Microsoft Word - 01_Bergami_LM02.doc Available online http:/amq.aiqua.it ISSN (print): 2279-7327, ISSN (online): 2279-7335 Alpine and Mediterranean Quaternary, 26 (1), 2013, 5-14 IONIAN SEA SURFACE TEMPERATURE DURING THE SAPROPEL S1 DEPOSITION INFERRED FROM PLANKTONIC FORAMINIFERAL Mg/Ca AND δ18O Caterina Bergami1, Lucilla Capotondi1, Daniela Salvagio Manta2, Mario Sprovieri2, Luigi Vigliotti1 1 CNR - Istituto di Scienze Marine, ISMAR, Bologna, Italy 2 CNR - Istituto per l’ambiente marino costiero, IAMC, Capo Granitola, Trapani, Italy Corresponding author: Caterina Bergami ABSTRACT: Temperature variations during the Holocene sapropel S1 has been investigated by means of a multiproxy study on core ET99-M11 collected in the western Ionian Sea at a water depth of 2800 m. Sea Surface Temperatures (SST) reconstruction has been made by measuring oxygen stable isotopes (δ18O) and Mg/Ca ratios on the planktonic foraminifers Globigerinoides ruber and Globigerina bulloides. Results indicate that the investigated interval was characterized by water temperature increase, both at surface and in the sub-surface layers. Paleotemperature reconstruction based on Mg/Ca ratios shows higher temperature values during the two sub-units (S1a and S1b) of the sapropel S1, and lower during the sapropel interruption, the latter being synchronous to the well known 8.2 cold event. In addition, a number of several short-term cold oscillations which can be correlated with millennial scale climate events in the North Atlan- tic region is evidenced. This indicates a possible atmospheric connection between the Central Mediterranean and the North Atlantic re- gion and the strong relation between climate and oceanographic changes during the sapropel deposition. Keywords: sapropel S1, planktonic foraminifera, paleotemperature, Central Mediterranean, Mg/Ca. 1. INTRODUCTION Organic-rich layers, named sapropels, character- ize the Neogene sediments of the Mediterranean Sea (Olausson, 1961; Cita et al., 1977). These sediments contain abundant and well-preserved planktonic micro- fossils that make these intervals particularly suitable for high-resolution paleoclimatic reconstructions. Planktonic foraminifera have proven to be excel- lent indicators of sea surface temperature, salinity, food availability and they have been used to detect long- and short-term climate changes in the Mediterranean Sea. Actually, the isotopic and trace elements composition of foraminifera shells provide a reliable record of seawater chemistry and as such are widely used by palaeocean- ographers to reconstruct ocean and climate variability on geological timescales. Specifically, the δ18O signal of planktonic foraminifera records the combined effects of global ice volume, sea surface temperature, and region- al evaporation/precipitation budgets, while the Mg/Ca ratio of foraminiferal tests mainly depends on the tem- perature of the water in which the foraminifer calcifies, as basically deduced from cultivating work and field studies (e.g., Nürnberg, 1995, 2000; Nürnberg et al., 1996, 2000; Lea et al., 1999; Mashiotta et al., 1999; Elderfield & Ganssen, 2000: Dekens et al., 2002). Foraminiferal Mg/Ca seawater thermometry is a rapidly developing and increasingly widely used tool for palaeoceanographic reconstructions (Nürnberg et al., 1996; Rosenthal et al., 1997; Lea et al., 1999; Elderfield & Ganssen, 2000; Lea at al., 2000; Anand et al., 2003; Barker et al., 2005). The exponential increase of bulk test Mg/Ca composition with seawater temperature is well established from deep-sea sediment core top (Rosenthal et al., 1997; Hastings et al., 1998; Elderfield & Ganssen, 2000; Lea at al., 2000; Rosenthal et al., 2000; Dekens et al., 2002; Rosenthal & Lohmann, 2002). However, the incorporation of Mg during shells calcification is a complex and imperfectly known mech- anism with potential species‐dependent effects and non‐temperature biases such as those associated to carbonate ion content of seawater (Russell et al., 2004; Kisakürek et al., 2008) or salinity (Nürnberg