2019 | 72/1 | 19–42 | 12 Figs. | 7 Tabs. | 2 Pls. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society 1. INTRODUCTION Sediments deposited in marginal marine environments, such as salt-marshes, lagoons, estuaries, deltas and coastal lakes exhibit distinctive micropalaeontological, geochemical and mineralogi- cal compositions due to the variability of physical and chemical conditions (MACKENZIE et al., 1995; SEN GUPTA, 1999; ALVE & MURRAY, 1999; DIX et al., 1999; TAHER, 2001; ANADÓN et al., 2002; FRONTALINI et al., 2011a). Variability occurs as a consequence of the position of these environments at the land-sea transition. Studies of marginal marine environments are necessary in palaeoenvironmental research, especially with regard to sea level changes (GEHRELS, 1994; EDWARDS et al., 2004; MARRINER et al., 2014; MÜLLER-NAVARA et al., 2017; BENJAMIN et al., 2017; EMMANOUILIDIS et al., 2018). The specific geomorphological setting of the karstified east- ern Adriatic coast (PIKELJ & JURAČIĆ, 2013), enabled devel- opment of unique marginal marine environments. Veliko and Malo Jezero on Mljet Island are examples of submerged karst Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia Dea Brunović1, Slobodan Miko1, Nikolina Ilijanić1, Zoran Peh1, Ozren Hasan1, Tena Kolar2, Martina Šparica Miko1 and Ivan Razum3 1 Croatian Geological Survey, Sachsova 2, 10000 Zagreb, Croatia; (dea.brunovic@hgi-cgs.hr) 2 University of Zagreb, Faculty of Mining, Geology and Petroleum Engineering, Pierottijeva 6, 10000 Zagreb, Croatia 3 Croatian Natural History Museum, Demetrova 1, 10000 Zagreb, Croatia doi: 10.4154/gc.2019.02 Abstract Numerous karst dolines have been formed along the Croatian coast and many have been sub- merged during the Late Glacial and Holocene sea level rise. The coastal area of Cres Island in the Northern Adriatic is a typical example of this geomorphological setting, where transitional forms from subaerial to submerged dolines are present. Once dolines are formed they can ac- cumulate soil, water and sediments due to their morphology. Sediments are an especially valu- able source of environmental data. This paper presents the results of the study of foraminiferal assemblages and sediment geochemistry, supplemented with grain-size and mineralogical da- ta, from the marine ponds developed in the karst dolines on Cres Island. Obtained data is cor- related with the sediment core record from submerged dolines in the present-day embayments along the coastal zone of Cres Island. In total, 3 sediment cores were collected in the marine ponds Marinska, Arcij and Podbrajde, while 2 longer sediment cores have been extracted from the Jaz and Sonte embayments. The Marinska, Arcij and Podbrajde marine ponds have distinct geochemical and mineralogical sediment compositions, with monospecific foraminiferal assem- blages and generally differ from each other. The common characteristics are their high N and P concentrations and the algal origin of organic matter. Agglutinated foraminiferal taxa (Haplo- phragmoides canariensis and Trochammina inflata), typical for intertidal environments, are abun- dant in the brackish-water Marinska pond, while stress-tolerant species Ammonia tepida has been identified in the Arcij marine pond. Environmental conditions in the Podbrajde marine pond did not facilitate the development of a rich foraminiferal fauna. Results from the present-day ma- rine ponds enabled recognition of similar environments in the sediment cores collected in the Jaz and Sonte embayments that were progressively inundated during the Holocene sea level rise. A palaeo-marine pond existed in the Sonte embayment until 6610 cal BP, when the sea flooded the investigated area. A marine pond in the Jaz embayment was formed at 711 cal BP. Low-diversity foraminiferal assemblages in these palaeo-ponds are similar to those recognized in the present-day Arcij marine pond on Cres Island. However, differences in the geochemical composition of palaeo-marine ponds, in comparison to the present-day ponds, exist. They might be attributed to climate variability over time and variations in the geological setting of each en- vironment. High Mo concentrations and abundant organic matter content are the main sediment characteristics of the recognized palaeo-marine ponds in the Jaz and Sonte embayments. dolines with surface connection to the sea. In the literature, this type of environment is termed a marine lake (JURAČIĆ et al., 1995; GOVORČIN et al., 2001; VANIČEK et al., 2000; SURIĆ, 2002; SURIĆ, 2005; SONDI & JURAČIĆ, 2010; PIKELJ & JURAČIĆ, 2013). Marine lakes can also be found on other parts of the eastern Adriatic coast, such as Zmajevo oko near Ro- goznica and Mir on Dugi otok Island. These shallow water envi- ronments have a subsurface connection to the sea allowing seep- age through karstified bedrock (SURIĆ, 2002; SURIĆ, 2005; PIKELJ & JURAČIĆ, 2013). Since marine lakes are located in the coastal karst zone and the marine influence on their develop- ment is substantial, these environments can be considered as mar- ginal marine types and they can preserve a record of the Holocene sea level rise (WUNSAM et al., 1999; GOVORČIN et al., 2001). Other types of marginal marine environments (lagoons, estuaries and salt-marshes) have also been developed along the Croatian coastline (PANDŽA et al., 2007; PIKELJ & JURAČIĆ, 2013). However, considerable work has yet to be conducted in terms of the description and characterization of the different types of tran- Article history: Manuscript received July 04, 2018 Revised manuscript accepted October 25, 2018 Available online February 15, 2019 Keywords: karst dolines, sediment cores, Holocene, marginal marine environments, sea level change, foraminifera, organic carbon, trace elements, Adriatic Sea G eo lo gi a C ro at ic a Geologia Croatica 72/120 sitional environments present along the karstified eastern Adri- atic coast. The focus of many foraminiferal studies worldwide is the de- termination of species and their dependence on sea level and other environmental conditions in the salt-marshes (e.g., GEHRELS, 1994; HAYWARD et al., 1999; EDWARDS et al., 2004; SERAN- DREI BARBERO et al., 2004; KEMP et al., 2013; STÉPHAN et al., 2014; MILKER et al., 2015; MÜLLER-NAVARA et al., 2017), estuaries and coastal lagoons (e.g., SERANDREI BARBERO et al., 1999; DEBENAY et al., 2001; DEBENAY & GUILLOU, 2002; TAKATA et al., 2006; JAYALAKSHMY & RAO, 2006; FRON- TALINI et al., 2011a; FRONTALINI et al., 2011b; FRONTALINI et al., 2013) and brackish-water coastal lakes (e.g., CARBONI et al., 2009). Evidence for the survival of these typically marine or- ganisms in inland saline lakes and freshwater lakes has also been postulated (BOLTOVSKOY & LENA, 1971; CANN & de DEK- KER, 1981). Physical and chemical water properties, sediment type, sediment geochemistry, tides, storms, winds, evaporation and distance from a direct marine influence are some of the main environmental parameters that have a crucial impact on the fo- raminiferal assemblages in the marginal marine environments (DEBENAY et al., 2001; DEBENAY & GUILLOU, 2002; FRON- TALINI et al., 2011a). In general, it is considered that the fauna in these environments is less diverse and dominated by agglutinated species (DEBENAY & GUILLOU, 2002). Recent foraminiferal studies along the eastern Adriatic coast have been mostly restricted to investigation of species distribu- tion (VIDOVIĆ, 2010; ĆOSOVIĆ et al., 2011) and to the possible application of foraminifera as indicators of anthropogenic pollu- tion (VIDOVIĆ et al., 2009; POPADIĆ et al., 2013; VIDOVIĆ et al., 2014). Only a few studies have focused on the determination of fauna inhabiting marginal marine environments and their de- pendence on environmental conditions, as well as their applica- tion in palaeoenvironmental reconstructions. However, fo- raminiferal assemblages in marine lakes on the Mljet Island have been described in detail (VANIČEK et al., 2000; ĆOSOVIĆ et al., 2016), while SHAW et al. (2016) conducted a study of assem- blages present in the Jadrtovac and Blace salt-marshes. Results have produced valuable data about sea level variations in the in- vestigated area and proven the utility of salt-marsh foraminifera in transfer functions. FELJA et al. (2015) determined a foraminif- eral fauna in sediment cores from the Mirna River valley in Istria in order to decipher the palaeoenvironmental development of the valley. The geochemical composition of sediments reveals impor- tant environmental data. For example, the C/N ratio can be use- ful in the determination of organic matter provenance (MEY- ERS, 1994; MEYERS, 2003; LAMB et al., 2006). Nitrogen (N) and phosphorus (P) concentrations coupled with total organic carbon (TOC) content are frequently used as indicators of nutri- ent availability and primary productivity (MEYERS, 1997; DE- LANEY, 1998; DI et al., 2015). Application of molybdenium (Mo) as a proxy for redox conditions is also common (PEDERSEN, 1989; CRUSIUS et al., 1996; CALVERT & PEDERSEN, 1993; ALGEO & LYONS, 2006; SCHOLZ et al., 2017). Lead (Pb) can be indicative of pollution (LORING, 1978; HELALI et al., 2013) by industries and transport or its origin could be Pb pellets shot during hunting practices in marsh environments (BIANCHI et al., 2011; MIGANI et al., 2015; BORGHESI, 2016). Examples of the previously conducted research of sediment geochemistry in the marginal marine environments along the Croatian coast of the Adriatic Sea include studies of the Veliko and Malo Jezero (CUCULIĆ et al., 2009; SONDI et al., 2017), Mir (MLAKAR et al., 2015) and Zmajevo oko (MIHELČIĆ et al., 1996) marine lakes. Furthermore, the geochemical composi- tion of sediments from the shallow marine environments in Ba- kar Bay (CUKROV et al., 2014) and Makirina Cove (ŠPARICA at al., 2005; MIKO et al., 2008; KOMAR et al., 2015) was studied extensively. Most of these studies focused on deciphering natural and anthropogenic metal enrichment and geochemistry was not used in order to reconstruct palaeoenvironments. Our study offers a new insight into foraminiferal assem- blages and sediment geochemistry in the marine ponds along the coastline of Cres Island. These environments have been formed in the karst dolines and should be considered as marginal marine environments due to their proximity to the sea and marine influ- ence through karst. The main aim was to document typical fo- raminiferal species and their distribution in these unique water bodies since such studies are lacking along the eastern Adriatic coast. Special emphasis was on the determination of the linkages between foraminiferal assemblages and established environmen- tal conditions manifested in the physical and chemical water properties and geochemical, mineralogical and sedimentological properties of the sediment. A further aim was to characterize en- vironments in the Jaz and Sonte embayments, similar to those in the present-day marine ponds on Cres Island, using extracted sediment cores. Obtained results would be indicative of the tim- ing of the existence of Holocene palaeo-marine ponds in these presently submerged karst dolines. We hypothesize that present- day marine ponds on Cres Island represent modern analogs of submerged Holocene palaeo-marine ponds in the Jaz and Sonte embayments. 