-36-A 3.8 ± 0.5 –8.7 25 120 ± 1200 29 800 43 Z-3037 B-36-B 1.0 ± 0.5 –9.0 > 37 000 44 Z-3039 B-34-A 8.5 ± 0.6 –8.8 18 500 ± 540 22 750 – 21 250 22 000 45 Z-3040 B-34-B 0.5 ± 0.5 –9.7 > 37 000 46 Z-3042 B-28-A 8.9 ± 0.6 –7.2 18 150 ± 520 22 350 – 20 850 21 600 47 Z-3054 P-23-A 3.6 ± 0.5 –7.5 25 480 ± 1230 30 300 48 Z-3055 P-23-B 2.1 ± 0.5 –8.5 29 730 ± 2110 34 800 49 Z-3057 R-21-A 5.0 ± 0.5 –6.8 22 750 ± 890 26 900 50 Z-3058 R-21-B 2.4 ± 0.4 –6.2 28 505 ± 1320 33 500 1 Measured 14C activity is expressed as pMC (percent of modern carbon). 2 Calibrated range for the ages <22 000 BP is obtained by calibration software OxCal v.3.10 (BRONK RAMSEY, 2005) 3 Calibrated age for 14C ages <22 000 BP is obtained as a mean of the calibrated range, and for 14C ages >22 000 BP by the proposed extension of the calibration curve (BARD et al., 2004). * Data 40–50 were presented in SURIĆ et al. (2005a) Fi gu re 3: Late Pleistocene-Holo- cene relative sea-level curve (blue) based on 14C and U-Th ages of 16 submerged speleothems (oran ge), correlated with the global sea-le v el curve (red), reconstructed from U- Th ages of coral reefs from Huan (Papua New Guini) and Bonaparte Bay (Australia) (adapted from LAM- BECK et al., 2002a), and the math- ematically derived curve (green) (adapted from POTTER & LAM- BECK, 2004). Last Glacial Maxim- um (LGM) period (light blue) ac- cording to LAMBECK & CHAPPELL (2001) and LAMBECK et al. (2002a; 2002b). Surić and Juračić: Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) Geologia Croatica 165 found. This could indicate glacial conditions unfavourable for speleothem deposition, as recorded throughout most of Europe during the LGM. Yet, we can assume that in coastal Croatia, speleothem deposition was possible during the MIS 6 glacial similarly to that during the LGM (SURIĆ et al., 2005a). The MIS 5 (130–73 ka BP) interglacial was marked by three distinct high sea levels, with the fi rst (MIS 5e at ~130 ka BP) being 6 m ± 3 m higher than at present (LAMBECK et al., 2004). Two subsamples had ages from that period. The surface parts of the stalagmite K-18 showed a U-Th age of 131.4 ka BP, but, as we know that the sea level was much higher than –18 m, the measured age was probably distorted by contamination of the surface by thorium from sea water or by leaching of uranium. An additional indicator for that contamination is the sequence of inner (younger) speleothem layers with correct stratigraphy. Another doubtful value is the age of 120.4 ka BP of the inner part of L-1 speleothem found at the depth of 1.5 m, which should have been sub- merged during the MIS 5e. Investigation of the interior re- veals an initial straw morphology (Pl. 1), which shows that it was originally a stalactite (although it was found on the cave fl oor in growth position of a stalagmite), probably at an elevation higher then the MIS 5e sea level (SURIĆ et al., 2007). Speleothems from the U vode Pit recorded some events from the MIS 5a period; precipitation of speleothems K-18 had been more or less continuous in subaerial condi- tions from >93 to ~90 ka, from ~82 to ~77 ka and from ~64 to 54 ka, whereas K-14 had been growing from >90 to ~87 ka and for a brief period at 82 ka. Hiatuses were marked by mineral associations (calcite, gypsum, halite) that precipitate due to the evaporation of seawater (Ca-carbonates, gypsum, anhydrite, halite, K-Mg chlorides, arranged from least to most soluble; SEIBOLD & BERGER, 1996). Apparently, these hiatuses recorded the periods 90–82 ka and 77–64 ka in K-18 and 87–82 ka in K-14, which can be attributed to two MIS 5a sea-level highstands known as the double peak at ~84 and ~77 ka, which has also been noticed on the up- lifted island of Barbados (POTTER & LAMBECK, 2004; POTTER et al., 2004; SCHELLMANN et al., 2004; RADTKE & SCHELLMANN, 2005). Comparison of the present eleva- tion of speleothems K-18 and K-14 to the ice-volume-equiv- alent global sea-level curve (LAMBECK & CHAPPELL, 2001) shows a difference of at least ~13–17 m (speleothems should have been located ~13–17 m lower than today in or- der to be submerged by MIS 5a sea-level