et al., 1996; Lea et al., 1999; Kisakürek et al., 2008; Mathien‐Blard & Bassinot, 2009; Arbuszewski et al., 2010). Although not numerically abundant, studies in the Mediterranean evi- denced some problems in the application of this meth- od. Ferguson et al. (2008) showed a significant re- sponse of foraminiferal Mg/Ca to salinity in the Mediter- ranean Sea revealing a clear relationship (16% Mg/Ca increase per psu) although associated to a large Mg/Ca data scattering. This result was later confirmed by Sab- batini et al. (2011), on the Mg/Ca ratios characterizing the planktonic species G. ruber from the whole Mediter- ranean Sea. Hoogakker et al. (2009) and Boussetta et al. (2011), who worked on core tops from the Red Sea and from the Mediterranean basin respectively, sug- gested that anomalously high Mg/Ca ratios of planktonic foraminifers from the Mediterranean Sea, could be also related to early diagenetic, high Mg‐calcite overgrowths formed from CaCO3 supersaturated interstitial seawater. Also, van Raden et al. (2011) suggested that the high Mg/Ca measured on two planktonic foraminifers (Glo- bigerina bulloides and Globorotalia inflata) in the West- ern Mediterranean Sea is due to inorganic calcite coat- ing on the foraminiferal tests. Finally, Kontakiotis et al. Bergami C. et al. 6 (2011) presented new Aegean Sea results which reveal Mg/Ca values that were unreasonably high to be ex- plained by temperature or salinity variations alone, con- firming that foraminiferal Mg/Ca is affected by diagene- sis. Studies regarding foraminiferal Mg/Ca ratios during sapropels deposition are rare, however Ní Fhlaithearta et al. (2010) reliably constrained the magnitude and du- ration of the sapropel S1 interruption and other short- term cooling events using Mg/Ca thermometry from the benthonic microfauna in the Aegean Sea. Here we present oxygen isotopes and Mg/Ca ratios data from planktonic foraminifera Globigerina bulloides and Globigerinoides ruber from sediments of sapropel S1 in the Ionian Sea, with the aim to reconstruct pale- otemperature and paleoenvironmental changes which occurred during the sapropel S1 deposition in this basin. 2. REGIONAL SETTING The Ionian Sea is a transition basin influenced by the flow and transformation of the major water masses constituting the intermediate and deep thermohaline cell of the Eastern Mediterranean conveyor belt (Malanotte- Rizzoli et al., 1997; Napolitano et al., 2000). Moreover, the Ionian circulation plays an important role in the re- distribution of the different water masses to adjacent seas (Gačić et al., 2010). At the near-surface level, which is the most im- portant part of the water column with regard to the bio- logical production, the Modified Atlantic Water (MAW) enters the western Ionian basin, the intermediate layer is influenced by salty and warm waters coming from the Levantine and Aegean basins (LIW: Levantine Interme- diate Waters), whilst dense and oxygenated waters, mainly of Adriatic origin, spread into the Ionian deep layer. The choice of the Ionian basin for this kind of high- resolution study is driven by the fact that its oceano- graphic setting is critical for the deep-water formation of the Mediterranean Basin and the oceanographic condi- tions, responsible of the sapropel deposition, are cer- tainly influenced by the deep-sea ventilation. Moreover, concerning the planktonic foraminiferal distribution, this basin appears as a transitional area between the Southwestern and Eastern Mediterranean area (Pujol & Vergnaud Grazzini, 1995). 3. MATERIAL AND METHODS The sedimentary core ET99M11 has been collected in the Ionian Sea (36°44’04”N, 15°50’94”E, 2800 m below sea level; Fig 1). In the core, the sapropel S1 interval is characterized by black-grey sediments extending from 54 to 22 cm depth in section IV of the core (Fig. 1). 3.1. Age model The age model is that provided by Vigliotti et al. (2011 and Table 2 therein) based on four 14C AMS da- Fig. 1 - Location map of the core ET99M11 and section IV of the core with the indication of the sapropel S1 position. 