How are spring zooplankton and autumn zooplankton influenced by water temperature in a polymictic lake?
Key words: spring zooplankton, autumn zooplankton, water temperature, polymictic lake.
Climate change is increasingly acknowledged as an important driver of lake ecocystems (Adrian, 1997; Williamson et al., 2009; Kernan et al., 2010; Jeppesen et al., 2014; Izmest'eva et al., 2016). Nevertheless, several authors (Moss et al., 2011; Wagner and Adrian, 2011; Battarbee et al., 2012; Bennion et al., 2012; Hobaek et al., 2012; Nicolle et al., 2012; Yates et al., 2013) have admitted that distinguishing climate impacts on water ecosystems from other drivers is complicated as climate signals are suppressed by other impacts, frequently by concurrent eutrophication, or because climate and other pressures may interact. Different types of lakes, as well as lakes located in different geographical and climate regions, respond to weather variations in different ways (Arvola et al., 2010; Noges et al., 2011; Dokulil et al., 2014); consequently, every lake is unique in this respect. Shallow lakes and deep lakes are differently affected by meteorological conditions; shallow polymictic freshwater ecosystems are particularly susceptible to climate warming (Mooij et al., 2005, 2007; Tuvikene et al., 2011; Jeppesen et al., 2014). Also, it is well documented that the effect of climate warming is more significant in winter and spring conditions (Adrian and Deneke, 1996; Weyhenmeyer et al., 1999; Thompson and Clark, 2008; Noges and Noges, 2014). Biological systems can respond to subtle signals in critical seasonal periods, serving as sensitive indicators of climate processes (Taylor et al., 2002; Wagner and Benndorf, 2007; Adrian et al., 2012). This can be explained by the fact that organisms are often adapted to a certain narrow temperature range and their life cycle strategies can be highly sensitive to variations in the ambient water temperature (Chen and Folt, 1996). The probability that future climate warming will cause major changes in the structure and functioning of freshwater ecosystems is very high (IPCC, 2007). The significant effect of water temperature on zoo-plankton is well known (Gerten and Adrian, 2002; Schalau et al., 2008; Dupuis and Hann, 2009; Straile, 2015).
Considering the above circumstances, we believed that the shallow polymictic Lake Vortsjarv, which is strongly influenced by climate (Tuvikene et al., 2011; Noges and Noges, 2014), was a proper medium for studying spring zooplankton and autumn zooplankton and their relationship with meteorological conditions.
The first data on the zooplankton of Lake Vortsjarv were presented in a monograph of Muhlen and Schneider (1920), where the lake was already classified as a eutrophic Chydorus-lake. Since 1965 up to the present (50 years) the zooplankton of the lake has been monitored monthly (in some years weekly and biweekly). Several authors have appreciated long-term ecological research into ecosystem's responses to environmental changes (Magnuson, 1990; Arvola et al., 2010; Kernan et al., 2010; Barr et al., 2013).
In Lake Vortsjarv zooplankton abundance has been relatively high (annual average 757 ind [L.sup.-1)] while its biomass has been low (0.874 mg [L.sup.-1]), which is characteristic of highly eutrophic water bodies with zooplankters of small weight (Andronikova, 1996). In Lake Vortsjarv, on average a rotifer weighed 0.7 ug, a cladoceran 9 ug, and a copepod 6 ug (Haberman and Haldna, 2014). Conditions for zooplankton are unfavourable in this lake. Phytoplankton is dominated by filamentous cyanobacteria (Aulacoseira spp. in spring, and Limnothrix planctonica, L. redekei, and Planktolyngbya limnetica in summer and in autumn), which are regarded as unsuitable food for zooplankton. Only 10% of the algae fall into the size fraction (<30 um) edible for zooplankton, and about 2% of the energy assimilated by the algae reaches zoo-plankton. As small-bodied zooplankton cannot effectively graze on large algae, there is no clear-water period in late spring in Lake Vortsjarv (Noges et al., 2004). According to Ger et al. (2014), cyanobacteria provoke selection in zooplankton and only more adapted species can live simultaneously with cyanobacteria. In Lake Vortsjarv zooplankton is dominated by rotifers, by small-bodied bakteriovorous cladocerans (Chydorus sphaericus, Bosmina longirostris), and by juveniles of cyclopoid copepods (Haberman, 1998).
All phytoplankton-based water quality indices, tested in long-term data, indicated deterioration in the water quality while none of them reflected a decline in the nutrient loadings to the lake in the 1990s. It seems that in Lake Vortsjarv the situation represents an expression of morphometric hypertrophy where the phytoplankton species indicating hypertrophy are favoured by changes in the water level (light limitation) rather than by changes in the nutrient content (Tuvikene et al., 2011). It has also been shown that an increase in water temperature plays an important role in the proliferation of cyanobacteria (Paerl and Huisman, 2008; Battarbee et al., 2012; Deng et al., 2014). Obviously, the prospect of improvement in the feeding conditions of zooplankton is low in Lake Vortsjarv.
According to some studies (Agasild et al., 2007; Zingel et al., 2007), the ciliate community of the lake is extremely rich (up to 191 cells m[L.sup.-1], usually >50% of the total zooplankton biomass). It has been found that ciliates consume about 20% of the standing stock of nanoplankton and almost 100% of the biomass production of bacteria during the growing season. As powerful predators on bacteria and small algae, ciliates can be strong food competitors for poorly fed cladocerans in this lake. Also, large predacious ciliates (haptorians) can reduce the abundance of small metazoans, such as rotifers (Noges et al., 2016). Aberle et al. (2012) reported that climate warming may be favourable to ciliates. It should also be noted that the water of the shallow and wind-stirred Lake Vortsjarv is rich in detritus, which may harm grazing cladocerans by clogging up their filter apparatus (Lougheed and Chow-Fraser, 1998). As zooplankton in Lake Vortsjarv is poor, the pressure of fish on it may be appreciable (Ginter et al., 2011).
