Introduction

Pleistocene extraglacial ice-dammed lakes were formed as a result of ice-barring of a river valley and damming up the river flowing toward the ice-dam. Clay-silty varves formed in such lakes are distinctive glacial features, due to the rhythmic sequence of deposition of sediments over a single year and are useful for Pleistocene stratigraphy. The method known as “varve chronology” was invented in Sweden (de Geer Reference De Geer and Goldthwait1912) and has been applied successfully in many areas around the world.

The Lębork ice-dammed lake provides an example of sedimentation in an extensive basin developed at an ice-sheet terminus. Ice-dammed lake sediment deposits develop in water bodies formed through the inhibition of runoff and damming waters flowing through the ice sheet terminus. They are lithologically distinctive and characterized by a sequence of facies, from fluvioglacial sands through glaciolimnic deposits, to ice-dammed lake rhythmites (Paluszkiewicz Reference Paluszkiewicz2004).

Rhythmically stratified (varved) series are sediments characteristic and diagnostic of glaciolimnic environments. The Lębork ice-dammed lake sequence was developed in the course of cyclical sedimentation defined as the development of deposits with systematic sequence of one or more facies, designated as the AB sequence. Such a sequence develops in the course of a single sedimentation cycle described as a cyclothem (Karnkowski Reference Karnkowski1993).

The term varve was defined by de Geer (Reference De Geer and Goldthwait1912), the creator of the varvochronological concept, as a periodically repeating pattern of layers of mineral series, rhythmically stratified, with dark and light laminae, differing in geochemical and granulometric composition, developed in the course of a single sedimentation cycle (De Geer Reference De Geer and Goldthwait1912). The material in the dark laminae has an homogeneous mineralogical composition of the finest clay fractions that persisted in suspension for a long time. Deposition occurred slowly, in the winter period under the ice cover, with an absence of coarser fractions from proglacial waters. The laminae thus developed are thin, dark clay layers. Light ‘summer’ laminae developed in the course of deposition during the summer season. The supply of the coarser fraction of mineral grains from ice ablation is considerably more intensive during that time. Particles of sandy and silty fractions are deposited much more quickly, developing light laminae which are thicker than ‘winter’ laminae, with variable mineralogical and granulometric composition. Considering single-cycle – light ‘summer’ and dark ‘winter’ laminae – de Geer (Reference De Geer and Goldthwait1912) determined that they correspond to the annual sedimentation cycle. Such an assumption permits absolute dating of varved deposits. This geochronological method was called the Swedish timescale.

The supply of material and the process of development of rhythmites in glaciolimnic basins are determined primarily by allocyclical processes related to external conditions (e.g. climate, current weather, rate of glacier ablation, volume of material supplied to the basin, etc.), and to a lesser extent by autocyclical processes (precipitation of mineral compounds, development of living organisms, activity of density currents (Karnkowski Reference Karnkowski1993)).

Two basic hypotheses exist in terms of the genesis and formation of fluvioglacial deposits – gravitational and turbiditic (Bakhmutov et al. Reference Bakhmutov, Yevzerov and Kolka2008). According to Antevs (Reference Antevs1951), deposition of summer varved laminae occurs as a result of the accumulation of silts after summer flooding of proglacial waters, and winter laminae, in the form of clays, occur as a result of the process of deposition from suspension under ice cover. Other authors defined varves as deposits developed as a result of seasonal activity of bottom currents or their specific type, namely “turbidity currents” (Kuenen Reference Kuenen1951). Typical “classic” varves defined by Sturm (Reference Sturm and Schluter1979) seem to be characterized by sharp boundaries between laminae and with a lack of gradation typical of the Bouma sequence; these are a result of the process of deposition of material from suspension and outside the range of activity of underflows from different zones of thermal convection of water and “interflow currents” (Sturm Reference Sturm and Schluter1979).

Varves are usually relatively thin, 0.5–5.0 cm, although light laminae are usually somewhat thicker. Light laminae which are much thicker, up to several cm, are also encountered, however. They commonly feature visible second-order laminae with a varved character. The second-order laminae are usually interpreted as daily or diurnal varves, or as repeatedly stratified aggradation silts developed by underflows. Inflow does not have to be constant over a single deposition season; it can also be related to daily ablation and weather changes. The ablation and changes in weather can indicate a variable supply of transported material. Light laminae are, therefore, considered to be the deposit of a single sedimentation cycle which can be developed over the course of many such cycles of a smaller order. The term “interseasonal laminae” seems more suitable for describing this type of multilayer deposit (Vyahirev Reference Vyahirev1997).

