, Volume 39, Issue 4, pp 831–839 | Cite as

Paleoecological assessment of cladoceran community dynamics in two subarctic peatlands

  • Jaakko Johannes LeppänenEmail author
  • Sanna Piilo
  • Yuan Li
  • Hui Zhang
  • Minna Väliranta
Open Access


Crustacean community structure and dynamics are very well studied in lakes, rivers and oceanic systems but wetlands, where moisture conditions fluctuate, have not received equal attention in research. For example, cladoceran communities in peatland systems in the subarctic region have not been fully investigated. We used paleolimnological and paleoecological methods to study plant and cladoceran assemblages and the community dynamics in two subarctic peatlands, which differ in their hydrological characteristics. At the first site, Iitto, river floods introduce planktonic species to fen pools and the steep topography of the catchment induces rapid but relatively short flooding periods. Fluctuating environmental conditions result in a high amount of cladoceran resting stages in the samples. At the other site, Kaamanen, the cladoceran assemblage goes through clear directional changes, which could be attributed to changes in fen hydrology and ultimately to climatic changes during the past two millennia.


Peatland hydrology Cladocera Peat plants Plant macrofossils Climate Flooding Paleolimology 


Subarctic fens are challenging habitats for aquatic biota due to fluctuating water levels and a long season of ice and snow cover. In Northern Finland, many peatlands are flooded in spring due to snowmelt, which is followed by gradual shrinking of the open water area in late summer and autumn. Lakes in the northern Finnish Lapland are covered by ice from late October to early June. For aquatic animals, which are capable of inhabiting temporary wetland pools, rapid emergence and fast reproduction are key survival characteristics. Cladocera, a group of crustacean zooplankton, are known to bypass drought or winter by diapause and are able to develop large populations in short period of time. The group is of pivotal importance in nearly all types of aquatic systems as they establish a link from primary producers to higher trophic levels. In addition, crustacean zooplankton are an important component in microbial loops, linking the group to aquatic carbon dynamics (e.g. Gaedge 2009; Matveev and Robson 2014). Moreover, cladocerans are regarded as an excellent indicator of environmental changes (Jeppesen et al. 2011) and the animals leave well preserved, identifiable remains upon death or molting, allowing the utilization of paleolimnological methods (Frey 1960). In addition to cladocerans, plant macrofossils are a paleoecological indicator for past habitat changes and changes in carbon accumulation patterns in Subarctic peatlands (Väliranta et al. 2007, 2017, Swindles et al. 2015, Teltewskoi et al. 2016, Gałka et al. 2017).

Flood frequency and the longevity of inundation period are known to control zooplankton communities in floodplain ponds (Medley and Havel 2007) and cladoceran community structure in different types of lakes in northern Finnish Lapland has been studied numerous times (Rautio 1998; Korhola 1999; Siitonen et al. 2011; Leppänen et al. 2017). Despite this, long-term monitoring studies or paleolimnological studies assessing the cladoceran community dynamics in subarctic peatland pools have not been conducted before. Similarly to cladocerans, the plants in subarctic peatlands are exposed to cold winters and occasional floods. The plant community reflects the average water level, nutrient status and acidity in northern peatlands (Mauquoy and Geel 2007; Väliranta et al. 2007). Slow decomposition in waterlogged and anoxic peat permits the usage of plant macrofossils (i.e. undecomposed plant remains) in paleoecological studies (Mauquoy and Geel, 2007; Väliranta et al. 2007; Mathijssen et al. 2014).

Here, we use subfossil cladocera and plant macrofossils to study the cladoceran community structure and historical community dynamics in two subarctic fen environments which vary in their hydrological regimes. Because peatland characteristics are strongly controlled by hydrology (e.g. Holden 2006) and peatlands are regarded highly as important ecosystems in terms of carbon dynamics and climate change (e.g. Gallego-Sala et al. 2018), we feel that faunal the aquatic component of peatland systems deserves more attention in research. Our main research question is whether cladoceran community structure is related to moisture conditions in subarctic peatlands. Ultimately, we attempt to assess whether cladoceran paleolimnology holds potential as additional proxy tool for peatland moisture conditions. In addition, our results contribute to current knowledge on subarctic peatland biodiversity.

Study sites

Both study sites (Fig. 1 a-c and Table 1) are located in subarctic sporadic permafrost zone in Finnish Lapland. The Kaamanen region is an ecotone between subarctic and northern boreal zone, whereas Iitto belongs to subalpine region, where mountain birch is the dominant and sole tree species. Dry habitats of both study sites are characterised by species such as dwarf shrubs Betula nana, Empetrum nigrum, Vaccinium uliginosum, Rhododendron tomentosum and the herbaceous Rubus chamaemorus, bryophytes e.g. Polytrichum strictum, Dicranum spp. and S. fuscum. More minerotrophic and moister fen surfaces support taxa such as Salix spp., sedges such as Eriophorum vaginatum, E. angustifolium and Carex spp., C. limosa, Trichophofum spp. and different bryophytes Scorpidium scorpioides, Sphagnum species such as, Sphagnum balticum, S. majus, S. lindbergii and S. riparium.
Fig. 1

a. Study site locations (stars) in northern Finland (a), Iitto (b) and Kaamanen (c) study sites. Dotted area represents the coverage of treeless peatland and thick line is the catchment boundary. Full catchment maps and elevation data are given in Online Resources (Kaamanen; Online Resource 1 and Iitto; Online Resource 2). Maps are based on data obtained from open databases of Finnish Environmental Institute ( and from National Land Survey of Finland (

