Spatial and seasonal patterns of water isotopes in northeastern German lakes
- 1Dept. 2 Community and Ecosystem Ecology, Leibniz Institute of Freshwater Ecology and Inland Fisheries, Müggelseedamm 301, Berlin, Germany
- 2Dept. 1 Ecohydrology and Biogeochemistry, Leibniz Institute of Freshwater Ecology and Inland Fisheries, Müggelseedamm 310, Berlin, Germany
- 3Dept. 3 Plankton and Microbial Ecology, Leibniz Institute of Freshwater Ecology and Inland Fisheries, Zur alten Fischerhütte 2, 16775 Stechlin, Germany
- 4Institute for Biochemistry and Biology, Potsdam University, Maulbeerallee, 14469 Potsdam, Germany
- 5Department of Ecology, Innsbruck University, Technikerstrasse 25, 6020 Innsbruck, Austria
Correspondence: Bernhard Aichner (firstname.lastname@example.org)
Water stable isotopes (δ18O and δ2H) were analyzed in samples collected in lakes, associated with riverine systems in northeastern Germany, throughout 2020. The dataset (Aichner et al., 2021; https://doi.org/10.1594/PANGAEA.935633) is derived from water samples collected at (a) lake shores (sampled in March and July 2020), (b) buoys which were temporarily installed in deep parts of the lake (sampled monthly from March to October 2020), (c) multiple spatially distributed spots in four selected lakes (in September 2020), and (d) the outflow of Müggelsee (sampled biweekly from March 2020 to January 2021). At shores, water was sampled with a pipette from 40–60 cm below the water surface and directly transferred into a measurement vial, while at buoys a Limnos water sampler was used to obtain samples from 1 m below the surface. Isotope analysis was conducted at IGB Berlin, using a Picarro L2130-i cavity ring-down spectrometer, with a measurement uncertainty of <0.15 ‰ (δ18O) and <0.0 ‰ (δ2H). The data give information about the vegetation period and the full seasonal isotope amplitude in the sampled lakes and about spatial isotope variability in different branches of the associated riverine systems.
The varying physical properties of stable oxygen and hydrogen isotopes of the water molecule (16O, 17O, 18O, 1H, 2H) result in isotope fractionation during evaporation and condensation processes. This causes spatial and temporal variability in the isotopic signature of water in both the liquid and the vapor phase (Craig, 1961; Dansgaard, 1964; Gat and Gonfiantini, 1981). Water stable isotopes are therefore ideal tracers of hydrological processes, for example in lacustrine and riverine systems. Specifically in lakes, their general morphology (water volume, lake area, depth, and shape), the mean residence time of the water, the balance between in- and outflows of multiple types (surface water, groundwater, precipitation), and their connectivity to other water bodies are important parameters controlling isotope ratios (Herzceg et al., 2003; Bocanegra et al., 2013; Wu et al., 2015; Kang et al., 2017, Mass-Dufresne et al., 2021).
The northeastern part of Germany is characterized by a complex system of rivers and lakes. The connectivity of those lakes is an important influence on how ecological and chemical water properties are propagated along the river–lake network. Water isotopes are ideal proxies to identify spatial patterns within these coupled riverine and lacustrine systems and therefore a potential tool to assess lake-to-lake connectivity. So far, available isotope data from this region are limited to large rivers (Reckert et al., 2017), punctual snapshot data (Richter and Kowski, 1990), or small-scale patterns in local settings (Kuhlemann et al., 2020; Vyse et al., 2020; Kleine et al., 2021).
Here, we provide a comprehensive dataset of water isotopes in lakes along the river–lake system of the northeastern German lowland area (Aichner et al., 2021), which covers the major riverine systems and evaluates the seasonal variability on selected spots, i.e., in lakes which are part of different riverine branches of the investigated systems. The two major questions are (a) what the seasonal variability in water isotope values across the northeastern German lacustrine systems is and (b) whether there are spatial trends that can be unraveled by water isotope data.
For future regional studies, answers to these questions and the assessment of whether water stable isotopes can be used as an accurate proxy for lake-to-lake connectivity will be valuable in the context of the potential relationship between hydrological, chemical, and biological properties of the studied systems.
