M Namik Çağatay

M Namik Çağatay

Kürşad Kadir Eriş

Özlem Makaroglu

Nurettin Yakuboğlu

Pierre Henry

Suzanne A G Leroy

Gülsen Uçarkuş

Mehmet Sakınç

Burak Yalamaz

Cerennaz Bozyiğit

Julia Kende

Alexander Francke

William Ryan

Gaia Sinopoli

Mustafa Ergin

Helge Arz

M Namık Çağatay

K Kadir Eriş

Özlem Makaroğlu

 Correlation of the Sea of Marmara records with regional and global records  Reporting of two new unidentified tephra The Sea of Marmara during Marine Isotope stages 5 and 6

Keywords: Sea of Marmara, Late Quaternary, Marine Isotope stages 5-6, Eastern Europe, Paleoceanography, Sedimentology-marine cores, Geochemical proxies, Sapropels Sea of Marmara, Late Quaternary, Marine Isotope stages 5-6, Eastern Europe, Paleoceanography, Sedimentology-marine cores, Geochemical proxies, Sapropels

Multi-proxy analyses and lithology of two cores, MRS-CS18 and MRS-CS27, from the İmralı Basin of the Sea of Marmara (SoM) provide important new information on environmental conditions, relative sea level, and sill depths of the straits of Bosporus and Dardanelles during the marine isotope stages (MIS) 5 and 6. The fossil and multi-proxy geochemical records show that lacustrine conditions prevailed in the SoM during most of MIS-6, from 173 to 134 ka BP, and that the transition to marine conditions during Termination II took place at ~134.06±1.10 ka BP. MIS5 interstadials a, c, and e witnessed the formation of three sapropels (MSAP-4, MSAP-3 and MSAP-2) under suboxic to anoxic marine conditions, whereas during stadials MIS5b (~94 -86) and MIS5d (~112 -105 ka BP), lacustrine and marine conditions with deposition of sediments having relatively low TOC contents (<2 %) prevailed, respectively. Consideration of the global sea level, together with the timing of the marine reconnection of the SoM during Termination II and persistence of the marine conditions during MIS5, except for the MIS5b, suggests that the Dardanelles sill depth was at ~-75±5 m during the reconnection at Termination II and at -55±5 m during most of MIS5. On similar considerations of the Black Sea marine reconnections and disruptions during the MIS5, a sill depth of -35 to -40 m (similar to the present day depth) is indicated for the Bosporus Strait. The SoM geochemical proxy records correlate well with the regional terrestrial and marine records and the NGRIP oxygen isotope record with its glacial and interglacial (GI) phases, showing the common effect of the North Atlantic climatic events triggered by the perturbations in the Atlantic Meridional Overturning Circulation (AMOC). However, the amplitude of the oscillations recorded in the SoM during MIS6 (Penultimate Glacial Period) is relatively smaller compared to the MIS4 to MIS2 (Last Glacial Period).

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Introduction

Late Quaternary paleoceanography and hydrography of the Sea of Marmara (SoM) have been extensively investigated since 1980s because of its key location between the Black Sea and the Mediterranean Sea (e.g., [START_REF] Stanley | Late Quaternary water exchange between the eastern Mediterranean and the Black Sea[END_REF][START_REF] Aksu | Oscillating Quaternary water levels of the Marmara Sea and vigorous outflow into the Aegean Sea from the Marmara Sea-Black Sea drainage corridor[END_REF][START_REF] Aksu | Last glacial-Holocene paleoceanography of the Black Sea and Marmara Sea: stable isotopic, foraminiferal and coccolith evidence[END_REF][START_REF] Çağatay | Late Glacial-Holocene palaeoceanography of the Sea of Marmara: timing of connections with the Mediterranean and the Black Seas[END_REF][START_REF] Cohen | Paleolimnology, The History and evolution of Lake Systems[END_REF]2009, 2015;[START_REF] Mchugh | The last reconnection of the Marmara Sea (Turkey) to the World Ocean: A paleoceanographic and paleoclimatic perspective[END_REF][START_REF] Vidal | Hydrology in the Sea of Marmara during the last 23 ka: Implications for timing of Black Sea connections and sapropel deposition[END_REF][START_REF] Eriş | The timing and evolution of the post-glacial transgression across the Sea of Marmara shelf south of Istanbul[END_REF][START_REF] Eriş | Late glacial to Holocene sea-level changes in the Sea of Marmara: new evidence from high-resolution seismics and core studies[END_REF][START_REF] Vardar | Late Pleistocene-Holocene evolution of the southern Marmara shelf and sub-basins: middle strand of the North Anatolian fault, southern Marmara Sea, Turkey[END_REF]. The SoM, together with the Bosporus and Dardanelles straits, known as the Turkish Straits System (TSS), is the gateway for the water-mass exchanges between its neighbouring seas (Fig. 1). Water exchange through this system is controlled by eustatic global sea-level in the Mediterranean, riverine and melt water input and water level in the Black Sea, and the sill depths of the connecting straits. Presently, a two-way water exchange exists via the TSS between the Mediterranean Sea and the Black Sea waters that constitute the lower and upper currents, respectively, with a permanent pycnocline at ~-25 m between the two (Ünlüata et al., 1990;[START_REF] Beşiktepe | The circulation and hydrography of the Marmara Sea[END_REF][START_REF] Aydoğdu | Circulation of the Turkish Straits System under interannual atmospheric forcing[END_REF]. The present sill depths of the Bosporus and Dardanelles straits are -35 and -65 m, respectively but might have been different during the various Quaternary stages (e.g., [START_REF] Ryan | An abrupt drowning of Black Sea shelf[END_REF]Ryan et al., , 2003;;[START_REF] Gökaşan | Factors controlling the morphological evolution of the Çanakkale Strait[END_REF][START_REF] Gökaşan | Late Quaternary evolution of the Çanakkale Strait region (Dardanelles, NW Turkey): implications of a major erosional event for the postglacial Mediterranean-Marmara Sea connection[END_REF][START_REF] Çağatay | Late Pleistocene-Holocene evolution of the northern shelf of the Sea of Marmara[END_REF], 2015). Moreover, the present hydrography of the SoM with the two-way water exchange might have been disrupted during the glacial periods due to eustatic sea level fall in the Mediterranean Sea and water-level changes in the Black Sea [START_REF] Ryan | An abrupt drowning of Black Sea shelf[END_REF][START_REF] Cohen | Paleolimnology, The History and evolution of Lake Systems[END_REF][START_REF] Aksu | Oscillating Quaternary water levels of the Marmara Sea and vigorous outflow into the Aegean Sea from the Marmara Sea-Black Sea drainage corridor[END_REF], 2002;[START_REF] Çağatay | Late Glacial-Holocene palaeoceanography of the Sea of Marmara: timing of connections with the Mediterranean and the Black Seas[END_REF], 2009, 2015;[START_REF] Eriş | The timing and evolution of the post-glacial transgression across the Sea of Marmara shelf south of Istanbul[END_REF][START_REF] Eriş | Late glacial to Holocene sea-level changes in the Sea of Marmara: new evidence from high-resolution seismics and core studies[END_REF][START_REF] Hiscott | Deltas south of the Bosphorus Strait record persistent Black Sea outflow to the Marmara Sea since ~10 ka[END_REF][START_REF] Hiscott | The Marmara Sea gateway since ~16 ky BP: non-catastrophic causes of paleoceanographic events in the Black Sea at 8.4 and 7.15 ky BP[END_REF].

The paleoceanography and hydrography of the SoM have been reasonably well established for the marine isotope stages 1 to 4 (MIS1 to MIS4), covering the last 70 kyrs, mainly because of the study of a continuous sedimentary record from the RV Marion Dufresne core MD01-2430, recovered from -580 m on the Western High (Çağatay et al., 2015) (Fig. 1a). The study showed that the SoM was a brackish water lake from early MIS-4 to early MIS-1, disconnected from the Mediterranean Sea and became a lake with brackish to fresh waters. A significant regression took place during MIS 2, which is recorded as erosional surfaces and terraces [START_REF] Aksu | Last glacial-Holocene paleoceanography of the Black Sea and Marmara Sea: stable isotopic, foraminiferal and coccolith evidence[END_REF][START_REF] Çağatay | Late Pleistocene-Holocene evolution of the northern shelf of the Sea of Marmara[END_REF][START_REF] Eriş | Late glacial to Holocene sea-level changes in the Sea of Marmara: new evidence from high-resolution seismics and core studies[END_REF].

Freshwater inputs from the Black Sea occurred during the Dansgaard-Oeschger (D-O) events (Greenland Interstadials, GI) of the MIS3 and MIS4 (Çağatay et al., 2009), that slowly converted the saline marine waters of the MIS5 to brackish water in the SoM [START_REF] Çağatay | Late Pleistocene-Holocene evolution of the northern shelf of the Sea of Marmara[END_REF][START_REF] Aloisi | Freshening of the Marmara Sea prior to its post-glacial reconnection to the Mediterranean Sea[END_REF]. The GIs in the SoM are well expressed by high Ca (carbonate) concentrations, relatively high total organic carbon (TOC) contents, low detrital inputs and negative oxygen isotope excursions, strongly suggesting high organic productivity and high input of nutrient-rich melt waters from the European ice sheets via rivers into the Black Sea and from there into the SoM (Çağatay et al., 2015).

The lacustrine phase of SoM lasted with the initial influx of the Mediterranean Sea waters via the Dardanelles Strait at ~14.7 cal ka BP [START_REF] Vidal | Hydrology in the Sea of Marmara during the last 23 ka: Implications for timing of Black Sea connections and sapropel deposition[END_REF]. Such a hydrologic modification lasted for 1000-2000 years, and was represented by colonization of the shelf areas by euryhaline Mediterranean organisms [START_REF] Çağatay | Late Glacial-Holocene palaeoceanography of the Sea of Marmara: timing of connections with the Mediterranean and the Black Seas[END_REF][START_REF] Cohen | Paleolimnology, The History and evolution of Lake Systems[END_REF], 2009;[START_REF] Aksu | Last glacial-Holocene paleoceanography of the Black Sea and Marmara Sea: stable isotopic, foraminiferal and coccolith evidence[END_REF][START_REF] Mchugh | The last reconnection of the Marmara Sea (Turkey) to the World Ocean: A paleoceanographic and paleoclimatic perspective[END_REF][START_REF] Vidal | Hydrology in the Sea of Marmara during the last 23 ka: Implications for timing of Black Sea connections and sapropel deposition[END_REF][START_REF] Eriş | Late glacial to Holocene sea-level changes in the Sea of Marmara: new evidence from high-resolution seismics and core studies[END_REF][START_REF] Vardar | Late Pleistocene-Holocene evolution of the southern Marmara shelf and sub-basins: middle strand of the North Anatolian fault, southern Marmara Sea, Turkey[END_REF][START_REF] Köprülü | Last Glacial-Holocene stratigraphic development at the Marmara Sea exit of the Bosphorus Strait, Turkey[END_REF]. The brackish lacustrine to marine transition with the appearance of euryhaline fauna is dated at 12.55±0.35 cal ka BP in core MD01-2430 on the Western High (Çağatay et al., 2015) (Fig. 1b). This is followed by the establishment of the present two-layer water exchange with Black Sea through Bosporus Strait starting around 5-6 ka BP [START_REF] Çağatay | Late Glacial-Holocene palaeoceanography of the Sea of Marmara: timing of connections with the Mediterranean and the Black Seas[END_REF][START_REF] Algan | Stratigraphy of the sediment infill in Bosphorus Strait: water exchange between the Black and Mediterranean Seas during the last glacial Holocene[END_REF].

Although the hydrography and paleoceanograpy of the SoM are reasonably well known for the MIS1-MIS4, our knowledge for the older Quaternary stages are scanty and based on discontinuous records from shelf cores (Çağatay et al., 2009, 2015). A recent study by Kende et al. (in review), using multi-proxy analyses of a 20.6 m long core (MRS-CS22) from 551 m water depth on the Western High, extends the record back to within MIS5 (Fig.s. 1b and 2).

However, the sequence more likely includes only the record of MIS5a to d.

