Water temperature and dissolved oxygen concentration were measured monthly from October 2007 to August 2010 at 1 m intervals over the northern deep point using a YSI 6820 Multiparameter sonde (YSI). Thirty-one sediment cores, LAZ–10/01 to LAZ–10/31, up to 96 cm long, were collected in 2010 with a gravity corer (Tylmann, 2007) equipped with a 60 mm diameter PVC tubes at a regular depth interval (Fig. 1). Retrieved cores were tightly sealed and transported to the GEOPOLAR laboratory (University of Bremen, Germany) and stored at a temperature of 4 °C. Afterwards, cores were split lengthwise, described macroscopically and photographed. Finally, samples from the top 1 cm of each core were taken, dried, and homogenized in an agate mortar.

For elemental (CNS) analysis of total carbon (TC), total nitrogen (TN), and total sulfur (TS), homogenized sediment samples were weighed into tin (Sn) capsules with tungsten trioxide (WO₃) catalyst. To analyze total organic carbon (TOC), a second batch of sediments was weighed into silver (Ag) capsules, heated to 80 °C, and acidified with 3 % and 20 % HCl to remove carbonates. The capsules were then rinsed with distilled water. Concentrations of TC, TN, and TS were determined with the EuroEA elemental analyzer (Eurovector). Total inorganic carbon (TIC) was calculated by subtracting TOC from TC. Biogenic silica (BSi) concentrations were determined after sample digestion in 1 mol NaOH at 70 °C using a segmented flow procedure (Müller and Schneider, 1993).

A non-destructive micro-X-ray fluorescence (μXRF) scan was performed with an ITRAX core scanner (Cox Analytical Systems) at the GEOPOLAR. Samples were fixed in an acrylic glass sample carrier (Ohlendorf, 2018) and scanned using a molybdenum (Mo) X-ray source (30 kV, 25 mA), with a 100 s count time per sample. Due to the compositional nature of μXRF data, results were converted to centered log-ratios (clr) (Bertrand et al., 2024).

A four-step sequential extraction of Fe and Mn fractions was performed following the procedure of Tessier et al. (1979) and Zimmerman and Weindorf (2010). Solutions of surface-bound ions, (oxy)hydroxides, organic matter-bound ions, and ions within the siliciclastic minerals' lattices were measured using an atomic absorption spectrometer AA-6800 (Shimadzu) at the Institute of Oceanology, Polish Academy of Sciences (Sopot). A detailed procedure is available in the Appendix.

All statistical procedures were conducted using R 4.5.1 (R Core Team, 2025). To achieve a better balance between groups, partially laminated and homogeneous sediments were aggregated. The “tidyverse” 2.0.0 (Wickham et al., 2019) was used for most of the analyses and visualization. μXRF data were processed using the “robCompositions” 2.4.1 (Templ et al., 2011). Due to the non-normal distribution of analyzed variables, Spearman's rank correlation was used to test relationships between the proxies. A robust principal component analysis (RPCA) was used to visualize the overall data structure and internal relationships between the variables using the “pcaPP” 2.0-5 (Filzmoser et al., 2024). Before the multivariate statistics, data were log-transformed, scaled, and centered. Spatial interpolation was performed using the thin plate spline regression with “fields” 16.3.1 (Nychka and Furrer, 2021). To test whether there are significant differences between the selected variables and between the sediment classes, we used a non-parametric Wilcoxon test. Generalized additive models (GAMs) were fitted using “mgcv” 1.9-3 (Wood, 2019).

Lake Łazduny water temperature exhibited seasonal stratification and homothermy typical of temperate-climate zone lakes in central Europe (Fig. 2a). Brief mixing in spring and fall separated the summer and winter stratification periods. The maximum surface water temperature reached 26.1 °C in July 2007. Under the ice, reverse stratification was typical but relatively weak, closer to homothermic conditions, and occurred shortly during the lake turnovers. The ice onset was stable, beginning in December, while the thaw depended on the spring temperatures. The ice cover lasted between 66 and 140 d, breaking up between early March (2008) and early May (2010). Oxygen concentrations during the study period varied with time and depth (Fig. 2b). The depth of the oxycline shifted between 6 and 20 m (complete turnover). On average, the boundary of hypoxic conditions (< 2 mg L⁻¹ DO) resided around the depth of 12 m, while anoxic conditions (< 1 mg L⁻¹ DO) established between 13 and 14 m deep (oxygen levels follow Nürnberg, 1995). Surface waters remained oxygenated. The highest oxygen concentrations were observed at 5–6 m, reaching 17.9 mg L⁻¹. In January 2009, under the ice cover, extremely low DO concentrations developed throughout the majority of water column, with only the first 5 m remaining oxygenated. Two complete turnovers were registered in Lake Łazduny during the study period, temporarily reoxygenating the hypolimnion. Mixing events began with an oxycline near the water's surface, which then migrated downward, occasionally reaching the sediments. Typically, less than 30 d were necessary for oxygen consumption and reestablishment of anoxia. During the stratification period, the oxycline migrated upwards.