highstands). This difference could have resulted from long-term regional up- lift at a rate of 0.15–0.25 mm/a (SURIĆ et al., 2009). During the MIS 4 (73–58 ka BP) glacial, precipitation of speleothem K-18 in U vode Pit continued with homoge- nous, dense carbonate indicating slow deposition in much dryer conditions, typical for glacial periods. Growth of spe- leothem M-19 also continued during MIS 4, and the preced- ing hiatus could have been of the same origin as that in K-18 caused by MIS 5 transgressions. During MIS 3 (58–22 ka BP), deposition of speleothem K-18 ceased, but not because of submergence, (sea level was probably ~70 m below the present one; LAMBECK et al., 2002a), nor because of environmental changes (it grew even during the colder MIS 4). A possible reason could be a change in groundwater fl ow paths or infi lling of the feeding channel. A change of growth direction during the last growth phase is also evident (Pl. 1). Similarly, the cessation of M-19 and M-14 growth during MIS 3 was probably not connected with submergence. MIS 3 U-Th ages for the speleothem L-10 are quite confusing, indicating the unsuitability of coralloids (popcorn speleothems) for dating. The majority of 14C results from the previous study (SURIĆ et al., 2005a) from the Cave in Tihovac Bay (Pag Island), Zmajevo uho Pit, and Pit in Lučice Bay (Brač Island) also fi t into MIS 3 period. Five of them fi t into the LGM (30–19 BP). No reliable results were obtained from MIS 2 (22–11.5 ka BP). Stalagmite Z-41, with one part dated to 21.9 ka BP, showed signifi cant stratigraphic inversion of U-Th ages, which could be expected owing to its obvious contamination with clay-rich material. The sea-level rise associated with MIS 1 (11.5 ka BP – Present) terminated the growth of speleothem Z-41 from Vrulja Zečica at 9.2 ka BP, probably by a rise in groundwa- ter level. So, after the subaerial phase, this void became a coastal spring, and subsequently a submarine one. The 14C age of the youngest part of speleothem L-10 possibly indi- cates cessation of growth ca. 7 ka BP, while the speleothem L-1 at –1.5 m was in vadose conditions, with needle-like de- posits on its surface ca. 3350 years BP. As expected, all the ages of marine overgrowth samples also fall into the MIS 1 period. Although the examined speleothems cover the last 220 ka, only a partial sea-level curve for the Eastern Adriatic could be constructed (Fig. 3) but it shows good correlation with the global sea-level curve. The few discrepancies in re- corded elevations probably result from long-term regional tectonics. 7.2. Palaeoenvironmental changes Sea-level changes have signifi cantly changed the palaeogeo- graphic scenery of the Eastern Adriatic region, but not evenly in all its parts. Relatively shallow parts of the northern Adri- atic and southern Dalmatia experienced substantial shifts in shoreline during low sea levels, whilst numerous regions with steep, even sub-vertical coasts remained almost un- changed even during sea-level fall of as much as 50 m (PIKELJ et al., 2009). Along with sea-level changes, coastal hydrology was considerably transformed, especially in terms of submergence of coastal springs and the activation of new ones at higher elevations during sea level rise, and their dry- ing up during sea-level fall. Lowering of the absolute ero- sional base level resulted in river incision far below present sea level. Emergence during regressional phases enabled not only deeper karstifi cation but also migration of Pleistocene fauna whose remnants can be found on today’s islands that are presently too small to sustain large Pleistocene animals (PAUNOVIĆ et al., 2001). Fossil remnants from the north- ern part of the Adriatic basin (Druška Peć Cave, Mošćenička Draga) consist exclusively of an alpine faunal assemblage Geologia Croatica 63/2Geologia Croatica 166 found at a relatively low elevation (335 m), suggesting sub- stantial climatic cooling (MALEZ et al., 1979). However, within the southeastern Adriatic region (Vela Spila on Kor- čula Island), there are no fossil remnants of Upper Pleistoce ne animals