In the present study, we present data from two giant piston cores MRS-CS27 (20.55 m long) and MRS-CS18 (14.20 m long) from the İmrali Basin of the SoM, extending the record back to MIS5 and MIS6, respectively (Fig. 1). The cores were recovered during the EC FP7 Marsite project cruise onboard RV Pourquoi pas? in 2014, and studied for their fossil content and geochemical and physical properties. The age-depth models of the cores were constructed using accelerated mass spectroscopy (AMS) radiocarbon dating, tephrochronology, and correlation of the SoM data with the North Greenland Ice Programme (NGRIP) δ 18 O record [START_REF] Svensson | The Greenland Ice Core Chronology 2005, 15-42 ka. Part 2: comparison to other records[END_REF][START_REF] Svensson | A 60000 year Greenland stratigraphic ice core chronology[END_REF][START_REF] Rasmussen | A new Greenland ice core chronology for the last glacial termination[END_REF][START_REF] Wolff | Millennialscale variability during the last glacial: the ice core record[END_REF]. We specifically concentrate on the paleoceanography and hydrography of the SoM during MIS5 and MIS6, which have not been previously discussed in detail. Using the new multi-proxy data from the cores, we discuss lake/sea level changes together with the sill depths of the Bosporus (İstanbul) and Dardanelles (Çanakkale) straits, water-mass exchanges through the TSS, and the concomitant paleoceanographic changes in the SoM during the MIS6 and MIS5. We also compare the SoM records with the regional and global records.

The Quaternary stratigraphic records are essential not only for determination of the eustatically-controlled water mass exchanges through the Turkish Straits System, water level changes and the sill depths of Dardanelles and Bosporus straits in relation to the relative sea level changes but also for the dating of some regional seismic reflecting surfaces (e.g., [START_REF] Sorlien | Uniform basin growth over the last 500 ka, North Anatolian Fault, Marmara Sea, Turkey[END_REF][START_REF] Grall | Slip rate estimation along the western segment of the Main Marmara Fault over the last 405-490 ka by correlating mass transport deposits[END_REF]Fig. 1), which is in turn important for determination fault slip rates and the earthquake risk assessment.

Oceanographic, hydrographic and climatic settings of the Sea of Marmara

The SoM, as part of TSS, is characterized by a two-way water exchange between the Aegean and Black seas having waters of different salinity (Fig. 1). The Mediterranean water (~38.5 psu) and Black Sea water (~18 psu) constitute the lower and upper currents, which are separated by a permanent pycnocline located at -25 m (Ünlüata et al., 1990;[START_REF] Beşiktepe | The circulation and hydrography of the Marmara Sea[END_REF][START_REF] Chiggiato | Dynamics of the circulation in the Sea of Marmara: numerical modeling experiments and observations from the Turkish straits system experiment[END_REF][START_REF] Aydoğdu | Circulation of the Turkish Straits System under interannual atmospheric forcing[END_REF]. The Black Sea has positive water balance, exporting ~600 km 3 of water of riverine and precipitation origin and receiving ~300 km 3 of Mediterranean waters through the TSS (Özsoy and Ünlüata, 1997). Some mixing between the lower and upper currents occurs during the passage through the relatively narrow Bosporus and Dardanelles straits with sill depths of -35 m and -65 m, respectively. As a result, the salinity of the surface and bottom waters are modulated to ~38 psu and ~22 psu (Ünlüata et al., 1990;[START_REF] Beşiktepe | The circulation and hydrography of the Marmara Sea[END_REF].

The surface Black Sea waters enter the SoM as a jet from the Bosporus Strait at speeds of 1 to 1.5 m/s, forms a series of eddies, and then exit through the Dardanelles Strait, while the Mediterranean waters flow through the Dardanelles Strait and then sink to form the bottom currents with velocities less than 0.1 m/s in the deep basins [START_REF] Beşiktepe | The circulation and hydrography of the Marmara Sea[END_REF][START_REF] Chiggiato | Dynamics of the circulation in the Sea of Marmara: numerical modeling experiments and observations from the Turkish straits system experiment[END_REF]. The upper and lower water masses have renewal times of 5-6 months and 6-7 years, respectively [START_REF] Beşiktepe | The circulation and hydrography of the Marmara Sea[END_REF]. The oxygen content of the bottom waters varies from 50 to than 18 µmol/kg, with the levels decreasing from the Tekirdağ Basin in the west to the Çınarcık Basin in the east [START_REF] Tryon | Quantifying submarine fluid seep activity along the North Anatolian Fault Zone in the Sea of Marmara[END_REF].

The main drainage basin of the SoM is located to its south with the Kocasu, Gönen and Biga rivers providing 5.80 km 3 /yr and 2.2 x 10 6 t/yr of suspended sediment in the SoM [START_REF] Eie | Sediment data and sediment transport amounts for surface waters in Turkish rivers[END_REF][START_REF] Kazancı | Late Holocene erosion in NW Anatolia from sediments of Lake Manyas, Lake Ulubat and the southern shelf of the Marmara Sea, Turkey[END_REF]. The southern catchment area is mainly under the influence of the Mediterranean climate with hot and dry summers and cold and wet winters. The average winter and summer temperatures are 5 and 24°C and the annual precipitation varies between ~500 and ~1000 mm [START_REF] Deniz | Spatial variations of climate indices in Turkey[END_REF]. The source of moisture is mainly the cyclonic Mediterranean [START_REF] Cullen | Climate change and the collapse of the Akkadian empire: Evidence from the deep sea[END_REF]Türkeş et al., 2009;[START_REF] Göktürk | Climate on the southern Black Sea coast during the Holocene: implications from the Sofular Cave record[END_REF], with some contribution from the Black Sea (Fleitmann et al., 2009;[START_REF] Badertscher | Pleistocene water intrusions from the Mediterranean and Caspian seas into the Black Sea[END_REF][START_REF] Göktürk | Climate on the southern Black Sea coast during the Holocene: implications from the Sofular Cave record[END_REF].

Cores and analytical methods

Cores

Cores MRS-CS 18 and MRS-CS 27 were recovered on board of the RV Pourquoi pas? from depths of 291 and 313 m in the north-eastern and western edges of the İmralı Basin, respectively (Fig. 1b, Table 1). The cores were split into halves and described at EMCOL Sedimentology laboratory, İstanbul Technical University (ITU) (Fig. 2). The working halves of the cores were sampled for total organic carbon (TOC) analysis at 5 cm interval but increased to a resolution of 2.5 cm in some parts of the sapropels. Sampling resolution for paleontological analyses was at 10 cm interval. For all sampling, each sample represents 1 cm core thickness.

The archive halves were used for µ-XRF (Itrax) and Geotek Multi Sensor Core Logger (MSCL) analyses.

Paleontological analysis

Paleontological analysis was carried out in sand size (>63 µm) fraction of 5 cm 3 samples. Micro-and macro-fossils, including benthic and pelagic foraminifera and bivalves, were identified and their abundances were qualitatively recorded in the samples.

Total organic carbon (TOC) and total inorganic carbon (TIC) analyses

The TOC content in freeze-dried samples of the cores was analysed using a Shimadzu TOC/TIC analyser at ITU-EMCOL Geochemistry Laboratory. First total carbon (TC) contents of samples were determined by the total catalytic combustion at 900 °C in the presence of purged oxygen and platinum catalyst, followed by measurement of the evolved carbon dioxide after dehumidification, using the infrared carbon dioxide detector of the analyser. Then, the total inorganic carbon (TIC) was analysed by treating the samples with 85% phosphoric acid, heating the sample to 200 °C and measuring the evolved carbon dioxide. The TOC is calculated as the difference between TC and TIC contents. The precision of the TOC analysis with this method is better than 5% at a 95% confidence level. TOC is used as proxy of organic matter production and preservation.

µ-XRF analysis

The cores were analysed for multi-element composition at 0.5 mm resolution using an Itrax μ-XRF Core scanner, equipped with XRF-EDS, X-Ray radiography and RGB colour camera at the ITU-EMCOL Core Analyses Laboratory [START_REF] Croudace | ITRAX: description and evaluation of a new multi-function X-ray core scanner[END_REF][START_REF] Thomson | A geochemical application of the ITRAX scanner to a sediment core containing eastern Mediterranean sapropel units, New Techniques in Sediment Core Analysis[END_REF]. A fine-focus Mo X-ray tube was used as the source. The X-ray generator was operated at 60 kV, and a counting time of 20 s was applied. The relative elemental abundances were recorded as counts per second (cps) and their profiles were used as proxies for paleoenvironmental reconstructions. We used both element counts and element ratios; although elemental ratios are useful for normalization and elimination of systematic errors, they do not show if a change in the ratio is related to the quantity of denominator or numerator element.

Bromine is commonly used as proxy for marine organic matter and Br/TOC as proxy for the ratio of marine/terrestrial organic matter [START_REF] Mayer | The distribution of bromine on coastal sediments and its use as a source indicator for organic matter[END_REF][START_REF] Mayer | Marine vs. terrigenous matter in Louisiana coastal sediments: The uses of bromine: organic carbon ratios[END_REF][START_REF] Ziegler | Bromine counts from XRF scanning as an estimate of the marine organic carbon content of sediment cores[END_REF].

Potassium is a proxy for detrital input, in particular illite-mica type of clays, which are mainly the weathering products of rock-forming minerals during soil formation. As, a large ion lithophile (LILE or incompatible) element, K is also useful in identification of tephra layers of potassium-rich alkaline affinity, which are in particular characteristic of those generated from Italian volcanic provinces (e.g., [START_REF] Perini | Evolution and Genesis of Magmas from Vico Volcano, Central Italy: Multiple Differentiation Pathways and Variable Parental Magmas[END_REF][START_REF] Wulf | Tephrochronology of the 100 ka lacustrine sediment record of Lago Grande di Monticchio (southern Italy)[END_REF][START_REF] Çağatay | The tephra record from the Sea of Marmara for the last ca. 70 ka and its palaeoceanographic implications[END_REF].

Similarly, zircon, as high field strength element (HFSE), is useful in alkaline tephra identification (Çağatay et al., 20014, 2015). Zircon is also an indicator of coarse silt to fine sand size detrital material in marine and lake sediments. Manganese is a sensitive indicator of redox conditions; it readily precipitates as Mn-oxides in sediments deposited under oxic conditions, but remains in solution and becomes depleted in sediments of anoxic environments (e.g., [START_REF] Calvert | Geochemistry of Recent oxic and anoxic marine sediments: Implications for the geological record[END_REF][START_REF] Thomson | Redistribution and geochemical behaviour of redox-sensitive elements around S1, the most recent eastern Mediterranean sapropel[END_REF]. Iron is another redox-sensitive element, which together with sulphur, forms Fe-monosulphides (i.e., greigite, mackinawite) or pyrite by authigenesis or diagenesis in organic-rich anoxic sediments [START_REF] Leventhal | An interpretation of carbon and sulfur relationships in Black Sea sediments as indicators of environments of deposition[END_REF][START_REF] Berner | Sulfate reduction, organic matter decomposition, and pyrite formation[END_REF][START_REF] Lyons | Sulfur isotopic trends and pathways of iron sulfide formation in upper Holocene sediments of the anoxic Black Sea[END_REF]. In oxic sediments, however, Fe occurs mainly as oxyhydroxides and in clay-mineral (chlorite, illite) structures, and hence, it is considered as a detrital mineral proxy, often showing a good correlation with Ti.

Ca is a proxy of endogenic carbonate production, and has been previously used in numerous marine and lacustrine environments (e.g., [START_REF] Cohen | Paleolimnology, The History and evolution of Lake Systems[END_REF][START_REF] Francke | Sedimentological processes and environmental variability at Lake Ohrid (Macedonia, Albania) between 637 ka and the present[END_REF][START_REF] Çağatay | Lake level and climate records of the last 90 ka from the Northern Basin of Lake Van, eastern Turkey[END_REF], 2015). Strontium is an indicator of aragonite in general. In carbonate shells, Sr-Ca ratio is an indicator of salinity and temperature in marine carbonates (e.g., [START_REF] Russell | Effects of seawater carbonate ion concentration and temperature on shell U, Mg, and Sr in cultured planktonic foraminifera[END_REF][START_REF] Rosenthal | Temperature and carbonate ion effects on Mg/Ca and Sr/Ca ratios in benthic foraminifera: Aragonitic species Hoeglundina elegans[END_REF][START_REF] Schöne | Sr/Ca and Mg/Ca ratios of ontogenetically old, long-lived bivalve shells (Arctica islandica) and their function as paleotemperature proxies[END_REF]. Sr-Ca ratio is also used to discriminate between marine and terrestrial carbonates, with marine carbonates having relatively higher ratios than those in terrestrial carbonates, because of the high concentration of Sr in seawater (~70 times the average river water concentration) [START_REF] Angino | Observed variations in the strontium concentration of sea water[END_REF][START_REF] Palmer | Controls over the strontium isotope composition of river water[END_REF].