The structure of the surface sediments in Lake Łazduny varied with distance from the shoreline and depth (Fig. 1), as well as with average oxygen availability. Homogeneous sediments were located closest to the lake shore at depths up to 12 m, where oxic conditions prevailed. Partially laminated sediments occupied a transition zone between 12 and 15 m, experiencing a migrating oxycline. The depth of this gradual change in sediment structure corresponds to the average depth of the anoxic/hypoxic boundary. Below 15 m, underneath the predominantly anoxic hypolimnion, only laminated sediments occurred.

Elemental data varied depending on the location (Fig. 3, Table A1). Organic matter, represented by TOC (5.5 %–24.3 %), was deposited mainly in the oxic littoral zone. Additionally, the northern part of the lake is dominated by Chara, which increases the abundance of aquatic organic matter (low C / N, Fig. A1). The western and south-western littoral is enriched with terrestrial organic matter originating from the catchment (higher C / N, Fig. A1). The central, anoxic part of the basin, where laminated sediments were found, was depleted in organic matter. The difference between homogeneous and laminated sediments is significant (W = 101, p < 0.05). Concentrations of TIC (2.4 %–8.3 %), representing the carbonates, were typically higher in the oxic zone. Mean TIC concentrations were higher in the homogeneous sediments and lower concentrations in the laminated sediments were statistically different (W = 85, p < 0.5). Total sulfur concentrations (0.2 %–1.6 %) were the highest close to the shores and outlet on the southern end. However, generally, TS exhibited a more random pattern. There was no substantial difference between mean concentrations of the massive and laminated sediments (W= 112, p > 0.5). Biogenic silica, a primary production proxy representing the deposition of siliceous algae such as diatoms, showed a deposition pattern that was somewhat opposite to that of TOC. The highest concentrations were found in the anoxic, laminated sediments (max = 25.2 %). In contrast, in the shallow, oxic, homogeneous sediments, concentrations were significantly lower (W=217, p < 0.5).

μXRF data (Fig. 4) showed similar trends to those of elemental data (Fig. 3). Titanium (Ti_clr), a terrigenous input proxy concentrated in the littoral zone, with the lowest values in the deep basins. Sulfur (S_clr) showed a similar pattern to TS, and it was primarily depleted in the deep sediments. Despite its expected detrital origin, silica (Si_clr) showed deposition patterns comparable to those of BSi (Figs. 3 and 4), with the highest concentrations in the lake's deepest, anoxic parts. Calcium (Ca_clr) was mainly associated with TIC concentrations. Furthermore, redox-sensitive iron (Fe_clr) and manganese (Mn_clr) showed enrichment in the deepest, anoxic parts of the lake, with an overall pattern opposite to that of sulfur. Si_clr, Fe_clr, and Mn_clr exhibited a sharp increase with depth and the spatial extent of anoxia. After controlling for detrital input, Fe / Ti and Mn / Ti ratios suggest that the highest deposition of both metals is confined mostly to the deepest parts of the lake. Manganese departs from this pattern slightly, also showing elevated values close to the lake outlet.

The distribution of four major Fe fractions is shown in Fig. 5. Overall, in agreement with μXRF data, most Fe was concentrated in the deepest, anoxic parts of the lake (Table A2). The total concentration of Fe (Fe_tot) in the laminated sediments differed significantly and was greater than in the homogeneous sediments (W=185, p < 0.05). The mean concentration in the laminated sediments reached 9649.93 µg g⁻¹, whereas in the homogeneous sediments it was 6020.25 µg g⁻¹. Fe_tot was highly correlated with the Fe_clr record (ρ= 0.92, Fig. A2). Especially surface-bound ions (Fe_surf) and Fe (III) (oxy)hydroxides (Fe_oxy) showed enrichment in the deepest parts of the lake. Fe ions bound to the organic matter (Fe_org) exhibited similar patterns to those of TOC (Fig. 3). Finally, ions bound within the crystal lattice of siliciclastic minerals (Fe_sili), showed distribution like Fe_surf and Fe_oxy, with the highest concentrations found in laminated sediments (Fig. 5). However, there was a noticeable shift towards the western littoral zone compared to Fe_oxy.