Varves considered to be deposits of annual sedimentation do not necessarily have to reflect deposition occurring over the entire year. This results in the problem of interpretation of varves as an accurate geochronological method.

According to Merta (Reference Merta1978), changes in the thickness of particular varves could be related to the width of the sedimentary basin and not just to climate change, e.g. a rapid change in varve thickness could be the result of rapid change in the width of the depositional area, an over-flooded, terrace-shaped river valley.

A detailed sedimentological analysis of glaciolimnic formations, based on the example of the Warsaw ice-dammed lake, was presented by Merta (Reference Merta1978) who designated the type of extraglacial ice-dammed lakes, simultaneously suggesting that it is dominant throughout the area of the Polish Lowland.

Varved deposit series are usually deposited horizontally in accordance with the terrain unevenness and inclination (Paluszkiewicz Reference Paluszkiewicz2004, following Krygowski Reference Krygowski1934). As in other depositional environments, syn- and post-sedimentary deformation processes can occur here. The development of runoff disturbances may be caused by an inclination as small as 1° (Peterss Reference Peterss, Ehlers, Kozarski and Gibbard1995); these are related to direct accumulation of sediment in various morphological conditions of the basin bottom, with deposition resulting from the activity of density currents or melting of rooted patches of dead ice.

The most frequent occurrence of ice-dammed lake sedimentation is observed in northern Poland in the Pomeranian Region, in marginal zones of the Pomeranian phase of the Vistula glaciation.

The purpose of the present study was to determine the geochemical and mineralogical composition of the Lębork sediments and their lateral and vertical variability. These results will allow the sedimentation process to be characterized and for the sediment supply over the ~2000 y of existence of the ice-dammed Lębork lake to be understood.

Characteristics of the Study Area

Deposits filling the Lębork ice-dammed lake, the so-called “Lębork clays” (Piątkowski Reference Piątkowski1960; Morawski Reference Morawski1989, Reference Morawski and Kostrzewski1991), are an example of the sedimentation record of an extensive, ice-dammed lake developed at the ice-sheet terminus. The lake was located in northern Poland (Fig. 1), in the Łeba and Reda ice-marginal valley. This mesoregion is a part of the Koszalin Coastal Area (Kondracki Reference Kondracki2000). The existence of the ice-dammed lake is related to the last occurrence of the Fennoscandian Ice Sheet in the territory of Poland (Stroeven et al. Reference Stroeven, Hättestrand, Kleman, Heyman, Fabel, Fredin, Goodfellow, Harbor, Jansen, Olsen, Caffee, Fink, Lundqvist, Rosqvist, Strömberg and Jansson2016) during the Gardno phase of the Vistula glaciation. The Lębork ice-dammed lake developed within the Łeba ice-marginal valley, 10–12 km southeast of the ice-sheet terminus during its retreat toward the Gardzieńsko–Łebska Lowland (Morawski Reference Morawski and Kostrzewski1991), when the main water outflow from the front of the ice-sheet terminus was to the west. Moreover, the ice-dammed lake was fed by smaller rivers: the Reknica channel from the north, and through the Kiszewa channel from the northeast (Fig. 2).

Fig. 1

Location of the Lębork ice-dammed lake (Lb), during the Late Vistulian in Poland, and neighboring areas. The figure was compiled from a number of previous studies. Selected, non-calibrated radiocarbon dates are shown. Ice sheet limits: L — Leszno (Brandenburg) Phase, Pz — Poznań (Frankfurt) Phase, Pm — Pomeranian Phase, G — Gardno Phase, SB — Słupsk Bank Phase, SMB — Southern Middle Bank Phase. Also indicated are limits of minor local glacial oscillations and proglacial lakes in the Middle Vistula and Middle Neman valleys (after Marks Reference Marks2005, modified)