2. STUDY AREA The investigated environments are located along the southwest- ern coastline of Cres Island, in the northern part of the Adriatic Sea in the Kvarner region (Fig. 1). This region is characterized by NW-SE elongated islands (Cres, Lošinj, Krk, Rab, Pag), with bays and channels (Rijeka Bay, Kvarnerić Bay, Kvarner Bay, Vinodol-Velebit Channel, Lošinj Channel) located between the Vinodol-Velebit coastline and the Istrian peninsula. Final forma- tion of the steep and rocky eastern Adriatic coast occurred dur- ing the Late Glacial and Holocene periods when sea flooded pre- existing folded, faulted and karstified relief. Anticlines became island chains while synclines became bays and channels (BENAC & JURAČIĆ, 1998; JURAČIĆ et al., 1999; KELLETAT, 2005; PIKELJ & JURAČIĆ, 2013). The Mesozoic carbonate rocks and their geological setting on Cres Island have been a target of many detailed studies (MAMUŽIĆ, 1968; MAGAŠ, 1968; HUSINEC et al., 2000; KORBAR et al., 2001; KORBAR & HUSINEC, 2003; FUČEK et al., 2012; FUČEK et al., 2014). Limestones and dolomites of Cretaceous age are predominant sedimentary rock formations. The oldest deposits have been formed during the Lower Creta- ceous. Younger Palaeogene strata (foraminiferal limestones and flysch) are sporadically present in the northern part of Cres Island (FUČEK et al., 2014). Quaternary sediments are rather scarce and present in the form of terra rossa outcrops, alluvial deposits and colluvial deposits on the slopes (MAGAŠ, 1968; BENAC & DURN, 1997). Subaerial exposure of Cretaceous deposits enabled the for- mation of numerous karst dolines on Cres Island, especially in its southwestern part. Dolines are enclosed karst depressions with variable depth and dimensions (FORD & WILLIAMS, 1989). It G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 21 is considered that post-Miocene karstification in the Mediterra- nean occurred in tectonically susceptible areas during periods of sea level lowstands. The most prominent and best preserved evi- dence of karstification developed during the most recent sea level lowstand (SURIĆ, 2005; MOCOCHAIN et al., 2009; PIKELJ & JURAČIĆ, 2013). The Marinska, Arcij and Podbrajde marine ponds investi- gated in this study have variable depths, sill elevations separating the pond from the direct marine influence, distances to the sea and size (Tab. 1). They have been developed in the karst dolines within two lithostratigraphic units (Fig. 1), which are composed of alternations of dolomites and shallow marine limestones as- signed to the Upper Albian-Lower Cenomanian boundary (Sis unit) and Cenomanian pelagic limestones (Belej unit) (FUČEK et al., 2014). The karstic nature of Cres Island enables sea-water seepage through the karstified sill separating the ponds from the sea. Dip directions trend towards the northeast (FUČEK et al., 2014) which possibly additionally facilitates this seepage through developed layering, underground fissures and conduits. The study area is microtidal, as recorded on the nearby tide gauge on Lošinj Island (http://tides.mobilegeographics.com/loca- tions/3554.html). The present-day climate on Cres Island is considered to be temperate and humid with hot summers, while at the highest ele- vations summers are warm (ŠEGOTA & FILIPČIĆ, 2003). Me- teorological measurements between 1971-2000 at the nearby me- Figure 1. Map of the investigated area. A) Overview, B) Kvarner region and Istrian peninsula, C) Geological map of Cres Island and Lošinj Island (modified from FUČEK et al., 2014) and a bathymetry map of the Lošinj Channel with core locations. Lithostratigraphic units shown on the map: CR-Upper Hauterivian to Barremi- an Cres limestones, dolomites, stromatolites, breccias and emerged surface alterations; KA- Aptian Kanfanar limestones; PO- Upper Aptian- Lower Albian Porozina breccia and limestones; CN- Albian Crna limestones with emersion breccias; HR- Upper Albian Hrasta dolomites; SIS- Upper Albian-Lower Cenomanian alteration of Sis dolomites and limestones with relict stromatolites, breccia and bauxite infillings; VR- Lower Cenomanian Vrana limestones; BE- Lower to Middle Cenomanian Belej pelagic limestones; NI- Cenomanian Niska limestones; SD- Upper Cenomanian to Turonian Sveti Duh pelagic limestones; GH- Turonian to Coniacian Gornji Humac limestones (FUČEK et al., 2014). Table 1. Main characteristics of the investigated environments and collected sediment cores. Core location Environment Core Core length (cm) Depth at the coring location (m) The lowest sill elevation (m) Distance to the sea (m) Area (km2) Jaz embayment LK-2 150 0.29 -0.5 — 0.029 Sonte embayment LK-3 371 5 -3 — 0.23 Marinska marine pond LK-5 35.5 0.15 1.1 50 0.005 Arcij marine pond LK-6 46.5 0.3 0.3 92 0.018 Podbrajde marine pond LK-7 34 0.15 0.7 136 0.03 G eo lo gi a C ro at ic a Geologia Croatica 72/122 teorological station in Mali Lošinj on the Lošinj Island indicate a mean summer air temperature of 23.1⁰C, with a maximum of 37.4⁰C occurring in August. During the winter, the temperature decreases significantly and mean air temperature reaches 8.3⁰C. The lowest measured air temperature in Mali Lošinj was –4.4⁰C (ZANINOVIĆ, 2008). Relatively high amounts of rainfall have been recorded in the area, with mean annual precipitation of ap- proximately 930.5 mm and the highest precipitation rates in the autumn (GAJIĆ-ČAPKA et al., 2008). The human presence on Cres Island is documented by nu- merous archaeological sites (REGAN & NADILO, 2010; DO- NEUS et al., 2017). The channel that separates islands of Cres and Lošinj in the Osor village has been dug artificially and today has a strong impact on water circulation in the Lošinj Channel, with currents causing deepening of the area south of Osor (DO- NEUS et al., 2017). 3. MATERIALS AND METHODS Short sediment cores (up to 45.5 cm long) were collected in the Marinska, Arcij and Podbrajde shallow marine ponds, by inser- ting a plastic pipe by hand into the sediment. Sampling was con- ducted in September 2015. In total, 3 cores were extracted (LK-5, LK-6 and LK-7) and subsampled in 1 cm sections in the field us- ing the core extruder (Tab. 1). Longer sediment cores (up to 371 cm long) from the Jaz and Sonte embayments were collected us- ing a piston corer and coring platform in April 2014 (Tab. 1). De- tailed subsampling of piston cores LK-2 and LK-3 was conducted after splitting the cores lengthwise. Additionally, physical and chemical water parameters such as conductivity, temperature, pH and dissolved oxygen content were determined at each coring lo- cation using a portable multiparameter Multi 3430 WTW probe. Five mollusc samples from sediment cores LK-2 and LK-3 were dated by radiocarbon dating method (AMS 14C) in order to establish core chronology and to determine the timing of palaeo- environmental changes in the present-day Jaz and Sonte embay- ments. Analyses have been conducted at Beta Analytics Labora- tory in USA. The radiocarbon data was corrected for the marine reservoir effect determined for the Adriatic Sea (FAIVRE et al., 2015). Grain-size was measured using a laser diffractometer Shi- madzu SALD-2300. Selected samples were treated with 30% hy- drogen peroxide (H2O2) in order to remove organic matter. Af- terwards, samples were centrifuged, decanted and resuspended in distilled water prior to the analysis. In total, grain-size was determined on 6 samples from sediment cores LK-5 and LK-7, 4 samples from core LK-6, while 25 and 73 samples were ana- lysed from sediment cores LK-2 and LK-3, respectively. Statisti- cal analysis of the grain-size results was conducted using the GRADISTAT software (BLOTT & PYE, 2001) and sediments were classified according to FOLK & WARD (1957). The bulk mineralogical composition of selected samples, as well as their clay mineralogy, was determined using a PANalyti- cal X’Pert Powder X-ray diffractometer. For the measurements, the diffractometer was set at 45 kV and 40 mA, with a step size of 0.02⁰ 2Ө. Different phases present in the samples were identi- fied following MOORE & REYNOLDS (1997). The clay fraction was analysed by mounting oriented aggregates on glass slides, after the removal of carbonates (where needed), using a buffered sodium acetate (NaOAc) solution. Oriented samples were scanned, air-dried, ethylene-glycolated and analysed after being heated to 400°C and 550°C. Core tops (1 cm thick) of the short sediment cores from ma- rine ponds (LK-5, LK-6 and LK-7) were used for micropalaeon- tological analysis. Samples were treated with rose Bengal stain and 70% ethanol in the field and left for 14 days before being washed, following the procedure described by the FOBIMO group (SCHÖNFELD et al., 2012). Piston cores LK-2 and LK-3 from the Jaz and Sonte embayments were analysed in more de- tail. Foraminiferal analysis on these cores focused on the first cm of each core and intervals where geochemical, sedimentological and mineralogical data indicated significant shifts. These samples were not treated with rose Bengal stain. For determination of the total foraminiferal assemblages (stained+empty tests) selected sediment samples were washed over a 63 µm sieve in the laboratory in order to remove silt and clay particles. According to SCHÖNFELD et al. (2012) >63 µm fraction is appropriate for foraminiferal analyses in palaeoenvi- ronmental studies. Each sample was divided by microsplitter and approximately 300 specimens were picked. In the samples where the total number of foraminifera