Table 1

Geographical characteristics of study sites

Study site



Latitude N (WGS84)

27 16.298’

21 25.327’

Longitude E (WGS84)

69 08.382’

68 43.428’

Altitude (m a.s.l.)



Peatland area (km2)



Catchment area (km2)



Elevation difference (m)



Average temperature (°C)



Average annual precipitation (mm)



Kaamanen peatland is a fen with strings, flarks, and non-permanently frozen hummocks. The catchment area is characterized by relatively small elevation difference and numerous lakes and ponds. The southern end of the catchment is flat whereas the northern part is divided by esker formations. The nearest permanent waterbodies are a small, meandering brook at a distance of ~50 m, with an eutrophic riparian zone (Aurela et al. 1998) and a small lake (1.8 ha) at a distance of ~300 m (Fig. 1c; Online Resource 1). The fen is located in an active groundwater region and there are numerous springs in the catchment suggesting a possibility for groundwater impact on water availability and water chemistry. According to available water chemistry data (OIVA database 2018), the lakes and rivers (n=5) in Kaamanen are nearly neutral pH (6.3-7.3), have relatively low nutrient concentrations (total phosphorus 4-12 μg l-1, total nitrogen 270-520 μg l-1) and low conductivity (2-11 mS m-1) and Ca (3.5-4 mg l-1).

Iitto is a palsa peatland, i.e. a fen complex with individual peat mounds (palsas) that have been uplifted from the surrounding fen surface by permafrost upheaval. On the studied peatland, separate palsa mounds rise approximately two to four meters above the surrounding fen complex. The Iitto catchment is characterized by the steep slopes of fells Latnjavarit (720 m.a.s.l) and Coreheapmi (605 m.a.s.l) resulting an elevation difference of over 300 m between the lowest and the highest point. In addition, a small lake (1.7 ha) and River Könkämeno are located in the vicinity of the sampling site at distances of 100 m and 300 m, respectively (Fig. 1b and Online Resource 2). According to water level monitoring data recorded at Kaaresuvanto monitoring station, 50 km downstream, the water level at River Könkämäeno can fluctuate by 4 meters, reaching its highest level during May-July. Surface waters (n=2) in the Iitto area are nearly neutral (pH 6.8-7.1), oligotrophic (total phosphorus 3-6 μg l-1, total nitrogen 200-250 μg l-1) and electric conductivity values are low (1.9-3.9 mS m-1) (OIVA database 2018).


Coring and subsampling

Two peat cores were collected with a box corer (60 cm x 7 cm) in September 2016, one from each peatland. Selected Sphagnum covered high lawn habitats (less than 30 cm from the surrounding wet peatland surface) represent transitional habitat between wet fen and dry hummock. Selecting these microhabitats, enables us to assess how cladoceran communities response to changes in moisture conditions and changes in vegetation assemblages, when there is a shift from wet to dry. Peat cores were wrapped in plastic film and placed inside PVC gutters for transportation to the University of Helsinki, where they were stored in a freezer until further analysis. The 60-cm long peat cores were defrosted and sliced in 1-cm intervals. The subsamples were stored in a cold room.

Plant macrofossil analysis

Plant macrofossil analysis was conducted at 2-cm intervals, increased to 1 cm for periods with prominent plant community changes. Volumetric 5 cm3 samples were rinsed through a 140-μm mesh under running water. The residue on a sieve was analysed under a stereomicroscope for relative (%) abundances. Further species level identification was conducted with a light microscope. The plant macrofossil analysis follows Mauquoy et al. (2010) and Väliranta et al. (2007). The highly decomposed plant matrix is called UOM, i.e. unidentified organic matter. Identification of plant macrofossils follows e.g. Viramo (1992); Mauquoy and Geel (2007); Laine et al. (2009). In addition, a plant reference collection was available.

Cladoceran analysis

Cladoceran analysis was conducted using standard procedures published by Korhola and Rautio (2001). In short, approximately 1 cm3 of wet peat sample was heated (90 °C) in 10% KOH bath for 1 hour and sieved through 50 μm mesh. The residue was stained using safranin and slides were prepared with gelatin glycerol jelly. Cladoceran remains were identified and counted using a light microscope at 100-400 x magnification. Cladoceran identification and nomenclature was based on (Szeroczyńska and Sarmaja–Korjonen 2007). A minimum number of 100 individuals was counted from each sample. Cladoceran resting eggs (ephippia) were counted but species were not specified.