Similarly, four Mn fractions were studied (Fig. 6, Table A3). The highest total Mn (Mn_tot) concentrations were observed in the central, anoxic part of the lake (Fig. 6), averaging 556.4 µg g⁻¹. In contrast, in the homogeneous sediments, Mn_tot averaged at 369.3 µg g⁻¹ (Table A3). Like the Fe_tot concentrations, Mn_tot concentrations were higher in the laminated sediments than in the homogeneous sediments (W=157.5, p < 0.05). Mn_tot was highly correlated with the Mn_clr (ρ=0.96, Fig. A2). Surface-bound ions (Mn_surf) were abundant in the central part of the basin, while the shallow northern part and lake shoreline were depleted. Mn (IV) (oxy)hydroxides (Mn_oxy) showed the most striking spatial pattern and were most abundant in the deepest parts of the lake (Fig. 6). Mn bound to organic matter (Mn_org) was enriched in the deepest parts of the lake. Mn within a crystal lattice of siliciclastic minerals (Mn_sili) once again showed enrichment in the deepest part of the lake. However, similarly to the Fe_sili, it was slightly shifted towards the western shore of the lake in comparison to Mn_oxy.

Relationships between the sampling depth, sediment type, oxygen conditions, and selected geochemical variables are shown in Figs. 7 and A4. Ti_clr and TOC behaved similarly, showing lower values with increasing depth and anoxia. The second group of elemental variables, Ca_clr and TIC, showed flat slopes and were influenced by outliers, with no clear separation between the oxidation zones. S_clr and TS showed a weak tendency towards lower values with increasing depth. A comparison between the Si_clr and BSi datasets showed agreement, indicating enrichment with depth and a baseline shift within the anoxic zone.

Fe_clr and Fe_tot had an almost linear relationship with the increasing depth (Fig. 7), with a clear separation between the homogeneous and laminated sediments and the oxic and anoxic zones (Figs. 5, 7, A3 and A4). The response of Mn_clr and Mn_tot to the depth increase was weaker (Fig. 7). Relations were non-linear, and the separation in intermediate depths was not as straightforward as for Fe. The lowest concentrations were associated with homogeneous sediments, while the highest were associated with laminated sediments. Similarly, Fe / Ti and Mn / Ti ratios followed patterns of both μXRF-derived and total concentrations based on sequential extraction, showing clear enrichment in the sediments from the deeper parts of the basin. Fe / Mn ratios, based on μXRF and sequential extraction, showed good agreement (Figs. A5, 7). Generally, the ratio exhibited a weak yet expected tendency towards higher values in the deeper lake zones. However, there were some outliers.

Figure 8 depicts the expected behavior of the Lake Łazduny water column, dissolved and particulate matter, and sediments in response to changing limnological conditions. Lake Łazduny exhibits a limnological regime like that of other temperate-climate lakes. The defining features are seasonal thermal stratification and spring and fall turnovers (Bonk et al., 2015; Roeser et al., 2021). Depending on the meteorological conditions, Lake Łazduny shifts between dimictic, monomictic, and meromictic mixing regimes (Szczerba et al., 2021). Even in deep lakes short and intense mixing events occasionally reoxygenate the hypolimnion (Żarczyński et al., 2022). Sedimentation in Lake Łazduny follows the well-described pattern observed in other lakes with varved sediments (Zolitschka et al., 2015), with diagnostic calcite laminae forming in the warm season (Tylmann et al., 2013a). Most calcite laminae are preceded by the deposition of diatom frustules, which in places produce distinct, macroscopically visible layers. During the warm season, increased primary production and higher water temperatures influence the epilimnetic pH and carbon budget, steering carbonate precipitation (Dean and Megard, 1993).