The aims of this study were (1) to review the spring zooplankton and autumn zooplankton of a shallow polymictic lake; (2) to assess how much the zooplankton of the transition seasons, i.e. spring and autumn, is influenced by water temperature; and (3) to clarify the factors that are the main drivers of water temperature in such lakes.
The shallow (mean depth 2.8 m, maximum 6 m) large (270 km2) eutrophic polymictic Lake Vortsjarv is situated in South Estonia. The volume of the lake is 0.75 km3 and the water residence time is about 1 year. The mean transparency in the ice-free period is typically less than 1.0 m but may be only 10-15 cm after storms. The water level of Lake Vortsjarv fluctuates strongly (3.2 m) and the ecosystem of the lake is highly sensitive to these fluctuations, which follow the pattern of the North Atlantic Oscillation (NAO) index (Jarvet, 2004; Tuvikene et al., 2011). Temperature in Lake Vortsjarv is usually the highest (about 20 [degrees]C) in the second half of July or early August. The period with rather high water temperatures (for example 27.5 [degrees]C on 16 July 1994) has lasted since 1988. During most of the ice-free period the lake water is well oxygenated while rare winter anoxia has occurred in winters with extremely low water level. The water is alkaline (pH 8.0-8.6) with a great buffering capacity. Palaeodata demonstrated that the ecological status of Lake Vortsjarv deteriorated already in the 1960s; the process continued in the 1970s (Leeben et al., 2013), peaked in the 1980s (total phosphorus concentration (TP) 53 mg [L.sup.-1]), showed a small decline in the 1990s (TP 51 mg [L.sup.-]) and declined in the 2000s (TP 43 mg [L.sup.-1], Haberman and Haldna, 2014). The average TP concentration in the water of the lake was 42 mg [L.sup.-1] in spring and 56 mg [L.sup.-1] in autumn; the respective data of total nitrogen concentration (TN) were 1414 mg [L.sup.-1] and 822 mg [L.sup.-1].
MATERIAL AND METHODS
The current study is based on long-term (1965-2014) research into spring zooplankton and autumn zoo-plankton and concurrent meteorological conditions (air and water temperature, ice phenomena) in the shallow polymictic Lake Vortsjarv (Estonia). Quantitative zoo-plankton samples were collected monthly (in some years weekly or biweekly) at a permanent monitoring site, located between the Centre for Limnology and Tondisaar Island (58[degrees]12'40"N, 26[degrees]06'20"E), in the pelagial of the lake. The methods of collecting and treating zooplankton samples were described earlier in detail by Haberman and Haldna (2014). The data of daily water temperature, air temperature, and ice cover conditions were obtained from the Estonian Environmental Research Agency.
In the present study, we divided the year into climatic (thermal) seasons by threshold water temperatures according to Jarvet (2004). By spring we refer to the period with water temperature ranging from 4 to 15 [degrees]C, and by autumn to the period with water temperature from 15 to 4 [degrees]C. When gathering zooplankton data the water temperature of the sampling time was used. Longterm data of the NAO index for the winter months (January--February) were drawn from the webpage http://www.cpc.ncep.noaa.gov/products/precip/CWlink/pna/nao.shtml. A shift detection calculator (SDC) (Rodionov, 2004) was used to expose significant changes in climate and zooplankton. To detect relationships between the weather variables (annual mean air and water temperature for different months, the duration of the ice cover, and winter NAO), correlation analysis (CA, N = 50) was used. Regression analysis (RA) was used to estimate long-term trends. Contrasts between cold water and warm water were calculated using ANOVA model (AOV) for zooplankton taxa and groups. Zooplankton data were performed as follows: for total abundance of zooplankton and zooplankton groups, logarithmic; for species abundances, square root. All other calculations were carried out using the R package (R Development Core Team, 2011).
RESULTS AND DISCUSSION
The long-term (1965-2014) average air temperature in South Estonia, where Lake Vortsjarv is located, was 5.2 [degrees]C in April (quartile range 1.9-7.6 [degrees]C) and 11 [degrees]C in May (8.7-13.4 [degrees]C). In autumn the average values were 11 [degrees]C (8.7-13.4 [degrees]C) in September, 5.7 [degrees]C (3-8.7 [degrees]C) in October, and 0.6 [degrees]C (from -2 to +4 [degrees]C) in November. The annual mean air temperature increased during the study period by an average (mean [+ or -] standard error) of 0.47 [+ or -] 0.04 [degrees]C per decade. The greatest estimated rise (RA, p < 0.0001) for the 50 years occurred in January (5.5 [+ or -] 0.05 [degrees]C) and in April (3 [+ or -] 0.03 [degrees]C, Fig. 1a). A marked regime shift (about 2 [degrees]C, from 3.8 [degrees]C up to 6 [degrees]C) in the mean April temperature took place in 1989, the year with the highest value of the winter NAO index. The effects of the winter NAO are highly pronounced in the case of spring air temperatures (r = 0.41, p = 0.03). It is well known that the climate of both winter and early spring is strongly influenced by the oscillation patterns of the North Atlantic (Straile and Adrian, 2000; Jaagus, 2006; Klavins et al., 2007; Noges et al., 2007). During the 50 years the average air temperature for the three autumn months also showed an increasing trend while the estimated rise was twice lower than for April, being on average 1.5 [degrees]C (RA, p = 0.008, Fig. 1b).