Chronological analyses

Chronology was established based on five accelerator mass spectrometry (AMS) radiocarbon 14C dated samples (2 samples from Kaamanen core, 3 samples from Iitto core). 14C samples were sent to Poznan Radiocarbon Laboratory (Poznan, Poland) and to the Finnish Museum of Natural History (LUOMUS, Helsinki, Finland). The dated samples were bulk peat, with roots and rootlets picked apart (Holmquist et al. 2016). Age-depth models were created using a bayesian BACON package (Blaauw and Christen 2011) using weighted mean ages and age-depth models in R version 3.4.3.

Statistical analysis

Analysis of Similarities (ANOSIM; Clarke 1993) was used to assess the similarities between cladoceran assemblages between sites. ANOSIM analysis was conducted using Bray-Curtis dissimilarity matrix for square root transformed proportional data. Similarity percentages analysis (SIMPER; Clarke 1993) was used to quantify the overall average dissimilarity of cladoceran communities between sites and to pinpoint the species which contribute to the differences. SIMPER analysis was conducted on percentage data. Shannon H’ diversity index (for cladocerans) was calculated using percentage data. Species richness (for cladocerans) was calculated using rarefaction method for count data (Birks and Line 1992). All analysis were conducted in the programme PAST (Hammer et al. 2001).



The deepest samples in Kaamanen (57 cm) and in Iitto (55 cm) were dated to ca. 755 cal. BC (before Christ) and ca. 1425 cal. AD (Anno Domini), respectively, whereas the ages for samples above (Kaamanen 37 cm and Iitto 26 cm) date to ca. 1365 cal. AD and ca. 1725 cal. AD, respectively. The peat accumulation rate for Kaamanen is approximately 0.1 mm y-1 and for Iitto the peat accumulation rate is approximately 1 mm y-1. The ages provided from the age-depth models are included in the stratigraphies (Fig. 2 and Fig. 3) and raw data is given in Online Resource 1.
Fig. 2

Cladoceran and plant community stratigraphy in Kaamanen. In x-axis, all bar data is proportional data, whereas Limosa-type remains, Eriophorum vaginatum and leaf material abundances are presented as follows: 0= not found, 1=present/rare, 2=occasional, 3=abundant

Fig. 3

Cladoceran and plant community stratigraphy in Iitto. In x-axis, all bar data is proportional data, whereas Limosa-type remains, Eriophorum vaginatum and leaf material abundances are presented as follows: 0= not found, 1=present/rare, 2=occasional, 3=abundant

Plant macrofossil results

Abrupt and clear changes from wet Cyperaceous fen vegetation assemblages to drier ligneous and/or lawn/hummock vegetation are characteristic for both peat records. The results of selected taxa are presented in Figs. 2 and 3. Ombotrophic plant assemblages are not presented (Fig. 2 and Fig. 3) because the cladoceran remains disappear after the abrupt changes in vegetation and hydrology.


The 57-cm long record is characterised by two distinct phases in plant assemblages. The first phase from ca. 755 cal. BC to ca. 1530 cal. AD is dominated by Scorpidium scorpioides and Cyperaceous fen species (Limosa type Carex spp. and Eriophorum spp.). As the fen peat is humified, the proportion of UOM is high. Diatoms and Chrysophyceae cysts were detected until ca. 1340 cal. AD together with high percentage of Scorpidium scorpioides. Ombrotrophic S. fucum appears after ca. 1530 cal. AD and abruptly replaces the fen plant assemblages. Along with S. fuscum, S. capillifolium and S. magellanicum prevail until ca. 1815 cal. AD. Dark roots, indicating presence of (dwarf) shurbs, are found throughout this second phase. Vaccinium oxycoccos leaves and Empetrum nigrum leaves are abundant with few Andromeda polifolia leaves from ca. 1815 cal. AD towards present.


The 55-cm long record is dominated by wet fen species until a sharp change at ca. 1725 cal. AD. Cyperaceae species Eriophorum spp. and limosa-type Carex remains occur with oligo- to mesotrophic S. lindbergii that usually thrives from pools to lawns (Laine et al. 2009). Around 1560 cal. AD S. lindbergii is replaced with Scorpidium scorpioides which is a typical fen taxon growing in wet hollows. Cf. S. platyphyllum is found until the plant composition shifts to ligneous and dwarf shrub remains around 1760 cal. AD. Peat layers with sedges and woody material are accompanied by high UOM. The phase with woody remains is characterised by high percentages of dwarf shrub roots and UOM, also Empetrum nigrum leaves are present. Around 1905 cal. AD Sphagna reappear with S. russowii (ombrotrophic to weakly minerotrophic) with Polytrichum strictum (from lawns to hummocks). Betula nana leaf remains are found throughout the ligneous phase to present.