Fig. 2

Range of the Lębork ice-dammed lake (source: Morawski Reference Morawski1989; simplified). Explanation: 1 – moraine areas; 2 – bottoms of river valleys and the Łeba ice-marginal valley; 3 – silts of the Lębork ice-dammed lake; 4 – clays of the Lębork ice-dammed lake; 5 – position of the ice-sheet terminus during the existence of the Lębork ice-dammed lake; 6 – areas of dead ice during the existence of the Lębork ice-dammed lake; 7 – maximum range of the ice-dammed lake before the erosion of clayey deposits in the bottom of the Łeba ice-marginal valley (data from, among others, Piątkowski Reference Piątkowski1960; Morawski Reference Morawski1989, Reference Morawski1990)

Horizons of sands deposited previously occurred west of the ice-dammed lake, blocking water outflow through the bottom of the Łeba ice-marginal valley. In the central part of the basin (with a surface area of ~25 km²), the finest clay material was deposited, whereas silts and sands were deposited in the bottoms of the tributary channels. The geological structure of the study area is presented in Fig. 3.

Fig. 3

Fragment of the detailed geological map at a scale of 1:50,000 (15 (west of the lake) – ice-dammed lake clay deposits) (source: Zaleszkiewicz Reference Zaleszkiewicz2005 sheet 13 Łęczyce, N-33-60-B, PGI)

The remains of the ice-dammed lake are varved laminae of clays and silty-sandy deposits (Fig. 5) reaching a maximum thickness of 14 m (Zaleszkiewicz Reference Zaleszkiewicz2005) to 16 m (Morawski Reference Morawski1990). The ages of the varves were determined by means of the thermoluminescence method (TL, measurement error ± 1.5–2.5 y) for fine sand deposits underlying clays directly. These had an age of 14 ky; silty laminae in the uppermost layer of varved clays had an age of 13 ky; locally occurring overlying sands were dated at 11 ky (Morawski Reference Morawski1989, Reference Morawski1990, Table 1).

Table 1

Stratigraphic table for the Late Pleistocene and Early Holocene

Italic indicates the period analysed in the present study (late glacial source: Richling and Ostaszewska Reference Richling and Ostaszewska2005, modified)

The clay deposits filling the basin are of considerable practical importance as raw material for the production of ceramics for construction. They are excavated on an industrial scale from an extensive excavation wall in Lębork, providing raw material for a large ceramics production plant (currently Wienenberger).

Documentation of the deposit recorded up to the 1980s (Morawski Reference Morawski1990) estimated the volume of the varved clays to be 4384 m³ in the Lębork deposit, and 8442 m³ in the Nowa Wieś Lęborska deposit within the same ice-dammed lake.

RESULTS AND DISCUSSION

The chemical compositions of the ice-dammed lake clays of the Lębork deposit showed that the dominant component of the clays is SiO₂ (Table 2)_. The mean SiO₂ content for the entire deposit is 56.13 wt.%, with a maximum of 60.74 wt.% for the middle part of the profile from location 1, and a minimum of 51.47 wt.% in the uppermost part of the profile at location 2. The standard deviation of the SiO₂ content is 3.27 wt.% (Table 3). The second most abundant component is Al₂O₃ (Table 2), with a mean content throughout the entire deposit of 11.61 wt.%, which has a maximum value of 12.56 wt.% in the middle part of the profile of location 3, and a minimum content of 10.41 wt.% in the middle of the profile of location 2 . The small standard deviation is noteworthy, just 0.72 wt.% for Al₂O₃ (Table 3.). The next most abundant component in terms of content in the analysed deposit is CaO (Table 2). The arithmetic mean CaO content for the entire deposit is 8.32 wt.%, with a maximum of 9.82 wt.% in the bottom of the location 2 profile and minimum of 6.11 wt.% in the top of the location 1 profile . The standard deviation of the CaO content was 1.20 wt.% (Table 3). The amount of Fe compounds in the analysed deposits is also noteworthy. The analysis for Fe(III) oxide (Fe₂O₃) showed a mean arithmetic content in the deposit of 5.33 wt.% (Table 3). The maximum of 6.42 wt.% was found in the uppermost part of the location 2 profile, and a minimum of 4.54 wt.% in the bottom part of the location 2 profile (Table 2). The very small standard deviation of Fe₂O₃ content, of 0.68 wt.% for the entire deposit, is also significant.