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In the neighbouring regions (i.e. the regions influenced by the Baltic Sea), changes in annual air temperatures were synchronous with the increase starting in 1988 (Springe et al., 2007; Kriauciuniene et al., 2012). In Latvia (1851 - 2006), the increase of the average air temperature was 1.4 [degrees] C (Lizuma et al., 2007), in Lithuania (1970 - 1990) 0.5 - 0.9 [degrees]C (Pernaraviciute, 2004), and in Poland 0.8 - 1.0 [degrees]C (Dabrowski et al., 2004). Noges and Noges (2014) found that in Estonia the mean air temperature increased by 0.09 [degrees]C per decade from 1866 and by 0.44[degrees] per decade from 1961 and that in terms of seasons the most significant change occurred in spring. According to IPCC (2007), the global average annual air temperature increased about 0.6 - 0.9 [degrees] C from the end of the 19th century to the end of the 20th century. Mooij et al. (2007) supposed that the average air temperature increased about 0.6 [degrees]C during the last century and will increase 1.4 - 5.8 [degrees]C by 2100 (0.07 - 0.29 [degrees]C per decade). On the basis of an earlier study (Jaagus, 2006), the annual air temperature in Estonia increased 1.0 - 1.7 [degrees]C (0.2 - 0.34 [degrees]C per decade) in the second half of the 20th century, and the most significant increase in the air temperature, i.e. 0.4 - 0.66 [degrees]C per decade, was typical of spring.
According to Mooij et al. (2005), water temperature is among the most relevant climate factors in shallow lakes. In Lake Vortsjarv, spring lasted generally from 10 April to 31 May and autumn lasted from 12 September to 7 November (Fig. 2). The water temperature in April was (mean [+ or -] SE) 4.6 [+ or -] 1.4 [degrees]C, in May 12.3 [+ or -] 1.5 [degrees]C, in September 13.2 [+ or -] 1.4 [degrees]C, in October 6.7 [+ or -] 1.6 [degrees]C, and in November 2 [+ or -] 1.2 [degrees]C. On average, the water of Lake Vortsjarv warmed up from 4 [degrees]C to 15 [degrees]C during 48 [+ or -] 2 days in spring and it cooled down from 15 [degrees]C to 4 [degrees]C during 57 [+ or -] 1.5 days in autumn. The change per day was slower in autumn (0.18 [degrees]C) than in spring (0.2 [degrees]C; RA, p < 0.0001). According to statistical analysis, the most marked rise in water temperature occurred in April and the most marked fall in October; the mean change per decade was about 0.3 [degrees]C (RA, p < 0.001) for both months.
In 1965 - 1980, spring with a water temperature of 4 [degrees]C began on average on 13 April while in 2000 - 2014 spring with such water temperature began on average on 7 April. For the same time periods, autumn terminated on 1 November and 6 November, respectively. The beginning of spring shifted to an earlier date and the end of autumn, to a later date. A sharp rise in water temperature in April occurred in 1989 when, compared to the previous April, it increased more than 5 [degrees]C; the average level of temperature was continuously about 1.2 [degrees]C higher in the following 24 years (SDC, p < 0.001, Fig. 3a). In autumn the increase in water temperature was also essential (Fig. 3b). A similar stepwise increase of water temperature in the 1980s has also been observed by other researchers (Livingstone, 1997; Pernaraviciute, 2004; Springe et al., 2007; Noges et al., 2010; Dokulil et al., 2014; Straile, 2015).
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The water temperature in shallow polymictic lakes is tightly coupled to the air temperature (Livingstone and Dokulil, 2001; Mooij et al., 2005; Noges and Noges, 2014). Also in Lake Vortsjarv, a strong positive correlation was found between the water temperature and air temperature (April r = 0.65, May r = 0.54, September r = 0.62, October r = 0.6). A negative correlation was found between the water temperature, on the one hand, and the first ice-off day (r = -0.71) and ice cover duration, on the other hand (r = -0.42).
The condition of the ice cover on the lake is an important sensitive indicator of the regional climate and its change (Magnuson et al., 2000; Mooij et al., 2005; Arvola et al., 2010; Dokulil et al., 2014; Choinski et al., 2015). As an average for 50 years (1965-2014), Lake Vortsjarv was covered with ice from 28 November to 7 April, i.e. 130 days per year. It is consistent with earlier data on the duration of the ice cover on the lake (Jarvet, 2004; Dokulil et al., 2014; Noges and Noges, 2014). The earliest ice-on occurred on 8 October and the latest, on 22 November; the earliest ice-off took place on 23 March and the latest, on 5 May. The ice-off shifted by 18 days to an earlier date (RA, p = 0.001) and the ice-on shifted by 17 days to a later date (RA, p = 0.001).
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The duration of the ice cover was quite variable and became 35 days shorter during the study period (RA, p = 0.0003; Fig. 4). A decrease in the duration of ice at a rate of about 0.5 days per year was found for Neusiedler See, Lake Balaton, and for several Polish shallow lakes (Dokulil et al., 2014). Choinski et al. (2015) found for 18 Polish lakes that the duration of ice cover decreased by 5.6 days per decade during 1961-2010. Magnuson et al. (2000) reported a 6.5 days earlier ice-break in lakes in the Northern Hemisphere in the past 100 years in response to an air temperature increase of 1.2 [degrees]C. The timing of ice-on and ice-off is driven by several meteorological variables of which air temperature has been shown to be the most important one (Livingstone, 1997; Weyhenmeyer et al., 2008; Noges and Noges, 2014). In Lake Vortsjarv, the date of ice-on was most correlated with air temperature in December (CA, r = 0.98, p = 0.002). The frequency of ice-free winters, particularly in large lakes, is known to have increased (Weyhenmeyer et al., 2008); large Lake Peipsi was ice-free in winter 2007/2008 (Laugaste et al., 2010).