450 m resolution DTM retrieved from http://portal.emodnet-hydrography.eu/EmodnetPortal/index.jsf#. The sapropel S1 in the Ionian Sea 7 tings integrated with tephra layers and planktonic foram- iniferal bioevents. On this base sapropel S1, is chrono- logically confined between 10.4 and 5.7 cal ka BP and appear synchronous with analogous layer reported in the eastern Mediterranean sea. In detail, three different time intervals have been recognized: the S1a sub-unit spanning from 10.4 to 8.3 cal ka BP, the sapropel inter- ruption from 8.3 to 7.8 cal ka BP, and the S1b sub-unit from 7.8 to 5.7 cal ka BP (Vigliotti et al., 2011). 3.2. Foraminiferal species used and their ecological features G. ruber is a species living in the surface mixed layer and occurring in subtropical to tropical latitudes (Deuser, 1987; Ravelo & Fairbanks, 1992; Niebler et al., 1999). It is found at the base of the mixed layer (Field, 2004) and even has moderate abundances within the thermocline. In contrast to other species, G. ruber has a low-slope response to a deepening isotherm, which makes this species the most suitable to document near- surface temperatures when other species are living deeper (Field, 2004; Tedesco et al., 2007). G. bulloides has a wide geographic distribution, ranging from the poles to the low latitudes (Niebler et al., 1999; Schmidt & Mulitza, 2002). This taxon most commonly lives in the surface mixed layer (Fairbanks et al., 1982; Hemleben et al., 1989), but it also occurs with- in the thermocline (Field, 2004). Each species records the temperature variations of the water mass in which it thrives. Hence, the warmest water mass is the one in which G. ruber lives, and corre- sponds to the summer mixed layer (Pujol & Vergnaud- Grazzini, 1995; Rohling et al., 2004). The water mass recorded by G. bulloides is assumed to be a mixture be- tween the late spring/early summer surface layer and deeper waters upwelled during those months at 50-100 water depth (Pujol & Vergnaud-Grazzini, 1995; Barcena et al., 2004; Hernàndez-Almeida et al., 2005). 3.3. Trace elements analysis (ICP-MS/ICP-AES) Forty to sixty specimens of G. ruber (var. alba) were selected from the > 150 µm size fraction (26 sam- ples) discarding specimens visibly contaminated by fer- romanganese oxides. The foraminifera tests were next cleaned using a multistep trace metal protocol including reductive cleaning with buffered hydrazine (Boyle & Keigwin, 1985). Mg/Ca ratios were measured on a in- ductively coupled plasma mass spectrometer Varian ICP-MS and an inductively coupled plasma atomic emission spectrophotometer Varian Vista MPX at the Geochemistry Laboratory of the IAMC-CNR (Naples). In detail, the tests were gently crushed and then cleaned following procedures modified from Lea & Boyle (1993). Briefly, samples were ultrasonically cleaned four times with ultrapure water (> 18 MΩ) and twice with methanol. Metal oxide coatings were reduced in a solu- tion consisting of anhydrous-hydrazine, citric acid, and ammonium hydroxide and organic matter was oxidized in a solution of hydrogen-peroxide and sodium- hydroxide. All the water samples were treated under a laminar air flow clean bench to minimize contamination risks and the sampling materials were cleaned with high purity grade reagents. The remaining tests material was then dissolved in 0.1N nitric acid and simultaneously analysed for magnesium with the Varian ICP-MS induc- tively coupled plasma-mass spectrometer. A multi- element standard was prepared with ICP-MS grade High-Purity Standards. Based on repeated analyses of the standard and samples over several runs, on differ- ent days, the 2s error in the ICP analyses is estimated at ±5%. Replicate analyses on five samples yielded an average external precision (1σ) of about 5%. Calcium was measured with a Varian Vista MPX inductively cou- pled plasma-optical emission spectrometer (ICP-OES). Metal to calcium ratios were determined from intensity ratios with an external matrix-matched standard using the method developed by Rosenthal et al. (1999). The cleaning protocol and analytical approach used in this study is also comparable to methods re- ported by Elderfield & Ganssen (2000). 