After stratification onset, oxygen in the deep water is rapidly consumed, leading to anoxia. Depending on hydrometeorological conditions and ice phenology, the bottom waters of Lake Łazduny can remain anoxic for extended periods, spanning multiple years (Szczerba et al., 2021). Thus, the water column is separated into the mixolimnion and the monimolimnion (Boehrer et al., 2017). Each year as the oxycline moves downward, a portion of the lake bottom reaching at times up to 14–15 m deep is oxidized (Fig. 8). Conversely, once stratification develops, the oxycline moves back toward the surface, and the lakebed area under anoxic conditions extends. Oxygen conditions control post-depositional sediment stability as laminations are easily destroyed by bioturbation and gas release. In the absence of oxygen, these processes are restricted, allowing varve preservation (Zolitschka et al., 2015).

The spatial diversity of the sediment lithology in Lake Łazduny corresponds to the average extent of hypoxic and anoxic conditions. Sediment structure therefore reflects the properties and dynamics of the water column. Geochemical composition records changing conditions more directly, whereas lamination is a secondary effect, preserved only when there are no disturbances (Zolitschka et al., 2015). This resembles Lake Suminko, where Tylmann et al. (2012) demonstrated that the spatial extent of the varved sediments mirrors the extent of the monimolimnion. In Lake Łazduny, homogeneous sediments occupy parts of the lake subject to intense mixing and permanent oxic conditions. The deeper transition zone (≈ 12–14 m depth), which is at least seasonally hypoxic, is characterized by partially laminated sediments, suggesting that recent conditions have been favoring the preservation of these sediment structures. The presence of laminations in the uppermost parts of the cores, overlying a homogeneous sediment, indicates that, at some point, monimolimnion was likely restricted to the deeper lake zones. Finally, below a depth of 14 m, the lakebed is primarily anoxic and is almost exclusively occupied by well-preserved laminated sediments. This demonstrates that oxygen conditions changing with the water depth control laminae preservation, providing evidence for the past extent of the hypolimnion. However, since wind stress and water column dynamics control mixing depth, the spatial variability of the sediments may also reflect mechanical sediment reworking, resuspension and resedimentation. Part of the relationships between detrital (Ti) and redox sensitive elements (Fe, Mn) could therefore be driven by transport processes, rather than geochemical focusing. Such sorting, however, would deposit finer fractions deeper in the lake, in contrast to coarser, detrital fractions, which are associated with erosive littoral zone and higher environment energy (Rowan et al., 1992). Then, Fe, Mn and Ti would covary, which is not a case in Lake Łazduny.

The chemical composition of the surface sediments of Lake Łazduny varies with lithological type and water depth. Spatial variability and GAMs (Fig. 7) indicate progressing differences between the sediments occupying different water depths, which in turn results in differentiation of homogenous and laminated sediments (Fig. A4). In the littoral zone, a mixture of minerogenic (Ti) and organic (TOC, TS) sediments dominate while sediments enriched in Fe and Mn dominate in deeper parts of the lake bottom, most probably as a result of geochemical focusing (Engstrom et al., 1985). The concurrence of organic and terrestrial matter is most probably a result of a broad littoral zone in the north. Lake Łazduny cuts into the outwash plain sands and gravels, and small gullies developed in the glacial drift supply the shallow waters with terrestrial matter. Sparse mineral grains of the larger fractions were found in the sediments. Organic matter in Lake Łazduny has two major sources. Primary production leads to a uniform distribution of organic matter, which can then be concentrated in the basin's deepest parts. However, the shoreline of Lake Łazduny is densely vegetated. Deciduous trees are a source of litter that locally provides large quantities of organic matter, primarily carbon (DeGasparro et al., 2019) and nutrients, and sulfur (Hongve, 1999) to the littoral. Abundant Chara meadows, especially in the lake's northernmost part, provide an additional source of organic matter.

Fe_org is correlated with biogenic silica, consistent with its organic provenance, as Fe is an important nutrient and a constituent of diatom cells (Hutchins and Bruland, 1998). BSi, resulting mainly from the deposition of redox-resistant diatom valves (Smol and Stoermer, 2010), follows the expected pattern of hydrodynamic focusing, with the highest concentrations in the deepest areas. As diatom frustules often undergo hydrodynamic sorting and transport (Anderson, 1990), the same process could control Fe_org, leading to its elevated concentrations in the deepest parts of the lake. Interestingly, most of the Fe is not correlated with sulfur concentrations. Only Fe_org shows a moderate correlation with S, suggesting that sulfide formation is not an important pathway for Fe. Interestingly, sulfur is deposited mainly in shallow areas, which are more often oxidized than deep sediments, suggesting deposition and cycling of organic-bound S (Couture et al., 2016). In the deeper parts of the lake elevated abundances of both Fe and Mn (oxy)hydroxides, which act as oxidizing agents, can be regarded as a occasional drivers of sulfur release (Urban, 1994). Furthermore, Charophyta meadows in the lake reside close to the shoreline, providing an additional source of algal organic matter and inducing calcite (CaCO₃) precipitation. This could explain higher TIC concentrations in the shallow lake zones rather than in the lake's deepest points.