Northeastern Germany, a section of the glacially formed North German Plain, is characterized by a complex system of rivers and 1000+ lakes (Fig. 1) with highly variable limnological features such as size, depth, shape, and biogeochemical properties (Ogashawara et al., 2020, 2021). Most of these inland waters are a part of the Elbe watershed, discharging into the North Sea, with the Spree–Dahme system and the Müritz–Havel system as major tributaries. Further to the northeast the Ucker system forms a major cluster of rivers discharging into the Baltic Sea. Smaller natural and artificial channels add to the complexity of this riverine and lacustrine network.
The study area is situated in the temperate climate zone with an annual precipitation and temperature of approximately 600 mm and 10 ∘C, respectively (Berlin; DWD, 2021). Isotope values of precipitation range from −84 ‰ (January) to −49 ‰ (July) for δ2H and from −11.6 ‰ to −6.9 ‰ for δ18O (OIPC, Online Isotopes in Precipitation Calculator; Bowen, 2022; Bowen et al., 2005; IAEA/WMO, 2022; Stumpp et al., 2014). Due to continental and altitude effects, i.e., isotopic depletion with progressive transport and rain-out of water vapor, δ values of precipitation isotopes decrease in the eastern part of Germany from the NW to the SE. This trend is mirrored in groundwater δ2H values, which decrease in the study area from −60 ‰ in Lake Müritz to −63 ‰ in the Spree–Dahme rivers (Richter, 1987; Richter and Kowski; 1990).
Lakes sampled for this study are listed in Tables 1 and 2 and can be clustered into nine geographical groups: (I) Lake Müritz and Kölpinsee, which discharge via the Erpe towards the northwest to the Elbe (Fig. 1); (II) deep Müritz–Havel lakes, which discharge towards the southeast and east before the confluence with the upper Havel river in Priebertsee (Schwarzer See, Zethner See, Vilzsee, Zotzensee, Labussee, Rätzsee, Canower See, Kleiner Pälitzsee, Großer Pälitzsee) (Fig. 2a); (III) the mostly shallow upper Havel lakes, located north of the confluence with the Müritz–Havel waterways (Zierker See, Useriner See, Großer Labussee, Woblitzsee, Großer Priepertsee) (Fig. 2b); (IV) Havel lakes, east of the confluence (Ellbogensee, Ziernsee, Röblinsee, and Stolpsee) (Fig. 2d); (V) Großer Lychensee, which is connected via the river Woblitz with the Stolpsee; (VI) Feldberg lakes (Feldberger Haussee, Breiter Luzin, and Schmaler Luzin), which are connected with each other via surface flow but only via groundwater flow with the lakes of group V (Fig. 2c); (VII) lakes connected to the Ucker system, mostly via smaller creeks and artificial channels (Krewitzsee, Mellensee, Wrechener See, Großer See, Große Lanke (southernmost sector of Oberuckersee), and Suckower Haussee) (Figs. 1 and 2c); (VIII) the Spree–Dahme system southeast of Berlin (Spree, Dämeritzsee, Große Krampe, Dahme, and Müggelsee) (Fig. 3); (IX) individual lakes Stechlin and Peetschsee, which are not connected to a major river but for which connectivity via groundwater flow and small artificial channels is partly still of relevance.
All of these sampled lakes show variable morphometric and ecological characteristics (Tables 1 and 2). The water depths range from 3 m (Zierker See) to 70 m (Lake Stechlin) and the volumes from approximately 5.6×106 to 99.6×106 m3 (same lakes). By lake area, the investigated water bodies range from small ponds such as Peetschsee (19.1 ha) to the largest German lake, the Müritz (10 910 ha). Most of the studied northeastern German lakes are mesotrophic or eutrophic according to the classification of LAWA (LAWA, 2014; Tables 1 and 2). Oligotrophic conditions only occur in the lake Schmaler Luzin. The water residence time in these lakes, i.e., the mean time that water spends in a particular lake, has been estimated by means of dividing the lake volume by the flow in or out of the lake (Wetzel, 2001). It ranges from a few weeks to few months in most river-connected lakes, while the Feldberg lakes and Lake Stechlin have longer residence times of ca. 3 to 16 years and >60 years, respectively (Table 2).
3.1 Water sampling
Water samples were taken at the shore of 31 lacustrine and riverine spots from 40–60 cm water depth between 8–19 March and 13–19 July 2020 (Figs. 1–3; Table 1). At Müggelsee, samples were taken from a boat pier before the outflow on the northwestern side of the lake, in 2–4-week intervals between March 2020 and January 2021. Additionally, more samples were taken at two sites further east on the northern shore of the lake (Fig. 3) on 19 June and 13 July 2020. Water samples were taken with a pipette and directly transferred in a gas chromatography (GC) vial, which was closed instantly after sampling and stored cold (6 ∘C) until further processing.