3.5. Geotek Multi-Sensor Core Logger analysis Physical properties, magnetic susceptibility and gamma density were measured at 2 cm resolution according to the standard procedures, using a Geotek Multi-Sensor Core Logger (MSCL) [START_REF] Weaver | Current methods for obtaininig, logging and splitting marine sediment cores[END_REF].

3.6. Chronological analysis and age-depth modelling 3.6.1. Accelerated mass spectroscopy (AMS) radiocarbon analysis AMS radiocarbon analyses on bivalve shell samples were carried out at Poznan Radiocarbon Laboratory, Poland. The shell samples were ultrasonicated to clean them from mud, washed in distilled water, and dried prior to the analysis. The 14 C ages of bivalve shell samples were calibrated to calendar ages using the INTCAL13 calibration curve of [START_REF] Reimer | IntCal13 and Marine13 radiocarbon age calibration curves, 0-50,000 years cal BP[END_REF] (Table 2). A reservoir age of 400 years for the upper marine unit and 1000 years for the preceding lacustrine unit were used for the calibration [START_REF] Siani | Radiocarbon reservoir ages in the Mediterranean Sea and Black Sea[END_REF][START_REF] Ryan | Status of the Black Sea flood hypothesis. The Black Sea Flood Question: Changes in Coastline, Climate, and Human Settlement[END_REF][START_REF] Kwiecien | Estimated reservoir ages of the Black Sea since the last glacial[END_REF][START_REF] Soulet | A revised calendar age for the last reconnection of the Black Sea to the global ocean[END_REF][START_REF] Çağatay | The tephra record from the Sea of Marmara for the last ca. 70 ka and its palaeoceanographic implications[END_REF]. All ages reported in this paper are reservoir corrected and calibrated to calendar years and expressed as ka BP unless otherwise stated.

3.6.2. Age data obtained by correlation of Marmara core µ-XRF Ca with NGRIP δ 18 O data It is well established that the GIs in the SoM and the Black Sea are characterized by endogenic carbonate precipitation, resulting from high primary production in surface waters (for details see [START_REF] Nowaczyk | Dynamics of the Laschamp geomagnetic excursion from Black Sea sediments[END_REF][START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF][START_REF] Çağatay | The tephra record from the Sea of Marmara for the last ca. 70 ka and its palaeoceanographic implications[END_REF]. Using the correlation of positive excursions in bulk sediment-Ca data with the onsets of GIs observed in the NGRIP δ 18 O data [START_REF] Svensson | The Greenland Ice Core Chronology 2005, 15-42 ka. Part 2: comparison to other records[END_REF][START_REF] Svensson | A 60000 year Greenland stratigraphic ice core chronology[END_REF][START_REF] Rasmussen | A new Greenland ice core chronology for the last glacial termination[END_REF][START_REF] Wolff | Millennialscale variability during the last glacial: the ice core record[END_REF], Çağatay et al. (2015) dated the core MD01-2430 in the SoM with the GICC05 time scale. In the present study, we used the same approach and wiggle-matched (tuned) the µ-XRF Ca with GIs in the NGRIP [START_REF] Svensson | The Greenland Ice Core Chronology 2005, 15-42 ka. Part 2: comparison to other records[END_REF][START_REF] Svensson | A 60000 year Greenland stratigraphic ice core chronology[END_REF] and synthetic NGIP data [START_REF] Barker | years of abrupt climate variability[END_REF] to obtain age data for cores MRS-CS18 and MRS-CS27 (Supplementary Tables S1 andS2, Fig. S1). The wiggle-matching of the SoM Ca data with NGRIP δ 18 O was made using an interactive computer software called "extended tool for correlation" (xtc), provided by courtesy of Norbert Nowaczyk (Deutsches GeoForschungsZentrum-GFZ, Potsdam, Germany) (Fig. 3).

We took special care to avoid the Ca peaks that are associated with Dreissena sp. shell debris (e.g., 2.92-3.03 mbsf interval in core MRS-CS18) and with secondary gypsum in the sapropel layers (e.g., 6.75-6.85 mbsf interval in core MRS-CS18) (Figs. 2, 3 and 6; section 4.1.2). The Dreissena sp. shells are of aragonite composition, whereas GI-related endogenic carbonate is of calcite composition which is associated with relatively high TOC values and low µ-XRF Sr counts. Despite their aragonite composition, Dreissena sp. shells are low in Sr because of the growth of shells in Sr-poor, fresh-brackish waters. The secondary gypsum is observed in the Fe-sulphide rich sapropel layers, and develops upon exposure of the split cores to atmospheric oxygen. Formation of the secondary gypsum starts with oxidation of Fesulphides near the core surface, which produces Fe 3+ , SO 4 2-and H + . The created acidity (H + ) dissolves carbonates and produces Ca 2+ that combines with SO 4 2-to form in situ the secondary gypsum (Çağatay, unpublished data). The µ-XRF measured Ca content at a specific location at the core surface would be mainly conservative, or only slightly magnified, because of the in situ formation of gypsum at or near the surficial site of the oxidizing pyrite. The gypsum could incorporate up to 0.2 % Sr [START_REF] Ichikuni | Partition of strontium between gypsum and solution[END_REF], and hence Ca anomalies due to the presence of secondary gypsum are accompanied by relativley high Sr counts.

Tephrochronology and sapropel age data

Distinct tephra layers observed in cores MRS-CS27 and MRS-CS18 were analysed for elemental composition by Itrax µ-XRF core scanner and for gamma density and MS by Geotek MSCL (Figs. 2, 5 and 6; sections 3.1 and 3.2). Using these general geochemical and physical properties and their stratigraphic positions, these layers are correlated with the well-known tephra layers (i.e., Marmara tephra, MT-1 and MT-2), previously documented in detail and correlated to their sources (i.e., Cape Riva eruption of Santorini and the Campanian Ignimbrite, respectively) by Çağatay et al. (2015) (Figs. 2, 5 and 6; Table S1 andS2). In addition, the onset and termination ages of the main Holocene Marmara sapropel (MSAP-1) were used for core MRS-CS27 (Çağatay et al., 2015) (Table S2).

Age-depth modelling

The age-depth models of the studied cores were constructed using all the age data, explained in sections 3.6.1 to 3.6.3, listed in Tables S1 andS22 and plotted in Fig. S1 of the Supplementary Information (Figs. 4a andb). For the construction the R-studio and the script "CLAM" [START_REF] Blaauw | Methods and code for 'classical' age-modelling of radiocarbon sequences[END_REF] was used. The script creates non-Bayesian, cubic spline age-depth model, calculating the %95 Gaussian confidence interval around the best model.

Results

Lithology, paleontology, geochemistry and physical properties

The lithological and paleontological description of the studied cores, together with the TOC contents, are presented as lithological logs in Figs. 2 and7, and their geochemistry is illustrated as element and element-ratio profiles in Figs. 5, 6 and 8. The detailed description and interpretations, based on the lithological, paleontological and geochemical data, are provided for each core below.

Core MRS CS-27

The core consists essentially of two marine units and an intervening lacustrine unit, based mainly on the fossil content (Fig. 2). The upper marine unit include a homogeneous olive gray clay (Munsell colour scale: 5Y5/2) from top to 0.45 mbsf and olive grey to dark olive grey (5Y4/2, 5Y3/2) sapropel (Marmara Sapropel-1, MSAP-1) between 0.45 and 2.15 mbsf, which contains up to 5.8 % TOC (Fig. 2). The MSAP-1 is commonly laminated with distinct laminations in its lower part from 1.85 to 2.15 mbsf, and shows some bioturbation in its upper 0.185 m and middle (0.80-1.09 mbsf) parts. The marine unit including the MSAP-1 contains benthic (mostly Bolivina sp., Bulumina and Brizalina sp.) and pelagic (mainly Globigerina sp.) foraminifera, echinoid spicules and juvenile bivalves. The MSAP-1 is also enriched in spores and spore aggregates and rare plant remains. The sand (>62 µm) fraction in the lower part of MSAP-1 contains some 0.5-1 mm euhedral, secondary gypsum crystals.

The marine unit is characterized by relatively low gamma density (<1.5 g/cm 3 ) and magnetic susceptibility (MS <50 SI) and high µ-XRF Br counts (up to 230 cps), especially in the MSAP-1 interval. The upper part of the marine unit including the upper part of MSAP-1 is also characterized by relatively high Br-TOC ratio (>60), whereas the lower part of MSAP-1 is lower in Br-TOC ratio than the upper marine and lower lacustrine units (Fig. 5). The MSAP-1 shows an upward decreasing gamma density and low magnetic susceptibility compared to the rest of the upper marine unit (Fig. 5).

The latest lake/marine transition occurs from 2.65 mbsf to 2.15 mbsf, and is characterized by a high µ-XRF Ca, with another smaller Ca peak at 2.95 mbsf (Fig. 5). This interval is a grey (Gley1 5/10Y) mud with black Fe-monosulphide spots, and contains a rich population of bivalve shells and shell fragments. The bivalve population consists of a mixture of juvenile marine and brackish-freshwater bivalves (e.g. Turritella sp., Turricaspia sp., Dreissena sp.). The sand fraction of the lower part of interval contains faecal pellets, 1-2 mmsize pyrite concretions and euhedral to subhedral secondary gypsum crystals.

The lacustrine unit below the latest lake/marine transition is 15.03 m-thick homogeneous grey (5Y5/1 to 5Y54/1) mud (Fig. 2). The upper part of this unit between 2.65 and 4.05 mbsf is enriched in Fe-monosulphide (FeS) spots between and small (1-3 mm) white bivalve (mostly Dreissena rostriformis) shell fragments. The FeS-rich upper part of the unit, as well as the carbonate-rich transitional interval, is high in MS (up to 450 SI) and downward increasing gamma density. The lacustrine unit contains up to 10 mm-thick laminae and beds of shell debris (fragments) at 2. 98, 10.825, 12.168, 12.273, 13.013, 13.088 and 13.173 mbsf. Some levels contain up to 20 mm thick silt lenses (e.g., 13.86-13.89, 14.14-14.17, 14.25-14.28, 15.78-15.88 mbsf). The interval from 14.20 to 15.80 mbsf is homogeneous olive grey mud (gley1 4/10Y) with high µ-XRF Ca counts (up to 7000 cps) and relatively high TOC contents (up to 2.1 wt%) (Figs. 2 and5). Below this carbonate-and TOC-rich layers, small correlative peaks of Ca and TOC occur until a 3 cm-thick, well sorted, medium to fine grade sand layer with an erosional basal contact at 18.83 mbsf above a marine unit. The lacustrine unit contains µXRF Ca peaks at 2. 85 mbsf, 4.40, 4.75, 5.00, 5.10, 5.35, 5.75, 6.40, 9.45, 11.90, 12.70, 13.85, 14.25, 14.85, a large peak between 15.75 and 15.90 mbsf, at 16.75 mbsf, 17.0 mbsf and 17.50 mbsf. Some of these Ca peaks (e.g., 12.70, 14.25, 14.85 mbsf) correspond to shell-rich (mostly Dreissena rostriformis) horizons and are characterised by high Sr-Ca ratio (Fig. 5). Most Ca peaks, including the large Ca peak in the 15.75-15.90 mbsf interval and in the lake/marine transition zone (2.65 mbsf to 2.15 mbsf), are low in Sr and Sr-Ca ratio. The Br content and Br-TOC ratio of the lacustrine unit are low compared with the upper part of latest marine unit, with some relatively high and fluctuating values of Br-TOC ratio in 2.25-5.50 mbsf and 12.7-14.0 mbsf intevals (Figs. 6 and8a).