Altogether 45 zooplankton taxa were found in the pelagial of L. Vortsjarv in spring: 11 cladocerans (24%), 10 copepods (22%), and 24 rotifers (54%). The respective data for autumn were 11 (27%), 8 (19%), and 22 (54%, Table 1). During the 50 years, essential changes occurred in the zooplankton composition of the lake. Already in the 1960s-1970s, i.e. at the time of the first signs of eutrophication (Leeben et al., 2013), species characteristic of oligo-mesotrophic waters (Asplanchna herricki, Bythotrephes longimanus) disappeared from the zoo-plankton. In the 1980s-1990s, in the period of the highest trophy of the lake (TP > 50 mg [L.sup.-1]) and a stepwise rise in the water temperature (Noges, 2009; Noges and Noges, 2014), species preferring lower trophy (Bipalpus hudsoni, Conochilus unicornis, Kellicottia longispina, Bosmina berolinensis, Cyclops kolensis, Eudiaptomus gracilis), which had been present in the 1960s-1970s, had disappeared. Despite the decrease in the loadings as well as in in-lake nutrient concentrations (Noges et al., 2007; Haberman and Haldna, 2014), these species did not reappear.
It is well known that zooplankton responds to changes in the trophic state of a water body with a certain lag (Jeppesen et al., 2002; Carvalho et al., 2012); however, as climate warming promotes eutrophication it is very difficult to distinguish interactions between trophic state and warming (Moss et al., 2011; Wagner and Adrian, 2011; Bennion et al., 2012). In Lake Vortsjarv, the genus Daphnia was only represented by D. cucullata, a character species for eutrophic water bodies. Thermophilous D. cucullata, appearing in spring zooplankton at a water temperature of about 12-13 [degrees]C, was never abundant in the spring zooplankton but was still relatively numerous in the autumn plankton. However, in the 1990s this species almost disappeared from the lake. This can be explained by unfavourable feeding conditions (Claska and Gilbert, 1998; Carvalho et al., 2012) and by strong fish predation (Ginter et al., 2011). Also Bosmina coregoni, which was relatively abundant in the 1960s-1970s, disappeared from the zooplankton starting from the 1990s and had not re-appeared by the end of the study period. At the same time, the cladoceran community became dominated by small-bodied B. longirostris. Davidson et al. (2011) described a similar change from Lake Sobygaard (Denmark), where it was most likely due to increased fish predation. Starting from the 1990s, the abundance of the rotifer genus Brachionus (B. calyciflorus, B. angularis) increased in Lake Vortsjarv. Evidently, this was supported by the rich community of ciliates (Mohr and Adrian, 2002) in this lake. During the 50 years the average annual number of zooplankton species decreased in both seasons about 1.4 species per year (RA, p < 0.05, Fig. 5). Several researchers (Wrona et al., 2006; Shurin et al., 2010; Haberman and Haldna, 2014) are of the opinion that freshwater species are at high risk of extinction and that the most influential drivers are related to climate induced stress.
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Frequency of zooplankton taxa
In spring, the most frequent (>70% of all collected samples) zooplankton taxa were Keratella cochlearis, Keratella quadrata, Polyarthra dolichoptera, Chydorus sphaericus, and copepodites and nauplii of cyclopoid copepods (Table 1). To resist unsuitable water temperature in winter, dormancy is common for zooplankton species (Sarvala, 1979; Ricci, 2001; De Stasio, 2004). Rotifers and cladocerans overwinter as resting eggs, while copepods mainly overwinter as fifth-stage copepodites. At proper water temperature and light conditions (Vandekerkhove et al., 2005; Dupuis and Hann, 2009), they will continue rapid development in spring. Copepod juveniles and species of the genus Bosmina were among the earliest zooplankters in Lake Peipsi (Laugaste et al., 2010), while D. cucullata was always among the latest (Haberman and Virro, 2004). According to Gulati (1978), the genus Bosmina is usually common in temperate lakes in early spring. In Lake Vortsjarv the most frequent zoo-plankters in autumn were C. sphaericus, B. longirostris, Polyarthra luminosa, K. cochlearis, and copepodites and nauplii of cyclopoid copepods (Table 1). The most characteristic cladoceran in Lake Vortsjarv was C. sphaericus. It usually appeared in May and disappeared in November; however, a few individuals may have been present in winter plankton. The species was found at water temperatures of 0.8-27.6 [degrees]C. Another dominating cladoceran in Lake Vortsjarv, B. longirostris, was also found at water temperatures of 0.8-27.6 [degrees]C. The species appeared as single individuals already in April, being, as a rule, the earliest among the cladocerans (Haberman and Virro, 2004).
Domination was calculated as the percentage of each zooplankton taxon of total zooplankton abundance (Green, 1993). In Lake Vortsjarv, the zooplankton species accounting for at least 20% of the total zooplankton abundance were considered dominants. Molina-Navarro et al. (2012) used the categories 'low' (0-5% of total zooplankton abundance), 'mid' (5-15%), 'high' (15-40%), and 'very high' (>40%) to estimate the share of zooplankton species in the total zooplankton abundance. In spring, zooplankton abundance was mainly built of K. cochlearis, P. dolichoptera, and K. quadrata. In autumn, zooplankton abundance was mainly formed by P. luminosa, K. cochlearis, and C. sphaericus (Table 1). A great majority of the zooplankton species of Lake Vortsjarv were of minor importance, with only a few (1-2) dominating species, which is characteristic of strongly eutrophic water bodies (Andronikova, 1996). The so-called functioning load was divided unevenly between species, which is quite expected for such water bodies. The number of dominants increases in parallel with a decrease in the trophic state of lakes. In the oligotrophic Lake Saimaa (Finland), the mean number of dominating species varied between 4 and 8 (Hynynen et al., 1999).