specimens was less than 300, the whole sample was examined and counted. Genera and spe- cies were recognized following the available literature and clas- sifications by CIMERMAN & LANGER (1991), SGARRELLA & MONCHARMONT ZEI (1993) and LOEBLICH & TAPPAN (1987). Calculation of the species richness, Shannon-Wiener in- dex, Fisher α index, Dominance, Evenness and Equitability was conducted using the PAST software (HAMMER et al., 2001). Cluster analysis of the total foraminiferal assemblages was per- formed using STATISTICA 10 software with Ward’s method and Euclidean distances (STATSOFT, 2011). Scanning electron mi- croscope (SEM) images of the common agglutinated and calcar- eous taxa observed in the samples were obtained using the Jeol 35 CF scanning electron microscope, while the chemical compo- sition of their tests was determined using the energy dispersive spectroscopy (EDS-Oxford X-ACT) and INCA detection unit. Analyses of the total organic (TOC) and inorganic carbon (TIC) and total nitrogen (N) were performed on 134 samples on a Thermo Fisher Scientific Flash 2000 NC Analyzer. Before anal- ysis, the samples were freeze-dried, finely ground and treated with hydrochloric acid (HCl) for TOC measurements (TUNG & TANNER, 2003). Calculation of TIC is based on the difference between total carbon (TC) (untreated samples) and TOC (samples treated with HCl). C/N ratio was calculated from TOC and N measurements. Elemental analysis was carried out on ground samples using Inductively Coupled Plasma-Mass Spectrometry (ICP-MS) in the ACME laboratory, Canada. Geochemical data was analysed us- ing multivariate statistical techniques. Discriminant function analysis (DFA) included a selection of geochemical compositions (TOC, TIC, N, Ca, Mg, Fe, K, Al, P, S, Cu, Pb and Mo) and a sin- gle ratio (C/N). Results of the geochemical analysis represent a typical example of compositional data (CoDa) where correlations between relative elemental abundances may not be unequivocal in the absence of any other information or assumptions (LOVELL et al., 2015). A detailed description of CoDa analysis is reported elsewhere (PEH & KOVAČEVIĆ GALOVIĆ, 2014; PEH & KO- VAČEVIĆ GALOVIĆ, 2016; GALOVIĆ & PEH, 2016; ŠORŠA et al., 2018), with sample references to the original explanations from the Research Group on CoDa Analysis (Girona). Discriminant function analysis (DFA) is a traditional multi- variate statistical technique which is particularly useful in build- ing the predictive model for the two- or multiple-group discrim- ination based on the suite of independent (predictor) variables. It G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 23 is commonly exercised in geo- and environmental sciences when geological logic calls for the use of some autonomous criterion with regards to the variables in the analysed dataset, such as, in this case, the multi-proxy sediment core data analysis. Objectives and principles of DFA are described comprehensively in many statistical textbooks (e.g., DAVIS, 1973; DAVIS, 1986; DILLON & GOLDSTEIN, 1984; ROCK, 1988; REIMANN et al., 2008). Geochemical data were processed using the statistical software package of STATISTICA 10 (STATSOFT, 2011) in the spirit of the CoDa analysis. 4. RESULTS 4.1. Physical and chemical water parameters The investigated environments showed variability of the mea- sured physical and chemical water parameters. Table 2. shows conductivity (Ec), pH, temperature (t) and dissolved oxygen (O2) concentrations. The Ec measurements reveal significant differen- ces, with the lowest Ec values in the Marinska marine pond (11.1 mS/cm) and the highest in the Podbrajde marine pond (56.8 mS/ cm). The pH ranged from 8.24 (Sonte embayment) to 9.07 (Pod- brajde marine pond). Measured O2 concentrations varied from 9.11 mg/l in the Sonte embayment up to 15.22 mg/l in the Arcij marine pond. The highest temperature of 28.1⁰C was determined in the Marinska pond. 4.2. Sediment core analysis Since the cores from marine ponds (LK-5, LK-6 and LK-7) are short (up to 45.5 cm) and analysis of the foraminiferal assem- blages focused only on the core tops, we did not section them into distinct units (Figs. 2 to 4). Based on the sediment characteristics such as grain-size, TOC, TIC and N content, and the geochemis- try of selected major and trace elements several units were dif- Table 2. Measured water parameters in the investigated environments. Core location Core Date of measurement Ec (mS/cm) pH O2 (mg/l) Temperature (⁰C) Jaz LK-2 09/09/2015 56 8.39 13.33 23 Sonte LK-3 09/09/2015 55.5 8.24 9.11 21.9 Marinska LK-5 10/09/2015 11.1 8.36 15.12 28.1 Arcij LK-6 10/09/2015 49.1 8.75 15.22 22.7 Podbrajde LK-7 09/09/2015 56.8 9.07 14.73 23.9 Figure 2. Downcore variations of sedimentological and geochemical parameters in the sediment core LK-5 collected in the Marinska marine pond. Figure 3. Downcore variations of sedimentological and geochemical parameters in the sediment core LK-6 collected in the Arcij marine pond. G eo lo gi a C ro at ic a Geologia Croatica 72/124 ferentiated in the longer sediment cores LK-2 and LK-3 from the Jaz and Sonte embayments, respectively (Figs. 5 and 6). In the LK-2 core two different units were recognized: 1. Unit LK-2-1: 150–60 cm 2. Unit LK-2-2: 60–0 cm The LK-3 core can be divided into four distinct units: 1. Unit LK-3-1: 371–330 cm 2. Unit LK-3-2: 330–260 cm 3. Unit LK-3-3: 260–50 cm 4. Unit LK-3-4: 50–0 cm The main features of the differentiated units are emphasized below. 4.2.1. Core chronology The radiocarbon data obtained from the macrofossils of the pis- ton cores LK-2 and LK-3 is shown in Table 3. The sediment se- quence in both cores is of Holocene age and spans >6610 years in core LK-3 and >711 years in core LK-2. Age reversal has been found in sediment core LK-3, with the result at the core depth of 354 cm being younger than the samples at 252 cm and 217 cm. Due to the fact that results at 252 and 217 cm have been obtained on single mollusc shells each and the result at 354 cm has been obtained on mixed shells of gastropods and bivalves, the former are thought to be more reliable. Therefore, the result at 354 cm has been discarded (Tab. 3). 4.2.2. Grain size analysis Grain-size analysis on 110 samples from all sediment cores re- vealed variations in the grain-size both between cores and within particular cores (Figs. 2 to 6, Tab. 4). Core tops are predominantly composed of coarse silt to medium sand. In most cores grain-size slightly decreases downwards with the general predominance of silty material (Figs. 2 to 6). The highest sand abundance has been measured in the core LK-5 (<75%). Generally, a significant amount of silty material (25-85%) has also been deposited, while the clay fraction (0-9%) is subordinate. Core LK-6 is predominantly composed of silt (80- 88%). Core LK-7 also shows a predominance of silty material (70-78%), while the sand (8-20%) and clay (11-14%) fractions are less abundant. Samples from the sediment cores LK-2 and LK-3 have the highest silt content, 41-88% and 40-91%, respectively. Figure 4. Downcore variations of sedimentological and geochemical parameters in the sediment core LK-7 collected in the Podbrajde marine pond. Figure 5. Downcore variations of sedimentological and geochemical parameters in the sediment core LK-2 collected in the Jaz embayment. G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 25 4.2.3. Mineralogical analysis Bulk mineralogical analysis of sediment core LK-5 indicates the predominance of calcite and quartz, while aragonite is also abun- dant. Halite, Mg calcite, aragonite, gypsum, quartz, muscovite/ illite and pyrite are present in sediment core LK-6. Sediment core LK-7 is characterized by the occurrence of halite, quartz, muscovite/illite and calcite. In the sediment cores LK-2 and LK- 3, quartz is the dominant mineral phase, while the calcite pre- sence is variable downcore. In the basal part of the LK-2 core quartz, muscovite/illite and kaolinite are abundant (unit LK-2-1). The upper part of the LK-2 core (unit LK-2-2) is characterized by calcite, Mg-calcite, aragonite and halite. Muscovite/illite and plagioclase are present throughout the LK-2 core. The lowermost part of the core LK-3 (unit LK-3-1) shows the presence of quartz, muscovite/illite, chlorite and kaolinite. Calcite and Mg-calcite predominate in the upper part of the core (units LK-3-2, LK-3-3 and LK-3-4). Aragonite, dolomite, halite, plagioclase, muscovite/ illite and kaolinite are less abundant. The presence of halite in all samples is a consequence of its crystallization from the pore water after sediment drying. The same clay minerals (chlorite, illite and kaolinite) characterize all the analysed cores. The only exception is the presence of Mg clay mineral sepiolite in the sedi- ment core LK-5. 4.2.4. Foraminiferal analysis Overall, 87 different species were identified in the total forami- niferal assemblages (all cores). Samples from cores LK-5, LK-6 and LK-7 were less diverse and encompass 13 species. In the samples from the sediment cores LK-2 and LK-3, 81 foraminife- ral species were determined. One sample (LK-2-1, 67-68 cm) did not contain foraminifera, while in the samples from the basal part of LK-3 core (unit LK-3-1) and from LK-7 core foraminifera spec- imens were scarce and poorly preserved. The first cm of sediment core LK-5 includes only aggluti- nated taxa. No live specimens were recognized. Dominant spe- cies are Haplophragmoides canariensis (48%) and Trochammina inflata (41%), while Miliammina fusca and Entzia macrescens are significantly less abundant (Tab. 5; Plate 1). In the LK-6 core top sample Ammonia tepida specimens predominate (97%) (Tab. 5; Plate 1). In total, 37 stained specimens were recognized in this sample, while 6 stained specimens showed morphological abnor- malities, including enlarged chambers and twisted coiling (Plate 1). Only 7 foraminifera specimens were discovered in the first cm of core LK-7 collected in the Podbrajde marine pond (Tab. 5). The lower part of the LK-2 core was barren of foraminifera (unit LK-2-1), while the gradual occurrence of foraminifera spe- cimens was observed at core depth of 62–63 cm. Foraminifera Figure 6. Downcore variations of sedimentological and geochemical parameters in the sediment core LK-3 collected in the Sonte embayment. Table 3. AMS 14C dating results of mollusc shells in sediment cores LK-2 and LK-3. The