Cladoceran results

Cladoceran remains were well preserved but relatively scarce in peat samples and in the top samples the remains became increasingly rare. An adequate number of subfossil remains for assemblage characterization (~100 individuals; Kurek et al. 2010) was found from 10 samples from each site. A total of 15 taxa were identified from the samples (min 3, max 11 in Kaamanen; min 6, max 12 in Iitto). Average Shannon (H´) diversity for Kaamanen was 1.48 (0.6 to 2.0) and 1.67 (1.16 to 1.91) for Iitto. The most common species in Kaamanen were Chydorus sphaericus (average relative abundance 39 % SD 25 %) and Alonella excisa (average relative abundance 18 % SD 11 %). The most common species in Iitto were Unapertura latens (average relative abundance 34 % SD 14 %) and Alonella nana (average relative abundance 30 % SD 8 %). Most common species in both sites were present in all samples. The cladoceran communities in Kaamanen and Iitto are not similar (ANOSIM R 0.74, p<0.001) and according to SIMPER analysis, the overall average dissimilarity is 69 %. The most important taxa which contributes to site-wise differences are U. latens (23 %), C. sphaericus (23 %) and A. nana (17 %) (Online Resource 2). The number of cladoceran resting eggs varied in Kaamanen from 0 to 15 per 100 cladoceran individuals (average 6) and from 14 to 26 per 100 cladoceran individuals (average 23) in Iitto. The results are presented in Fig. 2 and 3.


At the beginning of the record (57 cm level), the most abundant species are C. sphaericus, A.excisa and A. nana. The section between ca. 760 cal. BC (57 cm) and ca. 815 cal. AD (43 cm) is characterized by high cladoceran diversity and declining abundance of A. nana. Beginning at ca. 815 cal. AD (43 cm) the cladoceran diversity starts to decline and the next sample at ca. 1130 cal. AD (40 cm) is characterized by nearly total domination of Alona rustica. In the following samples ca. 1210 cal. AD and ca. 1365 cal. AD (39 cm and 37 cm) the most abundant species is C. sphaericus.


The cladoceran community in Iitto remains relatively stable through the record. The most distinct changes in the Iitto record are dated to ca. 1485 cal. AD (49 cm) and to ca. 1590 cal. AD (39 cm). 1485 AD pinpoints the beginning of an increase in diversity (H’) and an increase in proportional abundance of Eurycercus spp. and A. rustica. At ca. 1590 cal. AD (39 cm) and subsequent samples, Alona affinis exhibits a slight but visible increase in proportional abundance.


Cladoceran communities in Kaamanen and Iitto

In general, cladoceran species detected in both study sites are common in Finnish Lapland lakes (Leppänen et al. 2017) and ponds (Rautio 1998). In addition, many of the species detected in both sites are regarded as common in peat bog ponds (Glime 2017) and some of the species (A. nana, C. sphaericus, A. excisa, A. affinis, Acroperus harpae) were reported during the late stages of transition from hilltop lake to an acidic ombrotrophic bog in southern Finland (Korhola 1992). Moreover, A. excisa and C. sphaericus have been reported to be common in shallow peatland pools in Romania (Battes et al. 2014), Hungary (Vad et al. 2012) and Bolivia (A. excisa and Chydorus breivilabris; Coronel et al. 2007) which further confirms the ability of those species to inhabit temporary shallow water environments. In both sites, the amount of cladoceran remains declines abruptly in top samples and probably reflects the formation of a palsa mound or peat hummock, as also recorded in the plant macrofossil assemblages. The increase in height results in disappearance of aquatic habitat and explains the lack of cladoceran remains. In addition, in both sites, cladoceran communities are clearly connected to hydrological characteristics of the environment. The relationship between plant and cladoceran communities is visible in the hydrological preferences of plant species as the samples with high cladoceran diversity occur systematically together with high abundance of Scorpidium scorpioides, which is reported to inhabit the wettest microhabitats in Kaamanen (e.g. Heikkinen et al. 2002).

While the cladoceran species assemblages in both sites are largely comprised of common and well known littoral species (e.g. A. nana, A. excisa and C. sphaericus), the largest species-wise difference between the sites is related to high proportional abundance of U. latens in Iitto. Interestingly, U. latens, is a relatively newly described species (Sarmaja-Korjonen et al. 2000) and its taxonomy and ecology are not well resolved. Another species worth mentioning is Eubosmina longispina, detected only in Iitto, which is a planktonic species and common in large and deep lakes. Thus, the explanation for the presence of E. longispina in Iitto is most probably related to the flooding of nearby River Könkämäeno. Based on satellite images, the river floods regularly and may therefore introduce planktonic species into the fen pools. The third distinct difference between the sites is the high number of cladoceran resting eggs in the Iitto samples. The large numbers of resting eggs is a result of intense sexual reproduction and reflects a high frequency of disturbance because cladocera survive ecological hardships (e.g. winter or drought) by diapause. The disturbances in Iitto are probably related to catchment characteristics, namely, to the river flooding and to melt water dynamics. Due to the steep topography of the Iitto catchment and the absence of lakes, melt water flooding is probably ephemeral, resulting in rapid variations in peatland water level. In contrast, the Kaamanen region is characterized by vast wetlands and numerous lakes which slow down the water flow increasing the longevity of the flood phase (Bring et al. 2016). In Kaamanen, the major flood lasts from May to June (Väliranta et al. 2014) but flarks stay submerged longer (e.g. in 1995, until September; Heikkinen et al. 2002). Despite the direct contact to larger waterbodies, the absence of planktonic species in our samples suggests that the influx of cladocerans from upstream lakes into the Kaamanen fen pools is practically non-existent. This suggests that the flood water originates from regional snow melt rather than natural waterbodies upstream.