As spring and autumn (transition seasons) are the seasons with the most variable in-season water temperature conditions (continuous rise in spring and fall in autumn), also the in-season zooplankton was highly variable. In spring the abundance of zooplankton fluctuated between 61 and 3800 ind [L.sup.-1] (95% tolerance limits), being on average about three times as high as in autumn (43-1056 ind [L.sup.-1], Table 1).
In the strongly eutrophic Lake Vortsjarv zooplankton abundance was overwhelmingly dominated by rotifers. The share of rotifers in the zooplankton community was considerably larger in spring than in autumn, with a mean difference of 26% (AOV, p < 0.0001, Table 1). The high population growth potential of rotifers, owing to the short development time and parthenogenetic reproduction, allows them to respond quickly to favourable changes in a lake (Allan, 1976; Adrian et al., 2006). In spring food competition and mechanical interference by cladocerans should be negligible in view of their low abundance (Table 1). Predation by cyclopoid copepods may be strong (Brandl, 2005); however, in spring, when among copepods there are numerous non-predatory nauplii and copepodites, their impact on rotifers cannot be essential in Lake Vortsjarv. Also fish larvae prey on rotifers (Telesh, 1993), but at least in early spring this cannot be of significance, either. Rotifers are the first resource for newly hatched fish, and the advance in their phenology might affect fish recruitment negatively (Nicolle et al., 2011). Nicolle et al. (2012) suggested that rotifers may be a suitable indicator group for detecting changes in temperature regimes in freshwater ecosystems. The role of thermophilic cladocerans in the zooplankton abundance in spring was unimportant and significantly smaller than in autumn. The share of copepods (dominated by juveniles of cyclopoid copepods) in the total zooplankton abundance was modest and similar in both seasons (Table 1). Several studies (Talling, 2003; Sommer and Lengfellner, 2008; Straile, 2015) point to a possible mismatch between zooplankton and their food (algae) in spring. Cladocerans, dominating in Lake Vortsjarv, are prevalently bacteriovorous, and their relationship with algae is weak. At the same time, bacteria are known to boost as a result of a rise in water temperature (Sand-Jensen et al., 2007).
The impact of temperature on the development of zooplankton abundance was essential: a significant correlation (CA, p < 0.01) was found between the water temperature and the abundance of cladocerans (r = 0.47), copepods (r = 0.62), and rotifers (r = 0.53). The in-season distribution of zooplankton species also demonstrates close relationship between water temperature and zooplankton taxa (Fig. 6, Table 2). Zooplankton was influenced the most by average water temperature of 5 days preceding sampling. The influence of water temperature was more marked in spring than in autumn, and zooplankton was more stable in autumn (Fig. 6, Table 2). Statistical analysis showed that when water temperature rose one degree in spring, the abundance of zooplankton increased on average 27%, and when water temperature fell one degree in autumn, zooplankton abundance decreased 9% (RA, p = 0.001). According to Adrian et al. (1999), because of the low heat storage capacity of shallow lakes, the effects of winter on plankton communities in spring are short-lived and are soon overtaken by prevailing weather and by biotic interactions. Herzig (1994) indicated that abiotic factors (e.g. temperature) exert the most important impact on the zooplankton community in spring and autumn while biotic factors (e.g. food, predation) play a significant role in the summer months. Dupuis and Hann (2009) showed, on the basis of zooplankton hatching experiments, that the development of the zooplankton population within 60 days was promoted at temperatures of 12 [degrees]C, and a longer period was required at lower (6 [degrees]C, 9 [degrees]C) temperatures. Because water temperature is perceived differently by species with different thermal tolerance, we distinguished so-called 'winners' and 'losers' (Domisch et al., 2011) for cold-water versus warm-water periods of spring as well as for autumn (Table 2).
In Lake Vortsjarv, the species of spring zooplankton and autumn zooplankton can be divided into three groups: (1) eurytherms, which make up an overwhelming part of the zooplankton; (2) cold-water stenotherms K. hiemalis, P. dolichoptera, Synchaeta verrucosa, and (3) warm-water stenotherms Anuraeopsis fissa and Daphnia cucullata (Tables 1, 2).
A shift (i.e. a marked increase in zooplankton abundance, switch from cold-water to warm-water species) in the abundance of spring zooplankton occurred in Lake Vortsjarv at a water temperature of about 10 [degrees] C (critical time window). In autumn a comparable but less conspicuous change (a decrease in abundance, switch from warm-water species to cold-water species) was found at the same water temperature (Fig. 6, Table 2).
Several studies (Wagner and Benndorf, 2007; Wagner and Adrian, 2011; Adrian et al., 2012) emphasize that records of ecological processes should be not only sufficiently long but also collected at an appropriate temporal resolution as lake ecosystems respond to shortterm weather conditions during critical time windows in the year. In Lake Vortsjarv rotifers showed the most significant increase in abundance at a water temperature of 10 [degrees]C. Consequently, as spring zooplankton consists mainly of rotifers, they also increased the response of the total zooplankton to the rise in water temperature. Similarly, Chen et al. (2012) recorded a marked increase of rotifer densities at 10 [degrees]C in spring. As rotifers and cladocerans have a relatively short development period, a rise in water temperature can result in their increased abundance in only a few days. At the same time, the effect of temperature may be delayed in the case of copepods, which have a long development period and undergo multiple stages before adulthood (Adrian et al., 2006; Nicolle et al., 2012). As an average, a water temperature of 10 [degrees]C occurred in Lake Vortsjarv on 8 May in spring and on 10 September in autumn. During the 50 study years the period with a water temperature of 10 [degrees]C shifted by 7 days (RA, p = 0.04) to an earlier date in spring and by 6 days (p = 0.08) to a later date in autumn.