The lacustrine unit contains two distinct tephra layers (Marmara Tephra, MT-1 and MT-2) at 6.955-7.005 mbsf and 13.835-13.88 mbsf intervals, each ~ 50 mm in thickness. A cryptotephra (MT-3) is present at 16.18 mbsf, which consists of dispersed fine-sand-size glass shards and plagioclase crystals in a 2 mm-thick layer. It has high MS values (~360 IS) and high Ca (~3000 cps), with no particular enrichment in µ-XRF K and Zr. The presence of abundant plagioclase and relatively high Ca in this tephra suggests its calc-alkaline affinity.

MT-1 is brownish gray (10YR6/1 to 10YR4/2) with some dark laminae and a sharp basal boundary, and shows normal size grading. It is low in Zr (~400 cps) and K, and characterized by low gamma density (1.5 g/cm 3 ) and a high MS (450 SI) (Fig. 5). MT-2 is grey (5Y6/1) with sand size glass shards. It is enriched in µ-XRF K (1400 cps) and Zr (750 cps), and has a relatively high gamma density (1.8 g/cm 3 ) and low to moderate MS (~350 SI) (Fig. 5).

Considering their stratigraphic position, AMS radiocarbon ages, geochemical composition and MSCL physical properties, we correlate MT-1 and MT-2 with the tephra layers that were previously documented in the SoM cores, and correlated by Çağatay et al. (2015) with the Cape Riva eruption of Santorini and Campanian Ignimbrite (CI). The Santorini Cape Riva eruption (MT-1) and the CI (MT-2) are dated at 21.98±0.88 ka BP [START_REF] Pichler | Radiocarbon dates of Santorini volcanics[END_REF][START_REF] Pichler | Radiocarbon dates of Santorini volcanics[END_REF]39.28±0.11 ka (DeVito et al., 2001;[START_REF] Pyle | Wide dispersal and deposition of distal tephra during the Pleistocene 'Campanian Ignimbrite/Y5' eruption, Italy[END_REF], respectively. The crypto tephra MT-3 is not characterized by any distinct element anomalies, such as K and Zr, and is not so far correlated with its volcanic source.

Between 17.68 and 17.83 mbsf, the basal part of the lacustrine mud unit is a 15 cmthick, normally graded, fine sand to coarse silt layer (Fig. 2). This basal layer contains mm-size Dreissena sp. shell fragments and has a sharp erosional basal boundary. The second marine unit below includes two sapropels, MSAP-2 and MSAP-3, with an intervening 0.47 m thick lacustrine unit between 19.60 and 20.07 mbsf.

The MSAP-2 is 1.59 m thick, distinctly laminated, olive grey, very dark green to very dark greyish brown (5Y4/2, Gley1 3/10Y, 10YR 3/2) mud with up to 5.5 wt% TOC. The upper part of the MSAP-2 contains echinoid spicules, juvenile marine bivalve and <1 mm size pyrite concretions. MSAP-2 has a relatively low gamma density (<1.4 g/cm 3 ), low MS (<50 SI) and high µ-XRF Br (up to 170 cps), low Br-TOC ratio (<40) and high S-Ti ratio (Figs. 5 and8a). It also shows high µ-XRF Ca counts (up to 700 cps) in its lower part between 18.9 and 19.45 mbsf. The lacustrine unit between MSAP-2 and MSAP-3 is grey (5Y4/1), locally laminated mud with FeS spots, Dreissena sp. shell fragments and mm-size secondary euhedral gypsum crystals. This unit contains a 45 mm-thick, graded sand to silt bed and is characterized by relatively low (0.5-2 wt%) TOC values, high Sr-Ca ratio, moderate µ-XRF Zr (~200 cps), locally high µ-XRF Mn and local µ-XRF Ca peaks in its upper part (Fig. 5). The MSAP-3 between 20.07 mbsf to the base of the core is a dark olive grey laminated mud representing part of a sapropel unit. It contains up to 3.9 wt% TOC and is devoid of any macro-and micro-fossils.

The sand fraction of the MSAP-3 contains abundant euhedral mm-scale secondary gypsum crystals. It is relatively higher in K and Br than the MSAP-2 and MSAP-1 and has high S-Ti ratio (Fig. 5).

Core MRS CS-18

The core consists mainly of two lacustrine units separated by a marine unit (Fig. 2). The uppermost lacustrine unit is a 3.65 m thick homogeneous greenish grey, grey, to dark grey (5Y5/1 to 5Y54/1, gley 14/10Y) mud, containing fresh/brackish water bivalve (mainly Dreissena rostriformis) shells and shell fragments, which are relatively abundant at 0.175, 0.30, 0.50, 0.71, 0.745, 0.98, 1.12-1.155, 1.56, 1.643-1.68, 1.79-1.83, 1.935, 2.015-2.19, 3.06-3.64 mbsf (Fig. 2). There is a fine sand of 1 cm thickness between 3.64-365 mbsf with sharp upper and erosional lower contacts. The lacustrine unit contains two 1-2 mm-thick iron monosulphide (FeS) laminae at 1.20 and 1.85 mbsf and FeS spots at 120-124, 1.405-1.44, 2.533-2.61, and 2.85 mbsf, which display high MS values between 1.20 and 3.0 mbsf. It is faintly laminated dark grey mud (gley 1 4/10Y) between 2.35 and 3.05 mbsf and has a high density (>1.7 g/cm 3 ) in its lower part between 2.70-3.64 mbsf (Fig. 6). This lacustrine unit is characterized by lower TOC (mostly <1 wt %), lower Br (<150 cps) and higher Br-TOC ratio (>90) than those in the underlying marine unit (Figs. 6 and8b).

An 80 mm-thick brown ash layer is observed between 2.13 and 2.21 mbsf. It is characterized by high MS, high µ-XRF K (1050 cps) and Zr (~600 cps) counts and relatively low gamma density. With its geochemical and physical properties and stratigraphic position, it is similar to tephra layer MT-2 in core MRS-CS27, and is therefore correlated with the CI having an age 39.28±0.11 cal ka (DeVito et al., 2001;Pyle et al., 2006) (Figs. 2, 5 and 6). A dark grey silty mud layer between 3.07 and 3.09 cm displays high Ca-Ti ratio (~35) and low Fe-Mn ratio (~30) (Fig. 6). A faintly grey, 2 mm thick layer centred at 309.5 cmbsf is a crypto tephra with the presence of fine to very fine sand size glass fragments and plagioclase crystals. This tephra layer is characterized by a relatively high MS (~300 IS), high density (~1.8 g/cm 3 ) and low Sr-Ca ratio, and correlated with MT-3 observed in core MRS-CS27, based on its stratigraphic position and physical-chemical properties (Fig. 2).

The marine unit below the upper lacustrine unit is 4.05 m thick between 3.65 and 7.70 mbsf, interrupted by a 0.23 m-thick brackish lacustrine interval between 4.37 and 4.60 (Fig. 2).

The marine unit includes three sapropel layers, MSAP-2, MSAP-3 and MSAP-4, with TOC contents ranging from 2 to 4.9 wt % (Fig. 2). The upper sapropel unit, MSAP-2 between 3.65 and 4.37 mbsf, is an olive grey laminated sapropel (MSAP-2) with TOC contents of up to 3.7 wt % and low density and MS values (Figs. 2 and6). There is a lack of micro and macro fossils in this unit, except for a translucent juvenile marine bivalve at 4.15 mbsf and a few echinoid spicules. The sand fraction in MSAP-2 contains abundant well developed secondary gypsum crystals and pyritized faecal pellets. The lacustrine interval between MSAP-2 and MSAP-3 consists of a homogeneous dark greenish grey mud with less than 1.30 wt % TOC. It contains abundant Dreissena sp. shell fragments, ostracoda, rare gastropods (Turricasipa sp., one reworked Turritella sp. shell) (Fig. 7), faecal pellets, <1-mm size pyrite nodules, and some secondary euhedral gypsum crystals. This lacustrine unit in core MRSCS18 is correlated with the similar lacustrine unit in cores MRS CS27 in the same stratigraphic position (Fig. 2).

The sapropel layer MSAP-3 between 4.60 to 5.78 mbsf is a greenish grey to olive grey finely laminated mud containing up to 3.67 wt % TOC (Fig. 2). It has sharp upper and lower boundaries, marked with the occurrence of sand beds, with erosional bottom contacts. The sand at the base of MSAP-3 is 6-7 cm-thick, a dark green graded medium-grained sand layer, enriched in benthic foraminifera and shell fragments, whereas the one at the upper boundary is 1 cm-thick fine-grained sand. The MSAP-3 is devoid of any foraminifera, but contains abundant spores, rare echinoid, sponge spicules and Turritella sp. and some 1-2 mm euhedral gypsum crystals (Fig. 7). The interval between MSAP-3 and MSAP4 (5.80 and 6.30 mbsf) is a homogeneous, dark greenish grey mud, with relatively low (1.44-2.5 wt %) TOC values. This marine interval contains a very rich and diverse population of benthic foraminifera including Bolivina sp., Bulumina sp., Brizalina sp., Cassudilina sp., Elphidium sp., Nonion sp., Uvigerina sp. and Textularia sp. (Fig. 7). It also includes marine bivalves and pelagic foraminifera (mainly Globotrancana sp.), and is locally enriched in secondary euhedral gypsum crystals. The MSAP-4 between 6.30 and 7.01 mbsf contains the highest TOC contents with up to 4.9 wt %. It is greenish grey to olive grey mud that is faintly laminated in the upper part and distinctly laminated in the lower part. The upper faintly laminated part is devoid of foraminifera and bivalve fauna, whereas the middle distinctly laminated part from 6.55 to 6.85 mbsf includes a diverse benthic foraminiferal fauna, some pelagic foraminifera (mainly Globigerina sp.) (Fig. 7), and abundant secondary gypsum crystals. The lowest part of the sapropel from 6.85 to 7.01 mbsf is characterized by a very scarce marine fauna. The marine unit between 7.01 and 7.70 is a dark green grey to green grey sapropelic mud with TOC contents of 1.4-2.3 wt%. This part contains sparse fossil content consisting of mainly Elphidium sp. and Brizalina sp, Echinoid spicules and ostracods, with some pyritized faecal pellets and euhedral secondary gypsum crystals (Fig. 7).

The marine unit displays a relatively high µ-XRF Br counts (up to 185 cps), especially in the sapropel layers, with Br and S profiles paralleling that of the TOC (Fig. 6). The highest TOC interval MSAP-4 is characterized by the highest µ-XRF Br and S counts and high µ-XRF Ca and Sr counts (both ~7000 cps) and high Sr-Ca ratio, and low but upward increasing Br-TOC ratio (Figs. 2, 6 and8b). The MSAP-2 and MSAP-3 layers show and upward decreasing Br-TOC ratio. The low TOC interval of the marine unit between 5.65 and 6.15 mbsf has low Br (~65-125 cps), and displays relatively high µ-XRF Ca and K counts (600 cps) and low Br-TOC ratio. The sapropel layers have a relatively low gamma density and MS, except for the low TOC part of MSAP-3 which is relatively high in gamma density.

The unit from 7.70 mbsf down to the base of the core at 14.05 mbsf is homogeneous greenish grey lacustrine mud which contains less than 1.2 wt % TOC (Fig. 2). The unit commonly contains scattered bivalve (mostly Dresissena rostriformis) shells and shell fragments, ostracoda and pyritized faecal pellets and boring-infills. Some cm-thick intervals (e.g., 9.61, 10.70 and 12.25 mbsf) are enriched in white sand-size Dreissena sp. shell fragments, which commonly correspond to positive Ca excursions (Fig. 6). The interval including the lake/marine transition between 7.87-7.40 mbsf is also characterized by relatively high Ca counts (up to 3700 cps), Mn (up to ~500 cps) and a sharp S peak with up to 205 cps. The upper part of the lacustrine unit and the transition zone have high magnetic susceptibility, which corresponds to the dark grey to black FeS spots and bands. At 13.27-13.38 m interval, an unidentified cryptotephra characterized by high K counts (up to 850 cps) is observed. This crypto tephra with sparse volcanic glass shards in about an 11 cm-thick sediment layer has a slightly higher density (2.0 g/cm 3 ) than the surrounding background sediments, with no MS expression only slight enrichment in Zr. The layer also contains partially sericitized feldspars, polycrystalline and microcrystalline quartz grains.