last result (marked with asterisk) has been discarded. Core Depth (cm) Sample ID Material dated Conventional radiocarbon age (14C BP) Probability (%) Calibrated age (cal BP) LK-2 42 Beta – 387747 bivalve shell 1000 ± 30 50 506–571 44.7 580–651 LK-2 58 Beta – 387748 bivalve shell 1200 ± 30 88 641–782 6.9 564–590 LK-3 94 Beta – 387749 gastropod shell 2510 ± 30 95 1892–2148 LK-3 217 Beta – 387750 bivalve shell 5550 ± 30 95 5713–5940 LK-3 252 Beta – 387751 bivalve shell 6260 ± 30 95 6483–6737 LK-3* 354 Beta – 387752 bivalve and gastropod shell 4000 ± 30 95 3693–3976 G eo lo gi a C ro at ic a Geologia Croatica 72/126 Table 4. Statistical parameters for the physicochemical characterisation of sediment cores. LK-5 LK-6 LK-7 LK-2-1 LK-2-2 LK-3-1 LK-3-2 LK-3-3 LK-3-4 Ca (%) Mean 23.27 12.52 4.72 1.33 8.82 6.19 7.65 19.54 23.73 SD 6.85 6.65 2.39 3.03 2.27 1.90 2.02 2.26 2.36 Min 10.53 5.83 0.56 0.31 3.55 4.85 5.35 11.97 21.46 Max 29.77 21.38 7.88 10.93 11.12 7.53 9.15 22.40 28.67 Mg (%) Mean 0.91 1.28 1.06 0.64 0.78 0.91 1.20 1.08 1.05 SD 0.06 0.19 0.29 0.09 0.16 0.08 0.05 0.09 0.07 Min 0.81 1.09 0.68 0.46 0.63 0.85 1.17 0.92 0.92 Max 1.02 1.68 1.50 0.82 1.05 0.97 1.26 1.26 1.18 Fe (%) Mean 0.93 1.67 2.77 3.65 2.63 2.48 1.83 1.65 1.20 SD 0.31 0.87 1.09 0.73 0.74 0.05 0.10 0.39 0.21 Min 0.63 0.66 1.38 2.28 1.92 2.44 1.73 1.24 0.79 Max 1.52 3.25 4.57 5.22 3.89 2.51 1.92 2.89 1.43 K (%) Mean 0.51 0.59 1.24 1.57 0.99 1.37 0.91 0.65 0.50 SD 0.17 0.24 0.35 0.26 0.27 0.12 0.06 0.16 0.10 Min 0.22 0.33 0.60 0.93 0.71 1.28 0.86 0.51 0.31 Max 0.75 1.02 1.58 1.96 1.48 1.45 0.98 1.12 0.62 Al (%) Mean 2.05 2.21 4.97 6.84 4.27 6.21 4.14 2.86 2.03 SD 0.69 1.05 1.79 1.29 1.24 0.12 0.44 0.84 0.44 Min 0.80 0.98 1.83 4.21 3.03 6.12 3.73 2.05 1.19 Max 3.07 4.13 7.26 9.25 6.27 6.29 4.61 5.21 2.59 P (%) Mean 0.06 0.04 0.07 0.03 0.02 0.03 0.03 0.01 0.01 SD 0.03 0.01 0.01 0.00 0.00 0.01 0.00 0.00 0.00 Min 0.04 0.02 0.06 0.02 0.01 0.02 0.02 0.01 0.01 Max 0.11 0.05 0.09 0.04 0.03 0.04 0.03 0.02 0.01 S (%) Mean 0.70 2.87 1.06 0.32 1.69 1.85 2.20 1.36 0.85 SD 0.63 1.10 0.82 0.36 0.63 0.78 0.20 0.45 0.25 Min 0.20 1.40 0.10 0.10 1.00 1.30 2.00 0.90 0.30 Max 1.80 4.30 2.40 1.40 3.00 2.40 2.40 2.50 1.10 Cu (mg/kg) Mean 11.15 14.53 22.37 25.41 14.22 24.25 17.43 9.73 7.78 SD 2.44 6.42 2.74 4.65 3.37 2.33 1.85 3.30 1.35 Min 8.70 5.70 17.90 16.10 9.90 22.60 15.60 6.00 5.30 Max 15.80 22.30 26.60 33.20 20.80 25.90 19.30 19.40 9.60 Pb (mg/kg) Mean 22.61 23.41 57.36 28.66 25.63 24.90 16.00 10.81 10.98 SD 8.82 15.15 21.71 4.18 6.53 2.69 1.06 2.60 0.46 Min 13.60 5.80 30.40 19.10 16.10 23.00 15.20 7.90 10.20 Max 39.10 52.10 86.80 35.00 42.00 26.80 17.20 19.20 11.60 Mo (mg/kg) Mean 0.60 11.05 1.76 1.43 16.48 20.85 42.67 23.15 16.12 SD 0.66 4.74 1.18 0.76 7.13 8.27 2.20 4.98 8.62 Min 0.10 4.60 0.60 0.60 7.10 15.00 41.30 15.30 0.70 Max 1.90 18.60 4.70 3.60 33.10 26.70 45.20 38.60 26.60 TOC (%) Mean 5.40 9.58 6.24 0.50 2.14 6.00 13.34 2.51 1.38 SD 7.78 5.49 6.22 0.25 0.59 3.54 3.62 1.26 0.41 Min 0.65 2.76 0.31 0.20 1.17 2.26 8.44 1.18 0.61 Max 22.38 17.72 15.42 1.06 3.28 11.35 21.42 5.22 1.81 TIC (%) Mean 8.24 7.30 2.19 0.36 2.77 1.54 2.48 5.62 7.42 SD 2.02 3.79 1.08 1.01 0.58 0.85 2.12 1.02 0.64 Min 3.07 3.03 0.74 bdl 1.30 0.55 0.05 3.23 6.76 Max 10.34 11.80 4.16 3.56 3.30 2.81 8.52 7.00 8.57 N (%) Mean 0.77 1.39 0.97 0.04 0.16 0.32 0.62 0.18 0.14 SD 0.96 0.49 1.02 0.01 0.06 0.18 0.14 0.06 0.04 Min 0.12 0.90 0.07 0.02 0.08 0.13 0.41 0.10 0.07 Max 2.57 2.13 2.60 0.06 0.29 0.61 0.92 0.30 0.18 C/N Mean 6.22 6.49 6.93 12.77 13.20 18.70 21.50 13.74 9.86 SD 2.01 2.07 1.64 2.67 0.85 1.23 2.97 2.48 1.41 Min 3.49 3.04 4.14 9.46 11.30 17.35 14.74 10.66 7.65 Max 8.78 9.38 9.04 17.25 14.28 20.36 26.17 21.69 13.41 SAND (%) Mean 39.26 9.00 12.14 16.25 22.95 11.82 30.92 28.68 40.75 SD 27.53 6.63 4.41 14.41 17.57 12.96 15.78 12.53 9.89 Min 15.16 0.06 8.25 0.00 3.25 0.02 5.94 2.18 25.53 Max 74.67 14.77 19.53 30.22 55.76 29.91 56.13 50.35 59.45 SILT (%) Mean 56.74 83.82 75.07 70.43 70.67 77.12 63.52 65.87 55.92 SD 25.05 3.59 3.21 10.53 15.63 8.26 13.54 10.93 8.75 Min 25.33 80.18 69.78 61.12 40.81 64.42 42.71 46.76 39.70 Max 84.84 88.37 78.35 86.62 88.23 84.25 84.10 90.81 69.93 CLAY (%) Mean 4.00 7.18 12.79 13.32 6.39 11.07 5.56 5.45 3.33 SD 4.40 3.11 1.28 8.10 2.87 5.28 2.75 2.22 1.47 Min 0.00 4.90 10.68 7.37 3.20 5.67 1.17 1.94 0.85 Max 8.70 11.57 14.17 36.46 12.27 16.79 10.80 11.55 5.40 G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 27 abundances significantly increased at 58–59 cm (unit LK-2-2), with the predominance of A. tepida (39%) (Tab. 5). In the surface sample from this core different Ammonia species predominate (up to 51%), while Elphidium margaritaceum, Bolivina striatula, Haynesina depressula and Elphidium translucens are less abun- dant (Tab. 5, Plate 2). Samples from sediment core LK-3 also indicate the transi- tion from intervals barren of foraminifera (unit LK-3-1) to their significant diversification (unit LK-3-4) (Tab. 5). The predomi- nance of A. tepida (6–46%) and Cribroelphidium gerthi (0–21%) has been observed in all samples from the basal part of the core (unit LK-3-2) (Tab. 5). Miliolids (Quinqueloculina parvula and Figure 7. Cluster dendrogram developed based on the foraminiferal analysis results using Ward’s method and Euclidean distances. Table 5. The relative abundances of the foraminiferal species in sediment cores LK-5, LK-6, LK-7, LK-2 and LK-3. Sample from the LK-2 core interval 62–63 cm corre- sponds to unit LK-2-1, while samples 0–1 cm and 58–59 cm correspond to unit LK-2-2. The LK-3 core samples belong to the following units: 349–350 cm, 340–342 cm – unit LK-3-1; 275–277 cm – unit LK-3-2; 243–245 cm and 230–232 cm – unit LK-3-3; 0–1 cm – unit LK-3-4. Foraminifera (species) LK-5 LK-6 LK-7 LK-2 LK-3 0–1 0–1 0–1 0–1 58–59 62–63 0–1 230–232 243–245 275–277 340–342 349–350 Adelosina carinata-striata 0.0 0.0 0.0 0.4 0.0 0.0 0.4 1.2 2.5 0.3 0.0 0.0 Adelosina cliarensis 0.0 0.0 0.0 0.0 0.0 0.0 0.4 1.8 0.0 0.0 0.0 0.0 Adelosina elegans 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 Adelosina mediterranensis 0.0 0.0 0.0 0.0 0.0 0.0 0.7 0.0 0.0 0.0 0.0 0.0 Ammonia sp. 0.0 0.0 14.3 12.4 1.0 4.0 0.0 0.6 8.8 1.2 0.0 0.0 Ammonia beccarii 0.0 0.3 0.0 0.0 0.0 0.0 0.0 3.9 0.4 6.7 6.1 6.3 Ammonia parkinsoniana 0.0 1.7 0.0 15.7 8.2 4.0 0.7 0.3 3.2 3.9 0.0 12.5 Ammonia tepida 0.0 96.6 14.3 22.6 61.6 68.0 4.7 28.4 27.4 46.4 23.1 43.8 Asterigerinata adriatica 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.5 4.4 12.5 Asterigerinata mamilla 0.0 0.0 0.0 2.2 0.3 0.0 9.4 2.1 1.1 0.0 0.0 0.0 Aubignyna perlucida 0.0 0.0 0.0 0.4 2.0 0.0 0.7 0.3 0.4 0.3 0.4 0.0 Bolivina sp.1 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.9 0.0 0.0 0.0 0.0 Bolivina sp.2 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 0.0 0.0 Bolivina difformis 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 Bolivina pseudoplicata 0.0 0.0 0.0 0.7 0.0 0.0 5.4 0.3 0.0 0.6 0.0 0.0 Bolivina spathulata 0.0 0.0 0.0 0.0 0.0 0.0 1.4 0.0 0.0 0.0 0.0 0.0 Bolivina striatula 0.0 0.0 0.0 4.0 3.3 0.0 0.7 0.0 0.0 0.0 0.0 0.0 Bolivina variabilis 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 1.4 0.0 0.0 0.0 Buccella sp.2 0.0 0.0 0.0 1.1 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Cibicides advenum 0.0 0.0 0.0 1.5 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Cibicides refulgens 0.0 0.0 0.0 0.4 0.0 0.0 1.1 0.0 0.4 0.0 0.9 0.0 Cibicidoides variabilis 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Cornuspira involvens 0.0 0.0 0.0 0.0 0.0 0.0 2.5 0.0 0.0 0.0 0.0 0.0 Cribroelphidium excavatum 0.0 0.3 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Cribroelphidium gerthi 0.0 0.0 0.0 1.8 0.3 0.0 1.8 21.3 8.1 7.6 21.0 6.3 G eo lo gi a C ro at ic a Geologia Croatica 72/128 Foraminifera (species) LK-5 LK-6 LK-7 LK-2 LK-3 0–1 0–1 0–1 0–1 58–59 62–63 0–1 230–232 243–245 275–277 340–342 349–350 Cribromiliolinella sp.1 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 Cribrostomoides subglobosus 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Cycloforina sp. 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 Cycloforina contorta 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.6 0.0 0.0 0.0 0.0 Discorbinella sp. 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 0.0 0.0 Elphidium sp. 0.0 0.0 0.0 0.0 0.3 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Elphidium sp.1 0.0 0.0 0.0 0.0 0.7 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Elphidium sp.2 0.0 0.0 0.0 0.0 0.3 0.0 0.0 0.0 0.0 0.3 0.0 0.0 Elphidium sp.6 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.3 0.4 0.0 Elphidium sp.7 0.0 0.0 0.0 0.0 1.3 4.0 0.0 0.0 0.0 0.0 0.0 0.0 Elphidium aculeatum 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.8 0.0 0.4 0.0 Elphidium advenum subsp. limbatum 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 0.4 0.0 Elphidium cf. advenum 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 0.4 0.9 0.4 0.0 Elphidium crispum 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.7 0.9 0.0 0.0 Elphidium fichtelianum 0.0 0.0 0.0 0.0 1.0 0.0 0.4 6.9 1.1 7.0 5.7 0.0 Elphidium macellum 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.3 0.0 Elphidium maioricensis 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 Elphidium margaritaceum 0.0 0.0 0.0 9.5 0.3 8.0 0.7 0.0 0.4 0.3 0.0 0.0 Elphidium translucens 0.0 0.0 0.0 6.6 1.6 4.0 2.5 2.4 11.6 5.5 3.5 0.0 Entzia macrescens 2.1 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Fissurina lucida 0.0 0.0 0.0 1.1 0.0 0.0 2.2 0.0 0.0 0.0 0.0 0.0 Fursenkoina subacuta 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 0.0 0.0 0.0 0.0 Gavelinopsis praegeri 0.0 0.0 0.0 0.7 0.0 0.0 10.5 0.0 0.0 0.0 0.0 0.0 Haplophragmoides sp. 1 6.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Haplophragmoides sp. 2 1.2 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Haplophragmoides canariensis 48.8 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Haynesina sp.1 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.7 0.0 Haynesina depressula 0.0 0.0 0.0 8.4 5.9 0.0 11.9 2.4 0.7 2.4 19.7 18.8 Haynesina germanica 0.0 0.0 0.0 3.6 0.0 0.0 23.1 0.6 0.7 3.3 0.0 0.0 Miliammina fusca 0.3 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Miliolinella sp. 