3.4. Isotopic analyses The oxygen isotopic composition of G. ruber (var. alba) and G. bulloides were obtained from the sediment core. About 10-15 specimens in the > 150 µm size frac- tion were analyzed per sample (41 samples). Samples were measured with an automated con- tinuous flow carbonate preparation GasBench II device and a ThermoElectron Delta Plus XP mass spectrome- ter at the Laboratory of Geochemistry of the IAMC-CNR (Naples). Acidification of the samples was performed at 50°C. An internal standard (Carrara Marble with δ18O = - 2.43‰ vs. VPDB and δ13C = 2.43‰ vs. VPDB) was run every six samples and the NBS19 international standard was measured every 30 samples. Standard deviations of carbon and oxygen isotope measures were estimated at 0.1 and 0.08‰, respectively. All the isotope data are reported in δ‰ versus VPDB. 3.5. Determination of Calcification Temperatures 3.5.1. Temperature estimates from δ18Oforam To obtain the calcification temperatures we have used oxygen isotope data of G. ruber and G. bulloides (δ18Oforam) and of the water masses in which they calcify (δ18Oseawater). Different equations have been proposed to convert δ 18Oforam in SST but based on what reported on Grauel & Bernasconi (2010) on sediment surface samples, G. ruber yield the most reliable calcification temperature applying the Shackleton (1974) palaeotemperature equation. In fact, according to the authors, who made a core-top study on δ18O temperature reconstructions of G. ruber (white) and U. mediterranea in the central Med- iterranean, reliable temperatures were produced using the Shackleton (1974) equation, whereas too low tem- peratures compared to the recent temperature condi- tions (on average ~4.4°C lower than predicted by Shackleton (1974) equation) were produced using the Mulitza et al. (2003) equation. The equation of Shackleton (1974) is: where Tiso is the calcification temperature and δ 18Oforam and δ18Oseawater are reported vs. VPDB. δ 18Oseawater values for sapropel time are those re- ported in Kallel et al. (1997 and Table 4 therein). Bergami C. et al. 8 Values of δ18Oseawater have been converted to Vi- enna Standard Mean Ocean Water (V-SMOW)‰ using the following equation:   3.5.2 Temperature estimates from Mg/Ca ratios Although in the Mediterranean sea seems to be no significant correlation between Mg/Ca and δ18O‐derived calcification temperatures (Ferguson et al., 2008; Sab- batini et al., 2011), several studies suggested an expo- nential correlation between Mg/Ca ratios from G. ruber shells and SST (e.g. Elderfield & Ganssen, 2000; Anand et al., 2003; Dekens et al., 2002). Generally, the adopt- ed Mg/Ca-SST equation is that reported by Elderfield & Ganssen (2000) based on multispecies calibration:   where TMg/Ca is the calcification temperature and Mg/Ca is measured in mmol/mol. 4. RESULTS 4.1. δ18Oforam and SST The oxygen isotope data measured on the two spe- cies of planktonic foraminifera are illustrated vs. age in Fig. 2. The δ18O values from G. ruber and G. bulloides during the investigated period average -0.56‰ and 1.12‰, re- spectively (Fig. 2) with associated variances of 0.46‰ and 0.62‰. G. ruber shows lower values than G. bulloides but the two records show the same trend during the investi- gated period, with a general lightening during sapropel deposition, and particularly during the S1a subunit. The G. ruber calcification temperature, character- ized by a general increase throughout the whole investi- gated period, ranges between 22.8 and 14.1°C with an average value of 20°C, while G. bulloides records a simi- lar trend with an isotopic temperature ranging between 16.3 and 5.0°C, with an average value of 12.7°C (Fig. 2). The heaviest isotopic values throughout the record are observed at 11.6, 10.7, 10.0, 9.5, 8.2, and 6.4 cal ka BP suggesting colder conditions during these intervals. Fig. 2 - Down-core oxygen isotope