Chronology

The constructed age-depth model of the cores (Fig. s 4a andb), are in good agreement with the independently dated regional terrestrial records, such as those from the Lake Ohrid (Fig. 1a), located along the same latitudinal zone and affected by continental and Mediterranean climatic conditions. The TOC data sets of the studied cores MRS-CS18 and MRS-CS27, plotted with the NGRIP time scale, and the Lake Ohrid TOC data set, which is age-calibrated by tephrochronology (11 tephra layers) and by cross-correlation of geochemical proxy data with orbital parameters [START_REF] Francke | Sedimentological processes and environmental variability at Lake Ohrid (Macedonia, Albania) between 637 ka and the present[END_REF] show excellent correlation (Fig. 3), suggesting the robustness of the age models for the studied cores (see also section 5.3 and Fig. 8 therein).

Chronology of Core MRS-CS27

According to the age-depth model, the basal part of core MRS-CS27 reaches 94.52±1.35 ka BP, and the core includes a hiatus between 68.58 and 74.01 ka BP (Fig. 4a). This hiatus is represented by 15 cm-thick thick normally graded sand layer with an erosional basal boundary (Fig. 2). It is characterized by a sharp change in the density, magnetic susceptibility and geochemical parameters such as TOC (Fig. 5). The hiatus corresponds to the distinct reflection surface in high resolution seismic profiles (Fig. 1c), which is labelled as the "Red" surface by [START_REF] Sorlien | Uniform basin growth over the last 500 ka, North Anatolian Fault, Marmara Sea, Turkey[END_REF] and [START_REF] Grall | Slip rate estimation along the western segment of the Main Marmara Fault over the last 405-490 ka by correlating mass transport deposits[END_REF]. It is characterized by a distinct negative polarity in the synthetic seismograms because of the sharp density contrast between the lacustrine sediment above and the sapropel below (Kende et al., in review). The lacustrine unit between the MSAP-2 and MSAP-3 has an age spanning between 92.32±0.88 and 86.60±3.17 ka BP. The cryptotephra MT-3 (16.18 cmbsf) with a presently unidentified source, is dated at 57.02±2.90 ka BP.

The sedimentation rate for the late MIS5 (94.5-74 ka BP; 140 mm/kyr) is higher than that for MIS4-MIS3 (110 mm/kyr but much lower than that for MIS2 (620 mm/kyr).

Chronology of core MRS-CS18

The age-depth model of core MRS-CS18 shows that of the core section extends from 26.4 to 173.1 ka BP, with two hiatuses at 3.65 and 5.78 mbsf (Fig. 4b). The upper hiatus is represented by 1 cm-thick fine sand with a sharp erosional boundary, and characterized by a sharp change in density, MS, TOC, Br and Zr (Fig. 6). It is ~9 ka-long hiatus spanning from 79.28±1.00 to 70.08±0.96 ka BP during which the record of GI 19, GI 20 and later part of GI 21 is missing (Figs. 3a,c,f). As in core MRS-CS27, this hiatus is located between the lacustrine sediment above and the sapropel below, and matches the distinct reflecting surface in the seismic profile in Fig. 1D and the "Red" reflecting surface of [START_REF] Sorlien | Uniform basin growth over the last 500 ka, North Anatolian Fault, Marmara Sea, Turkey[END_REF] and [START_REF] Grall | Slip rate estimation along the western segment of the Main Marmara Fault over the last 405-490 ka by correlating mass transport deposits[END_REF]. The lower hiatus at 5.78 mbsf is represented by the 5-6 cm-thick normally graded sand layer, and corresponds to a sharp change in density, MS, TOC, Br and K. The hiatus corresponds to ~5 ka long gap from 108.20±0.97 to 103.36±0.91 ka BP, which covers the period of GI 24 (Figs. 3a,b,e). The 1 cm-thick very fine sand, marking the upper boundary of MSAP-3 at 4.60 cmbsf (~92 ka BP), does not represent a significant hiatus according to the correlation with the NGRIP oxygen isotope data and the age-depth model (Figs. 3 and4).

The crypto-tephra MT-3 at 309.5 cmbsf in core MRS-CS18 is dated at 57.77±1.00 ka BP, and the lake/marine transition of the SoM during the penultimate glacial/interglacial transition (i.e. MIS6/MIS5 transition) took place at ~134.06±1.10 ka BP. The sapropel units MSAP-2, MSAP-3 and MSAP-4 with TOC contents greater than 2 wt % were deposited during 87.16±0.98 -79.28±1.00 ka BP (hiatus), 103.36±0.91 (hiatus) -91.95 ±0.74 ka BP and 131.17±1.02 -112.25±1.37 ka BP, with an intervening relatively low TOC (2-2.5 wt%) interval between MSAP-4 and MSAP-3 during 112.25 -108.20 ka BP. The lacustrine interval with relatively low TOC values (< 2 wt %) is dated between 79.28 (hiatus) -87.16 ka BP, and the potassium-rich tephra near the base of the core at 160.61±0.79.

The sedimentation rate for MIS5 and MIS6 in core MRS-CS18 are 90 mm/ kyr and 145 mm/kyr, respectively (Fig. 4b). A sharp change in sedimentation rate occurs at ~40 ka BP, with the rate increasing from 45 mm/kyr between 71 ka and 40 ka BP to 170 mm/kyr between 40 and 27 ka BP. A decrease in the sedimentation rate is observed for the period between ~160 and ~166 k BP near the bottom of the core.

Correlation of cores MRS-CS18 and MRS-CS27 with cores MRS-CS22 and MD04-2745

Using the lithology and fossil content, the stratigraphic units in lower part of cores MRS-CS18 and MRS-CS27 of the İmralı Basin can be correlated with those in core MRS-CS22 from the Western High studied by Kende et al. (in review) (Fig. 2) and the units in the latter core can be dated using the age-depth model of core MRS-CS18. The lowest foraminifera-rich part of core MRS-CS22 below 19.3 mbsf is correlated with a lithologically and paleontologically similar marine unit of MIS5d age in core MRS-CS18 (Figs. 2 and7). Hence core MRS-CS22 in its lower part includes a sedimentary section covering the periods of MIS5d to MIS5a (~116 -70 ka BP). The overlying unit between 18.3 and 19.3 in core MRS-CS22 is a sapropel with TOC contents of up to 3 wt % and can be matched with sapropel MSAP-3 of MIS5c age in İmrali cores (Fig. 2). The interval between 16.8 and 18.3 mbsf is low in TOC and is tentatively correlated with the lacustrine unit corresponding to MIS5b in the İmralı cores, although the lacustrine nature of the unit in core MRS-CS22 has not yet been established (Kende et al. in review). This presumably brackish unit is overlain by a sapropel unit between 15.5 and 16.8 mbsf according to its TOC content (>2 wt %). This sapropel is correlated with the MSAP-3 in the İmralı cores. Finally, the interval between ~14.0-15.5 mbsf in core MRS-CS22 below the hiatus is deposited under brackish conditions, based on the absence of alkenones (Kende et al., in review). However, this unit is likely to have been deposited during marine connection of the SoM, with a strong Black Sea outflow forming a brackish surface water.

The stratigraphy of MIS5 in core MD04-2745 recovered from -98 on the northern shelf edge in the SoM (for location see Fig. 1b) (Çağatay et al., 2009) and İmrali cores MRS-CS18 and MRS-CS27 can be correlated, with the presence the two sapropel layers, MSAP-2 (MIS5a) and MSAP-3 (MIS5c), and the intervening lacustrine unit (MIS5b), in all the cores. The unit below MSAP-3 with 1-1.5 % TOC in core MD04-2745 likely represents MIS5d, observed in the İmrali cores.

Discussion

Timing of the Aegean and Black Sea connections and hydrological changes during MIS5 and MIS6

The paleontological data, together with the age model for studied cores and MRS-CS27, shows that the SoM was connected with the Aegean Sea for most part of the MIS5, except between ~93.9-87.2 ka (in core MRS-CS18) or between 92.4-86.6 ka BP (in core MRS-CS27), during which the connection was disrupted for 6-7 ka. This lacustrine unit deposited in this interval corresponds to the stadial MIS5b, which spans from 92 to 87 ka BP according to [START_REF] Martrat | Abrupt temperature changes in the Western Mediterranean over the past 250,000 years[END_REF]. This age interval is therefore in agreement with our model age for this stratigraphic interval in the studied cores. The SoM was disconnected also between 173 and 134 ka BP, which includes the MIS6. The marine connection of the SoM during the Termination II (MIS6/MIS5 transition) took place at 134.0±2.1 ka BP, according to our age model of core MRS-CS18 (Fig. 4).

The timings of these events in the SoM are in general agreement with the U/Th-dated speleothem oxygen isotope data from Sofular near the SW Black Sea coast in NW Anatolia, which shows relatively high δ 18 O values over the periods of marine connections (i.e., during MIS5 interstadials e, c, and a) and low values during the marine disconnections (i.e, MIS5 stadials b and d) of the Black Sea, resulting mainly from the source-water effect (Baderstcher et al., 2011). The only disparity between environmental conditions in the SoM and Black Sea is found for MIS5d, during which marine conditions in the former basin and lacustrine conditions in the latter prevailed. This implies that the sea level remained below the Bosporus sill at that time to prevent the passage of marine waters to the Black Sea "lake". This conclusion is supported by the sea level curve of [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF] (Fig. 8d), which shows a sea-level below -40 m (the present sill depth of Bosporus) during the main part of MIS5d.

Based on paleontological evidence, however, different depositional conditions have been suggested for the Black Sea during MIS5. For example, [START_REF] Zubakov | Climatostratigraphic scheme of the Black Sea Pleistocene and its correlation with the oxygen isotope scale and glacial events[END_REF] shows marine conditions during MIS5 interstadials c and e, while [START_REF] Svitoch | Paleohydrology of the Black Sea Pleistocene basin[END_REF] determined marine conditions only during MIS5a. For MIS6, [START_REF] Zubakov | Climatostratigraphic scheme of the Black Sea Pleistocene and its correlation with the oxygen isotope scale and glacial events[END_REF] shows the existence of lacustrine conditions in the Black Sea, whereas [START_REF] Svitoch | Paleohydrology of the Black Sea Pleistocene basin[END_REF] suggests marine conditions during ~170-150 ka BP (MIS6). [START_REF] Svitoch | Paleohydrology of the Black Sea Pleistocene basin[END_REF] findings are in disagreement with our data from the SoM as well as with the Sofular speleothem data from SW Black Sea coast in NW Anatolia (Baderstcher et al., 2011), which show no marine connection neither for the SoM nor for the Black Sea at that time.

Considering the global sea level curve of [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF] (Fig. 8d), the marine connection of the SoM at ~134 ka BP and the disconnection during MIS5b would occur if the sill depth of the Dardanelles Strait was below ~ -80 m (i.e., lower than the present sill depth of -65 m) during Termination II. A similar sill depth of -84 m for the Dardanelles Strait existed during Termination I, as testified by the widespread existence of paleoshorelines of the Marmara "Lake" in the form of berms and wave-cut notches, which are dated at ~12.5 cal ka BP [START_REF] Çağatay | Sea-level changes and depositional environments in the Izmit Gulf, eastern Marmara Sea, during the late glacial-Holocene period[END_REF], 2009;[START_REF] Polonia | Holocene slip rate of the North Anatolian Fault beneath the Sea of Marmara[END_REF][START_REF] Eriş | Late glacial to Holocene sea-level changes in the Sea of Marmara: new evidence from high-resolution seismics and core studies[END_REF]. This implies that the Dardanelles Strait's sill depth during the glacial periods was deeper than that during the interglacial periods, probably due to fluvial down-cutting under a relatively low base level; the isostatic effect of increased water column on the strait's channel after the marine reconnection is estimated to be negligible because of limited width of the strait [START_REF] Smith | High resolution seismic reflection profiling in the Sea of Marmara (northwest Turkey): late Quaternary sedimentation and sea-level changes[END_REF].