Table 2

Chemical compositions of ice-dammed lake clays from the Lębork deposit (wt.%)

Table 3

Statistical parameters of the primary components of ice-dammed lake clays

Magnesium and potassium are expressed as oxides because of the aforementioned process of ignition of samples. The occurrence of Mg may be related either to the presence in the moraine till of the Gardno phase of Paleozoic dolomites found by Nowacka and Neumann (Reference Nowacka and Neumann2008), and/or to processes of weathering of aluminosilicates.

For the purposes of statistical calculations (Table 4), a matrix of correlation coefficients was applied to describe relationships between the main chemical compounds of the deposits analysed. Significant correlations (>|0.7|) are highlighted in red.

Table 4

Matrix of correlation coefficients; correlations of >|0.7| are shown in italic

Table 5

Contents of significant elements in the Lębork deposit

In accordance with the methodology of processing results of geochemical analyses, linear Pearson correlation analysis was performed (Table 6). This provided the basis for the division of the study material in terms of genesis and composition of rock material, as well as characteristics of the processes of weathering and transport.

Table 6

Statistical parameters of the chemical analyses

Table 7

Average REE contents in igneous and sedimentary rocks; data for clays are indicated in bold (source: Kabata-Pendias and Mukherjee Reference Kabata-Pendias and Mukherjee2007)

Small lateral and vertical variability in mineralogical composition and the amounts of trace elements present suggest continuous sedimentation and consistent sediment supply. The sedimentation process itself probably occurred slowly and the material was supplied from suspension currents, with no evident catastrophic episodes such as rapid temperature changes, landslides, etc. Some variability in SiO₂ content was noted (vertically and laterally: Fig. 6), possibly caused by variability in quartz abundance, especially in light (silty) laminae.

Fig. 6

Chemical composition of ice-dammed lake clays from the Lębork deposits

The general chemical composition of ice-dammed lake clays from Lębork is very close to that of varved clays from Opaleń, located ~110 km to the southeast, dated to the Mazovian II interglacial or Varsovian insterstadial (Domański Reference Domański1961).

Literature relating to Ca content in sedimentary rocks has shown that Ca in the Lębork could have originated both from the weathering of plagioclase (Na-Ca feldspars) from Scandinavian crystalline rocks, and/or from Scandinavian Paleozoic limestones, the occurrence of which was determined in the moraine till of the Gardno phase (Nowacka and Neumann Reference Nowacka and Neumann2008).

Variability in the chemical composition of ice-dammed lake clays in the Lębork ice-dammed lake deposits profile is considerably less prominent than that in the vertical profile of the ice-dammed lake clays from Opalenie (Domański Reference Domański1961). In the latter, the variability of SiO₂ content reaches as much as 25 wt.%, and varved clays of the Lębork ice-dammed lake are very different from the clays from Poznań, showing variations in terms of elements found, depending on the region of deposition (Bojakowska et al. Reference Bojakowska, Brański, Iwasińska-Budzyk and Retka2010).

The occurrence of Cretaceous and Paleogene dinoflagellate cysts showed that sediments of these ages could also be reworked and redeposited as varved clays at Lębork. This may confirm a Tertiary origin of the quartz grains in the varves of the Lębork ice-dammed lake (Gedl Reference Gedl2011).

Mineralogical Composition of Ice-dammed Lake Clay

The mineralogical composition, determined by XRD, showed that the primary minerals of the deposits analysed include quartz, muscovite, calcite, and the clay minerals illite, kaolinite, and montmorillonite. Illite and chlorite are the main components, and are products of weathering of crystalline and metamorphic rocks (Fig. 5) (Millot Reference Millot1970), but can also form during diagenesis of clay-rich sediments (Środoń Reference Środoh1996). Smectite illitization is another common mineralogical reaction occurring during the burial diagenesis of clay-rich sediments (Lanson et al. Reference Lanson, Sakharov, Claret and Drits2009).

The XRD analyses confirmed the small variability of the chemical and mineralogical composition of sediments from the Lębork deposit, demonstrated above by other means (Figs. 7, 8).

Fig. 7

XRD pattern of a sample of ice-dammed lake deposits from the uppermost part of the deposit from location 3

Fig. 8

XRD patterns of samples from location 1: the bottom (black), middle (red) and top (green)

Supplementary Material Table S1 includes the matrix of correlations for elements determined in the Lębork deposit.