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.7 0.0 0.0 0.0 Miliolinella elongata 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.8 0.3 0.0 0.0 Miliolinella subrotunda 0.0 0.0 0.0 0.0 0.0 0.0 1.8 2.1 1.1 0.0 0.0 0.0 Neoconorbina terquemi 0.0 0.0 0.0 0.4 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.0 Peneroplis pertusus 0.0 0.0 0.0 0.0 0.0 0.0 0.7 0.3 0.0 0.3 0.0 0.0 Peneroplis planatus 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.3 0.0 0.0 0.0 0.0 Porosononion sp.1 0.0 0.0 0.0 0.7 0.0 0.0 0.0 5.1 0.0 2.1 0.0 0.0 Porosononion sp.2 0.0 0.0 0.0 0.0 0.0 0.0 0.7 3.0 0.0 0.3 7.0 0.0 Pseudotriloculina lecalvezae 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 Quinqueloculina bosciana 0.0 0.0 0.0 0.4 0.3 0.0 0.7 0.9 0.0 0.3 0.0 0.0 Quinqueloculina irregularis 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.0 Quinqueloculina jugosa 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.5 1.1 0.0 0.0 0.0 Quinqueloculina laevigata 0.0 0.0 0.0 0.0 0.0 0.0 0.7 3.0 1.1 0.0 0.0 0.0 Quinqueloculina parvula 0.0 0.0 0.0 0.0 0.0 4.0 0.0 0.3 7.4 0.0 0.0 0.0 Quinqueloculina schlumbergeri 0.0 0.0 0.0 0.0 0.0 0.0 1.4 0.0 0.7 0.0 0.0 0.0 Quinqueloculina seminula 0.0 0.3 0.0 0.0 2.3 4.0 3.6 0.3 6.0 0.9 0.0 0.0 Reussella spinulosa 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.0 Rosalina bradyi 0.0 0.0 0.0 0.7 0.7 0.0 0.0 2.4 1.1 1.8 1.7 0.0 Rosalina floridensis 0.0 0.9 14.3 0.7 0.0 0.0 1.8 1.2 0.0 0.0 0.0 0.0 Rosalina macropora 0.0 0.0 0.0 0.4 0.3 0.0 1.1 1.2 0.0 0.0 0.0 0.0 Sejunctella sp. 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.3 0.4 0.0 0.0 0.0 Sigmavirgulina sp.1 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 0.0 0.0 Sigmoilina costata 0.0 0.0 0.0 1.1 0.0 0.0 1.1 0.3 1.8 1.2 0.0 0.0 Siphonoaperta sp. 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 0.0 0.0 Siphonaperta aspera 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.3 0.0 0.0 Spiroloculina sp. 0.0 0.0 0.0 0.0 0.0 0.0 0.4 1.2 0.0 0.0 0.0 0.0 Spiroloculina cymbium 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 0.0 0.0 Triloculina adriatica 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.2 0.0 0.6 0.0 0.0 Table 5. Continued. G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 29 Quinqueloculina seminula) become especially abundant at core depths of 243–245 cm (unit LK-3-3). The sample from the first cm of the core is characterized by the highest abundance of Hay- nesina germanica (23%), H. depressula (12%) and Gavelinopsis praegeri (10%) (unit LK-3-4) (Tab. 5, Plate 2). Calculation of the relative species abundances (Tab. 5) re- vealed that 49 species were abundant at more than 1% in at least one analysed sample, with only 9 species abundant >1% in the LK-5, LK-6 and LK-7 core top samples. Different locations and core depths yielded variablity in the number of species in the sam- ples, from 7 (LK-6 core top) to 41 (LK-3 core top). Samples from cores LK-5, LK-6 and LK-7 were generally less diverse in com- parison to samples from cores LK-2 and LK-3. Species richness decreased downcore in the sediment cores LK-2 and LK-3. The same trend was observed in the Fisher α index and Shannon-Wie- ner index, while Dominance shows the opposite trend. All calcu- lated diversity indices and their variability is shown in Table 5. Cluster analysis indicated the existence of two clusters (Fig. 7). Cluster 1 encompasses two subclusters (1.1 and 1.2). Subclus- ter 1.1 includes LK-2 and LK-3 core top samples, and several sam- ples from the middle part of LK-3 core (230–232 cm, 243–245 cm and 340–342 cm). Samples from cores LK-5 and LK-7 were grouped together in subcluster 1.2. Cluster 2 consists of samples from LK-2 core (62–63 cm and 58–59 cm), basal part of LK-3 core (349–350 cm and 275–277 cm) and LK-6 core top sample. Altogether, 52 SEM-EDS analysis were conducted on selec- ted grains of agglutinated taxa from the LK-5 core, while several analysis were performed on calcareous taxa from the first cm of LK-5 and LK-6 sediment cores. The mineralogical composition of agglutinated taxa is variable. Quartz, amphibole, mica (biotite and muscovite) and feldspars (plagioclase and potassium feld- spars) are common mineral phases found in agglutinated forami- niferal tests (Fig. 8). 4.2.5. Geochemical analysis The result of the geochemical analyses is summarized in Table 4. and Figures 2 to 6. The highest TOC content has been measured in the cores LK-5 (22.38%), LK-6 (17.72%) and LK-7 (15.42%) and samples from the basal part of the sediment core LK-3 (units LK-3-2 and LK-3-1; 21.42% and 11.35%, respectively) (Fig. 9I). The highest TIC content has been determined in cores LK-5 (10.34%) and LK-6 (11.8%) and in the samples from the topmost part of the core LK-3 (unit LK-3-4; 8.57%) (Fig. 9H). The N was most abundant in the cores LK-5 (2.57%), LK-6 (2.13%) and LK-7 (2.6%), with somewhat lower abundances in the basal part of the LK-3 core (units LK-3-2 and LK-3-1; 0.92% and 0.61%, respec- tively) (Fig.9G). Most of the samples from cores LK-5, LK-6 and LK-7 were characterized by very low C/N ratios (<<12), while the highest values of C/N ratio (>12) were observed in the samples from the basal part of LK-3 (units LK-3-2 and LK-3-1) (Tab. 4). The highest calcium (Ca) concentrations were measured in LK-5 core (29.77%), while the lowest concentrations were ob- served in LK-2 core (unit LK-2-1; 7.88%). Magnesium (Mg) has the highest concentrations in core LK-6 (1.68%), while terrige- nous elements (Fe, K, Al) are the most abundant in the topmost part of the LK-2 core (unit LK-2-1; e.g., Fe up to 5.22%) (Fig. 9B). Samples from the LK-5 core have the highest P concentrations (0.11%). Furthermore, the highest Pb concentrations were measu- red in core LK-7 from Podbrajde pond (86.8 mg/kg). Molybde- num (Mo) proved to be abundant in most cores (0.1–45.2 mg/kg), with the highest concentrations measured in the LK-3 core (unit LK-3-2) (Fig. 9D). Sulfur (S) concentrations vary between 0.1% and 4.3%. The highest S concentrations were found in core LK-6 (4.3%) (Tab. 4; Fig. 9E). 4.2.6. Discriminant function analysis (DFA) of the geochemical data Discriminant function analysis (DFA) of geochemical data is summarized in the composite Table 6., describing the geochemi- cal exploratory model for the sediment cores. The table comprises both the multivariate test for the overall significance of discrimi- nation and the test of residual roots (discriminant functions). The Wilks’ k statistical test is commonly used with the purpose of validating the probability level (p < 0.05) required to proceed safely with computing discriminant functions (DFs). It is used to select both the statistically significant functions as well as ex- plaining the maximum of the within-group variation. The scat- terplots of variable loadings and group centroids are constructed for the first three DFs that explain the greatest proportion of the between-group variance, almost 92% (Fig. 10). In the computed model the first discriminant function DF1 plays by far the grea- test role in discrimination between the groups, accounting for more than 60% of the total variance (Tab. 6). In the context of the environmental conditions studied, this multivariate method is particularly helpful in chasing the major sources of between-group differences originating from dissemi- nation of the chemical elements in the sediment cores. In com- bining the cores from marine ponds (LK-5, LK-6 and LK-7) and Foraminifera (species) LK-5 LK-6 LK-7 LK-2 LK-3 0–1 0–1 0–1 0–1 58–59 62–63 0–1 230–232 243–245 275–277 340–342 349–350 Triloculina marioni 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0 Triloculina oblonga 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.3 2.8 0.3 0.0 0.0 Trochammina inflata 41.3 0.0 42.9 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 unidentified 0.3 0.0 14.3 0.4 8.2 0.0 2.5 0.3 1.8 0.6 0.9 0.0 Number of specimens (N) 334 352 7 274 305 25 277 334 285 330 229 16 Number of live specimens (NL) 37 Number of species (S) 7 6 32 21 39 38 38 35 20 Dominance (D) 0.413 0.933 0.116 0.400 0.098 0.141 0.116 0.238 0.152 Simpson (1-D) 0.587 0.067 0.884 0.601 0.902 0.859 0.884 0.762 0.848 Shannon-Wiener (H) 1.053 0.194 2.559 1.573 2.849 2.609 2.734 2.235 2.207 Evenness (e^H/S) 0.409 0.202 0.404 0.230 0.443 0.358 0.405 0.267 0.454 Equitability (J) 0.541 0.108 0.738 0.517 0.778 0.717 0.752 0.629 0.737 Fisher α 1.252 1.027 9.393 5.116 12.4 11.04 11.78 9.90 5.27 Table 5. Continued. G eo lo gi a C ro at ic a Geologia Croatica 72/130 Table 6. Multivariate test for the overall significance of discrimination and tests of residual roots. No. of variables 14 Wilks’ lambda 0.00001 Approximate F ratio 24,968 Degrees of freedom [112; 642] p-level <0.0000 DF Eigen Eigen (%) Canon. Wilks’ Chi2 df p- value R l level 1 42,984 60.43 0.989 0.000 1170.3 112 0.000 2 17,966 25.26 0.973 0.000 793.8 91 0.000 3 4,388 6.17 0.902 0.007 501.0 72 0.000 4 2,359 3.32 0.838 0.035 333.4 55 0.000 5 1,988 2.80 0.816 0.118 212.9 40 0.000 6 1,131 1.59 0.729 0.352 103.9 27 0.000 7 0.211 0.30 0.418 0.750 28.7 16 0.026 8 0.101 0.14 0.303 0.908 9.6 7 0.214 Figure 8. 1-3 Potassium feldspar mineral grain recognized in Haplophragmoides canariensis specimen using the SEM-EDS method; 4-6 Plagioclase mineral grain recognized in Trochammina inflata specimen using the SEM-EDS method. G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 31 distinguished sediment core units from LK-2 and LK-3 cores, nine groups of cored sediments were created to provide the most effective rapport between their geochemical signature and im- mediate sedimentary environment. As seen from the scatterplot of variable loadings (Fig. 10), DF1 is highly bipolar separating principally the LK-5 and LK-7 groups from most of the LK-3 sediment core groups (LK-3-2, LK- 3-3 and LK-3-4) while other groups remain to a great extent poorly differentiated sticking closer to the point of the axis inter- section. The rationale for this separation is founded primarily in the negative association between P and Mo. Geochemically it can be understood as the LK-5 and LK-7 cores are relatively enriched in P and depleted in Mo in comparison to the upper three LK-3 units. The groups positioned in the middle reflect the average composition of all the investigated core units – a “mixed” geo- chemical signature. DF2, comprising over 25% of the total variance of geochemi- cal data is also bipolar and can be interpreted as reflecting a nega- tive correlation between the element suite including Cu, Pb, K, Al, Fe against another set of elements led by TIC, Ca, N. This pattern is a geochemical signature dividing the LK-2-1 from LK-6 groups on the basis of the clay/carbonate (inorganic carbon) back- ground. Despite making only a minor contribution to the overall model significance (6%), DF3 as a monopolar function clearly highlights the LK-3-1 and LK-3-2 groups based on their affinity with C/N with a slight TOC association (Fig. 10). 