The Sr-Ca and U-Ca ratios of ostracod shells [START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF] and marine dynocysts distribution (Shumilovskikh et al., 2013b) indicate that marine reconnection of the Black Sea occurred at 128.1 ±0.7 ka BP, during Termination II (Fig. 8e). The timing of this marine reconnection is ~6 ka later than marine reconnection of the SoM at ~134.0±2.13 ka BP. During Termination I (MIS2/MIS1 transition), the initial marine reconnection of the SoM started at 14.7 cal 14 C kyr BP [START_REF] Vidal | Hydrology in the Sea of Marmara during the last 23 ka: Implications for timing of Black Sea connections and sapropel deposition[END_REF] and the full connection with the appearance of Mediterranean euryhaline fauna occurred at 12.56 ka BP (Çağatay et al., 2015). This was followed by the initial marine reconnection of the Black Sea at 9.4 cal 14 C kyr BP [START_REF] Major | The co-evolution of Black Sea level and composition through the last deglaciation and its paleoclimatic significance[END_REF][START_REF] Ryan | Status of the Black Sea flood hypothesis. The Black Sea Flood Question: Changes in Coastline, Climate, and Human Settlement[END_REF][START_REF] Bahr | Abrupt changes of temperature and water chemistry in the late Pleistocene and early Holocene Black Sea[END_REF] or 9 cal 14 C ka BP [START_REF] Soulet | A revised calendar age for the last reconnection of the Black Sea to the global ocean[END_REF], and the colonization of the sea with the Mediterranean marine fauna around 7.5 cal 14 C kyr BP [START_REF] Ryan | Noah's Flood: The New Scientific Discoveries About the Event that Changed History[END_REF]. Hence, time lag between the marine connections of the Black Sea and SoM during Termination I ~5 ka, which is similar to the time lag during the Termination II. As discussed by [START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF], the timing of connections of the Black Sea during Terminations I and II are compatible with the present sill depth of the Bosporus at -35 to-40 m.

The MIS5 period with its sapropels is characterized by a low sedimentation rate of ~10.5 mm/kyr, which is similar to the sedimentation rate for MIS4, but lower than that for MIS2, MIS3 and MIS6. Despite the warm and high precipitation conditions during MIS5, the relatively low sedimentation rate can be explained by the dense vegetation cover resulting in low erosion rates in the catchment area and the high sea levels causing the landward migration of the coastline and increase in relative distance of the core site from the sediment source (river mouths on the southern coastline). Accordingly, the detrital input varied in conformity with stadial and interstadial oscillations within the MIS5, as indicated by variations in the K profile (Fig. 6). For example, high detrital mineral input, in the form of illite clay, occurs during the period of 111.5-108 ka BP (stadial MIS5d), whereas this input decreases during 128.5-112.9 ka BP (mainly interstadial MIS5e) and Termination II (Fig. 6), which can be explained by changes in precipitation, vegetation density and sea level, as explained above. High K counts also occurs during 150-135 ka BP, which is likely due to low lake levels during the stadial period, when the coastline and river mouths migrated closer the core site.

However, high K counts in the Black Sea record were previously interpreted as evidence of glacier melt-water inputs from the European ice sheets arriving in the Black Sea mainly from the Caspian Sea via the Manych-Kerch Strait [START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF]. [START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF] detected two such melt water pulses in the Black Sea during Termination ka BP) by high K/Al of the bulk sediments and the very low Sr/Ca of ostracod shells. Other melt-water pulses in the Black Sea during various global warming (interstadial) events have been also documented [START_REF] Mangerud | Ice-dammed lakes and rerouting of the drainage of northern Eurasia during the Last Glaciation[END_REF][START_REF] Chepalyga | The late glacial great flood in the Ponto-Caspian Basin[END_REF][START_REF] Bahr | Abrupt changes of temperature and water chemistry in the late Pleistocene and early Holocene Black Sea[END_REF]Baderstcher et al., 2011;[START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF]). For example, Baderstcher et al. (2011) correlated negative δ 18 O values of -13 to -17.5 per mil in the Sofular speleothem in NW Anatolia, with melt water inputs in the Black Sea during 16.5-14.5, ~135, and 175-180 ka BP; the first two correspond to transitions before the Terminations I and II. Evidence of similar warming events, with positive excursions of Ca, MS, density, and K, are also present in in the SoM records during MIS5 and MIS6 (Figs. 6 and7), suggesting high detrital input. However, the source of the detrital input cannot be unequivocally attributed to the Black Sea outflow events in the SoM using the presently available proxy data.

Marine Isotope Stage 5 sapropels

Three sapropel units (MSAP-4, MSAP-3 and MSAP-2) with TOC values greater than 2 wt% were deposited during MIS5, which correspond mainly to the interstadial sub-stages e, c, and a (Fig. 2). However, the upper part of MSAP-2 is missing in both studied cores due to the hiatuses. The formation of this hiatus can be explained by sliding and slumping of sediments over the weak substrate of the sapropel during a period of low sea level (e.g., [START_REF] Kopf | Marine deepwater free-fall CPT measurements for landslide characterisation off Crete, Greece (Eastern Mediterranean Sea) Part 2: Initial data from the Western Cretan Sea[END_REF], which would be especially the case in core MRS-CS18, with its location on a slope and with its hiatus representing a longer time span than that in core MRS-CS27 (Fig. 1d).

Sapropel layers are well defined by µ-XRF Br, mirroring the TOC profiles with similar positive excursions (Figs. 5 and6). This indicate the strong association between Br and the marine organic matter, as has been documented in previous studies [START_REF] Mayer | The distribution of bromine on coastal sediments and its use as a source indicator for organic matter[END_REF][START_REF] Mayer | Marine vs. terrigenous matter in Louisiana coastal sediments: The uses of bromine: organic carbon ratios[END_REF][START_REF] Ziegler | Bromine counts from XRF scanning as an estimate of the marine organic carbon content of sediment cores[END_REF]. Sapropel layers in the SoM are characterized by relatively low Br/TOC values compared to the lacustrine sediments of MIS -2 to MIS-4, except for the upper part of MSAP-1 and the uppermost marine unit in core MRS-CS27 (Fig. 6). In MSAP-3 and MSAP-2, there is a relative upward decrease in Br/TOC values, suggesting an increasing contribution of terrestrial organic matter with decreasing age, whereas a reverse (upward increasing) trend is observed for MSAP-4 (MIS5e)(Fig. 6). The Br/TOC profile shows high values for the lacustrine period from ~70 ka BP (end of hiatus) to 26.40 ka BP (core top) in core MRS-CS18, with a very high peak at 53.2 ka BP (Fig. 6). The much higher ratio during the lacustrine MIS4-MIS3 than that for the lacustrine MIS6 is due to the relatively higher Br and lower TOC vales during the former period (Fig. 6). The high Br values during MIS4-MIS3 sediments are in turn likely due to algal organic matter production under brackish water conditions, because the freshening of the SoM was slow, with partial continuation of marine conditions after the MIS5, as suggested by the oxygen isotope analysis (Çağatay et al., 2009) and modelling studies, based on pore-water analysis [START_REF] Aloisi | Freshening of the Marmara Sea prior to its post-glacial reconnection to the Mediterranean Sea[END_REF]. On the other hand, low Br (average: ~100 cps) and relatively high TOC values (0.4-1.5 %), with low Br/TOC values (<50), during MIS6 imply relatively high terrestrial organic matter input under fresh water conditions (Fig. 5).

The high S enrichment just below the lacustrine/marine transition, prior to each sapropel deposition in the SoM is similar to the one observed immediately below the Mediterranean sapropels [START_REF] Passier | Diagenetic pyritisation under eastern Mediterranean sapropels caused by downward sulphide diffusion[END_REF]; this enrichment results from the formation of pyrite by reaction of the downward diffusing HS -from the marine sediments with the upward diffusing Fe 2+ from the underlying lacustrine sediments.

The first marine species such as benthic foraminifera (Elphidium sp., Brizalina sp.) and Echinoid spines appear after the marine reconnection at 134 ka BP (Fig. 7). Sapropel MSAP-4 of Eemian age with TOC contents of 2 -4.9 wt% started depositing at ~131 ka BP, about ~3 ka after the marine reconnection, considering a lower cut off limit of 2% TOC for the sapropel.

Low diversity of benthic foraminifera and absence of pelagic foraminifera indicate low salinity conditions during the period from 134 to 128.6 ka BP including the period from the marine reconnection and the early part of MSAP-4 deposition. Part of MSAP-4 deposited between 128.4 and 122.9 ka BP has a diverse population of benthic foraminifera, characteristic of suboxic conditions, and pelagic foraminifera (mainly Globigerina sp.), which together with relatively high Mn contents, indicate increased sea surface salinities and the suboxic bottom water conditions (Figs. 6 and7). This in agreement with the dinoflagellate cyst data from the Black Sea, which show that high sea-surface salinity of ~28-30 psu is already established there around the same time, during the Eemian (Shumilovskikh et al., 2013a). The upper part of MSAP-4 is devoid of benthic and pelagic fauna strongly suggesting low salinity surface waters and bottom water anoxia during 123-112 ka BP (Fig. 7). The anoxic bottom water conditions are supported by low µ-XRF Mn counts observed in this interval (Fig. 6).

The period from 112 to to the hiatus at 108 ka BP, corresponding to a part of stadial MIS5d (MIS5d: 115-105 ka BP, [START_REF] Martrat | Abrupt temperature changes in the Western Mediterranean over the past 250,000 years[END_REF]) (Fig. 8j), is characterized by relatively low TOC, high diversity of benthic foraminifera, abundance of pelagic (mainly Globigerina sp.) foraminifera, and relatively high µ-XRF Mn counts (Figs. 6 and7). These attributes indicate low organic matter preservation under relatively oxic bottom waters and reasonably high surface salinities, comparable to the present-day conditions in the SoM. The MSAP-3 and MSAP-2 are characterized by rare Echinoid spines, sponge spicules and juvenile marine bivalves, and the near absence of benthic and pelagic foraminifera, suggesting low surface salinity and bottom water dysoxic/anoxic conditions (Fig. 7). The deposition of these two sapropels, MSAP3 and MSAP2, are separated by a period of lacustrine conditions during ~93 -87 ka BP (i.e., stadial MIS5b), as indicated by the presence of fresh/brackish water bivalve fauna, implying sea level below the sill depth of the Dardanelles Strait (Fig. 8d).

Although, the sapropels in the SoM, Black Sea and Mediterranean Sea are related to the same climatic events of global warming and sea level rise, the causal mechanisms and timings of their deposition in these basins were different. The sapropel deposition in the SoM (and the Black Sea) appears to have been triggered by marine flooding events, the timing of which is determined by the rate of sea level rise and the sill depth of the connecting shallow straits of Bosporus and Dardanelles at the time (Çağatay et al., 2009, 2015). The marine flooding of the fresh-brackish basins of the SoM and Black Sea would cause a density stratification of the water column, decreased renewal of deep waters and increased organic matter preservation, all leading to the sapropel formation (Çağatay et al., 2009, 2015). On the other hand, the sapropel formation in the Mediterranean is believed to have been controlled by sea level rise and precession minima, with the former causing preconditioning and prevention of deep water formation, and the latter enhanced monsoon intensity and runoff from North Africa, resulting in density stratification and stagnation (see Rohling et al., 2015 for discussion). The Mediterranean sapropels S3, S4 and S5 were formed during interstadial periods of MIS-5 (a, c, and e), whereas sapropel S6 was deposited during ~180-170 ka BP within the glacial MIS6 [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF]. Thus, MSAP2, MSAP-3 and MSAP-4 sapropels of the SoM are broadly the time equivalent of S3, S4 and S5 sapropels in the Mediterranean, but the equivalent of Mediterranean S6 sapropel should be absent in the SoM and the Black Sea, based on the considerations of the global sea level curve [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF] (Fig. 8d) and the Sofular speleothem oxygen isotope data (Baderstcher et al, 2011) (Fig. 8f).

Although sapropels were deposited in the same interstadial sub-stages of the MIS5 and during MIS1 in the SoM, Black Sea and Mediterranean Sea, the timing of their formation was different in these basins. The onset of MIS5 sapropels, MSAP-2 and MSAP-4, in the SoM is dated at 86.6, and 131.2 ka BP, while that of MSAP-3 could not only be constrained between 108.2 and 103.3 ka BP, because of its disconformable basal boundary. The sapropels S3, S4 and S5 in the Mediterranean Sea started forming at ~85 ka BP, ~107 ka and ~128 ka BP, respectively [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF], and the MIS5e (Eemian) sapropel in the Black Sea at 127.6 ka BP [START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF]. Therefore, the onset ages of formation of the two SoM MIS5 sapropels are in general 1-3 ka older than the corresponding Mediterranean sapropels of MIS5.