adapted to colder conditions (ČEČUK & RADIĆ, 2005), meaning that even during the cold MIS 2, climate- driven environmental changes were not so signifi cant as in the northern region. Apart from the faunal migrations, emer- gent continental regions presented refuge areas for plant spe- cies that could not adapt to glacial conditions. Thus, during the climate cooling in Europe, vegetation zones did not move as a whole to the south and there was no forest belt; forests could not be maintained in southern Europe, either in low- lands which were too dry, or in higher parts of mountain ranges where it was too cold. Steppe vegetation dominated and forests survived in narrow zones with appropriate moist conditions (ZAGWIJN, 1992). According to palynological re- search, one such zone spread along the Eastern Adriatic region as a refuge area for plant species from the north – coniferous forest interspersed with deciduous trees (ZAGWIJN, 1992). Aside from migrating fl oral and faunal species, conditions were probably also appropriate for early humans. Abundant moisture and forest cover provided the soil and groundwater conditions ideal for dissolution and depositional karstifi cation during the LGM, and probably also during pre- vious glacial periods. Speleothem deposition and vegetation that requires damp conditions suggest that during the LGM the Eastern Adriatic coast was a border between a relatively temperate Mediterranean zone and the periglacial part of Eu- rope to the north. Along with geographic position (latitude), the Adriatic Sea and the Alps and Dinarides were the key cli- mate modifi ers that mitigated the infl uence of climate changes, which were very severe throughout most of Europe. Namely, mountain ranges partly alleviated cold infl uences from the north, while the Adriatic Sea to the south ensured suffi cient humidity. During the LGM, the average annual temperature in the coastal area was probably 10 ± 5 °C lower than today (PEYRON et al., 1998), so the idea of speleothem deposition in such an environment [e.g., LGM temperature in Hvar was estimated to be 7.5 °C by MIRACLE (1995)] can be supported by recent speleothem growth in the region where temperatures are similar [e.g. in Gorski Kotar with annual average temper- ature of 7 °C (CASALE et al., 2004)]. The similarity between LGM and Holocene d18O values (–6.7‰ to –4.1‰ and –6‰ to –3.5‰, respectively) suggests similar climatic conditions during these two periods. But, prior to carbonate deposition, the d18O signal in meteoric water is infl uenced not only by temperature but also by the transport pathway of the water vapour, distance from the coast, amount of rainfall, etc. Therefore, different coastline positions during the LGM and Holocene could induce d18O signal changes that would produce similar values for the two periods despite the temperature difference of 10 ± 5 °C. 8. CONCLUSIONS Climate changes associated with the Late Pleistocene-Holo- cene period had considerable infl uence on the Eastern Adriatic region, in both the palaeogeographic and palaeoenvironmen- tal sense. According to U-Th and 14C ages, and minera logical composition of 16 submerged speleothems, the curve of rela- tive sea-level changes during the last 220 ka has been partially constructed for the Eastern Adriatic coast, and it generally cor- responds to the global sea-level curve. Some sea-level stands are better resolved: sea level lower than –23 m during MIS 7b (202 ka BP), the double peak during the MIS 5a (84 ka and 77 ka BP) with sea level above –14 m and low sea-stand in-between at ~80 ka BP, and rapid Holocene sea-level rise with sea level lower than –41.5 m (9.2 ka BP), –10 m (7.8 ka BP) and –1.5 m (3.4 ka BP). The ages of other dated samples correspond to periods with sea-level lower than present. Spe- leothem growth cessations were not caused by climate changes – if so, simultaneous terminations should have been noticed. Moreover, several speleothems grew even during the LGM. Growth cessation was probably caused by infi lling of the fe- ed er channels, changes in groundwater fl ow paths, or by sub- mergence