Between March and October 2020, water samples from a subset of 19 lakes (Table 2) were taken in 1–2-month intervals from a boat close to buoys, which were temporarily deployed as part of the project CONNECT at the deepest points of the lakes or (if a site coincided with a waterway) near the outflow of the lake (Ogashawara et al., 2020, 2021): 17–19 March, 25–28 May, 29 June–2 July, 3–6 August, 1–3 September, 5–8 October. On 29 and 30 September, four lakes (Zierker See, Großer Priepertsee, Ellbogensee, Röblinsee) were sampled at a higher spatial resolution by taking six or seven surface samples, distributed over the whole lake surface area at positions close to all shores, in addition to the sample at the deepest point and/or center of the lakes (Fig. 2).
A Limnos water sampler (Limnos, Komorów, Poland), capturing 2.5 L volume, was used to obtain water samples from 1 m depth. Samples were transferred into 10 L canisters, closed after sampling, and immediately transported to the lab. Canisters were carefully turned upside down 10 times to guarantee constant mixing of samples before samples were transferred into GC vials with a pipette for isotope analysis. Vials were stored in a cold room (6 ∘C) in the dark until isotope measurement.
3.2 Isotope analysis
Water samples were filtered with 0.2 µm cellulose acetate (Faust Lab Science GmbH, Fabrikstraße 17, 79771 Klettgau, Germany) prior to analysis of stable isotopes (δ18O and δ2H values) in the water isotope lab at IGB Berlin using a L2130-i cavity ring-down spectrometer (Picarro, Santa Clara, CA, USA). All measurements were post-processed with the Picarro ChemCorrect™ software, which compared the measured spectra of the lab standards with the spectra of the samples. If statistical differences (i.e., baseline offset, spectral interference of organic compounds) between the two were too high, a warning flag was assigned, and the sample was excluded.
Isotope values and standard deviations are based on three replicate measurements of each sample, with three additional discarded measurements prior to avoid memory effects. To improve precision, all injections with a water concentration below 17 000 and above 23 000 ppm and with a standard deviation higher than 400 ppm of the measured water concentration across an injection's averaging window were excluded.
For instrument calibration three laboratory standards for each group of 24 samples were used: L (δ18O −17.86 ‰ and δ2H −109.91 ‰), DEL (δ18O −10.03 ‰ and δ2H −72.81 ‰), H (δ18O 2.95 ‰ and δ2H 0.29 ‰). A fourth lab standard, M (δ18O −7.68 ‰ and δ2H −56.70 ‰), was used as quality and drift control after every six samples, i.e., serving as lab-internal control and not being used for calibration. Mean values calculated from all measured M lab standards were −7.68 ‰ for δ18O with a SD of 0.10 ‰ and −55.93 ‰ for δ2H with a SD of 0.31 ‰. All lab standards were referenced against primary measurement standards: VSMOW2 (Vienna Standard Mean Ocean Water 2), GRESP (Greenland Summit Precipitation), and SLAP2 (Standard Light Antarctic Precipitation 2) from the IAEA (International Atomic Energy Agency, Vienna International Centre, 1400 Vienna, Austria).
Based on error propagation from (a) the uncertainty in reference lab standards, (b) root mean square errors in the calibrations, and (c) average standard deviation of replicate measurements of standards and samples, the overall measurement uncertainty in water isotope analysis was quantified to <0.15 ‰ (δ18O) and <0.40 ‰ (δ2H).
4.1 Time series
Isotopes exhibit a clear seasonal trend in the investigated lakes (Figs. 4 and 5). Minimum δ2H and δ18O values occur at the end of March/early April, while maximum values were measured at the end of September/early October. This is 6–8 weeks after the minimum and maximum water temperatures are reached and independent from the annual trends of water pH and O2 saturation (Fig. 4). In the biweekly sampled Müggelsee, the isotope values vary from −53 ‰ to −44 ‰ (δ2H) and from −7.2 ‰ to −5.3 ‰ (δ18O), equivalent to seasonal isotope amplitudes of ca. 9 ‰ and 1.9 ‰, respectively. The monthly sampled lakes showed variable seasonal amplitudes (i.e., offsets between October and March), ranging from δ2H 2–13 ‰ (average: 4 ‰) and δ18O 0.4–2.6 ‰ (average 0.9 ‰).