The long-term (1965-2014) study on spring (season with a water temperature of 4-15 [degrees]C) versus autumn (15-4 [degrees]C) zooplankton and on concurrent meteorological (air and water temperature, ice phenomena) conditions in the shallow (mean depth 2.8 m) polymictic Lake Vortsjarv (Estonia) allowed us to draw the following conclusions:
1. The main drivers of water temperature were air temperature and ice conditions;
2. Both air temperature in the territory of Lake Vortsjarv and water temperature in the lake increased, while the duration of the ice cover on the lake decreased;
3. The beginning of spring shifted to an earlier date and the end of autumn, to a later date;
4. The abundance of zooplankton in the seasons with highly variable water temperature was also variable and largely dependent on water temperature. Zoo-plankton was influenced the most by average water temperature on 5 days preceding sampling and was more affected by water temperature in spring than in autumn. Autumn zooplankton was more stable than spring zooplankton;
5. A shift in the abundance of zooplankton in spring and to a lesser degree in autumn occurred at a water temperature of 10 [degrees]C (critical time window). During the 50 study years, the period with a mean water temperature of 10 [degrees]C shifted by 7 days to an earlier date in spring and by 6 days to a later date in autumn;
6. During the 50 years, the number of zooplankton species declined in both seasons. In the 1980s-1990s, i.e. the period of the highest trophy of the lake and a stepwise rise in water temperature, the species preferring lower trophy disappeared from the zooplankton;
7. Zooplankton abundance was three times as high in spring as in autumn and was dominated by rotifers, small-bodied cladocerans, and juveniles of cyclopoid copepods. The domination of rotifers was more pronounced in spring (92%) than in autumn (70%). The share of cladocerans was negligible in the spring zooplankton (2%), but appreciable (24%) in the autumn zooplankton. The share of copepods in the total zooplankton abundance (6%) was modest and similar in both seasons.
In the study hydrobiological collections of the Centre for Limnology of the Estonian University of Life Sciences and data from the Estonian State Monitoring Programme were used. We are indebted to Mrs Ester Jaigma for revising the English text of this paper. The contribution of the referees is highly appreciated.
The publication costs of this article were covered by the Estonian Academy of Sciences.
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Juta Haberman and Marina Haldna (*)
Centre for Limnology, Estonian University of Life Sciences, 61117 Rannu, Tartumaa, Estonia
Received 3 February 2017, accepted 16 March 2017, available online 19 June 2017
(*) Corresponding author, firstname.lastname@example.org
Kuidas on kevade ja sugise zooplankton mojutatud veetemperatuurist madalas polumiktilises veekogus?
Juta Haberman ja Marina Haldna
Too eesmark oli saada ulevaade: 1) koige muutlikumate meteoroloogiliste tingimustega sesoonide, kevade ja sugise zooplanktonist madalas polumiktilises jarves; 2) uurida, kui palju on zooplankton nn ulemineku- (transition) sesoonidel mojutatud veetemperatuurist; 3) millest oleneb seda tuupi veekogus veetemperatuur.
Kevadena kasitlesime perioodi, mil veetemperatuur on 4-15 [degrees]C, ja sugisena perioodi veetemperatuuriga 15-4 [degrees]C (joon 3). Viiekumne aasta (1965-2014) materjalide pohjal uuriti madala (2,8 m) polumiktilise Vortsjarve kevade versus sugise zooplanktonit ja neid mojutavaid meteoroloogilisi tingimusi, vee- ja ohutemperatuuri ning jarve jaakatte perioodi. Jarve vesi soojenes 4-st 15 kraadini keskmiselt 48 paevaga kevadel ja jahenes 15-st 4 kraadini 57 paevaga sugisel.