of the speleothems in fresh water or sea water. d18O signals could not be interpreted as a proxy for tem- perature due to kinetic fractionation during speleothem deposi- tion. But speleothem growth during cold phases, preconditioned by adequate humidity and vegetation cover, suggests that the Eastern Adriatic area was transitional between periglacial Eu- rope and the temperate Mediterranean zone, with favourable conditions not only for karstifi cation, but also for migrating plants and animals, and most probably for early humans. To obtain more precise records of palaeoenvironmental changes in the Croatian coastal zone, future studies should encompass not only submerged speleothems from a wider range of depths and locations, but should also compare sim- ilar inland features and coastal sea-level markers below and above the present sea level. ACKNOWLEDGEMENT The Ministry of Science, Education and sport of the Republic of Croatia funded this research (Projects: 2693084-1177 "Geographical features in the development of Croatian coastal regions" and 1191152-1169 "Re- cent sediments and fossil environments of the Adriatic coastal zone"). Part of this research was supported by the Coimbra Group association who enabl ed M. SURIĆ, to undertake research and U-Th measurements at the School of Geographical Sciences, University of Bristol, where the assistan ce of D. RICHARDS and D. HOFFMANN was most helpful and is gratefully acknowledged. We would like to thank N. HOR- VATINČIĆ, I. KRAJCAR BRONIĆ and J. BAREŠIĆ from the Radio- carbon and Triti um Laboratory of Ruđer Bošković Institute for 14C mea- surements, D. TIB LJAŠ for the XRD analyses, A. SUCKOW for stable isotope measurements, and T. BAKRAN-PETRICIOLI for the identi- fi cation of marine organisms. Special thanks go to the speleodivers B. JALŽIĆ, V. JALŽIĆ, P. TASIĆ, T. RAĐA, A. NOVOSEL, M. KUHTA, M. GARAŠIĆ, M. KVARANTAN, H. HRELIĆ, A. ŽULJE VIĆ, D. PETRICIOLI and S. TRAJBAR for providing samples, photos and sketches of submerged caves. We are also grateful to the reviewers D.C. FORD and A.N. PALMER whose suggestions and comments greatly improved the paper. REFERENCES ALESSIO, M., ALLEGRI, L., ANTONIOLI, F., BELLUOMINI, G., FERRANTI, L., IMPORTA, S., MANFRA, L. & PROPOSITO, A. (1992): Risultati preliminari relativi alla datazione di speleotemi Surić and Juračić: Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) Geologia Croatica 167 sommersi nelle fasce costiere del Tirreno centrale [Preliminary results on dating of submerged speleothems in central Tyrrhenian coastal zone – in Italian].– Giornale di Geologia, ser. 3., 54/2, 165–193. ANTONIOLI, F., SILENZI, S. & FRISIA, S. (2001): Tyrrhenian Holo- cene paleoclimate trends from spelean serpulids.– Quat. Sci. Rev., 20/15, 1661-1670. doi:10.1016/S0277-3791(01)00012-9 ANTONIOLI, F., BARD, E., POTTER, E.-K., SILENZI, S. & IMPRO- TA, S. (2004): 215-ka History of sea-level oscillations from marine and continental layers in Argentarola Cave speleothems (Italy).– Global Planet. Change, 43, 57–78. doi:10.1016/j.gloplacha.2004. 02.004 ANTONIOLI, F., ANTIDEI, M., LAMBECK, K., AURIEMMA, R., GADDI, D., FURLANI, S., ORRÙ, P., SOLINAS, E., GASPARI, A., KARINJA, S., KOVAČIĆ, V. & SURACE, L. (2007): Sea-lev- el change during the Holocene in Sardinia and in the northeastern Adriatic (central Mediterranean Sea) from archaeological and geo- morphological data.– Quat. Sci. Rev., 26, 2463–2486. doi:10.1016/j. quascirev.2007.06.022 BAR-MATTHEWS, M., AYALON, A., KAUFMAN, A. & WASSER- BURG, G. (1999): The Eastern Mediterranean paleoclimate as a refl ection of regional events: Soreq Cave, Israel.– Earth Planet. Sci. Lett., 166, 85–95. doi:10.1016/S0012-821X(98)00275-1 BARD, E., ANTONIOLI, F. & SILENZI, S. (2002): Sea-level during the penultimate interglacial period based on a submerged stalagmite from Argentarola Cave (Italy).– Earth Planet. Sci. Lett., 196, 135– 146. doi: 10.1016/S0012-821X(01)00600-8 BARD, E., ROSTEK, F. & MÉNOT-COMBER, G. (2004): A better ra- diocarbon clock.