Similarly, the Holocene MSAP-1 sapropel started forming at 12.33±0.35 (Çağatay et al., 2015), nearly 1.5 ka earlier than the Mediterranean S1 sapropel (10.8 cal yr BP; De Lange et al., 2008), ~4 ka earlier than the onset of the formation of the Holocene Black Sea sapropel, dated at ~8 cal yr BP [START_REF] Jones | Radiocarbon chronology of Black Sea sediments[END_REF][START_REF] Bahr | Late glacial to Holocene climate and sedimentation history in the NW Black Sea[END_REF][START_REF] Bahr | Late glacial to Holocene paleoenvironmental evolution of the Black Sea, reconstructed with stable oxygen isotope records obtained on ostracod shells[END_REF][START_REF] Lamy | Multicentennial-scale hydrological changes in the Black Sea and northern Red Sea during the Holocene and the Arctic/North Atlantic Oscillation[END_REF]. The formation of sapropels in the SoM being earlier than those in the Mediterranean sapropels does not necessarily indicate a causal link between the Black Sea outflow and the sapropel formation in the Eastern Mediterranean, as claimed by some earlier studies [START_REF] Olausson | Carbon and oxygen isotope composition of foraminifera in two cores from the Bannock Basin area, eastern Mediterranean[END_REF][START_REF] Aksu | Paleoclimatic and paleoceanographic conditions leading to development of sapropel layer S1 in the Aegean Sea[END_REF]. They suggest that substantial fresh water outflows from glacial Black "Lake" after each marine reconnection was the trigger for sapropel formation in the Eastern Mediterranean.

However, this hypothesis is now mainly discarded especially for the sapropel S1 formation, because it was demonstrated that the sea surface salinity was up to 6 psu higher-than-present in the SoM during the deposition of S1 and that the salinity gradients indicated a southern Mediterranean source fresh water in the Levantine Basin [START_REF] Sperling | Black Sea impact on the formation of eastern Mediterranean sapropel S1? Evidence from the Marmara Sea[END_REF][START_REF] Vidal | Hydrology in the Sea of Marmara during the last 23 ka: Implications for timing of Black Sea connections and sapropel deposition[END_REF]. Instead, the differences in timing of the sapropel deposition in the silled SoM and Black Sea marginal basins, relative to those of the quasi-equivalent Mediterranean sapropel, are likely related to timing of establishment of the suboxic/anoxic bottom water conditions, which would in turn be controlled by the sill depth of the connecting shallow straits, rate of primary productivity, the rate and extent of sea level rise, and the size and depth of the basins. The shallow sill depths of straits would delay the marine connections, but would result in establishment of early anoxic conditions, thereby shortening the time lag between the marine connection and the onset of sapropel deposition in the marginal silled basins. Similarly, high sea levels with a rapid rise, as in the case of MIS5e would result in early connections, but cause a delay in the sapropel formation because of the relatively effective bottom water circulation in small basins such as the SoM. This would explain the difference in the time lapse between the marine connection and the formation of sapropels during MIS5e (MSAP-4) and Holocene (MSAP-1), which is ~3 ka (this study) and ~0.3 ka (Çağatay et al., 2015), respectively.

Comparison with the global and regional records and paleoclimatic implications

As already explained in section 3.4.2, the µ-XRF Ca data, related to the endogenic carbonate production in the epilimnion of the Marmara "lake", show good correlation with the NGRIP oxygen isotope data (NGRIP, 2005), with the increase (decrease) in Ca corresponding to Greenland interstadials (stadials) (Figs. 3,9a,d). There is also a very close correlation between the TOC data of the SoM with the continental records from Lake Ohrid in Macedonia/Albania in the Balkans (i.e., TOC data of [START_REF] Francke | Sedimentological processes and environmental variability at Lake Ohrid (Macedonia, Albania) between 637 ka and the present[END_REF]pollen data of Sinopoli et al., 2018) (Figs. 8f, i, j). The SoM and Lake Ohrid are located ~500 km apart along similar latitudes and are presently both affected by continental and Mediterranean climatic conditions. The TOC data of SoM and TOC and pollen data of Lake Ohrid show conformable sharp changes during the stadial and interstadial periods of MIS5, with high organic productivity and preservation during the interstadial periods in both basins. The SoM data also show excellent correlation with the global sea level curve (Fig. 8d) and oxygen isotope ratio of pelagic foraminiferal data from the SE Aegean Sea [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF] (Fig. 8d), surface temperature (SST) data from core ODP-977 [START_REF] Martrat | Four climate cycles of recurring deep and surface water destabilizations on the Iberian margin[END_REF] (Fig. 8j), and benthic and planktonic oxygen isotope data from the Western Mediterranean [START_REF] Sanchez-Goni | High resolution palynological record off the Iberian margin: direct land-sea correlation for the Last Interglacial complex[END_REF], 2005;2012; not plotted), as well as with the pollen and TOC data of the Black Sea for MIS5e that show warm and high precipitation conditions during 126.4-122.9 ka BP in north Anatolia (Shumilovskikh et al., 2013b;[START_REF] Wegwerth | Meltwater events and the Mediterranean reconnection at the Saalian-Eemian transition in the Black Sea[END_REF] (Fig. 8e).

The close correlation of the marine and continental records from the western and central Mediterranean regions including the SoM, Aegean Sea, Black Sea, southern Europe, and Anatolia with the Greenland interstadials and stadial events shown by the NGRIP oxygen isotope record [START_REF] Svensson | The Greenland Ice Core Chronology 2005, 15-42 ka. Part 2: comparison to other records[END_REF][START_REF] Svensson | A 60000 year Greenland stratigraphic ice core chronology[END_REF][START_REF] Rasmussen | A new Greenland ice core chronology for the last glacial termination[END_REF][START_REF] Wolff | Millennialscale variability during the last glacial: the ice core record[END_REF] indicates the common strong influence of the North Atlantic climatic events in the region, triggered by the changes in the Atlantic Meridional Overturning Circulation (AMOC) [START_REF] Ganopolski | Simulation of rapid glacial climate changes in a coupled climate model[END_REF][START_REF] Drysdale | Stalagmite evidence for the precise timing of North Atlantic cold events during the early last glacial[END_REF][START_REF] Sinopoli | Palynology of the Last Interglacial Complex at Lake Ohrid: palaeoenvironmental and palaeoclimatic inferences[END_REF]. The geochemical proxy-records, such as the Ca and TOC excursions suggest that the amplitude of the millennial and multimillennial climate oscillations in the SoM during the MIS6 (Saalian or Penultimate Glacial Period) was much less than those during MIS4-MIS2 (Last Glacial Period).

5.4 Age of the "Red" seismic reflecting surface From the chronology of cores located in different parts of the SoM, it is clear that the "Red" or "H1" seismic reflecting surface with a high amplitude and a negative polarity [START_REF] Sorlien | Uniform basin growth over the last 500 ka, North Anatolian Fault, Marmara Sea, Turkey[END_REF][START_REF] Grall | Slip rate estimation along the western segment of the Main Marmara Fault over the last 405-490 ka by correlating mass transport deposits[END_REF] corresponds to a hiatus developed during the sea level lowering at the MIS5/MIS4 transition. Hence, the age of the prominent seismic reflecting surface is considerably different from the age of 110 ka BP, estimated by [START_REF] Sorlien | Uniform basin growth over the last 500 ka, North Anatolian Fault, Marmara Sea, Turkey[END_REF] on the basis of extrapolated sedimentation rates (see Kende et al, in review, for further discussion). [START_REF] Sorlien | Uniform basin growth over the last 500 ka, North Anatolian Fault, Marmara Sea, Turkey[END_REF] and [START_REF] Grall | Slip rate estimation along the western segment of the Main Marmara Fault over the last 405-490 ka by correlating mass transport deposits[END_REF] used the ages of the "Red" reflecting surface and other surfaces to estimate the fault slip rates and the age of mass transport deposits in the SoM.

The hiatus (and Red seismic reflecting surface) is most likely related to mass-wasting events during the sea-level lowering at the MIS5/MIS4 transition. However, its duration appears to be distinct in different locations in the SoM; in cores MRS-CS18, MRS-CS27 and MRS-CS22, the hiatus corresponds to time intervals of 79.3-70.1 ka BP, 74.0 -68.6 ka BP and ~72-70 ka BP, respectively. The length of hiatus interval appears to be related to the site of the core location, with the sites on relatively steep slopes (e.g., core MRS-CS18, Fig. 2d) having a relatively long gap in the stratigraphy, because of causal processes of the mass-wasting and/or non-deposition.

Possible sources of the new cryptotephra

The two unidentified tephra (MT-3 and MT-4), with model ages of 57.02±2.90 ka BP and 160.61±0.79 ka BP, can be definitely correlated to their specific sources only after the detailed electron probe micro analysis (EPMA), which is presently underway. However, based on the general chemical composition and model-age, some preliminary evaluation can be made about their possible source regions. The MT-3, with plagioclase-and Ca-rich and incompatibleelement (K, Zr)-poor composition, has calc-alkaline characteristics, and hence, likely originated from the Aegean volcanic arc province [START_REF] Druitt | Santorini Volcano[END_REF]Hardiman, 1999;[START_REF] Bachmann | The 40Ar/39Ar and U/Pb dating of young rhyolites in the Kos-Nisyros volcanic complex, Eastern Aegean Arc, Greece: Age discordance due to excess 40Ar in biotite[END_REF].

Considering its potassium-rich composition, stratigraphic position and model age, several candidate regions can be proposed for the source of MT-4, such as the Vico volcano in Lazio region of Italy [START_REF] Bear | Volcanological constraints on the post-emplacement zeolitisation of ignimbrites and geoarchaeological implications for Etruscan tomb construction (6th-3rd century BC) in the Tufo Rosso a Scorie Nere, Vico Caldera, Central Italy[END_REF], the southern Aegean Sea [START_REF] Smith | Single crystal 40Ar-39Ar dating of a Late Quaternary paroxysm on Kos, Greece: Concordance of terrestrial and marine ages[END_REF][START_REF] Bachmann | The 40Ar/39Ar and U/Pb dating of young rhyolites in the Kos-Nisyros volcanic complex, Eastern Aegean Arc, Greece: Age discordance due to excess 40Ar in biotite[END_REF], the Cappadocia volcanic province in Central Anatolia [START_REF] Druitt | Late Quaternary rhyolitic eruptions from the Acigol complex, Central Turkey[END_REF][START_REF] Aydar | The geology of Mount Hasan stratovolcano, central Anatolia, Turkey[END_REF][START_REF] Kuzucuoğlu | Identification and dating of tephra layers from Quaternary sedimentary sequences of Inner Anatolia, Turkey[END_REF][START_REF] Siebel | Acigöl rhyolite field, central Anatolia (part II): geochemical and isotopic (Sr-Nd-Pb, d18O) constraints on volcanism involving two high-silica rhyolite suites[END_REF], and the Eastern Anatolian volcanic province (Pierce et al., 1990;[START_REF] Özdemir | Volcanostratigraphy and petrogenesis of the Nemrut stratovolcano (East Anatolian High Plateau): the most recent postcollisional volcanism in Turkey[END_REF]Sumita, M., Schmincke, 2013a,b).

The potassium-rich alkaline "Ignimbrite B" (Vico B) eruption of Vico occurred at 157±3 ka [START_REF] Laurenzi | 40Ar/39Ar chronostratigraphy of Vico ignimbrites[END_REF], and its record is dated in Lake Ohrid at 162±6 ka BP (Leicher et al., 2016). Plinian eruptions of high-silica rhyolitic compositions occurred from Kos-Nisyros volcanic complex and the Acıgöl volcanic complex of Cappadocia in Central Anatolia around the same time, with the former eruption dated at 161±2 ka BP [START_REF] Bachmann | The 40Ar/39Ar and U/Pb dating of young rhyolites in the Kos-Nisyros volcanic complex, Eastern Aegean Arc, Greece: Age discordance due to excess 40Ar in biotite[END_REF] and the latter (the Upper Acıgöl Tuff) 163±7 ka BP [START_REF] Schmitt | Acigöl rhyolite field, Central Anatolia (part 1): high-resolution dating of eruption episodes and zircon growth rates[END_REF]. A major potassium-rich eruption of similar age (160±13 ka BP) occurred from the Nemrut volcano in Eastern Anatolia depositing the potassium-rich Ahlat Pumice (AP-2) unit (Sumita and Schmincke, 2013a).

