Main physical and biogeochemical parameters were measured at 97 stations in the Sea of Marmara (Fig. 1) in the winter and summer of 2019 by R/V Bilim-2 of METU-IMS. Sediment core samples were obtained with a multicorer (Octopus, Kiel) from 13 selected stations in the İzmit Bay, Çınarcık Basin, and southern Marmara Sea. The upper parts of the sediment columns were generally brown in color with a fine-grained sediment texture. However, at below 6–8 cm depth, the sediments, specifically in the Çınarcık Basin and İzmit Bay, became darker suggesting the reducing conditions. Core slices were used to measure porewater nutrients (PO₄, Si, NO3+ NO₂, NH₄), major ions (Cl, SO₄, Br, Li, Na, K, Mg, Ca), hydrogen sulfide (H₂S), dissolved iron (dFe), solid-state total carbon / organic carbon (TC / TOC) and nitrogen (TN) concentrations.

The temperature and salinity of the water column were measured in situ by a SEABIRD 9plus CTD probe that was coupled to a 12-Niskin bottle Rosette System. The Secchi Disk Depth (SDD), an estimation of water transparency, was collected from each water column station (Fig. 1). In addition to the CTD sensor-derived measurements, dissolved oxygen measurements were also carried out by the Winkler titration (UNEP/MAP, 2005). Total phosphorus concentrations were determined by the wet digestion methods and using the conventional colorimetric detection at 880 nm wavelength (Strickland and Parsons, 1972; Grasshoff et al., 1983) after persulfate oxidation of seawater samples (Menzel and Corwin, 1965). Water column and porewater dissolved inorganic nutrients (nitrate + nitrate, ammonium, phosphate, and silicate) were measured using a Bran + Luebbe Model four-channel Autoanalyzer (Grasshoff et al., 1983). The detection limits of dissolved nutrients were 0.05, 0.04, 0.01, 0.04, and 0.03 µM for nitrate + nitrite, ammonium, phosphate, silicate, and total phosphorus, respectively. Chlorophyll a (Chl a) measurements were carried out by the conventional spectrofluorometric method after digestion of filtered samples by 90 % (v/v) acetone solution using a HITACHI model F-2500 fluorescence spectrophotometer (Strickland and Parsons, 1972; UNEP/MAP, 2005). Hydrogen sulfide (H2S/HS-) concentrations in seawater and porewater samples were measured on board by the spectrophotometric methylene blue method at 670 nm wavelength (Cline, 1969). Porewater dissolved iron (sum of Fe²⁺ and Fe³⁺) concentrations were measured on board by spectrophotometry, after reducing all Fe(III) to Fe(II) by dithionite, followed by ferrozine-based assay and detection of the color-producing Fe complex at 562 nm wavelength (Stookey, 1970; Jeitner, 2014).

Sediment core samples were obtained by a multiple-corer (Oktopus, Kiel). Each sediment core was sliced on board under anoxic conditions using N₂ or Ar gas. After obtaining sliced sediments, each sample was put in a 50 mL falcon tube and centrifuged at 6000 rpm for 20 min. Then, the porewater samples were extracted using syringe-coupled GF/F filters through 0.45 µm. Dissolved iron and hydrogen sulfide concentrations of porewater sub-samples were immediately determined on board by the methods mentioned above, and the remained sub-samples were placed in 15 mL falcon tubes and stored at -20 °C for the analysis of dissolved nutrients and major ions. Analyses of porewater nutrients were carried out by the same method as water column samples. Analysis of major ions (Cl⁻, SO42-, Li⁺, Na⁺, K⁺, Mg²⁺, Ca²⁺) in porewater samples was conducted by ion chromatography.