– Science, 303, 178–179. BELIJ, S. (1986): Komparativnost krškog, glacialnog i periglacialnog procesa u reliefu Južnog Velebita [Comparison of karst, glacial and periglacial process in the relief of southern Velebit – in Croatian].– Acta carsologica, XIV–XV, 183–196. BOGNAR, A., FAIVRE, S. & PAVELIĆ, J. (1991): Tragovi oledbe na Sjevernom Velebitu [Glaciation traces on the Northern Velebit – in Croatian].– Geografski glasnik, 53, 27–39. BRONK RAMSEY, C. (2005): The OxCal Program Manual, v.3.10, sub- mitted on WWW http://c14.arch.ox.ac.uk/embed.php?File=oxcal. html CASALE, A., GIACHINO, P.M. & JALŽIĆ, B. (2004): Three new spe- cies and one new genus of ultraspecialized cave dwelling Lepto- dirinae from Croatia (Coleoptera, Cholevidae).– Nat. Croat., 13/4, 301–317. CHURCH, J.A., WHITE, N.J., COLEMAN, R., LAMBECK, K. & MIT- ROVICA, J.X. (2004): Estimates of the regional distribution of sea level rise over the 1950–2000 period.– J. Climate, 17/13, 2609– 2625. doi: 10.1175/1520-0442(2004)017<2609:EOTRDO>2.0.CO;2 COYNE, M.K., JONES, B. & FORD, D. (2007): Highstands during Ma- rine Isotope Stage 5: evidence from the Ironshore Formation of Grand Cayman, British West Indies.– Quat. Sci. Rev., 26/3–4, 536– 559. doi:10.1016/j.quascirev.2006.06.013 ČEČUK, B. & RADIĆ, D. (2005): Vela spila – višeslojno pretpovijesno nalazište – Vela Luka, otok Korčula [Vela spila – A stratifi ed pre- historic site – Vela Luka, Island of Korčula (Croatia) – in Croatian].– Centar za kulturu "Vela Luka", Vela Luka, 299 p. DREYBRODT, W. (2005): Speleothem Deposition.– In: CULVER, D.C. & WHITE, W.B. (eds.): Encyclopedia of Caves. Elsevier Academ- ic Press, Burlington, 431–435. DUPLANČIĆ LEDER, T., UJEVIĆ, T. & ČALA, M. (2004): Coastline length and areas of islands in the Croatian part of the Adriatic Sea determined from the topographic maps at scale of 1:25000.– Geo- adria, 9/1, 5–32. DUTTON, A., BARD, E., ANTONIOLI, F., ESAT, T.M., LAMBECK, K. & MCCULLOCH, M.T. (2009): Phasing and amplitude of cli- mate and sea level during the penultimate interglacial.– Nat. Geo- sci., 2, 355–359. doi:10.1038/NGEO470. FAIRBANKS, R.G. (1989): A 17000-year glacio-eustatic sea level record: infl uence of glacial melting rates on the Younger Dryas event and deep-ocean circulation.– Nature, 342, 637–642. doi: 10.1038/342637a0 FORD, D. (1997): Dating and Paleo-Environmental Studies of Spele- othems.– In: HILL, C. & FORTI, P. (eds.): Cave Minerals of the World, 2nd ed., National Speleological Society, Huntsville, 271– 284. FORD, D.C. & WILLIAMS, P. (1989): Karst Geomorphology and Hy- drology.– Chapman & Hall, London, 601 p. FORNÓS, J.J., GELABERT, B., GINÉS, A., GINÉS, J., TUCCIMEI, P. & VESICA, P. (2002): Phreatic overgrowths on speleothems: a use- ful tool in structural geology in littoral karstic landscapes. The ex- ample of eastern Mallorca (Balearic Islands).– Geodinamica Acta, 15, 113–125. doi:10.1016/S0985-3111(02)01083-5 GARAŠIĆ, M. (1991): Morphological and hydrogeological classifi ca- tion of speleological structures (caves and pits) in the Croatian karst area.– Geološki vjesnik, 44, 289–300. GARAŠIĆ, M. (2006): Pronađeni i snimljeni najdublji speleothemi u moru [Found and documented deepest speleothems in the sea – in Croatian].– Spelaeologia Croatica, 7, 58. GASCOYNE, M. (1992): Paleoclimate determination from cave calcite deposits.– Quat. Sci. Rev., 11, 609–632. doi:10.1016/0277-3791- (92)90074-I GASCOYNE, M., BENJAMIN, G.J., SCHWARCZ, H.P. & FORD, D.C. (1979): Sea-Level Lowering During the Illinoian Glaciation: Evi- dence from a Bahama "Blue Hole", Science, 205, 806–808. doi: 10.1126/science.205.4408.806 HANEBUTH, T.J.J., STATTEGGER, K. & BOJANOWSKI, A. (2009): Termination of the Last Glacial Maximum sea-level lowstand: The Sunda-Shelf data revisited.– Global Planet. Change, 66/1–2, 76–84. doi:10.1016/j.gloplacha.2008.03.011 HARMON, R.S., SCHWARCZ, H.P. & FORD, D.C. (1978): Late Pleis- tocene Sea Level History of Bermuda.– Quat. Res., 9, 205–218. doi:10.1016/0033-5894(78)90068-6 HENDY, C.H. (1971): The isotope chemistry of speleothems I. The cal- culation of the effects of different modes of formation on the isoto- pic composition of speleothems and their applicability as paleocli- matic indicators.