Considering its 11-cm thickness, together with the close age interval of these eruptions, the cryptotephra MT-4 may represent a composite record of most, if not all, of these eruptions.

Considering the easterly wind trajectories, however, the Eastern Anatolia appears to be less likely source than the others.

Conclusions

Multy-proxy records of two cores MRS-CS18 and MRS-CS27 from the SoM provide significant paleo-environmental and hydrographic records for MIS5 and MIS6, reaching back to 173 ka BP. These records show that the marine reconnection of the SoM during Termination II (MIS6/MIS5 transition) occurred at ~134.06±1.10 ka BP and that three sapropels (MSAP-4, MSAP-3 and MSAP-2) were deposited during the three MIS5 interstadials, e, c and a. During stadial MIS5b (~92.7-87.2 ka), the marine connection was disrupted when sea level dropped below the sill depth of the Dardanelles Strait, whereas marine conditions, with relatively low TOC contents (<2 %) prevailed during the stadial MIS5d.

Sapropel MSAP-4 of Eemian age started forming at ~131 ka BP, about ~3 ka after the marine reconnection. Low salinity and oxic to suboxic bottom conditions prevailed during the period from 134 to 128.4 ka including the period from the marine reconnection to the early part of MSAP-4 deposition. During 128.4 and 122.9 ka BP MSAP-4 deposition continued under relatively high salinity and suboxic bottom water conditions, whereas the low sea surface salinities and anoxia prevailed during 122.9-112.3 ka BP. Relatively high sea surface salinity water existed and the sapropel formation was disrupted from 112 ka BP to 103-108 ka BP (part of stadial MIS5d) because of the increased bottom water circulation, similar to present-day conditions. The MSAP-3 and MSAP-2 were deposited under low surface salinity and dysoxic/anoxic bottom water conditions.

The marine conditions during MIS5d and disconnection during MIS5b suggests that a threshold sill depth of -50 to -60 m for the Dardanelles Strait during most of MIS5, which is 5-15 m higher than the present sill depth of -65. However, the sill depth must have been lower

(at least at ~-75 m) during the reconnection at Termination II. A disruption in the marine connection of the Black Sea during MIS5b (as well as its marine reconnection at ~128 ka BP) is in agreement with a sill depth of ~-35 to -40 m for the Bosporus Strait, a depth similar to that of the present day.

The SoM geochemical proxy records correlate well with the regional terrestrial and marine records and the NGRIP oxygen isotope record with its glacial and interglacial (GI) phases, showing the important common effect of the North Atlantic climatic events triggered by the perturbations in the Atlantic Meridional Overturning Circulation (AMOC). The sedimentary records of the studied cores also indicate the presence of two distinct and two crypto tephra layers. The distinct tephra layers, MT-1 and MT-2, are previously known from the SoM, which are correlated with the Cape Riva eruption of Santorini Volcano (22 cal kyr BP) and the Campanian Ignimbrite (39.3 ka BP), respectively. The newly discovered but unidentified cryptotephra layers, MT-3 and MT-4, were dated at 57.02±2.90 ka BP and 160.61±0.79 ka BP, respectively. The former is of calc-alkaline affinity and whereas the latter is of potassium-rich alkaline affinity. Detailed EPMA analyses are underway to match the crypto-tephra MT-3 and MT-4 with their sources.

The regional "Red" seismic reflecting surface in the SoM corresponds to a hiatus that developed during the sea-level lowering at the MIS5/MIS4 transition, as result of removal the sediments by mass wasting processes. This hiatus represents different gaps in the stratigraphy in different parts of the SoM. [START_REF] Martrat | Four climate cycles of recurring deep and surface water destabilizations on the Iberian margin[END_REF], Deep core in Lake Ohrid (Francke et al., 2016;[START_REF] Sinopoli | Palynology of the Last Interglacial Complex at Lake Ohrid: palaeoenvironmental and palaeoclimatic inferences[END_REF], core LC-21 south Aegean Sea [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF], Sofular Cave in NW Anatolia (Fleitmann et al., 2009;Baderstcher et al, 2011) and core 22GC-8 in south Black Sea (Wegreth et al., 2014). (b) Bathymetric map of the (SoM) showing the location of the cores MRS-CS18 and MRS-CS27 (this study), MD01-2430 [START_REF] Vidal | Hydrology in the Sea of Marmara during the last 23 ka: Implications for timing of Black Sea connections and sapropel deposition[END_REF][START_REF] Çağatay | The tephra record from the Sea of Marmara for the last ca. 70 ka and its palaeoceanographic implications[END_REF]MD04-2745MD04- (Çağatay et al., 2009) ) Note the presence of sapropel units MSAP-1, MSAP-2, MSAP-3 and MSAP-4 with TOC contents greater than 2 wt % and the tephra units, MT-1 (Santorini, Cape Riva), MT-2 (Campanian Ignimbrite), and , on core logs. For location of cores see Fig. 1b. tuned to GICC05 time scale of NGRIP ice core oxygen isotope data (a) (NGRIP, 2004;[START_REF] Svensson | A 60000 year Greenland stratigraphic ice core chronology[END_REF] (red) and synthetic NGRIP data (Barker et al., 2011) (black). Also for comparison are TOC data sets for cores MRS-CS18 (e) and MRS-CS27 (f) (this study) and for Lake Ohrid (d) [START_REF] Francke | Sedimentological processes and environmental variability at Lake Ohrid (Macedonia, Albania) between 637 ka and the present[END_REF]. Note that the Marmara TOC data is plotted with NGRIP time scale, and Lake Ohrid TOC data are dated by tephrochronology and crosscorrelation of geochemical proxy data with orbital parameters. Numbers on NGRIP profile refers to Greenland interstadials (GI). Fig. 4. Age-depth model for cores MRS-CS27 (a) and MRS-CS18 (b), constructed using Rstudio and the script "CLAM" [START_REF] Blaauw | Methods and code for 'classical' age-modelling of radiocarbon sequences[END_REF]. For a detailed description of the data used in modelling see text of sections 3.4.5 and 4.2.1 and Table S1 of Supplementary Data.

Figure captions

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  Figure 1.pdf [Figure]

Figure 2 .

 2 Figure 2.pdf [Figure]

Figure 3 .

 3 Figure 3.pdf [Figure]

Figure 4 .

 4 Figure 4.pdf [Figure]

Figure 5 .

 5 Figure5.pdf[Figure]

Figure 6 .

 6 Figure6.pdf[Figure]

Figure 7 .

 7 Figure 7.pdf [Figure]

Figure 8 .

 8 Figure 8.pdf [Figure]

Fig. 1 .

 1 Fig. 1. (a) Location of the Sea of Marmara (SoM) and other sites discussed in the text: ODP-977A in Western Mediterranean[START_REF] Martrat | Four climate cycles of recurring deep and surface water destabilizations on the Iberian margin[END_REF], Deep core in Lake Ohrid(Francke et

  and MRS-CS22 (Kande et al., in review). (c, d) Chirp seismic profiles showing location of cores MRS-CS18 and MRS-CS27and the red seismic reflector surface of[START_REF] Sorlien | Uniform basin growth over the last 500 ka, North Anatolian Fault, Marmara Sea, Turkey[END_REF] and[START_REF] Grall | Slip rate estimation along the western segment of the Main Marmara Fault over the last 405-490 ka by correlating mass transport deposits[END_REF].

Fig. 2 .

 2 Fig. 2. Lithological logs of cores MRS-CS18 and MRS-CS27 (this study) and MRS-CS22 (Kande et al., in review), with their cross-correlation based on lithology and fossil content.

Fig. 3 .

 3 Fig. 3. Correlation of µ-XRF Ca (x 1000 cps) of cores MRS-CS27 (b) and MRS-CS18 (c)

Fig. 5 .

 5 Fig.5. Gamma density, magnetic susceptibility (MS) and µ-XRF geochemical element and element-ratio profiles (K, Ca, Mn, Br, Zr, Ca/Ti, Fe/Mn, Sr/Ca, S/Ti, Br/TOC) for core MRS-CS27.

Table 1 .

 1 Location, water depth and lengths of cores used in this study.

	Core ID	Latitude / Longitude	Water depth	Core length (m)
			(mbsl)
	MRS-CS18 40°39,724'/28°52,775' 291	14,20
	MRS-CS27 40°42,029'/28°24,053' 313	20,45

Table 2 .

 2 AMS radiocarbon and calibrated ages of fossil shell samples in the studied cores. INTCAL13 calibration curve of[START_REF] Reimer | IntCal13 and Marine13 radiocarbon age calibration curves, 0-50,000 years cal BP[END_REF], with the respective reservoir ages of 400 and 1000 yrs for the latest marine and lacustrine units, are used for the calibration.

	Sample No/Laboratory No/Dated	Core Depth	Radiocarbon yrs	Calibrated age (yrs before
	Material	(cmbsf)	± 2 σ error	1950 ± 2 σ error)
	CS 27 S4/Poz-94035/Marine Bivalve	300	13050±70 BP	14994±282 BP
	CS 27 S13/Poz-94036/Dreissena sp.	1218	27820±260 BP	30933±345 BP
	CS 18 S3/Poz-97852/Dreissena sp.	186	34.800±500 BP	37986±1336 BP
	CS18-S2-2/Poz-99211/Dreissena sp.	120	28200±180	31151±239 BP
	__________________________________________________________________

Acknowledgements

The authors would like to thank the scientific team of Marsite cruise, and in particular the cochiefs, Louis Geli and Livio Ruffine, and the captains and crews of RV Pourquoi pas? The Marsite cruise was co-funded by the EC FP7 project MARSITE (grant number: 308417) "Longterm monitoring experiment in geologically active regions of Europe prone to natural hazards:the Supersite concept" under the call ENV.2012.6.4-2 and by the "Laboratoire d'Excellence" LabexMER (ANR-10-LABX-19) through the projects called MicroGaMa and MISS Marmara, and by a grant from the French government under the program "Investissements d'Avenir".

Fig. 6. Gamma density, magnetic susceptibility (MS) and µ-XRF geochemical element and elemental ratio profiles (K, Ca, Mn, Br, Zr, Ca/Ti, Fe/Mn, Sr/Ca, S/T), Br/TOC) for core MRS-CS18. Note that Br in cps and TOC is in wt % units. (NGRIP, 2004;[START_REF] Svensson | A 60000 year Greenland stratigraphic ice core chronology[END_REF][START_REF] Barker | years of abrupt climate variability[END_REF], sea level curve [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF]) (d), Black Sea TOC data (Wegreth et al., 2014) (e), δ 13 O speleothem data from Sofular in NW Anatolia (Baderstcher et al, 2011) (f), TOC and pollen data from Lake Ohrid [START_REF] Francke | Sedimentological processes and environmental variability at Lake Ohrid (Macedonia, Albania) between 637 ka and the present[END_REF]Sinopoli et al., 2018) (g, h), surface foraminiferal δ 18 O data from SE Aegean Sea core LC21 [START_REF] Grant | Rapid coupling between ice volume and polar temperature over the past 150,000 years[END_REF] (i), and sea surface temperature (SST) from Iberian margin core ODP-977A (Martrat et al., 2007) (j). The horizontal dashed lines show the present sill depths of Bosporus and Dardanelles straits at -35 m and -65 m, respectively. SoM data tuned with GICC05 and synthetic time scales. All other data sets ware plotted using their original time scales.

Supplementary Figure and Data

Supplementary Fig. S1. Age-depth plot for cores MRS-CS27 (A) and MRS-CS18 (B), generated from correlation of µ-XRF Ca (x 1000 cps) with Greenland Interstadials (GI) of NGRIP ice core oxygen isotope data [START_REF] Svensson | A 60000 year Greenland stratigraphic ice core chronology[END_REF], tephrochronology, and the onset and end of Holocene Marmara sapropel for core MRS-CS27 (MSAP-1; Çağatay et al., 2015).

For detailed description see text of sections 3.4.5 and 4.2.1 and Supplementary Data, Table 1). Supplementary Table S1 and Supplementary Data, Table 1).