Solid phase sediment samples were also stored for the determination of TC, TOC, and TN concentrations and surface sediment porosity measurements. Sediment samples for the TC, TOC, and TN measurements were initially freeze-dried. Dry sediments were then powdered and sieved on 63 µm pore size for the homogenization of the samples. For TOC analysis, about 30 mg of dry and homogeneous sediment samples were put into the silver cups, which had been pre-combusted at 400 °C for 6 h. Then, 10 µL of distilled water was added into each silver cup to wet the samples. After the addition of distilled water, 10 µL of 20 % HCl (v/v) was added to remove inorganic carbon from the sediment samples. The HCl additions were continued until all weak-acid soluble carbonates were removed. Then, the samples were dried at 60–70 °C for 24 h. After drying the sediment samples, silver cups were compacted and put into the autosampler of the CHN analyzer. TC and TN analyses in sediments were performed by the same method as for the TOC analysis, but without acid addition. TN concentrations were also determined on HCl-added sediment samples, and there was no significant difference between HCl-treated and untreated samples, indicating that a significant fraction of the TN pool was in the organic nitrogen form. Therefore, TN concentrations of HCl-untreated sediment samples were reported in this study. Total carbon (TC), organic carbon (TOC), and nitrogen (TN) concentrations were determined by the dry oxidation method using the Vario El Cube Elementar Model CHN Analyzer (UNEP/MAP, 2006). Porosity of wet sediments was determined by the displacement method as described by Mu et al. (2017).

We have calculated the diffusive nutrient fluxes based on Fick's first law of diffusion (Cheng et al., 2014; Mu et al., 2017): 1F=ϕDs(dC/dz) Where F corresponds to the diffusive flux across the sediment-water interface, dC/dz to the concentration gradient of nutrients across the sediment-water interface, ϕ to the porosity of sediment, and Ds to the actual molecular diffusion coefficient corrected for the sediment tortuosity.

Ullman and Aller (1982) proposed an empirical formula related to the actual diffusion coefficient, Ds, and porosity, ϕ: 2Ds=ϕD0(ϕ<0.7)Ds=ϕ2D0(ϕ>0.7) where D0 is the self-diffusion coefficient of ions at infinite dilution corrected by in situ temperature. For phosphate, nitrate, nitrite and ammonium, D0 values were taken from Li and Gregory (1974) and for silicate, D0 values were taken from Rebreanu et al. (2008) as 7.34×10-6 cm² s⁻¹ for PO₄, 19.0×10-6 cm² s⁻¹ for NO₃, 19.1×10-6 cm² s⁻¹ for NO₂, 19.8×10-6 cm² s⁻¹ for NH₄ and 11.7×10-6 cm² s⁻¹ for Si at 25 °C, respectively.

We describe the general oceanography of the system based on the two expeditions performed in the Sea of Marmara in the summer and winter periods of 2019 by R/V Bilim-2. Physical and chemical oceanographic properties of the two-layer Marmara Sea ecosystem are principally dominated by the brackish (S: 17.0–17.5) Black Sea and the salty Mediterranean inflow (S: 35–38) through the Dardanelles (Ünlüata et al., 1990; Beşiktepe et al., 1994; Polat and Tuğrul, 1995; Tuğrul and Polat, 1995; Polat et al., 1998; Tuğrul et al., 2002). Driven by the physical properties of the exchange flows, temperatures of the upper layer waters ranged from 6.93–10.98 °C in winter to 19.06–26.17 °C in summer for the study period. The surface water salinity values increased from 17.29 in the Bosphorus exit to 29.40 in the entry to Dardanelles (Table 1, Fig. 2). Water transparency increased from the Eastern Marmara (SDD 4–5 m) towards Dardanelles (SDD 17–18 m) in the summer months. The winter SDDs displayed less pronounced spatial variations, ranging between 4 and 11 m (Table 1). Lowest values were recorded in the Eastern Marmara, notably in the Çınarcık Basin and the İzmit Bay (Fig. 2).