– Geochim. Cosmochim. Acta, 35, 801–824. HOFFMANN, D.L., PRYTULAK, J., RICHARDS, D.A., ELLIOTT, T., COATH, C.D., SMART, P.L. & SCHOLZ, D. (2007): Procedures for accurate U and Th isotope measurements by high precision MC- ICPMS.– Int. J. Mass Spectrom., 264/2–3, 97–109. doi:10.1016/j. ijms.2007.03.020 HORVATINČIĆ, N., KRAJCAR BRONIĆ, I. & OBELIĆ, B. (2003): Differences in the 14C age, d13C and d18O of Holocene tufa and spe- leothem in the Dinaric Karst.– Palaeogeogr. Palaeocl, 193, 139– 157. doi:10.1016/S0031-0182(03)00224-4 HORVATINČIĆ, N., BAREŠIĆ, J., BRONIĆ, I.K. & OBELIĆ, B. (2004): Measurement of low 14C activities in a liquid scintillation counter in the Zagreb Radiocarbon Laboratory.– Radiocarbon, 46/1, 105–116. JURAČIĆ, M., BAKRAN-PETRICIOLI, T. & PETRICIOLI, D. (2002): Cessation of Karstifi cation Due to the Sea-level Rise? Case Study of the Y-Cave, Dugi otok, Croatia.– In: GRABOVŠEK, F. (ed.): Evolution of Karst: From Prekarst to Cessation. Založba ZRC, Pos- tojna – Ljubljana, 319–326. KORBAR, T. (2009): Orogenic evolution of the External Dinarides in the NE Adriatic region: A model constrained by tectonostratigraphy of Upper Cretaceous to Palaeogene carbonates.– Earth Sci. Rev., 96/4,296–312. doi:10.1016/j.earscirev.2009.07.004 LAMBECK, K. & CHAPPELL, J. (2001): Sea level change through the Last Glacial Cycle.– Science, 292, 679–686. doi: 10.1126/sci- ence.1059549 Geologia Croatica 63/2Geologia Croatica 168 LAMBECK, K., ESAT, T.M. & POTTER, E.K. (2002a): Links between climate and sea level for the past three million years.– Nature, 419, 199–206. doi:10.1038/nature01089 LAMBECK, K., YOKOYAMA, Y. & PURCELL, T. (2002b): Into and out of the Last Glacial Maximum: sea level change during Oxygen Isotope Stages 3 and 2.– Quat. Sci. Rev., 21, 343–360. doi:10.1016/ S0277-3791(01)00071-3 LAMBECK, K., ANTONIOLI, F., PURCELL, A. & SILENZI, S. (2004): Sea-level change along the Italian coast for the past 10,000 yr.– Quat. Sci. Rev., 23, 1567–1598. LOWE, J.J. & WALKER, M.J.C. (1998): Reconstructing Quaternary Environments. 2nd ed.– Longman, Essex, 446 p. LUNDBERG, J. & FORD, D.C. (1994): Late pleistocene sea level change in the Bahamas from mass spectrometric U-series dating of submerged speleothem.– Quat. Sci. Rev., 13/1, 1–14. doi: 10.1016/ 0277-3791(94)90121-X MALEZ, M. & BOŽIČEVIĆ, S. (1965): The Medvjeđa pećina (Bear Cave) on Lošinj Island, A rare case of submerged cave.– Interna- tional Speleological Conference, Brno, 1964, Problems of Speleo- logical Research, Prague, 211–216. MALEZ, M. & RABEDER, G. (1984): Neues Fundmaterial von Kle- insäugern aus der altpleistozänen Spalten-füllung Podumci 1 in Norddalmatien (Kroatien, Jugoslawien).– Beiträge zur Paläontolo- gie, 11, 439–510. MALEZ, M. & LENARDIĆ-FABIĆ, J. (1988): New subspecies of the southern elephant (Mammuthus meridionalis adriacus n. ssp.) from the bottom of the Adriatic Sea (Croatia, Yugoslavia).– Palaeontolo- gia Jugoslavica, 37, 1–36. MALEZ, M., SLIEPČEVIĆ, A. & SRDOČ, D. (1979): Određivanje sta- rosti metodom radioaktivnog ugljika kvartarnim naslagama na ne- kim lokalitetima u Dinarskom kršu [Radiocarbon dating of Qua- ternary deposits on some localities in Dinaric karst – in Croatian]. Rad JAZU, 383, Razred za prirodne znanosti, 18, 227–271. MCGARRY, S., BAR-MATTHEWS, M. MATTHEWS, A., VAKS, A., SCHILMAN, B. & AYALON, A. (2004): Constraints on hydrolog- ical and paleotemperature variations in the Eastern Mediterranean region in the last 140 ka given by the δD values of speleothem fl uid inclusions.– Quat. Sci. Rev., 23, 919–934. doi:10.1016/j. quascirev.2003.06.020 MIHEVC, A. (2001). Speleogeneza Divaškega krasa [The Speleogen- esis of the Divača Karst – in Slovenian].– Založba ZRC, Ljubljana, 180 p. MIRACLE, P.T. (1995): Broad-spectrum adaptations re-examined: Hunt- er-gatherer responses to Late Glacial environmental changes in the Eastern Adriatic.– Unpubl. PhD Thesis, University of Michigan, USA. MOOK, W.G., VAN DER PLICHT, J. (1999): Reporting 14C activities and concentrations. Radiocarbon, 41, 227–239. MURPHY, L.N., KIRK-DAVIDOFF, D.B., MAHOWALD, N. & OTTO- BLIESNER, B.L. (2009): A numerical study of the climate response to lowered Mediterranean Sea level during the Messinian Salinity Crisis.