Thus, the major difference between the sites is therefore the longer flooding periods of the Kaamanen pool habitat during the growing season whereas the Iitto site is characterized by continuous influx of planktonic species and the fluctuating conditions.

Cladoceran community dynamics in Kaamanen

The most interesting section in the cladoceran record is dated between ca. 760 cal. BC (57 cm) and ca. 815 cal. AD (43 cm) where the diversity is highest and namely, where the relatively large bodied species Eurycercus, A. harpae, A. affinis and Ophryoxus gracilis occur in high proportional abundances while small-sized A. nana declines. The elevated abundance of S. scorpioides, which inhabits the wettest microhabitats in Kaamanen (Heikkinen et al. 2002), indicates wetter overall conditions between ca. 760 cal. BC and ca. 815 cal. AD. This time period corresponds to late Holocene climate cooling, which is characterized by intensified flooding in northern Scandinavia (Labuhn et al. 2018) and increasing water levels in Finnish Lapland lakes due to high effective moisture (Seppä and Birks 2001; Korhola et al. 2005). During wet conditions, the strong spring floods would have induced coalescence of multiple flarks resulting in larger pools with higher potential to harbor a more diverse cladoceran community (DiFonzo and Campbell 1988; Fig. 4). However, the same is probably true for invertebrate predators (e.g. copepods) and may explain the decline of A. nana, which, due to its small size, is the potential prey for many small predators (Gliwicz and Umana 1994). Another distinct change in the record is the rapid proportional increase and dominance of A. rustica at ca. 1130 cal. AD (40 cm) accompanied by decline in cladoceran diversity and species richness, and a simultaneous decrease in S. scorpioides abundance which suggests drier conditions. This may be caused by a relatively warmer climate and subsequently decreased effective moisture conditions during medieval climate anomaly roughly around 900-1200 AD (Esper et al. 2012). However, the dominant species at ca. 1130 cal. AD is A. rustica, which is reported to prefer groundwater habitats (stygophilic species) (Strayer 1988; Dumont 1995). Kaamanen is groundwater influenced and the momentary dominance of A. rustica suggests the possibility of changes in surface water chemistry related to groundwater discharge (Glaser et al. 1990). The dominating cladoceran species in the following samples dated to ca. 1210 cal. AD and ca. 1365 cal. AD (39 and 37 cm, respectively) are C. sphaericus and A. excisa which are known to thrive in acidic lakes in e.g. Norway (Sandøy and Nilssen 1986) and are regarded to reflect slightly eutrophic conditions (Błędzki and Rybak 2016). Both species are common in temporary peatland pools. The reason for the dominance of these two species is thus probably related to decreased water level, microhabitat water chemistry changes, or both. Fen microhabitats may exhibit considerable spatial variation in surface water chemistry in northern Finland (Tahvanainen et al. 2002). Temporally, such differences can be induced by hydrological changes, e.g. when flarks are isolated from ground- or surface water source or vice versa. Other possible explanations for flark water chemistry changes include changes in river channel routing. Even though the meandering channels in north Lapland fens may exhibit rapid channel route changes (Kalliola and Puhakka 1988), traces of abandoned channels are not visible in the aerial photographs or LiDAR (Light Detection and Ranging) images. Moreover, when the aerial photographs from the 1990s (Aurela et al. 1998) were compared with the up-to-date aerial photography, the river channel routing seemed identical. Interpretation of shifts in cladoceran community, plant community and climate are illustrated in fig. 5.
Fig. 4

During the high water level phase, the coalescent flarks provide increased availability of microhabitats for cladocerans

Fig. 5

Generalized temporal trajectories for Kaamanen study site

Cladoceran community dynamics in Iitto

Even though the annual variability in water level is probably very high due to Könkämäeno river floods and ephemeral melt water flooding, the cladoceran community dynamics suggest stable change towards wetter conditions since ca. 1485 cal. AD (49 cm). The abundance of S. scorpioides and cladoceran diversity increase synchronously from ca. 1485 cal. AD towards upper parts of the record suggesting increased water availability due to e.g. prolonged flooding, increased precipitation or other factors, which have increased the water volume in Iitto flarks. In addition, the planktonic E. longispina occurs in higher proportional abundance in samples above 49 cm, which further suggests prolonged or more frequent river floods. However, any generalizations regarding temperature or precipitation trends for ca. 1485 cal. AD – ca. 1730 cal. AD are challenging due to chronological uncertainty. For example, it is possible that this section dates to a slightly warmer period between two cold periods of the Little Ice Age (LIA) in Northern Finnish Lapland identified by Luoto et al. (2017), or to a colder period of LIA. However, based on cladoceran community structure and the high abundance of wet indicators in our macrofossil data, it is very likely that this period was characterized by wet conditions. The interpretation of shifts in cladoceran community, plant community and climate are illustrated in fig. 6.
Fig. 6