5. DISCUSSION 5.1. Foraminiferal assemblages and geochemical characterization of the surface sediments from the marine ponds on Cres Island Studies of the foraminiferal assemblages or sediment geochemi- stry in the marginal marine environments along the eastern Adri- atic coast have been relatively scarce (MIHELČIĆ et al., 1996; VANIČEK et al., 2000; CUCULIĆ et al., 2009; MLAKAR et al., 2015; FELJA et al., 2015; SHAW et al., 2016; SONDI et al., 2017). The focus of many studies worldwide, including the western coast of the Adriatic Sea, has been determination of the foraminiferal fauna inhabiting these transitional environments (e.g., SERAN- DREI-BARBERO et al., 1999; CARBONI et al., 2009; KEMP et al., 2013; STÉPHAN et al., 2014; MILKER et al., 2015). Different environmental parameters and sediment geochemistry are con- sidered to be important for foraminiferal distribution (DEBENAY et al., 2001; DEBENAY & GUILLOU, 2002; FRONTALINI et al., 2011a; FRONTALINI et al., 2013). The main sediment and water characteristics of the Marinska, Arcij and Podbrajde marine ponds investigated here are shown in Table 7. At the sampling time, water in the Marinska pond was brackish with a temperature above 28⁰C and oxygen saturation of 15.12 mg/l. Sediments in this marine pond are characterized by their high N and P contents (Figs. 9F and 9G). A high P con- centration in the surface sediments probably occurs due to delay in mineralisation of recently settled organic material (HOLTAN Figure 9. Box and whisker plots of sediment core data. The squares in the each box represent median values. The 25th and 75th percentile are the bottom and the top of the each box, respectively. Whisker ends are the non-outlier minimum and maximum values. G eo lo gi a C ro at ic a Geologia Croatica 72/132 et al., 1988). A source of these elements could also be input of bird faeces (guano) into the ponds (BATANERO et al., 2017), considering that the investigated areas are habitats for migratory marsh birds (most commonly mallard- Anas platyrhynchos), as well as woodcock (Scolopax rusticiola) and seagulls (KRALJ, pers.comm.). The mallard and woodcock are also frequently hunted in the area. High nutrient concentrations enabled the de- velopment of environmental conditions that facilitated accumu- lation of organic matter in the sediments (Figs. 9F and 9G). A low C/N ratio implies an algal origin of the preserved organic matter (MEYERS, 1994; MEYERS, 2003; LAMB et al., 2006). The TIC also proved to be an important sediment component (Tab. 5, Fig. 9H). The Mo and S concentrations in the Marinska pond sedi- ments are low (Figs. 9D and 10E; Fig. 11A). Preserved Mo is not an indicator of anoxic environmental conditions and can be linked to the input of terrestrial soil material based on the high correlation of Mo with Al (Fig. 11C) (GOLDBERG et al., 1996). Terra rossa topsoils from sites in Dalmatia have a mean concen- tration of 3 mg/kg Mo (MIKO et al., 2007). Only agglutinated taxa typical of intertidal environments are present in the Marinska marine pond. The species H. canariensis and T. inflata predominate, while E. macrescens and M. fusca are significantly less abundant. Different species of the genus Hap- lophragmoides have already been recognized in the Adriatic Sea (CIMERMAN & LANGER, 1991; SERANDREI BARBERO et al., 2004; SHAW et al., 2016), while T. inflata appears to be fre- quent in the marginal marine environments along the Croatian coast of the Adriatic Sea (FELJA et al., 2015; SHAW et al., 2016). Generally, this species has been reported from many restricted, brackish water environments in the Mediterranean region (SE- RANDREI BARBERO et al., 1999; SERANDREI BARBERO et al., 2004; DEBENAY & GUILLOU, 2002; FRONTALINI et Table 7. The main sediment and water characteristics of the Marinska, Arcij and Podbrajde marine ponds. MARINE POND WATER WATER COLUMN DEPTH NUTRIENTS AMOUNT ORGANIC MATTER Mo MAIN FORAMINIFERAL ASSEMBLAGES Marinska marine deeper (no drying out) high high terrestrial Ammonia tepida Arcij brackish very shallow high high redox conditions Haplophragmoides canariensis Podbrajde marine shallow (drying out phases possible only at the margins of the pond) high high terrestrial scarce but present Figure 10. Comparison between variables and groups in the clr-transformed data discriminant function model (DFM): the scatterplots of variable loadings and discriminant scores (samples) in the reduced discriminant space of the first three discriminant functions (DF1–DF2 and DF1–DF3). G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 33 al., 2011a) and elsewhere (LIDZ & ROSE, 1989; SEN GUPTA et al., 2009). Recognized agglutinated foraminiferal fauna typically occur in the zone between mean sea level and mean high water level in salt-marsh areas of the Adriatic Sea (SERANDREI BAR- BERO et al., 1999; SHAW et al., 2016), indicating that in the in- vestigated environment tidal influence is important. The Marin- ska marine pond is located 50 m from the sea and the possible tidal influence could be through karst features. Although fo- raminiferal species richness in the Marinska pond is low, recog- nized species seem to be well adapted to the restricted environ- mental conditions due to their abundance. However, a significant number of damaged tests were also observed, possibly indicating conditions unsuitable for their preservation (Plate 1). DEBENAY (2001) observed the presence of T. inflata in marshes with vari- able salinity and TOC content, while DEBENAY & GUILLOU (2002) reported the preference of this species for muddy sedi- ments in microtidal Mediterranean environments. However, our results proved that although TOC content was high, this species occurred in the brackish water environment with high percenta- ges of sand (up to 75%). Grain-size distribution, as well as the mineralogical composition of the sediment, has important impli- cations for agglutinated taxa (ALLEN et al., 1999; ARMYNOT DU CHÂTELET et al., 2008; ARMYNOT DU CHÂTELET et al., 2013). SEM-EDS analysis showed that identified agglutinated foraminifera from the Marinska pond used variable mineral grains for building their tests (quartz, amphibole, mica and feld- spars) (Fig. 8). Some mineral grains were not recognized in the bulk mineralogical composition of the sediment, probably due to their low abundances. This indicates the preference of aggluti- nated taxa for specific mineral grains. ALLEN et al. (1999), AR- MYNOT DU CHÂTELET et al. (2008), MAKLED & LANGER (2010) and ARMYNOT DU CHÂTELET et al. (2013) in their studies have determined that some species preferentially select certain mineral grains from their surroundings, while significant differences among species also exist. Mineral analysis also revealed the presence of the clay mine- ral sepiolite, usually found in restricted environments, ponds or shallow brackish lakes with high evaporation rates (ORDÓÑEZ et al., 1991; VELDE, 1995; MEUNIER, 2003; BUSTILLO & ALONSO-ZARZA, 2007). Direct precipitation of sepiolite oc- curs from solutions with abundant Mg and Si (MAYAYO et al., 1998) in the high pH environments (STARKEY & BLACKMON, 1984). BUSTILLO & ALONSO-ZARZA (2007) indicate that se- piolite can be formed by the transformation of illites or smectites in a vadose alkaline environment with Mg rich groundwater ori- ginating from dolomitic aquifers. The presence of sepiolite im- plies the significant impact of climate conditions (precipitation, evaporation) on the water level in the Marinska pond that has been developed in a generally dolomitic lithological setting. Sea- sonal climatic variability with periods of high evaporation from the marine pond, could have enabled the development of envi- ronmental conditions that favoured the precipitation of sepiolite in the Marinska pond. Conductivity (Ec) and O2 measurements in the water in the Arcij marine pond indicate the existence of an oxygenated en- Figure 11. Scatterplots of A) Mo (mg/kg) against S (%) B) N (%) against P (%), C) Mo (mg/kg) against Al (%), D) TOC (%) against C/N. G eo lo gi a C ro at ic a Geologia Croatica 72/134 closed marine environment. Regardless of the larger distance of this marine pond from the sea (92 m), a stronger seepage of sea water probably occurs due to the well-developed karstification and fissures system of the ridge separating the pond from the sea. A silty surface sediment is enriched with TOC (7.58%) and TIC (8.29%), while the organic matter is predominantly of algal ori- gin (C/N<12; MEYERS, 1994; MEYERS, 2003; LAMB et al., 2006). Similarly to the Marinska marine pond, the primary pro- ductivity indicators (N and P) are abundant. The Mo and S con- centrations in the sediment are higher in comparison to the other marine ponds, causing reducing sediment conditions and thus further facilitating the preservation of organic matter. In the Ar- cij pond, the source of Mo could be different to that of the Ma- rinska pond (Fig. 11C). In many papers (PEDERSEN, 1989; CRU- SIUS et al., 1996; CALVERT & PEDERSEN, 1993; ALGEO & LYONS, 2006; SCHOLZ et al., 2017) the application of Mo as an indicator of redox conditions was emphasized. It is considered that Mo precipitation often occurs in anoxic and organic matter- rich silled basins (ALGEO & LYONS, 2006). We suggest enrich- ment with Mo in the Arcij pond is a consequence of stagnant bot- tom water and reducing conditions. The S concentrations are also high (Fig. 9E). The presence of hydrogen sulfide (H2S) seems to be important for the uptake of Mo, especially in shallow water environments and non-silled basins (PEDERSEN, 1989; ALGEO & LYONS, 2006; SCHOLZ et al., 2017). This can be applicable to the Arcij pond (Fig. 11A), where pyrite is formed. Established environmental conditions do not seem to be a limiting factor for the presence of foraminifera. The most common species occur- ring in the Arcij pond is A. tepida, with a relative abundance of almost 97% (Tab. 5). This species has been identified in numer- ous shallow water marine environments, restricted marginal ma- rine environments (lagoons, estuaries, salt-marshes) and inland saline pools due to its tolerance to normal, brackish and hyper- saline water conditions (JORISSEN, 1988; DEBENAY, 1990; ALMOGI-LABIN et al., 1992; DEBENAY et al., 2001; DEBE- NAY & GUILLOU, 2002; DEBENAY & GUIRAL, 2006; MUR- RAY, 2006; VIDOVIĆ, 2010; FRONTALINI et al., 2011a). In previously conducted research, the ability of A. tepida to tolerate environmental stress has been emphasized (ALMOGI-LABIN et al., 1992; DEBENAY et al., 2001; DEBENAY & GUILLOU, 2002). Abundance of this species in the organic matter-rich Arcij marine pond further supports this. A significant number of living specimens was observed, implying their adaptation to the envi- ronmental conditions in the investigated marine pond. Ammonia specimens with abnormal test morphology have also been recog- nized, further indicating the existence of environmental stress or possibly genetic or mechanical influences (ALMOGI-LABIN et al., 1992). A relatively small number of living deformed speci- mens (6 specimens; Tab. 4) was observed in the analysed sample, which does not facilitate explanation of the dominant factor caus- ing the stress in the Arcij pond. Oxygen deficiency and nutrient abundance in the sediment could be possible factors. In the Podbrajde marine pond, located 136 m from the sea, only 7 foraminifera specimens have been found in the analysed core top (Tab. 5). This general absence of abundant foraminiferal assemblages, in comparison to the other marine ponds, could be explained by the greater distance of this environment from the sea and a more prominent disconnection from a direct marine influence. However, measured Ec values indicate the existence of normal marine conditions which makes it difficult to explain the lack of rich foraminiferal assemblages. Geochemical sediment analysis revealed similar conditions to those in the previously de- scribed marine ponds, especially the Marinska pond, with nutri- ent enrichment and an algal source of organic matter (MEYERS, 1994; MEYERS, 2003; LAMB et al., 2006) (Tab. 4). The Mo in the Podbrajde marine pond also seems to be of terrestrial origin (Fig. 11C) (GOLDBERG et al., 1996). The only notable difference in the geochemical record, in comparison to the previously de- scribed ponds, is the high Pb concentration (Fig. 9C). Generally, it is considered that elevated concentrations of Cd, Pb, Cu and Zn are a consequence of anthropogenic activities (CLARK, 2001). Sediment enrichment with Pb could also occur due to the spent shot during hunting (MATEO, 2009; MIGANI et al., 2015). The results from ROMANO et al. (2016) imply that metallic Pb from spent shot during hunting is oxidized and dissolved in wetlands leading to its mobilization and redistribution in wetland sedi- ments. MIGANI et al. (2015) came to similar conclusions for la- goons on the northern Adriatic coast. SUOKHRIE et al. (2017) provided an overview of studies related to foraminifera exposed to different pollutants including heavy metals. Most studies indi- cate that high Pb concentrations in marine sediments result in low diversity of fauna and the predominance of opportunistic species, as well as an increase in the abnormalities of foramini- feral tests. FRONTALINI et al. (2015) exposed Ammonia parkin- soniana specimens, cultured in mesocosms, to various concen- trations of Pb in sediments. Specimens showed cytological modifications that might be related to pollutant-induced stress. The elevated concentrations of Pb could possibly inhibit the de- velopment of abundant foraminiferal assemblages within the studied coastal marine pond. If the concentrations of Pb in the studied marine pond have a major influence on the lack of an abundant foraminiferal fauna, then correlation of modern envi- ronments with those of the past (pre-flooding) could be somewhat limited. The presence of foraminifera in environments isolated from a direct marine influence has been attributed to transport by birds (DEBENAY, 1990; ALMOGI-LABIN et al., 1992). The same transport mechanism can explain the foraminiferal presence in the investigated marine ponds. However, seepage through the karstified underground is probably the dominant factor contribu- ting to the foraminiferal dispersal. Sirocco and bora winds, that are common along the eastern Adriatic coast (PANDŽIĆ & LIKSO, 2005; SIGNELL et al., 2010), could also introduce ma- rine fauna into the ponds. 5.2. Palaeo-marine ponds and the palaeoenvironmen- tal evolution of the Jaz and Sonte embayments Differentiated units from sediment cores collected in the sub- merged dolines in the Jaz and Sonte embayments, correspond to different Holocene palaeoenvironments. Foraminiferal analysis was conducted only in intervals were the existence of a transi- tional terrestrial to marine environment was assumed. Further- more, recognized foraminiferal fauna and geochemical data were compared to the data from the Marinska, Podbrajde and Arcij marine ponds in order to possibly detect Holocene analogs of the marginal marine environments that nowadays exist in the coastal zone of Cres Island. Foraminiferal assemblages from the core tops collected in the embayments were also investigated in order to compare typical shallow marine assemblages in the area with the taxa present downcore and in the marine ponds. A similar type of research has already been conducted in the Adriatic Sea in the Venice lagoon (SERANDREI BARBERO et al., 2004). Two distinct intervals were recognized in the sediment core LK-2 collected in the Jaz embayment. The first interval (unit G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 35 LK-2-1), comprising the basal part of the core, implies soil accu- mulation with high metal concentrations (Al, Fe, K, Cu, Pb) (Fig. 10) in the karst depression. The geochemical and mineralogical signature is typical for terra rossa soils developed in carbonate terrains (DURN et al., 1999; MIKO et al., 2001). Foraminiferal absence is a prominent characteristic of this environment, which further supports the palaeoenvironmental interpretation (Figs. 12A and 12B). The abrupt change in the core data (unit LK-2-2) (Fig. 5) was observed at approximately 711 cal BP evidencing an important environmental transition. A significant rise in the Mo and S concentrations (Fig. 5) probably indicates establishment of an oxygen depleted restricted water body (PEDERSEN, 1989; CRUSIUS et al., 1996; CALVERT & PEDERSEN, 1993; ALGEO & LYONS, 2006; SCHOLZ et al., 2017). The high TOC content supports this, while also implying increased primary productivi- ty (Fig. 5). However, it seems that this environment was not as productive as the present-day marine ponds on Cres Island or these differences could be a consequence of diagenesis (Figs. 9F Figure 12. Schematic drawing of the palaeoenvironmental development of the Marinska, Arcij and Podbrajde marine ponds and the Jaz and Sonte embayments at A) approximately 7000 cal BP, B) approximately 6610 cal BP, C) approximately 711 cal BP, D) present. G eo lo gi a C ro at ic a Geologia Croatica 72/136 and 9G; Fig. 11B). The C/N ratio is indicative of a mixed terres- trial and algal organic matter provenance, which also differs in comparison to the present-day marine ponds (Fig. 11D) (MEY- ERS, 1994; MEYERS, 2003; LAMB et al., 2006). At this transi- tion in core LK-2, a more detailed analysis of foraminiferal as- semblages was conducted (Fig. 3). The presence of foraminifera proved that the marine influence in the Jaz embayment begun at approximately 711 cal BP. A poorly diversified assemblage was determined, predominantly composed of numerous specimens of foraminifera typical of the brackish or shallow marine conditions usually established in the marginal marine environments (A. tep- ida, A. parkinsoniana and H. depressula) (MURRAY, 2006; VANIČEK et al., 2000). Differentiated species seem to be well adapted to the reduced oxygen availability in the sediment. The susceptibility of A. tepida and the genus Haynesina to environ- mental stress has been previously determined (ALMOGI-LABIN et al., 1992; DEBENAY et al., 2000; DEBENAY et al., 2001; DE- BENAY & GUILLOU, 2002; VIDOVIĆ et al., 2009). However, A. parkinsoniana is not considered to be a stress-tolerant species (VIDOVIĆ et al., 2014). Cluster analysis enabled the identifica- tion of different core intervals characterized by similar assem- blages (Fig. 7). We consider the similarity of samples from the transitional zone of the Jaz core and samples from the Arcij ma- rine pond as evidence of the establishment of similar environ- ments. Therefore, a palaeo-marine pond with a strong marine influence, analogous to the present-day Arcij marine pond, de- veloped at approximately 711 cal BP when the sea-water level ap- proached the depth of the sill at –0.5 m (Fig. 12C). However, sta- tistical analysis of geochemical data does not fully support this interpretation (Fig. 10), possibly due to differences in the geolo- gical setting of the Arcij marine pond and the Jaz embayment where siliciclastic input is more prominent (Fig. 10). It is probable that this environment existed for a very short time before it was flooded with sea-water and the Jaz embayment was formed. The LK-2 core top analysis implies the existence of an oxy- gen depleted sedimentary environment in the present-day Jaz embayment (Fig. 12D). Geochemical analysis of the surface sedi- ment revealed high Mo concentrations (8.2 mg/kg) and lower TOC and TIC contents in comparison to the investigated inland marine ponds. A significant difference is in the nutrient availabi- lity and source of organic matter, with a high C/N ratio indicat- ing mixed algal and terrestrial organic matter origin (MEYERS, 1994; MEYERS, 2003; LAMB et al., 2006). The core top sample proved to contain a highly diversified foraminiferal assemblage in comparison to present-day marine ponds, with 32 recognized species. The most common species A. tepida, A. parkinsoniana, Ammonia sp., B. striatula, E. margaritaceum, E. translucens and H. depressula are typical for organic matter enriched marine en- vironments along the eastern Adriatic coast (VIDOVIĆ, 2010). Palaeoenvironmental development of the Sonte embayment encompasses a longer time span (Figs. 12A and 12D). The pre- sent-day Sonte embayment has a maximum depth of 5 m, while the sill depth is 3 m. Accumulation of the sediment sequence was possible due to the morphology