records (‰ versus VPDB) and calculated isotopic temperature in °C in G. ruber var. alba and G. bulloides for core ET99M11 across the sapropel S1. The grey areas, representing the extent of the two sub-units of the sapropel S1, are from Vigliotti et al. (2011). B5-B7 label Bond cycles (Bond et al., 1997; 2001). The sapropel S1 in the Ionian Sea 9 4.2. Mg/Ca ratios and SST estimates During the interval of sapropel deposition Mg/Ca ratios range between 1.8 and 4.7 mmol/mol (Fig. 3) with an average value of 3.37 mmol/mol. The estimated SST values range between 22.3 and 15.7°C during the subunit S1a, with an average value of 20°C, and between 22.4 and 18.6°C (average value 18.6°C) during the subunit S1b, while during the interruption the average value is 14.8°C (Fig. 4). The warmest period is observed at the beginning of the sap- ropel S1 deposition, and throughout the interruption a gradual cooling took place, leading to another warming phase during the subunit S1b. 5. DISCUSSION 5.1. Paleotemperature estimates and difference be- tween the two proxies Our results show temperatures comparable to those reported during the sapropel S1 by Kallel et al. (1997). In detail, in the investigated period, both proxies record comparable temperatures in terms of average values, however there are some dissimilarities at a smaller scale: in fact, whereas the isotopic temperature after a sharp increase at 10 cal ka BP does not show great fluctuations, paleotemperature reconstruction based on Mg/Ca ratios shows higher values in the inter- val from 10 to 8.8 cal ka BP and from 6.6 to 6.3 cal ka BP during the deposition of the two sub-units of sapro- pel S1, and lower values in the interval from 8.8 to 7.2 cal ka BP, with the lowest temperature recorded at 8.2 cal ka BP corresponding to the sapropel interruption (Fig. 4). In detail, based on calculated isotopic tempera- tures, the sapropel S1 interval was characterized by a general increase in water temperatures at the surface and in the sub-surface layers, as clearly evidenced by G. ruber and G. bulloides, respectively. The mean temperature estimate for G. ruber (20°C) is consistent with the growth temperature pro- posed by Kallel et al. (1997 and Table 4 therein) for the same species during the sapropel S1 deposition in the Ionian basin. The sapropel SST is also taken to be equivalent to the modern one in the Ionian basin and the growth temperature of G. ruber is found to correspond to the mean SST of the summer mixed layer (Manca et al., 2004). This datum further supports that, during the sapropel interval, the SSTs in the Ionian Sea were simi- lar to the present ones. The amplitude of the temperature changes rec- orded by G. ruber is broad, up to 8°C from the warmest to the coldest values and is consistent with paleotem- perature variations documented in the same area during the sapropel S1 deposition by Emeis et al. (2000). This broad amplitude is due to the very thin summer mixed layer really sensitive to any runoff event or heating anomaly which would have great impact as compared with other thicker water masses (Gonzalez-Mora et al., 2008). The variability of the G. bulloides data are even wider than those of G. ruber (around up to 10°C of differ- ence between the coldest and the warmest samples), this although the general trends are similar. The mean tem- perature estimate for G. bulloides (12.7°C) is cooler by about 2°C respect to that of today. As G. bulloides is pro- lific at depths below the thermocline (Pujol & Vergnaud- Grazzini, 1995), the observed difference in temperature estimate respect to G. ruber suggest the presence of a marked thermocline or an increasing summer thermal gradient. Moreover, the large gradient between the tem- peratures recorded by G. ruber and G. bulloides can be interpreted as related to their seasonality (Pujol & Vergnaud-Grazzini, 1995) suggesting that the two differ- ent water masses remained isolated at the seasonal scale, due to a permanent seasonal stratification. The mean temperature estimate, based on Mg/Ca ratios, for