Manganese shows spatial patterns similar to those of iron (Figs. 5 and 6). However, the majority of Mn lies between the deposition of calcium-dominated carbonates and Fe-bearing matter (Fig. A3). Opposite trends in Mn concentrations relative to organic and terrestrial matter suggest that geochemical focusing controls manganese concentrations in the sediments. This is further strengthened by the spatial variability of Mn / Ti ratios, with the highest values observed in the deepest parts of the lake, except for the lake outflow, where hydrodynamically induced lateral transport could play a more important role. Opposite signs in PC2 (Fig. A3) indicate that manganese concentrations peak while organic matter concentrations decline. The decomposition of organic matter is a well-known process that alters water pH and CO₂ availability, creating a pathway for carbonate formation. Mn and Fe carbonates in lacustrine settings are most often reported in varved sediments. Recent studies show that these carbonates are a plausible pathway for manganese burial in sediments of anoxic hypolimnion and are controlled by Mn availability or pH changes (Bonk et al., 2021; Dräger et al., 2017; Müller et al., 2021). High-resolution observations and sedimentological studies from Lake Żabińskie have shown that rhodochrosite (MnCO₃) can constitute up to 15 % of the annual mineral mass in the sediments (Żarczyński et al., 2022). This represents the intrinsic connection between seasonal changes in the redox conditions that control the formation of these minerals (Davison et al., 1982) and the preservation of the varves (Zolitschka et al., 2015).

Mn and Fe carbonates and their dependence on water column stratification have also been reported in numerous marine settings (Astakhov et al., 2006; Burke and Kemp, 2002; Frederichs et al., 2003). Meister et al. (2009) suggest that the presence of Mn-oxides and their partial reduction during H₂S oxidation increases alkalinity and promotes the precipitation of Ca-rhodochrosite at geochemical focusing sites. This could also influence low sulfur concentrations in the deepest sediments of Lake Łazduny. Häusler et al. (2018) demonstrated that periods of deep-water oxygenation trap dissolved Mn in the reducing sediments, thereby facilitating carbonate formation. A diagnostic feature of the laminations of Lake Łazduny is autochthonous calcite (Tylmann et al., 2013b). Organic matter decomposition and elevated HCO₃ supplied by calcite dissolution can lead to supersaturation of the sediment-water interface with respect to the Mn-carbonates (Stevens et al., 2000). Contact of the carbonate-rich surface waters with the Mn-enriched bottom waters was suggested early on (Dean and Megard, 1993) as a driving of Mn-carbonate formation. In Lake Ohnuma, rhodochrosite is associated with summer stratification and organic-rich lamina as a product of the Mn ions reacting with the HCO3- (Katsuta et al., 2020).

Yet, in mesotrophic Lake Łazduny primary production is a relatively low (Szczerba et al., 2021). Therefore, the decomposition of organic matter in sediments, the release of CO₂, and pH changes are less notable than in more productive lakes. Furthermore, Mn in Lake Łazduny sediments is deposited mainly as (oxy)hydroxides. Undoubtedly, the formation and preservation of Mn-bearing minerals in sediments is a complex problem that depends on water ventilation and pH (Jouve et al., 2013), as well as on the presence of organic matter and other minerals (Wittkop et al., 2020).