A seasonal isotopic signal has been observed in many riverine and lacustrine systems (e.g., Dutton et al., 2005; Ogrinc et al., 2012; Halder et al., 2015; Reckerth et al., 2017). Usually, the lake and river isotopes reflect the annual isotope trend of precipitation, but often with significant attenuation of the signal and a delay of 1–3 months (Rodgers et al., 2005; Jasechko et al., 2016; Reckerth et al., 2017, Bittar et al., 2016). This agrees with data from our study area, where precipitation isotopes reach their minimum and maximum in December/January and July/August, respectively, and exhibit a seasonal variability of ca. 35 ‰ (δ2H) and 4.7 ‰ (δ18O) (OIPC data for Berlin; Bowen et al., 2005; IAEA/WMO, 2022; Bowen, 2022). The reasons for the time delay between precipitation and river or lake water isotopes as well as the smaller seasonal amplitude of the latter can be attributed to multiple catchment characteristics and processes. Crucial influencing factors on how fast a precipitation isotope signal is transferred into fluvial systems are the discharge regime of rivers and the area and topography of their catchment (Sklash et al., 1976; Maloszewski et al., 1992; McGuire et al., 2005; Rodgers et al., 2005).
In our study area, the lowest seasonal (March–October) isotope variability was observed in Lake Stechlin, followed by the Feldberg lakes (Fig. 5), most likely due to their high water residence time and lack of connection to rivers (Table 2). In contrast, the highest amplitude is found in the shallow Zierker See, which also has the lowest volume of all studied lakes. Therefore it is most susceptible to summer evaporation with related isotopic enrichment of the lake water and also to inflow events, causing more negative values, as is visible in March (Fig. 5). Lake morphology can similarly explain the wide isotope amplitude of Müggelsee (Fig. 4), which is relatively large in area but also among the shallowest of the studied lakes. Data from most Havel lakes exhibited average seasonal isotope amplitudes (Figs. 5 and 7). The Spree–Dahme locations, Kölpinsee and Müritz, and the small Peetschsee showed relatively large deviations between March and July (Fig. 7). All those lakes are either very shallow or have at least a large area-to-depth ratio.
These results show that the seasonal isotope amplitude is influenced by multiple characteristics of the studied lakes. Aside morphological parameters (lake area, depth, and volume), hydrological features (e.g., water residence time) are of importance.
4.2 Spatial patterns
In the four lakes with increased spatial coverage from September samples, little intra-lake variability in isotope values (0.5 ‰–1 ‰ for δ2H and 0 ‰–0.2 ‰ for δ18O) was observed (Fig. 6). In contrast, along the transects, the multiple lakes showed an isotope variability of ca. 25 ‰ (δ2H) (Fig. 7) and of ca. 3 ‰ (δ18O).
In general, lakes showed decreasing δ values from the northwest (Müritz) towards the southeast (Spree–Dahme). This follows a similar spatial trend to isotopes in precipitation and groundwater (Richter, 1987; Richter and Kowski, 1990).
In addition, the lakes from the different geographical clusters can be distinguished according to their water isotope signatures: (I) the highest values were measured in the two lakes associated with the Müritz–Erpe system (I). The upper Havel is characterized by lower isotope values than the Müritz–Havel (II and III). The two lakes Schwarzer See and Zethner See are an exception, which show more negative values than the other Müritz–Havel lakes (Fig. 7). Those form a chain of headwater lakes in the Müritz–Havel system, whose major inflow is north of Zotzensee (Fig. 2a). Schwarzer See is characterized by a comparably large mean residence time of lake water (Table 2) and is probably under increased influence of isotopically depleted groundwater. The influence of the different isotopic signatures of the two upper Havel branches is also visible at their confluence in Ellbogensee (Fig. 2a). Here, two samples, ELL 2 and ELL 3 (white squares in Fig. 6), taken before the upper Havel, show approximately 1 ‰ 2H enrichment compared to the samples taken after the confluence. In general, the Havel lakes after the confluence (IV) carry a mixed isotope signature of the Müritz–Havel and upper Havel, with stronger influence of the first, depending on season (Figs. 5–7). Isotope depletion was observed towards the Stolpsee, probably due to the influence of the Lychen lakes (V), which discharge into the upper Havel at Stolpsee via the Woblitz river and which showed the most negative values of all sampled lakes in the upper Havel system (Figs. 5 and 7).