Uuringu pohjal voib jareldada:
1) veetemperatuuri pohilisteks kujundajateks kevadel ja sugisel olid ohutemperatuur ning jarve jaakatte kestus. Tugev positiivne korrelatsioon oli vee- ja ohutemperatuuride vahel nii kevadel (aprillis r = 0,65, mais r = 0,54) kui ka sugisel (septembris r = 0,62, oktoobris r = 0,6). Negatiivne korrelatsioon leiti veetemperatuuri ja esimese jarve jaavaba paeva (r = -0,71) ning veetemperatuuri ja jaakatte kestuse vahel (r = -0,42). Uuringuperioodil veetemperatuur (joon 2) ja ohutemperatuur (joon 1) jarve territooriumil tousid, jaakatte kestus paevades luhenes (joon 4), kevade algus nihkus varasemale ning sugise lopp hilisemale ajale;
2) kokku leiti Vortsjarve pelagiaali zooplanktoni kvantitatiivsetest proovidest uurimisperioodil kevadel 45 ja sugisel 41 zooplanktoni taksonit (tabel 1). Aasta keskmine taksonite arv vahenes 50 aasta jooksul nii kevadel kui ka sugisel (joon 5). Aasta koige muutlikumate meteoroloogiliste tingimustega sesoonidel, kevadel (ohu- ja veetemperatuuri tous) ja sugisel (temperatuuri langus), oli zooplanktoni arvukus vaga varieeruv (kevadel 61-3800 ind [L.sup.-1] ning sugisel 43-1056 ind [L.sup.-1]). Zooplanktoni arvukus oli kevadel (922 ind [L.sup.-1]) peaaegu kolm korda suurem kui sugisel (325 ind [L.sup.-1]). Zooplanktoni arvukuse moodustasid tugevalt eutroofses Vortsjarves ulekaalukalt (kevadel 92%, sugisel 70%) keriloomad (Rotifera). Vesikirbuliste (Cladocera) osa zooplanktonis oli tuhine kevadel (2%), oluliselt suurem (24%) sugisel. Aerjalgsed (Copepoda) olid nii kevadel kui ka sugisel zooplanktoni arvukuses esindatud tagasihoidlikult (6%). Sagedamad ja arvukuselt domineerivad zooplankterid on esitatud tabelites 1 ning 2. Esinenud zooplankteritest oli enamik vaikese tahtsusega, domineerisid vaid 1-2 liiki (tabel 1);
3) veetemperatuuri moju zooplanktonile oli kevadel tugevam kui sugisel. Statistiline analuus naitas, et veetemperatuuri tous 1 kraadi vorra kevadel suurendas zooplanktoni arvukust keskmiselt 27%, samal ajal 1-kraadine temperatuuri langus sugisel vahendas zooplanktoni arvukust keskmiselt 9%. Markimisvaarne zooplanktoni arvukuse tous ja langus sugisel toimusid veetemperatuuril 10 [degrees]C (critical time window, joon 6). Kevadel oli muutus oluliselt suurem kui sugisel. Kriitilise veetemperatuuri periood nihkus 50 aasta jooksul kevadel keskmiselt 7 paeva vorra varasemale ja sugisel 6 paeva vorra hilisemale ajale, mis viitab selgelt kliima soojenemisele.
Table 1. Frequency and abundance of zooplankton in spring and in autumn (1965-2014). Percentages indicate the share in total zooplankton abundance Taxon Spring (N = 91) Frequency, Abundance % ind [L.sup.-1] % Total zooplankton 922.3 Rotifera 849.3 92.1 Anuraeopsis fissa (Gosse) 15.1 31.7 3.4 Ascomorpha ecaudis Perty 1.9 0.5 0.1 Asplanchna girodi de Guerne 7.5 0.2 0.0 Asplanchna priodonta Gosse 30.2 3.7 0.4 Bdelloida gen. sp. 5.7 0.3 0.0 Bipalpus hudsoni (Imhof) 2.8 <0.1 0.0 Brachionus angularis Gosse 8.5 0.4 0.0 Brachionus c. calyciflorus Pallas 26.4 2.5 0.3 Conochilus unicornis Rousselet 17.9 9.9 1.1 Filinia longiseta (Ehrenberg) 52.8 5.7 0.6 Gastropus stylifer Imhof 10.4 0.9 0.1 Kellicottia longispina (Kellicott) 23.6 11.2 1.2 Keratella cochlearis (Gosse) 90.6 394.1 42.7 Keratella hiemalis Carlin 15.1 2.5 0.3 Keratella quadrata (Muller) 85.8 126.7 13.7 Notholca labis Gosse 0.9 <0.1 0.0 Notholca squamula (Muller) 7.5 0.4 0.0 Polyarthra dolichoptera Idelson 74.5 144.4 15.7 Polyarthra luminosa Kutikova 41.5 89.6 9.7 Synchaeta verrucosa Nipkow 44.3 12.9 1.4 Trichocerca porcellus (Gosse) 2.8 0.4 0.0 Trichocerca rousseleti (Voigt) 9.4 10.7 1.2 Trichotria tetractis (Ehrenberg) 1.9 <0.1 0.0 Trichotria pocillum (Muller) 1.9 <0.1 0.0 Cladocera 19.0 2.1 Alona guttata Sars 0.9 <0.1 0.0 Alona costata Sars 0.9 <0.1 0.0 Alona rectangula Sars 0.9 <0.1 0.0 Alonella nana (Baird) 6.6 <0.1 0.0 Bosmina berolinensis Imhof 14.2 0.3 0.0 Bosmina c. coregoni (Baird) 39.6 1.8 0.2 Bosmina longirostris (O.F. Muller) 63.2 5.0 0.5 Bosmina obtusirostris Sars 2.8 <0.1 0.0 Chydorus sphaericus (O.F. Muller) 74.5 10.0 1.1 Daphnia cucullata Sars 10.4 0.1 0.0 Leptodora kindti (Focke) 8.5 0.1 0.0 Copepoda 54.1 5.9 Copepodites 93.4 14.8 1.6 Nauplii 91.5 33.6 3.6 Acanthocyclops viridis (Jurine) 2.8 0.1 0.0 Cyclops kolensis Lilljeborg 16 1.7 0.2 Eucyclops macrurus (Sars) 0.9 0.1 0.0 Eucyclops serrulatus (Fischer) 3.8 <0.1 0.0 Eudiaptomus gracilis (Sars) 15.1 0.3 0.0 Mesocyclops crassus (Fischer) 13.2 0.3 0.0 Mesocyclops leuckarti Claus 47.2 1.8 0.2 Mesocyclops oithonoides Sars 35.8 1.2 0.1 Taxon Autumn (N = 119) Frequency, Abundance % ind [L.sup.