of this depression. Analysed sam- ples from the lowermost part of the core exhibit similarity in geo- chemical and mineralogical composition to the basal part of the LK-2 core (Fig. 10) and indicate terrestrial soil (DURN et al., 1999; MIKO et al., 2001). Within this interval (unit LK-3-1) poorly preserved specimens of foraminifera occur in low numbers, mak- ing it difficult to interpret an established environment. The rare specimens were probably deposited due to transport by waves and/or winds as a consequence of the gradual Mid-Holocene sea level rise on the seaward side of the karstified sill/barrier. Further up-core (unit LK-3-2), a significant rise in the TOC content was observed (Fig. 9I). We suggest development of a stag- nant water body at approximately 8000 cal BP (according to the age-depth model) on previously formed soil. Increased nutrient availability could facilitate organic matter production, similar to the Marinska, Podbrajde and Arcij marine ponds (Fig. 11B). How- ever, most of the organic matter has a terrestrial source possibly indicating input from the land under a different climatic setting or the enhanced growth of terrestrial plants (Fig. 11D). This in- terval could be correlated with the Holocene pluvial period reco- gnized in the Adriatic Sea (WUNSAM et al., 1999; SCHMIDT et al., 2001) and in the lacustrine sediments from karst poljes and lakes located along the eastern Adriatic coast (SCHMIDT et al., 2000; BALBO et al., 2006; ILIJANIĆ et al., 2018). The established environment was probably poorly oxygena- ted, which enabled the preservation of organic matter. Relatively high values and covariation of Mo and TOC corroborates this conclusion (CRUSIUS et al., 1996; CALVERT & PEDERSEN, 1993; ALGEO & LYONS, 2006; SCHOLZ et al., 2017). The Mo concentrations are significantly higher in comparison to the pre- sent-day concentrations in the marine ponds (Fig. 9D), indicating low oxygen abundance due to the development of a restricted en- vironment with water stratification. The S concentrations are high and similar to those in the Marinska, Arcij and Podbrajde marine ponds on Cres Island, further supporting the development of a restricted and oxygen poor water body (Fig. 9E, Fig. 11A). Dominant taxa, A. tepida, Ammonia beccarii, H. depressula, As- terigerinata mamilla, Porosononion sp., Elphidium fichtelianum and C. gerthi imply the existence of shallow marine to possibly slightly brackish water environmental conditions (MURRAY, 2006). A. tepida and A. beccarii have been frequently observed in the sediments along the eastern coast of the Adriatic Sea with high P and TOC content (VIDOVIĆ et al., 2014). The presence of the genus Haynesina can also be correlated with the enrich- ment of TOC in sediment (DEBENAY et al., 2001; VIDOVIĆ et al., 2009; VIDOVIĆ et al., 2014). Statistical analysis demon- strated the highest similarity of the foraminiferal assemblages from this unit with the present-day Arcij marine pond and previ- ously described transitional zone in the core from the Jaz embay- ment. This suggests development of a palaeo-marine pond with normal marine water (Fig. 12A). However, such similarity was not observed in the statistically analysed geochemical data, where this unit correlates well with the topmost part of the Jaz embay- ment core therefore implying similarity of these environments (Fig. 10). Micropalaeontological data and geochemistry therefore suggest different palaeoenvironments, but generally provide evi- dence of a significant marine influence during the deposition of sediments from unit LK-3-2. At 6610 cal BP (unit LK-3-3) a decrease in TOC content and Mo concentrations, followed by an increase in TIC indicate ma- jor environmental change in comparison to the previously des- cribed unit (Fig. 6). Carbonates become a more important sedi- ment component (Fig. 9H, Fig. 10). Surface sediments deposited along the present-day eastern Adriatic coast are also enriched in carbonates (PIKELJ et al., 2009; PIKELJ, 2010). The newly for- med environment was nutrient-deprived, which prevented orga- nic matter accumulation (Fig. 11B). However, preserved organic matter has mixed algal-terrestrial origin (Tab. 4, Fig. 6) (MEY- ERS, 1994; MEYERS, 2003; LAMB et al., 2006). Foraminiferal assemblages became highly diversified and dominated by A. tep- G eologia C roatica Brunović et al.: Holocene foraminiferal and geochemical records in the coastal karst dolines of Cres Island, Croatia 37 ida, E. translucens, A. beccarii, Ammonia sp., C. gerthi, E. fichtelianum, Porosononion sp.1, Q. parvula and Q. seminula specimens. Dominant species are similar to the previously de- scribed interval. However, species richness and diversity in- creased significantly. Increases in the relative abundance of mil- iolids were also observed. This can suggest the existence of an enclosed environment (DEBENAY & GUILLOU, 2002; LIDZ & ROSE, 1989) or hypersaline lagoon (DEBENAY et al., 2001). Ge- nus Quinqueloculina is abundant in the Mljet Lakes (ĆOSO-VIĆ et al., 2016), while DEBENAY & GUILLOU (2002) reported the association of A. tepida and Q. seminula in the subtidal areas, marshes and mudflats with developed seaweeds. According to VIDOVIĆ (2010) miliolids are common in marine environments along the Croatian coast of the Adriatic Sea. The determined as- semblage, predominantly comprising the genera Ammonia, El- phidium, Haynesina and Quinqeloculina, can be compared to the previously recognized Haynesina-Ammonia assemblage from the shallow marine environments in the Soline embayment and Nin Bay (VIDOVIĆ, 2010). Cluster analysis grouped samples from this unit into the same subcluster as the surface sample from the Jaz embayment where shallow marine environmental conditions prevail today. Statistical analysis of the geochemical data also indicated this similarity. It is our interpretation that at 6610 cal BP a marine influence became more prominent in the Sonte em- bayment, possibly with the sea water spilling over the sill (Fig. 12B). This is in general agreement with the published global and regional sea level curves (CORREGGIARI et al., 1996; WAEL- BROEK et al., 2002; LAMBECK et al., 2014; VACCHI et al., 2016). The topmost part of the core (unit LK-3-4) can be geochemi- cally distinguished from the previously described core intervals (Fig. 6). This is probably indicative of the establishment of a more permanent, fully marine environment (Fig. 12D). A highly diver- sified foraminiferal assemblage consisting of 41 recognized spe- cies was determined in the LK-3 core top. The dominant Sonte embayment foraminiferal fauna (G. praegeri, H. depressula, H. germanica, A. tepida, A. mamilla and Bolivina pseudoplicata) is typical for littoral environments in the Adriatic Sea (JORISSEN, 1988; VIDOVIĆ, 2010). In the investigated embayment, the determined surface as- semblage is present in the sand dominated sediment, with low Mo and S concentrations, low TOC content and high TIC values (Fig. 6). However, although the sediment is oxygenated, measu- red oxygen concentrations in the water were the lowest among all the investigated environments (Tab. 2), probably due to the greater depth of this environment. Primary productivity in the Sonte embayment is limited due to the nutrient deficiency (Fig. 11B) and therefore organic matter content is low (Fig. 9I). Cluster analysis grouped foraminifera from this sample into the same subcluster as the previously described marine samples (Fig. 7). Statistical analysis of the geochemical data indicated a similarity to other marine units from the LK-3 and LK-2 cores (Fig. 10). 6. CONCLUSIONS Marine ponds have been developed in the coastal karst dolines along Cres Island. Sediments preserved in the Marinska, Arcij and Podbrajde marine ponds revealed important micropalaeon- tological and geochemical data that was used to characterize these marginal marine environments. Detailed analysis of sedi- ment cores from the Jaz and Sonte embayments, developed in now submerged dolines, revealed the complex palaeoenviron- mental evolution of the investigated area. The downcore micro- palaeontological and geochemical data enabled detection of the Holocene palaeo-marine ponds. We suggest the development of a palaeo-marine pond, similar to the present-day Arcij pond, at approximately 711 cal BP in the Jaz embayment. A palaeo-marine pond in the Sonte embayment existed up to 6610 cal BP. These palaeo-marine ponds were flooded during the Holocene sea level rise, when the marine environment was established. Therefore, recognition of different environments developed in the karst dolines, located in the coastal zone of Cres Island, was possible. The research of the present-day marginal marine environments along the eastern Adriatic coast could prove to be valuable for palaeoenvironmental studies and especially Holocene sea level change research. ACKNOWLEDGEMENT This research was funded by the Croatian Science Foundation (HRZZ) through the interdisciplinary project „Lost Lake Land- scapes of the Eastern Adriatic Shelf“ (LoLADRIA; project no. 9419). The authors would like to thank Hrvoje BURIĆ and Edin BADNJEVIĆ for their help during the fieldwork campaign and Ana-Maria HESKI and Helena ĆUĆUZOVIĆ for performing grain-size analysis. We would also like to thank Editor Mladen JURAČIĆ and two anonymous reviewers whose comments sig- nificantly improved the manuscript. 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Foraminifera specimens from marine ponds: 1-3 Trochammina inflata (MONTAGU), 1 spiral side, 2 umbilical side, 3 spiral side with deflated chambers; 4-6 Haplo- phragmoides canariensis (d’ORBIGNY), 4 side view, 5 face view, 6 side view; 7 side view; 7-11 Ammonia tepida (CUSHMAN), 7 deformed specimen, 8 umbilical view, 9 enlargement of the test surface with diatoms, 10 enlargement of the test surface. G eo lo gi a C ro at ic a Geologia Croatica 72/142 Plate 2. Foraminifera specimens from the Jaz and Sonte embayments: 1 Peneroplis planatus (FICHTEL & MOLL) side view; 2 Elphidium aculeatum (d’ORBIGNY) side view; 3 Cri- broelphidium gerthi (van VOORTHUYSEN) side view; 4 Buccella sp.2 umbilical side; 5 Rosalina macropora (HOFKER) spiral side; Asterigerinata mamilla (WILLIAMSON) spi- ral side; 7 Haynesina depressula (WALKER & JACOB) side view; 8 Bolivina striatula (CUSHMAN) side view; 9 Bolivina pseudoplicata (HERON-ALLEN & EARLAND) side view.