Generalized temporal trajectories for Iitto study site


Our results clearly indicate that cladoceran communities in subarctic peatlandsare relatively diverse. Species richness and diversity is related to water availability which, in turn is controlled mainly by climatic factors. This observation is important in terms of future climate change because the hydrological shifts may have high-magnitude impacts on aquatic diversity in subarctic peatlands. This study confirms the ability of crustacean zooplankton to thrive in harsh subarctic environments and identifies hydrological dynamics as the most important drivers of peatland cladoceran communities. In addition, our findings highlight the applicability of cladoceran remains in peatland studies and namely their potential as additional indicators of hydrological conditions. In addition, this potential could be further utilized in e.g. food web and carbon dynamics studies in flood prone peatland systems.



Open access funding provided by University of Helsinki including Helsinki University Central Hospital. This study was funded by Academy of Finland, Tellervo and Juuso Walden Foundation and University of Helsinki Funds. In addition, H.Z. acknowledges China Scholarship Council (grant no. 201404910499) and Y.L. acknowledges China Scholarship Council (grant no. 201706180087).

Supplementary material

13157_2018_1118_MOESM1_ESM.pdf (216 kb)
ESM 1 (PDF 216 kb)
13157_2018_1118_MOESM2_ESM.pdf (335 kb)
ESM 2 (PDF 335 kb)
13157_2018_1118_MOESM3_ESM.pdf (280 kb)
ESM 3 (PDF 280 kb)
13157_2018_1118_MOESM4_ESM.pdf (178 kb)
ESM 4 (PDF 178 kb)