Altogether, our observations on the state of the Sea of Marmara as of 2019 are in line with the previous reports, pointing out to the combined effect of brackish Black Sea inflow and land-based sources (Tuğrul and Morkoç, 1989; Polat and Tuğrul, 1995; Tuğrul and Polat, 1995; Polat et al., 1998; Ediger et al., 2016; Yalçın et al., 2017; Tan and Aslan, 2020). We have found that the brackish surface waters of Black Sea origin were relatively rich in NO_x (NO_x: NO2+ NO₃) and PO₄ concentrations in winter, and this enrichment is due to enhanced inputs of nutrients from the lower layer by vertical mixing processes (Tuğrul et al., 2002; Ediger et al., 2016; Yalçın et al., 2017). Similar seasonal and regional variations were also recorded in the concentrations of NH₄ and reactive Si, with the maximum values recorded at the Bosporus southern exit and Eastern Marmara Sea; İzmit Bay and Çınarcık Basin (Fig. 2). The surface water chlorophyll a (Chl a) concentrations increased towards eastern basin (Fig. 2) and from summer (0.01–1.81 µgL-1) to winter (0.26–3.77 µgL-1) due to enhanced inputs of inorganic nutrients from lower layer and Black Sea in winter (Tuğrul and Polat, 1995). According to eutrophication assessment based on the Chl a values (Simboura et al., 2005), trophic status of the Eastern Marmara upper layer and bays were classified as “mesotrophic/moderate” to “dystrophic/bad” levels of ecological status. Enhanced primary productivity (in terms of Chl a) in the upper layer has led to development of eutrophication and hypoxia in the lower layer over the basin and development of anoxic conditions in deep waters of the Eastern Marmara Sea and Izmit Bay (Fig. 2). In the Çınarcık Basin of Eastern Marmara Sea (max depth 1270 m), dissolved oxygen was entirely depleted and anoxia developed in the deep waters particularly below 750 m. Development of similar anoxic conditions were consistently observed in the central deep waters of the Izmit Bay in the last two decades as well. Here, limited dissolved oxygen inputs from the oxygen-depleted Eastern Marmara deep waters remained insufficient for aerobic oxidation of POM, leading to denitrification and sulfate reduction processes and thus hydrogen sulfide accumulation in the bottom waters of the bay during summer months (Yücel et al., 2023a).

A comparison of averages of data from >1000 m water depth in the Çınarcık Basin indicated an accumulation of reactive Si and PO₄ but consumption of NO_x (via denitrification) in the oxygen-depleted deep waters of Marmara (Fig. 3). These findings indicate enhanced inputs of POM from the highly productive layer to the lower layer during at least the last three decades, and subsequent burial in the sediment phase.

In order to address the apparent long-term changes in the nutrient and organic matter cycles in the oxygen-depleted deep-waters (Fig. 3), sediment core samples were obtained from three key regions in the Marmara: the highly eutrophic İzmit Bay, eutrophic Çınarcık Basin displaying permanently anoxic properties in the deep waters, and from the mesotrophic/eutrophic southern Marmara Sea shelf with still-oxygen-rich bottom waters. The bottom water physical and biogeochemical variables of the core stations presented in Table 2 and also surface water spatial variability of the parameters (Fig. 2) indicated that the selected regions displayed significantly different physico-chemical and biogeochemical properties, allowing the discerning of redox- and organic matter-driven effects on sediment biogeochemistry.

Porewater nutrient concentrations throughout the obtained sediment core samples ranged between 0.47 and 58.2 µM for PO₄, 0.34 and 91.5 µM for NO₃, 0.17 to 666 µM for NH₄ and 9.02 to 335 µM for Si, respectively (Fig. 4). Biogeochemical cycling of key nutrients (N, P) is highly linked to dissolved oxygen concentrations and metal (Mn, Fe) cycles due to rapid degradation of labile organic matter by the redox-processes as denitrification, manganese and iron reduction as well as sulfate reduction and methanogenesis. These respiratory pathways in the uppermost centimeters of sediment column result in net nutrient efflux from the sediments (Williams, 1987; Christensen et al., 1988; Jørgensen, 1996; Ignatieva, 1999; Rasheed, 2004; Al-Rousan et al., 2004; Hille et al., 2005; Rasheed et al., 2006; Rydin et al., 2011; Cheng et al., 2014; Mu et al., 2017). Expectedly, maximum porewater PO₄, NH₄, and Si concentrations were measured in the İzmit Bay (Fig. 4), with the vertical profiles of nutrients displaying an increasing trend with depth throughout the POM-enriched muddy sediment. Porewater NO₃ concentrations were highest in the porewaters of core samples (0–5 cm) from the southern Marmara Sea having oxic conditions in the deep waters and lower surface water primary productivity (in terms of Chl a) (Fig. 2). Vertical profiles of porewater NO₃ concentrations in the studied sites suggested that denitrification process dominated the uppermost millimeters of sediments of the reducing İzmit Bay and Çınarcık Basin while oxic respiration was the major process for the organic matter remineralization in the upper 15–20 cm of sediment cores obtained in southern Marmara Sea.