The Feldberg lakes (VI) are a group of lakes located approximately 35 km northeast of the upper Havel system and with insignificant surface connection to the adjacent lake systems. They are characterized by relatively high water residence time and slow surface flow from Feldberger Haussee to Breiter Luzin and Schmaler Luzin. δ2H and δ18O values are higher compared to the upper Havel and the main branch of the Havel (i.e., after the confluence at Großer Priepertsee and Ellbogensee), yet these are typical values of the Müritz–Havel. Among the three lakes, Feldberger Haussee shows the highest isotopic values, probably due to its lower water depth and volume (compared to Breiter and Schmaler Luzin) and therefore increased susceptibility to evaporative isotope enrichment.
Variable isotope values are observable in the six sampled lakes associated with the Ucker lake–river system (VII). Complex subsurface and surface flow patterns, mostly via smaller creeks and channels, their wide geographical distribution, and variability in morphometric properties, can explain the isotopic heterogeneity in those lakes. A geographic trend, i.e., lower δ2H and δ18O values in the Oberuckersee (Große Lanke) compared to the more northern lakes (e.g., Mellensee, Krewitzsee), can be inferred from the data. The most negative isotope values in the study area were measured in samples from the lakes and rivers of the Spree–Dahme system (VIII), located approximately 100 km southeast of the Müritz–Havel–Ucker systems.
The final group of lakes is characterized by low surface flow connectivity to riverine systems and other lakes (IX). Those lakes (Lake Stechlin and Peetschsee) show higher isotopic values than adjacent lakes and rivers, which can be attributed to evaporation effects. Those in turn are more pronounced in the smaller water bodies, which is visible from the large seasonal isotope amplitude in Peetschsee compared to small seasonal variability in the deep and large Lake Stechlin (Fig. 7).
All data in this paper are available at PANGAEA: https://doi.org/10.1594/PANGAEA.935633 (Aichner et al., 2021). This dataset is open for being extended in subsequent years.
Stable isotope δ2H and δ18O values of water samples collected in northeastern German lakes and rivers show clear spatial and seasonal trends. While isotope data exhibit a tendency from relatively high values in the northwest towards lower values in the southeast, evaporation and groundwater inflow influence the isotope values on a local scale. In this context, morphometric parameters (water depth, area, volume, and overall shape) and related hydrological properties (water residence time, susceptibility to lake water evaporation and groundwater inflow) are crucial features, with effects on both absolute isotope values and their seasonal amplitude.
The comprehensive dataset of stable water isotopes and lake morphological characteristics described here can help to set biological and biogeochemical data in the context of hydrological processes in the northeastern German riverine and lacustrine systems. The ecological and chemical characteristics of these lake–river systems are driven by (a) connectivity between the lakes associated with river systems in addition to (b) local influencing factors, which in turn often depend on lake morphology. Water isotopes are able to reflect both those aspects, as shown by the different isotope patterns in the different branches of the Müritz–Havel–Ucker–Spree–Dahme system.
BA designed the isotope study and wrote the manuscript in close cooperation with the CONNECT project, coordinated by SAB and SW and performed by CK, AJ, KK, IO, JCN, HPG, FH, GS, SW, and SAB. DD analyzed water samples collected by BA, SFH, KK, CK, IO, AJ, SAB, SW, JCN, HPG, and FH. All co-authors contributed to data evaluation and interpretation and editing of the manuscript.
The contact author has declared that neither they nor their co-authors have any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We thank Solvig Pinnow, Gregorio Lopez Moreira Mazacotte, Bianca Schmid-Paech, Fabian Göppel, Maren Lentz, and Gary Gottschall for help with sampling and sample preparation for isotope analysis. Funding was provided by the German Science Foundation (DFG) (project Ai 134/3-1). Part of this work was funded by the Leibniz Association within the Collaborative Excellence program for the project CONNECT – Connectivity and Synchronisation of Lake Ecosystems in Space and Time (K45/2017).
This research has been supported by the Deutsche Forschungsgemeinschaft (grant no. Ai 134/3-1) and the Leibniz Association (grant no. K45/2017).
This paper was edited by Attila Demény and reviewed by Gabriel Bowen and one anonymous referee.
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