The iron and manganese phases change with redox conditions and pH (Davison, 1993; Davison et al., 1982). As a result, Fe and Mn have been widely used in paleolimnological studies as paleoredox tracers, with the expectation that higher Fe and Mn concentrations reflect greater oxygen availability (Engstrom et al., 1985; Mackereth, 1966; Vegas-Vilarrúbia et al., 2018). However, other processes often control their abundance and spatial differentiation, such as delivery rates and provenance (Tribovillard et al., 2006) or biogeochemical cycling (Klaveness, 1977). Therefore, the interpretation of Fe and Mn in geological records requires caution (Tribovillard et al., 2006) and controlling for detrital delivery. This is achieved through elemental ratios, considering inert elements such as Ti (Kylander et al., 2011) or by testing multivariate relationships between the terrestrial inputs and trace metal abundances (Żarczyński et al., 2019). In Lake Łazduny, Ti_clr shows low importance in the dataset, whereas K_clr is either uncorrelated or anticorrelated with Fe and Mn (Figs. A3, 4). Therefore, we interpret Fe and Mn concentrations as diagnostic of at least partially redox-dependent processes. Furthermore, the spatial variability of Fe / Ti and Mn / Ti (Fig. 4) indicates that both redox-sensitive metals are enriched in the deepest parts of the basin even after accounting for detrital input, arguing against detrital delivery as the main control on their distribution. We argue that the influence of hydrodynamic focusing, in which particulate matter is being transported, plays a less important role in Lake Łazduny, where the littoral zone is limited except in the northern part. This does not exclude the process but rather limits its magnitude. Our monitoring data, especially the depth of the oxycline and spatial Mn patterns, suggest a strong link between lake turnover, hypolimnetic oxygenation, and Mn burial in sediments.

As the oxycline migrates deeper into the water column, reductive dissolution and reoxidation processes increase the concentrations of Mn and Fe in the water and sediments (Fig. 8, Davison, 1993). Fe and Mn mobilization and migration toward the deepest point depend partially on the development of anoxic conditions (Engstrom et al., 1985). Remobilized and geochemically focused, Fe and Mn are trapped in the hypolimnion and immobilized by short oxidation pulses. Sediment trap and core studies from Elk Lake suggest that (oxy)hydroxide could form during the mixing as oxycline migrates downwards, whereas (oxy)hydroxide rains occur likely during the stratification periods as redissolved Mn and Fe migrate upwards, possibly redistributing the Mn and Fe to the shallower depths (Nuhfer et al., 1993). Primarily, Fe (oxy)hydroxides are known to withstand anoxia to some extent and form semi-stable deposits (Dean and Megard, 1993; Żarczyński et al., 2019). Thus, geochemical focusing, coupled with rapid oxidation, can immobilize Fe and Mn in sediments. These, in turn, can act as electron acceptors during the oxidation of the other sediment components.

Scholtysik et al. (2020) showcased continuous sedimentation of Mn oxides throughout the summer and enrichment in the anoxic hypolimnion of Lake Stechlin. That kind of Mn behavior can lead to an interpretation of Mn (and Fe) profiles in the lake sediments that is contrary to the majority of the paleolimnological studies. Żarczyński et al. (2022) used Mn deposition events to accurately pinpoint holomixis in Lake Żabińskie, as Mn had to be first enriched in a seasonally anoxic environment. Even when Fe and Mn are remobilized in the anoxic hypolimnion, lake stratification hinders their possible loss via outflow, as, depending on lake morphology, dissolved Fe and Mn would have to cross the oxycline threshold and be mostly flushed out.

However, it must be stressed that the stratigraphic position of Fe and Mn enrichments must be accounted for. In Lake Łazduny once spatial variability is accounted for, a weak tendency for increased Fe and Mn burial in the deeper zones is visible, even though some of the deepest samples from Lake Łazduny exhibited a slightly lower Fe / Mn ratio, typically suggesting higher redox (Naeher et al., 2013). However, on longer scales, minuscule variability within the anoxic zone should not play an important role. A study of Sanchini et al. (2020) based on μXRF, sedimentary pigments, and hyperspectral imaging provides independent evidence that, since its formation ca. 9750 cal BP, Lake Łazduny has experienced periods of either stable meromixis or seasonal anoxia, punctuated by mixing events. The former, especially over the last ca. 400 years, is linked to elevated Mn burial in sediments (Sanchini et al., 2020), driven by intensified lake mixing, supporting our interpretation. Yet, even during these periods of increased mixing intensity, Lake Łazduny remained seasonally anoxic. Therefore, we interpret mixing as a process leading to increased geochemical focusing. Our findings based on the uppermost sediments of Lake Łazduny suggest that even though seasonal anoxia is necessary for Fe and Mn enrichment and their geochemical focusing, these elements can be successfully used as proxies of past oxygenation of bottom water. In this sense, anoxia should be seen as a starting point which ultimately could lead to permanent Fe and Mn burial in the sediments once they become oxidized (Żarczyński et al., 2019).