G. ruber is consistent with the isotopic tem- perature during S1a subunit (20°C) while is cooler by about 1.5°C during S1b subunit (18.6°C). Discrepancies between temperature estimates from Mg/Ca ratios and calculated isotopic temperature may be ascribed to the different variables influencing the two proxies. The oxygen isotopic temperatures are based on biogenic δ18Oforam which is affected by δ 18Owater. The variability between the Mg/Ca and oxygen isotope temperature reconstructions of G. ruber may, in part, be explained by changes in δ18Owater. In our reconstructions, we assumed a constant δ 18Owater during the entire investigated interval, but it is Fig. 3 - Down-core Mg/Ca ratios of G. ruber var. alba for core ET99M11 across the sapropel S1. The grey areas, represent- ing the extent of the two sub-units of the sapropel S1, are from Vigliotti et al. (2011). Bergami C. et al. 10 reasonable that during the sapropel deposition the well documented enhanced run-off and the subsequent dif- ferent evaporation/precipitation budget, and the pres- ence at the surface of freshwater-diluted lenses influ- enced this value. On the contrary, Mg/Ca ratios in modern planktonic foraminifera are assumed and have been demonstrated to be predominantly a function of the temperature of the water in which they grew, while salinity is a secondary factors that exert influences on shell Mg content, but not in the Mediterranean, where several authors (Ferguson et al., 2008; Sabbatini et al., 2011 and references therein) suggested that Mg/Ca ratios can be strongly affected by the high salinity val- ues typical of this basin. In detail, measured Mg/Ca values of planktonic foraminifera, collected in the east- ern and central Mediterranean basins, correlate poorly with the calcification temperatures but more significant- ly with calcification salinities, demonstrating that the salinity can be a primarily influencing factor in these environments. However, during the sapropel deposi- tion, surface water salinity decreased and became al- most homogeneous over the whole Mediterranean ba- sin with an average value for the Ionian sea of 35.2 PSU (Kallel et al., 1997 and Table 4 therein), which is close to that of the western Mediterranean basin (e.g. Alboran Sea) where the Mg/Ca ratios are not influenced by the salinity regime (Ferguson et al., 2008). Then it is reasonable that, during the sapropel deposition, the salinity did not exert influences on shell Mg content, being the Mg/Ca ratios primarily influenced by SST var- iations. In addition, we may exclude the possibility that post-deposition process or the presence of a Mg‐rich calcite coating influences the results, firstly because sapropel layers are really conservative environments often characterized by the lack of bioturbation and often apparently high sedimentation rates. Secondarily, we observed in our samples, that the sapropel microfauna Fig. 4 - δ18O and Mg/Ca G. ruber var. alba inferred temperature records from core ET99M11. The grey areas, representing the extent of the two sub-units of the sapropel S1, are from Vigliotti et al. (2011). Open symbols represent Mg/Ca data, overlain with a line represent- ing a 200 year Gaussian smoothing. The sapropel S1 in the Ionian Sea 11 association was typically characterized, as observed by other authors (Capotondi et al., 1999; Negri et al., 1999), by the occurrence of specimens showing a very thin test structure, easily observed at the optical micro- scope, which point to a very good test preservation with no or few secondary calcite overgrowth. Concluding, our data show that fluctuations in the Mg/Ca ratios are more pronounced than in the isotopic values suggesting a promising tool for paleotemperature reconstruction also in the Mediterranean, but only when the influence of salinity will be entirely clarified. 