Diffusive nutrient fluxes across the sediment-water interface were calculated based on the Fick's first law of diffusion in the Sea of Marmara (Table 3). Calculated porewater diffusive fluxes showed spatial variability in the Sea of Marmara. In all sites, sediments acted as a source for PO₄, NH₄ and Si, whilst sediments in the highly eutrophic and anoxic/sulfidic sites of the İzmit Bay acted as a sink for NO_x (referred to NO3+ NO₂) due to rapid utilization of NO₃ ion as a terminal electron acceptor by the denitrification process. Porewater diffusive PO₄, NH₄ and Si fluxes from the sediment to bottom waters were highest in the İzmit Bay with the anoxic bottom waters whereas the negative sign of the diffusive NO_x fluxes here indicated NO_x loss by denitrification. The diffusive fluxes of PO₄, NH₄ and Si to the bottom water decreased in the Çınarcık basin, and further minimized in in the southern Marmara Sea sediments in line with increasing bottom water dissolved oxygen levels (Table 3). These flux estimations indicate that that the increase in diffusive fluxes of dissolved inorganic nutrients (PO₄, NH₄, Si), reactive iron and manganese in the organic-rich muddy shelf sediments of the anoxic regions are likely to lead to nutrient accumulation in bottom waters and contribute to the upper layer chemical fluxes through vertical mixing across the studied basins, intensifying during winter (Konovalov et al., 2007; Noffke et al., 2012; Mu et al., 2017).

The relationship between calculated diffusive nutrient fluxes and the deep water dissolved oxygen concentrations clearly indicated the redox-dependent benthic nutrient mobilization in the Sea of Marmara (Fig. 5); the lower deep water dissolved oxygen concentrations resulted in the higher porewater diffusive PO₄, NH₄, and Si fluxes in the POM–rich muddy sediments. The apparent denitrification in sediment pore waters must have contributed to the apparent deep-water nitrate loss signal in the Çınarcık Basin during the last decades (Fig. 3). Furthermore, the diffusive nutrient fluxes also in the anoxic benthic interface of the highly productive NE shelf region of the Marmara Sea and eutrophic inner Izmit bay might further enhance eutrophication in the NE Marmara shelf and bays by vertical mixing processes (Table 3). The Si/N and N/P molar ratios of the measured nutrients in the shelf and deep basin waters of Marmara Sea ranged between 1.8 and 5.5 for Si/N and 5.6–12 for N/P, respectively. The Si/N molar ratios of the diffusive nutrient fluxes (Si/N: 1.0–5.5) were similar to the ratios in deep waters of the studied sites whereas the N/P molar ratios of diffusive nutrient fluxes (8.4–31) were greater than deep water nutrient (N/P) molar composition; but comparable with the N/P molar ratios calculated in the diffusive nutrient fluxes in the Baltic Sea (N/P: 20–30) (Ignatieva, 1999; van Helmond et al., 2020).