  1. Aurela M, Tuovinen J-P, Laurila T (1998) Carbon dioxide exchange in a subarctic peatland ecosystem in northern Europe measured by the eddy covariance technique. Journal of Geophysical Research 103:11289–11301CrossRefGoogle Scholar
  2. Battes KP, Moldovan I, Sas A (2014) Planktonic microcrustaceans (Crustacea:Cladocera,Copepoda) from several protected peat wetlands, differing in trophic state. North-Western Journal of Zoology 10(supplement 1):S78–S86Google Scholar
  3. Birks HJB, Line JM (1992) The use of rarefaction analysis for estimating palynological richness from Quaternary pollen−analytical data. The Holocene 2:1–10CrossRefGoogle Scholar
  4. Blaauw M, Christen JA (2011) Flexible paleoclimate age-depth models using an autoregressive gamma process. Bayesian Analysis 6:457–474Google Scholar
  5. Błędzki LA, Rybak JI (2016) Freshwater crustacean zooplankton of Europe. Springer International Publishing, SwizerlandGoogle Scholar
  6. Bring A, Fedorova I, Dibike Y, Hinzman L, Mård J, Mernild SH, Prowse T, Semenova O, Stuefer SL, Woo M-K (2016) Arctic terrestrial hydrology: A synthesis of processes, regional effects, and research challenges. Journal of Geophysical Research: Biogeosciences 121:621–649.
  7. Clarke KR (1993) Non−parametric multivariate analysis of changes in community structure. Australian Journal of Ecology 18:117–143CrossRefGoogle Scholar
  8. Coronel JS, Declerck S, Brendonck L (2007) High-altitude peatland temporary pools in Bolivia house a high cladoceran diversity. Wetlands 27:1166–1174CrossRefGoogle Scholar
  9. DiFonzo CD, Campbell JM (1988) Spatial partitioning of microhabitats in littoral cladoceran communities. Journal of freshwater ecology 4:303–313CrossRefGoogle Scholar
  10. Dumont HJ (1995) The evolution of groundwater cladoceran. Hydrobiologia 307:69–74CrossRefGoogle Scholar
  11. Esper J, Frank DC, Timonen M, Zorita E, Wilson RJS, Luterbacher J, Holzkämper S, Fischer N, Wagner S, Nievergelt D, Verstege A, Büntgen U (2012) Orbital forcing of tree-ring data. Nature Climate Change 2:686866 CrossRefGoogle Scholar
  12. Frey DG (1960) The ecological significance of cladoceran remains in lake sediments. Ecology 41:684–699CrossRefGoogle Scholar
  13. Gaedge U (2009) Trophic dynamics in aquatic ecosystems. In: Likens GE (ed) Plankton of inland waters. Elsevier, pp 344–350Google Scholar
  14. Gałka M, Szal M, Watson EJ et al (2017) Vegetation Succession, Carbon Accumulation and Hydrological Change in Subarctic Peatlands, Abisko, Northern Sweden. Permafrost and Periglacial Processes 28:589–604CrossRefGoogle Scholar
  15. Gallego-Sala AV, Charman DJ, Brewer S et al (2018) Latitudinal limits to the predicted increase of the peatland carbon sink with warming. Nature Climate Change.
  16. Glaser PH, Janssens JA, Siegel DI (1990) The response of vegetation to chemical and hydrological gradients in the Lost River Peatland, northern Minnesota. Journal of Ecology 78:1021–1048CrossRefGoogle Scholar
  17. Glime JM (2017) Arthropods: Crustacea – Copepoda and Cladocera. Chapter 10-1. In: Glime JM (ed) Bryophyte Ecology. Volume 2. Bryological Interaction. Michigan Technological University and the International Association of Bryologists. Accessed 20 March 2018
  18. Gliwicz ZM, Umana G (1994) Cladoceran body size and vulnerability to copepod predation. Limnology and Oceanography 39:419–424CrossRefGoogle Scholar
  19. Hammer Ø, Harper DAT, Ryan PD (2001) PAST. Paleontological statistics software package for education and data analysis. Palaeontologia Electronica 4(1):9Google Scholar
  20. Heikkinen JEP, Maljanen M, Aurela M, Hargreaves KJ, Martikainen PJ (2002) Carbon dioxide and methane dynamics in a sub-Arctic peatland in northern Finland. Polar Research 21:49–62CrossRefGoogle Scholar
  21. Holmquist JR, Finkelstein SA, Garneau M et al (2016) A comparison of radiocarbon ages derived from bulk peat and selected plant macrofossils in basal peat cores from circum-arctic peatlands. Quaternary Geochronology 31:53–61. CrossRefGoogle Scholar
  22. Holden J (2006) Chapter 14 Peatland hyrdology. In: Martini IP, Martinez Cortizas A, Chesworth W (eds) Developments in Earth surface processes. Volume 9: Peatlands: Evolution and records of environmental and climate changes. Elsevier, pp 319-346Google Scholar
  23. Jeppesen E, Nõges P, Davidson T, Haberman J, Nõges T, Blank K, Lauridsen T, Søndergaard M, Sayer C, Laugaste R, Johansson L, Bjerring R, Amsinck S (2011) Zooplankton as indicators in lakes: a scientific−based plea for including zooplankton in the ecological quality assessment of lakes according to the European Water Framework Directive (WFD). Hydrobiologia 676:279–297CrossRefGoogle Scholar
  24. Kalliola R, Puhakka M (1988) River dynamics and vegetation mosaicism: a case study of the River Kamajohka, northernmost Finland. Journal of Biogeography 15:703–719CrossRefGoogle Scholar
  25. Korhola A (1992) The early Holocene hydrosere in a small acid hill-top basin studied using crustacean sedimentary remains. Journal of Paleolimnology 7:1–22CrossRefGoogle Scholar
  26. Korhola A (1999) Distribution patterns of Cladocera in subarctic fennoscandian lakes and their potential in environmental reconstruction. Ecography 22:357–373CrossRefGoogle Scholar
  27. Korhola A, Rautio M (2001) Cladocera and other Branchiopod crustaceans. In: Smol JP, Birks HJB, Last WM (eds) Tracking environmental change using lake sediments. Volume 4: Zoological indicators. Kluwer Academic Publishers, Dordrecht, pp 5–41CrossRefGoogle Scholar
  28. Korhola A, Tikkanen M, Weckström J (2005) Quantification of Holocene lake-level changes in Finnish Lapland using a cladocera – lake depth transfer model. Journal of Paleolimnology 34:175–190CrossRefGoogle Scholar