5.2. Mediterranean connection with the North Atlan- tic Ocean Climate changes during the Holocene have been gathering increasing attention because of the occur- rence of millennial‐scale abrupt climate changes, of possible hemispheric extent, during this period (e.g., Bond et al., 2001; Gupta et al., 2003; Mayewski et al., 2004), when the boundary conditions such as CO2 con- centration and ice volume were relatively constant and similar to the present ones. In the North Atlantic, ice‐rafted debris (IRD) events exhibit a distinct pacing on millennial‐scale during the Holocene (Bond et al., 2001). Recently, several authors identified the expression of these events also in the sed- imentary record of the Mediterranean Sea (e.g. Cacho et al., 2001; Frigola et al., 2007; Rouis-Zargouni et al., 2010; Incarbona et al., 2008; 2010; Vallefuoco et al., 2011; Capotondi & Vigliotti, 1999). Comparison of our record of δ18Oforam with North Atlantic Holocene millennial scale climatic variability (Bond et al., 1997) allowed to highlight several short- term cold oscillation at around 10.7, 9.5, and 8.2 cal ka BP comparable with the events numbered 7, 6, and 5 by Bond et al. (2001; 1997) (Fig.2). This indicates a possible atmospheric connection between the Central Mediterranean and the North Atlan- tic region and the strong relation between climate and oceanographic changes during the sapropel S1 interval. One of these climatic features has been already docu- mented by several authors in other areas of the Mediter- ranean Sea (e.g. Rohling et al., 1997; De Rijk et al., 1999; Sangiorgi et al., 2003; Vigliotti et al., 2011; Asioli et al 1999; Ariztegui et al., 2000), and was related to the so-called “8.2 event” (Alley et al., 1997) and the associ- ated δ18O increase of Greenland ice cores. Based on the isotopic temperature signal, during the three events the magnitude of the sea surface cool- ing is comparable to that proposed by Bond et al. (1997) in cores from the North Atlantic ocean, and does not exceed 2°C. Based on the Mg/Ca temperature recon- struction, the cooling exceeded 2°C only during the event centred at 8.2 cal ka BP with a decrease in tem- perature of at least 5°C corresponding to the shift also proposed by Alley et al. (1997) during this event. Then in the studied core the Mg/Ca method evidences very sharp short time fluctuations much less evident with the isotope paleotemperature method. Then, our data suggest a strong sensitivity of the Central Mediterranean basin, during the sapropel S1 time interval, to changes occurred in the North Atlantic and therefore supports the high low latitude climatic Mediterranean interplay also evidenced in Colleoni et al. (2012) for the Plio-Pleistocene time interval. 6. SUMMARY A high-resolution investigation on the Holocene sapropel S1 in the Ionian Sea was performed based on planktonic foraminifera geochemical data (stable oxygen isotopes and Mg/Ca ratios) proxies. This study documents promising results of the Mg/Ca paleothermometry applied to planktonic species. The first phase of the sapropel S1 was character- ized by higher temperature, also consistent with the modern ones in the Eastern Mediterranean basin, while the second phase registered cooler temperature by about 2°C. During the sapropel interval, several cooling epi- sodes, time equivalent to the millennial climatic variabil- ity in the North Atlantic, were recognized at 10.7, 9.5, and 8.2 ka BP, the latter corresponding to the well known “8.2 event” and synchronous to the sapropel in- terruption. The climatic oscillations recorded by our study suggest an hemispheric-scale atmospheric con- nection in the Central Mediterranean basin. ACKNOWLEDGEMENTS Part of this study was funded by the projects SIN- APSI and Ricerca Spontanea a Tema Libero (RSTL n. 154; “Sapropels S1 e S5: archivi della variabilità climati- ca indotta dal regime monsonico”). We thanks M. Col- telli, P. Del Carlo and L. Vezzoli to provide Core ET99M11. We also thank Alessandra Negri and an anonymous rewiever who greatly improved the manu- script with their comments. This is the ISMAR contribu- tion 1784. REFERENCES Alley R. B., Mayewski P. A., Sowers T., Stuiver M., Tay- lor K. C., Clark P. U. 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