Close examination of vertical profiles for the geochemical variables clearly showed that solid-state total carbon (TC), total organic carbon (TOC) and total nitrogen (TN) concentrations in the upper 40–50 cm of sediment from different regions of the Sea of Marmara displayed spatial variability (Fig. 6). TC concentrations varied regionally from 1.97 to 4.12 mmol g⁻¹ dw (dry weight) in the upper 3 cm of the obtained core samples and decreased to 0.92–3.25 mmol g⁻¹ dw levels below 30 cmbs (Fig. 6). Maximum concentrations of TOC and TN were determined in the surface sediments from the İzmit Bay where anoxic and sulfidic conditions have developed in the deep waters (Fig. 6). TOC values were in the range of 0.47–2.70 mmol g⁻¹ dw while TN values varied between 0.04 and 0.23 mmol g⁻¹ dw. The apparent decrease in the TOC and TN concentrations with the increasing depth throughout the sediment column indicated organic matter deposition exceeding the decomposition in the top 8–20 cm of the sediment column. Below this depth, TOC and TN concentrations were relatively constant and did not change noticeably, suggesting the dominancy of refractory organic matter below 20 cmbs buried in the anoxic sediments. The Çınarcık and İzmit bay bottom sediments had higher TOC levels compared to other regions in the Sea of Marmara, in line with their more reducing deep-water conditions, also in agreement with the previous studies (Evans et al., 1989; Çağatay et al., 2004; Sarı and Çağatay, 2010; Ruffine et al., 2018; Yang et al., 2018; Tan and Aslan, 2020). Maximum TOC and TN concentrations were detected in the surface sediments of the İzmit Bay due to excess anthropogenic inputs from point and diffuse land sources (Tuğrul and Morkoç, 1989; Yalçın et al., 2017; Tan and Aslan, 2020). The study findings further show the development of anoxic conditions in the bottom waters and the organic matter degradation mainly by denitrification and sulfate reduction in the bottom water and underlying sediments in the Çınarcık Basin and İzmit Bay. Our results also report for the first time the accumulation of H₂S (starting from 0.52 µM at 29 m) in the bottom waters of the İzmit inner bay (depth >150 m) in summer months, showing that the bottom waters have shifted to reducing conditions as a result of the general environmental degradation in the Sea of Marmara.

The porewater and solid-state results altogether show that maximum sediment TOC and TN concentrations (Fig. 6) in the İzmit Bay might further enhance eutrophication in the Sea of Marmara, analogous to benthic “vicious cycle” in the much shallower Baltic Sea due to release of increased amount of dissolved nutrients, biologically available for the phytoplankton (Ignatieva, 1999; van Helmond et al., 2020). In the Çınarcık Basin, relatively lower concentrations of TC, TOC, and TN were measured compared to eastern İzmit Bay, but comparable to those measured in the western İzmit Bay, having similar deep-water physical and biogeochemical properties (Table 2), indicating redox-dependency on the benthic organic matter dynamics. In the southern Marmara Sea, levels of TOC and TN were also lower compared to eastern İzmit Bay. However, the TC concentrations were comparable with the İzmit Bay and Çınarcık Basin. Maximum porewater nutrients (Si, PO₄, NH₄) and sediment TOC and TN concentrations were measured in the anoxic and sulfidic İzmit Bay and Çınarcık Basin of the Sea of Marmara, having sedimentation rates ranging between 70 and 190 cm per 1000 years (Ergin and Yörük, 1990; Ergin et al., 1994; Çağatay et al., 2004). In the southern Marmara Sea, with the lower Chl a concentrations in the surface waters and more oxygenated deep waters, relatively low concentrations of porewater nutrients and sediment organic matter were measured with a moderately low sedimentation rate of 45 cm per 1000 years (Çağatay et al., 2004). The lower primary productivity (in terms of Chl a) and also lower sedimentation rate (Çağatay et al., 2004) in the southern Marmara Sea resulted in low organic matter accumulation at the sediment and the higher deep water dissolved oxygen concentrations (Fig. 2, Table 2) prevented the release of reactive phosphate, silicate, and ammonium fluxes from the surface sediments. Therefore, development of eutrophication and deep-water hypoxia/anoxia in the Çınarcık Basin and İzmit Bay caused accumulation of excess amount of organic matter in the upper sediment column highly enhancing the release of dissolved nutrients whereas in the oxic southern Marmara Sea, lower sediment organic matter (C, N) concentrations resulted in lower porewater nutrients concentrations and their diffusive fluxes due to high concentrations of deep water dissolved oxygen.

Benthic nutrient fluxes play a critical role in nutrient cycling and productivity in marine ecosystems. Climate change can intensify deoxygenation and enhance ocean stratification, which limits vertical mixing. These changes may disrupt nutrient dynamics and primary productivity more profoundly than diffusive benthic nutrient fluxes. However, hypoxia and anoxia potentially lead to the long-term release and transport of nutrients to the surface layer. Additionally, although natural eutrophication may occur in certain regions, such as Çınarcık Basin due to Black Sea inflow, human-induced nutrient fluxes may further enhance eutrophication. In the context of marine management efforts, it is essential to consider both benthic nutrient fluxes and larger-scale climate impacts to effectively address nutrient dynamics and sustain ecosystem health.