– Palaeogeogr. Palaeocl, 279/1–2, 41–59. doi:10.1016/j. palaeo.2009.04.016 NIKLER, L. (1973): Nov prilog poznavanju oledbe Velebita [New con- tribution to understanding of glaciation of Velebit Mt. – in Croatian]. – Geološki vjesnik, 25, 109–112. OBELIĆ, B. (1989): The radiocarbon data base at Rudjer Bošković In- stitute Radiocarbon Laboratory.– Radiocarbon, 31, 1057–1062. ONAC, B. (2005): Minerals.– In: CULVER, D.C. & WHITE, W.B. (eds.): Encyclopedia of Caves, Elsevier Academic Press, London, 371–378. PAUNOVIĆ, M. & RABEDER, G. (2000): Paleoecological Analysis of the Pleistocene Vertebrate Fauna from Razvodje and Tatinja draga (Croatia).– Beiträge zur Paläontologie, 25, 87–94. PAUNOVIĆ, M., JAMBREŠIĆ, G., BRAJKOVIĆ, D., MALEZ, V. & MAUCH LENARDIĆ, J. (2001): Last Glacial Settlement of Croatia: Catalogue of fossil sites dated to the OIS 2 & 3.– Acta Geo logica, 26/2, 27–70. PELTIER, W.R. & FAIRBANKS, R.G. (2006): Global glacial ice vol- ume and Last Glacial Maximum duration from an extended Barba- dos sea level record.– Quat. Sci. Rev., 25, 3322–3337. doi:10.1016/j. quascirev.2006.04.010 PEYRON, O., GUIOT, J., CHEDDADI, R., TARASOV, P., REILLE, M., DEBEAULIEU, J.L., BOTTEMA, S. & ANDRIEU, V. (1998): Climatic reconstruction in Europe for 18,000 yr BP from pollen data.– Quat. Res., 49/2, 183–196. doi:10.1006/qres.1997.1961 PIKELJ, K., ŽIGIĆ, V. & JURAČIĆ, M. (2009): Origin and distribution of surface sediments in the Grgur Channel, Adriatic Sea, Croatia.– Geol. Croat., 62 /2, 95–105. PIRAZZOLI, P. A. (2000): Sea-Level Changes – The Last 20000 Years.– Wiley & Sons Ltd, Chichester, 211 p. POTTER, E.K. & LAMBECK, K. (2004): Reconciliation of sea-level observations in the West North Atlantic during the last glacial cy- cle.– Earth Planet. Sci. Lett., 217/1–2, 171–181. doi:10.1016/ S0012-821X(03)00587-9 POTTER, E.K., ESAT, T.M., SCHELLMANN, G., RADTKE, U., LAM- BECK, K. & MCCULLOCH, M.T. (2004): Suborbital-period sea- level oscillations during marine isotope substages 5a and 5c.– Earth Planet. Sci. Lett., 225, 191–204. doi:10.1016/j.epsl.2004. 05.034 PRELOGOVIĆ, E., PRIBIČEVIĆ, B., IVKOVIĆ, Ž., DRAGIČEVIĆ, I., BULJAN, R. & TOMLJENOVIĆ, B. (2003): Recent structural fab- ric of the Dinarides and tectonically active zones important for petro- leum-geological exploration in Croatia.– Nafta, 55/4, 155–161. PRENTICE, I.C., GUIOT, J. & HARISON, S.P. (1992): Mediterranean vegetation, lake levels and palaeoclimate at the Last Glacial Maxi- mum.– Nature, 360, 658–660. doi:10.1038/360658a0 RADTKE, U. & SCHELLMANN, G. (2005): Timing and magnitude of sea level change during MIS 5 derived from Barbados coral reef terraces: A critical literature review and new data.– J. Coastal Res., 21, spec. iss. 42, 52–62. RICHARDS, D.A. & DORALE, J.A. (2003): Uranium-series Chronol- ogy and Environmental Applications of Speleothems.– In: BOUR- DON, B., HENDERSON, G.M., LUNDSTROM, C.C. & TURNER S.P. (eds.): Uranium Series Geochemistry, Reviews in Mineralogy & Geochemistry, Geochemical Society, Mineralogical Society of America, 52, 407–460. RICHARDS, D.A., SMART, P.L. & EDWARDS, R.L. (1994): Maxi- mum sea levels for the last glacial period from U-series ages of submerged speleothems.– Nature, 367, 357–360. doi:10.1038/ 367357a0 SCHELLMANN, G. RADTKE, U., POTTER, E.K., ESAT, T.M. & MCCULLOCH, M.T. (2004): Comparison of ESR and TIMS U/Th dating of marine isotope stage (MIS) 5e, 5c, and 5a coral from Barbados – implications for palaeo sea-level changes in the Carib- bean.– Quat. Int., 120/1, 41–50. doi:10.1016/j.quaint.2004.01. 005 SEIBOLD, E. & BERGER, W.H. (1996): The Sea Floor – An Introduc- tion to Marine Geology. 3rd ed.– Springer, Berlin, 356 p. SPALDING, R.F. & MATHEWS, T.D. (1972): Stalagmites from Caves in the Bahamas: Indicators of Low Sea Level Stand.– Quat. Res., 2, 470–472. doi:10.1016/0033-5894(72)90085-3 SRDOČ, D., SLIEPČEVIĆ, A. & BREYER, B. (1971): Datiranje arheoloških nalaza biološkog porjekla metodom radioaktivnog ug- ljika C-14 [Radiocarbon dating of archaeologic samples of biolog- ical origin – in Croatian].