  29. Kurek J, Korosi JB, Jeziorski A, Smol P (2010) Establishing reliable minimum count sizes for cladoceran subfossils sampled from lake sediments. Journal of Paleolimnology 44:603–612CrossRefGoogle Scholar
  30. Labuhn I, Hammarlund D, Chapron E, Czymzik M, Dumoulin J-P, Nilsson A, Régnier E, Robydg J, von Grafenstein U (2018) Holocene hydroclimate variability in central Scandinavia inferred from flood layers in contourite drift deposits in Lake Storsjön. Quaternary 1:2. CrossRefGoogle Scholar
  31. Laine J, Harju P, Timonen T, Laine A, Tuittila E-S, Minkkinen K, Vasander H (2009) The Intricate Beauty of Sphagnum Mosses – a Finnish Guide to Identification. Publications 39. University of Helsinki Department of Forest Ecology, HelsinkiGoogle Scholar
  32. Leppänen J, Siitonen S, Weckström J (2017) The stability of Cladoceran communities in sub-Arctic NW Finnish Lapland lakes. Polar Biology 40:2211–2223. CrossRefGoogle Scholar
  33. Luoto TP, Kivilä HE, Rantala MV, Nevalainen L (2017) Characterization of the medieval climate anomaly, little ice age and recent warming in northern Lapland. International Journal of Climatology.
  34. Mathijssen P, Tuovinen J-P, Lohila A, Aurela M, Juutinen S, Laurila T, Niemelä E, Tuittila E-S, Väliranta M (2014) Development, carbon accumulation, and radiative forcing of a subarctic fen over the Holocene. The Holocene 24:1156–1166CrossRefGoogle Scholar
  35. Matveev V, Robson BJ (2014) Aquatic food web structure and the flow of carbon. Freshwater Reviews 7:1–24CrossRefGoogle Scholar
  36. Mauquoy D, Van Geel B (2007) Plant macrofossil methods and studies: Mire and Peat Macros. In: Elias SA (ed) Encyclopedia of Quaternary Science. Elsevier Science, Amsterdam, pp 2315–2336. CrossRefGoogle Scholar
  37. Mauquoy D, Hughes P, Van Geel B (2010) A protocol for plant macrofossil analysis of peat deposits. Mires and Peat 7:1–5Google Scholar
  38. Medley KA, Havel JE (2007) Hydrology and local environmental factors influencing zooplankton communities in floodplain ponds. Wetlands 27:864–872CrossRefGoogle Scholar
  39. OIVA database (2018) Finnish environmental institute open database. Accessed 10 Feb 2018.
  40. Rautio M (1998) Community structure of crustacean zooplankton in subarctic ponds – effects of altitude and physical heterogeneity. Ecography 21:327–335CrossRefGoogle Scholar
  41. Sandøy S, Nilssen JP (1986) A geographical survey of littoral crustacea in Norway and their use in paleolimnology. Hydrobiologia 143:277–286CrossRefGoogle Scholar
  42. Sarmaja-Korjonen K, Hakojärvi M, Korhola A (2000) Subfossil of an unknown chydorid (Anomopoda: Chydoridae) from Finland. Hydrobiologia 436:165–169CrossRefGoogle Scholar
  43. Seppä H, Birks HJB (2001) July mean temperature and annual precipitation trends during the Holocene in the Fennoscandian tree-line area: pollen-based climate reconstructions. The Holocene 11:527–539CrossRefGoogle Scholar
  44. Siitonen S, Väliranta M, Weckström J, Juutinen S, Korhola A (2011) Comparison of Cladocera –based water-depth reconstruction against other types of proxy data in Finnish Lapland. Hydrobiologia 676:155–172CrossRefGoogle Scholar
  45. Strayer D (1988) Crustaceans and mites (Acari) from hyporheic and other underground waters in southeastern New York. Stygologia 4:192–207Google Scholar
  46. Swindles GT, Morris PJ, Mullan D et al (2015) The long-term fate of permafrost peatlands under rapid climate warming. Scientific Reports 5:17951. CrossRefGoogle Scholar
  47. Szeroczyńska K, Sarmaja–Korjonen K (2007) Atlas of subfossil cladocera from central and northern Europe. Friends of the Lower Vistula society, WarzawGoogle Scholar
  48. Tahvanainen T, Sallantaus T, Heikkilä R, Tolonen K (2002) Spatial variation of mire surface water chemistry and vegetation in northeastern Finland. Annales Botanici Fennici 39:235–251Google Scholar
  49. Teltewskoi A, Beermann F, Beil I et al (2016) 4000 Years of Changing Wetness in a Permafrost Polygon Peatland (Kytalyk, NE Siberia): A Comparative High-Resolution Multi-Proxy Study. Permafrost and Periglacial Processes 27:76–95CrossRefGoogle Scholar
  50. Vad CF, Horváth Z, Kiss KT, Ács É, Török JK, Forró L (2012) Seasonal dynamics and composition of cladoceran and copepod assemblages in ponds of a Hungarian cutaway peatland. International Review of Hydrobiology 97:420–434. CrossRefGoogle Scholar
  51. Viramo J. (editor) (1992): Oulanka Reports, Suokasviopas. Oulanka Biological Station, University of Oulu, 11.Google Scholar
  52. Väliranta M, Korhola A, Seppä H, Tuittila E-S, Sarjama-Korjonen K, Laine J, Alm J (2007) High-resolution reconstruction of wetness dynamics in a southern boreal raised bog, Finland, during the late Holocene: a quantitative approach. The Holocene 17:1093–1107CrossRefGoogle Scholar
  53. Väliranta M, Oinonen M, Seppä H, Korkonen S, Juutinen S, Tuittila E-S (2014) Unexpected problems in AMS 14C dating of fen peat. Radiocarbon 56:95–108CrossRefGoogle Scholar
  54. Väliranta M, Salojärvi N, Vuorisalo A et al (2017) Holocene fen–bog transitions, current status in Finland and future perspectives. Holocene 27:752–764CrossRefGoogle Scholar

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Authors and Affiliations

  1. 1.Environmental Change Research Unit (ECRU) Ecosystems and Environment Research Programme and Helsinki Institute of Sustainability Science (HELSUS), Faculty of Biological and Environmental SciencesUniversity of HelsinkiHelsinkiFinland
  2. 2.Key Laboratory of Desert and Desertification, Northwest Institute of Eco-Environment and ResourcesChinese Academy of SciencesLanzhouChina

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