In order to complement the above-described solid state and porewater parameters, we further describe and discuss in this section additional parameters that enables us to present a fuller picture of the early diagenetic processes in the Sea of Marmara. Concentrations of Cl, SO₄, H₂S, Li, Na, K, Mg, Ca and dFe in porewaters of the collected core samples were determined. Although the measured concentrations of the selected ions exhibited minimal spatial variability within the study region, they demonstrated significant variations with depth (Fig. 7). The ranges of the measured concentrations throughout the sediment column were 326–747 mM for Cl, 0.84–32.6 mM for SO₄, 1.6–3204 µM for H₂S, 8.64–31.7 µM for Li, 313–614 mM for Na, 9.2–15.2 mM for K, 43.9–77 mM for Mg, 3.3–15.8 mM for Ca and 0.2–31.8 µM for dFe, respectively (Fig. 7), similar to previous studies (Çağatay et al., 2004; Tryon et al., 2010; Ruffine et al., 2018). The variations in the porewater concentrations of dissolved nutrients (Fig. 4) and major ions (Fig. 7) throughout the sediment column were affected by a series of microbially mediated diagenetic reactions modifying the geochemical composition of the porewaters in the studied sites.

An important process that needs to be considered while interpreting major ion data in the porewaters of Marmara's surface sediments is the presence of older, lake period-derived porewaters. It was shown that there is a downward freshening gradient of major ions (specifically Cl and Na) due to mixing with the buried brackish water from the Marmara Lake which was observed at all sites in the Sea of Marmara with the exception of Western High and this freshening was more pronounced below 250–300 cmbs in the Marmara Sea (Tryon et al., 2010). As shown in Fig. 7, the lowermost part of our Na and Cl profile (after 35–40 cmbs) started displaying a decreasing trend, supporting the phenomenon of a downcore freshening in the Marmara Sea (Fig. 7). Similar trends were obtained for Mg and K as well, while the decrease in Li and Ca was less pronounced. Still, these data show that most of the porewaters studied in the upper 50 cm of Marmara's current seafloor are well under the influence of the current deep Marmara waters, which are Mediterranean in origin. Hence, we can interpret these data as well as other porewater data in the framework of marine sediment diagenesis.

In that context of major ions discussed above, we can conclude that porewater geochemistry is under the main influence of the series of microbially mediated organic matter degradation reactions such as respiration by NO₃ (denitrification), Fe/Mn oxides, and SO₄, as well as the processes of the SO₄ depletion by anaerobic oxidation of methane (AOM). Carbonate precipitation and the silicate diagenesis also shaped porewater profiles. Vertical profiles of porewater nutrients (Fig. 4) and solid-state TOC / TN (Fig. 6) concentrations indicated that organic matter degradation processes take place in the upper 10–20 cmbs, introducing high concentrations of porewater reactive Si, PO₄, and NH₄ and removing oxidized nitrogen (NO₃) through denitrification. The decrease in SO₄ concentrations with depth in the sediments was due to sulfate reduction as well as the AOM, releasing H₂S, Mg, and Ca in the eastern İzmit Bay. The release of Mg and Ca, then, resulted in carbonate precipitation reactions reducing the porewater concentrations of these ions with depth throughout the sediment column in the eastern İzmit Bay (Fig. 7). Similar chemical composition and diagenetic reactions in the porewaters in different regions of the Sea of Marmara have been observed by the studies performed by Halbach et al. (2002), Çağatay et al. (2004), Tryon et al. (2010), Ruffine et al. (2018) and the strong correlation between gas emissions and fast depletion of sulfate in the upper sedimentary column of the Sea of Marmara suggested the important role of AOM for preventing complete releases of methane originating from the North Anatolian Fault (N.A.F.) and associated faults (Géli et al., 2008, Ruffine et al., 2018). The porewater geochemistry of the obtained core samples from this study and previous studies in different regions of the Sea of Marmara (mainly Çınarcık, Central and Tekirdağ Basins, southern Marmara Sea, İzmit Bay) revealed that the sulfate-depletion zone, corresponding to the sulfate-methane transition zone (SMTZ), ranged from a few meters to less than 15 cm below seafloor (Halbach et al., 2002; Çağatay et al., 2004; Tryon et al., 2010; Ruffine et al., 2018). The findings of this study also showed a shallower SMTZ, less than 50 cm, in the eastern İzmit Bay (Fig. 7) due to an increase in AOM reaction rates by intense emissions of methane resulting in fast depletion of sulfate in the upper sedimentary column (Ruffine et al., 2018). It should be also noted that the SMTZ depth in the Sea of Marmara is controlled by multiple factors in addition to the dissolved oxygen of the bottom waters. These controls include the upward flux of methane (from deeper, lake-derived sediments) and sedimentation rates. The upward methane flux is in turn related to tectonic activity and gas hydrate dissociation, which might be controlled by warming of the bottom waters and hydrostatic pressure changes. As reported previously, spatial variability in methane flux is evident across different sub-basins; in particular, the Çınarcık Basin and İzmit Bay exhibit elevated fluxes in proximity to active fault zones, where the SMTZ occurs at or near the seafloor (Bourry et al., 2009; Crémière et al., 2012; Çağatay et al., 2018).