– Rad JAZU, 349/2, 109–157. STATISTICAL YEARBOOK 2008 (2009): Geographical and meteoro- logical data, Republic of Croatia. – Central Bureau of Statistics, 38–59. Surić and Juračić: Late Pleistocene-Holocene environmental changes – records from submerged speleothems along the Eastern Adriatic coast (Croatia) Geologia Croatica 169 SURIĆ, M. (2005): Submerged karst – dead or alive? Examples from the Eastern Adriatic coast (Croatia).– Geoadria, 10/1, 5–19. SURIĆ, M. (2006): Promjene u okolišu tijekom mlađeg pleistocena i holocena – zapisi iz morem potopljenih siga istočnog Jadrana [Late Pleistocene – Holocene palaeoenvironmental changes – records from submerged speleothems from the Eastern Adriatic Sea (Cro- atia) – in Croatian, with an English Summary].– Unpubl. PhD The- sis, Faculty of Science, University of Zagreb, 213 p. SURIĆ, M. (2009): Reconstructing sea-level changes on the Eastern Adriatic Sea (Croatia) – an overview.– Geoadria, 14/2, 181–199. SURIĆ, M., JURAČIĆ, M., HORVATINČIĆ, N. & KRAJCAR BRONIĆ, I. (2005a): Late Pleistocene-Holocene sea-level rise and the pattern of coastal karst inundation – records from submerged speleothems along the Eastern Adriatic Coast (Croatia).– Marine Geology, 214, 163–175. doi:10.1016/j.margeo.2004.10.030 SURIĆ, M., HORVATINČIĆ, N., SUCKOW, A., JURAČIĆ, M. & BAREŠIĆ, J. (2005b): Isotope records in submarine speleothems from the Adriatic coast, Croatia.– Bulletin de la Société Géologique de France, 176/4, 363–373. doi: 10.2113/176.4.363 SURIĆ, M., JALŽIĆ, B. & PETRICIOLI, D. (2007): Submerged spele- othems – expect the unexpected. Examples from the Eastern Adri- atic coast.– Acta carsologica, 36/3, 389–396. SURIĆ, M., RICHARDS, D.A., HOFFMANN, D.L., TIBLJAŠ, D. & JURAČIĆ, M. (2009): Sea level change during MIS 5a based on submerged speleothems from the eastern Adriatic Sea (Croatia).– Mar. Geol., 262, 62–67, doi: 10.1016/j.margeo.2009.03.005 SURIĆ, M., LONČARIĆ, R. & LONČAR, N. (2010): Submerged caves of Croatia – distribution, classifi cation and origin.– Environ. Earth Sci. doi: 10.1007/s12665-010-0463-0 ŠEGOTA, T. & FILIPČIĆ, A. (2003): Köppenova podjela klima i hrvat- sko nazivlje [Köppen’s classifi cation of climates and the problem of corresponding Croatian terminology – in Croatian].– Geoadria, 8/1, 17–23. TEŠIĆ, M. (1958): O postdiluvijalnom pozitivnom pomeranju obalske linije na istočnoj obali Jadranskog mora [On postdiluvial positive shift of the eastern Adriatic coastline – in Croatian].– Hidrografski godišnjak 1956.–1957., 153–162. VESICA, P.L., TUCCIMEI, P., TURI, B., FORNÓS, J.J., GINÉS, A. & GINÉS, J. (2000): Late Pleistocene paleoclimates and sea-level change in the Mediterranean as inferred from stable isotope and U- series studies of overgrowths on speleothems, Mallorca, Spain.– Quat. Sci. Rev., 19, 865–879. doi:10.1016/S0277-3791(99)00026-8 VLAHOVIĆ, I., TIŠLJAR, J., VELIĆ, I. & MATIČEC, D. (2002): The Karst Dinarides are Composed of Relics of a Single Mesozoic Plat- form: Facts and Consequences.– Geol. Croat., 55/2, 171–183. VLAHOVIĆ, I., TIŠLJAR, J., VELIĆ, I. & MATIČEC, D. (2005): Evo- lution of the Adriatic Carbonate Platform: Palaeogeography, main events and depositional dynamics.– Palaeogeogr. Palaeocl, 220, 333–360. doi:10.1016/j.palaeo.2005.01.011 VON RICHTHOFEN, F. (1901): Führer für Forschungreisende. Hanno- ver: Verlag Von Gebrüdek Jänecke, 734 p. VRHOVEC, T., MIHEVC, A., LAURITZEN, S.E. & LUNDBERG, J. (2001): O starosti potopljenih stalaktitov v jami pri otočku Galiola, Dalmacija, Hrvatska [On the ages of submerged speleothems in the cave near Galiola Islet, Dalmatia, Croatia – in Slovenian].– Naše jame, 43, 31–36. ZAGWIJN, W.H. (1992): Migration of vegetation during the Quaterna- ry in Europe.– In: VON KOENIGSWALD W. & WERDELIN, L. (eds.): Mammalian Migration and Dispersal Events in the Europe- an Quaternary, Courier Forschungsinstitut-Senckenberg, Frankfurt a. M., 153, 9–20. Manuscript received December 15, 2009 Revised manuscript accepted February 25, 2010 Available online May 31, 2010 Geologia Croatica 63/2Geologia Croatica 170