-1] % Total zooplankton 324.6 Rotifera 227.5 70.1 Anuraeopsis fissa (Gosse) 11.7 23.5 10.3 Ascomorpha ecaudis Perty 1.5 0.2 0.1 Asplanchna girodi de Guerne 0.7 0.1 0.0 Asplanchna priodonta Gosse 51.8 3.2 1.4 Bdelloida gen. sp. 4.4 0.2 0.1 Bipalpus hudsoni (Imhof) 4.4 <0.1 0.0 Brachionus angularis Gosse 0.0 0.0 Brachionus c. calyciflorus Pallas 12.4 0.9 0.4 Conochilus unicornis Rousselet 5.8 0.6 0.3 Filinia longiseta (Ehrenberg) 33.6 4.4 1.9 Gastropus stylifer Imhof 8 1.3 0.6 Kellicottia longispina (Kellicott) 5.8 0.1 0.0 Keratella cochlearis (Gosse) 70.0 42.0 18.5 Keratella hiemalis Carlin 1.5 0.1 0.1 Keratella quadrata (Muller) 51.8 10.8 4.7 Notholca labis Gosse 0.7 0.1 0.0 Notholca squamula (Muller) Polyarthra dolichoptera Idelson 26.3 16.1 7.1 Polyarthra luminosa Kutikova 74.5 109.5 48.1 Synchaeta verrucosa Nipkow 16.8 1.9 0.8 Trichocerca porcellus (Gosse) 4.4 0.6 0.3 Trichocerca rousseleti (Voigt) 13.9 10.2 4.5 Trichotria tetractis (Ehrenberg) 1.5 <0.1 0.0 Trichotria pocillum (Muller) 0.7 <0.1 0.0 Cladocera 0.7 77.1 23.8 Alona guttata Sars 0.7 <0.1 0.0 Alona costata Sars 20.4 0.8 0.3 Alona rectangula Sars 39.4 1.4 0.6 Alonella nana (Baird) 8.8 0.1 0.0 Bosmina berolinensis Imhof 28.5 0.6 0.2 Bosmina c. coregoni (Baird) 63.5 7.5 3.3 Bosmina longirostris (O.F. Muller) 78.1 8.0 3.5 Bosmina obtusirostris Sars 5.1 <0.1 0.0 Chydorus sphaericus (O.F. Muller) 95.6 55.1 24.2 Daphnia cucullata Sars 33.6 1.4 0.6 Leptodora kindti (Focke) 1.5 <0.1 0.0 Copepoda 20.0 6.2 Copepodites 84.7 12.1 5.3 Nauplii 73.7 6.2 2.7 Acanthocyclops viridis (Jurine) 1.5 <0.1 0.0 Cyclops kolensis Lilljeborg 0.7 0.0 0.0 Eucyclops macrurus (Sars) 0.0 0.0 Eucyclops serrulatus (Fischer) 0.7 <0.1 0.0 Eudiaptomus gracilis (Sars) 16.8 0.6 0.2 Mesocyclops crassus (Fischer) Mesocyclops leuckarti Claus 18.2 0.9 0.4 Mesocyclops oithonoides Sars 5.1 0.1 0.0 Table 2. Comparison of zooplankton abundances for cold-water (4-9.9 [degrees] C) spring and autumn and for warm-water Mean abundance, ind [L.sup.-1] Cold-water Warm-water Difference N = 34 N = 57 SPRING Total zooplankton 437.85 1325.66 882.24 Copepods 18.62 79.17 57.58 Rotifers 417.02 1218.77 790.24 Cladocerans 2.21 27.73 34.42 Copepodites 6.71 20.04 13.63 Nauplii 9.56 51.96 39.12 Bosmina berolinensis 0.01 0.62 0.61 Bosmina coregoni 0.21 3.03 3.44 Bosmina longirostris 0.89 8.33 7.13 Chydorus sphaericus 0.99 13.17 20.20 Mesocyclops oithonoides 0.44 1.40 1.11 Asplanchna priodonta 0.13 6.93 5.47 Keratella cochlearis 119.70 597.47 478.02 Keratella hiemalis 5.49 0.48 --5.13 Polyarthra luminosa 1.13 163.76 173.04 Synchaeta verrucosa 27.29 2.86 --25.07 N = 72 N = 47 AUTUMN Copepods 12.51 33.96 24.51 Copepodites 7.38 20.92 16.44 Nauplii 3.77 10.75 7.35 Daphnia cucullata 0.46 3.33 2.82 Anuraeopsis fissa 2.61 60.80 52.53 Polyarthra dolichoptera 25.06 0.05 -25.01 Synchaeta verrucosa 2.92 0.00 -2.92 Results of the tests Ratio p-Value Total zooplankton 3.03 <0.0001 Copepods 4.25 <0.0001 Rotifers 2.92 0.0002 Cladocerans 12.54 <0.0001 Copepodites 2.98 0.0003 Nauplii 5.44 <0.0001 Bosmina berolinensis 51.67 0.0132 Bosmina coregoni 14.59 0.0166 Bosmina longirostris 9.34 <0.0001 Chydorus sphaericus 13.29 0.0019 Mesocyclops oithonoides 3.16 0.0104 Asplanchna priodonta 51.75 0.0043 Keratella cochlearis 4.99 0.0005 Keratella hiemalis 11.44 0.0062 Polyarthra luminosa 144.67 0.002 Synchaeta verrucosa 9.54 <0.0001 Copepods 2.71 <0.0001 Copepodites 2.84 <0.0001 Nauplii 2.85 <0.0001 Daphnia cucullata 7.33 <0.0001 Anuraeopsis fissa 23.28 0.0004 Polyarthra dolichoptera 472.85 0.0042 Synchaeta verrucosa 0.02
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|Author:||Haberman, Juta; Haldna, Marina|
|Publication:||Proceedings of the Estonian Academy of Sciences|
|Date:||Sep 1, 2017|
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