Organic matter degradation by the Fe/Mn oxides released the reduced forms of these metals into the sediment porewaters (Jørgensen, 1996). Though the dissolved manganese was not measured in this study, previous studies performed in the oxic, suboxic, and anoxic regions showed that anoxic conditions support the accumulation of dissolved manganese, whereas oxic sediments become depleted in manganese (Jørgensen, 1996). In the oxic region of the Black Sea, for example, redox transformations and physical processes caused redistribution of manganese from its initial sources across the bottom water, leading to accumulation of manganese in oxidized form in the upper sedimentary column (Konovalov et al., 2007). A similar process was observed with the relative depletion of reduced iron in sediments in the Southern Marmara Sea having oxic deep waters and its accumulation in the sediments under hypoxic conditions in the Çınarcık and İzmit Bay as also experienced in the oxic, suboxic and anoxic marine environments (Jørgensen, 1996; Konovalov et al., 2007; Yücel et al., 2010) (Fig. 7). According to a study performed in the sediment cores obtained from oxic, suboxic, anoxic/sulfidic parts of the Black Sea (Konovalov et al., 2007), FeS production is faster than pyrite reacting with zerovalent sulfur or H₂S to form FeS₂. If the Fe(III) is available in the sulfidic sediments, Fe(III) reacts with the H₂S to form Fe(II), which in turn reacts with H₂S to form FeS phases. In the Sea of Marmara, the obtained geochemical profiles indicated that the H₂S produced by AOM formed iron-sulfide precipitates in the presence of reduced iron (Halbach et al., 2002). In this study, dFe (referred to sum of Fe(II) + Fe(III)) concentrations ranged from 0.2 to 31.8 µM in the porewaters of the obtained sediment core samples, displaying a maximum in the upper sedimentary column, decreasing to undetectable values below 10–15 cmbs, indicating iron-sulfur precipitation reactions, as also experienced in the anoxic/sulfidic sediments of the Sea of Marmara (Halbach et al., 2002) and Black Sea (Konovalov et al., 2007). The decrease in SO₄ concentrations with depth in the sediments was due to sulfate reduction as well as the AOM, releasing H₂S, Mg, and Ca, specifically in the eastern İzmit Bay as discussed above. The release of Mg and Ca, then, results in carbonate precipitation reactions reducing the porewater concentrations of these ions with depth throughout the sediment column (Fig. 7). However, the release of Ca might also be the result of low-temperature silicate diagenetic processes as also shown in a recent study performed in the Sea of Marmara (Tryon et al., 2010) since low-temperature silicate diagenetic processes depend not only on the availability of the silicate minerals but also available cations such as K, B, Li, Mg and Na. The end products of these diagenetic reactions, Ca and Sr, are released to the porewaters in the Sea of Marmara (Tryon et al., 2010, and references therein). The downcore decreases in the concentrations of Mg, K, Na and Li obtained from this study were also associated with the low-temperature silicate diagenetic processes in the Sea of Marmara.