Changes in Phytoplankton Biomass in the Western Scheldt Estuary During the Period 1978–2006
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- Kromkamp, J.C. & Van Engeland, T. Estuaries and Coasts (2010) 33: 270. doi:10.1007/s12237-009-9215-3
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We investigated whether climate change results in long-term changes in phytoplankton biomass and phenology in a turbid eutrophic coastal plain estuary. Changes in annual mean chlorophyll a (chla) concentrations were studied for the period 1978–2006 in the eutrophic and turbid macro-tidal Western Scheldt estuary. Three stations were investigated: WS1, at the mouth of the estuary; station WS6, halfway up the estuary; and station WS11, near the Dutch–Belgian border near the upstream end of the estuary. No significant long-term changes in yearly averaged chla concentrations were observed in WS1 and WS6, but in WS11 the phytoplankton biomass decreased considerably. This is most likely due to an increase in grazing pressure as a result of an improvement in the dissolved oxygen concentrations. Spectral analyses revealed a possible periodicity of 7 years in the mean chla which was related to periodicity in river discharge. We also observed strong phenological responses in the timing of the spring/summer bloom which were related to a well-documented increase in the temperature in the estuary. The fulcrum, the center of gravity or the day at which 50% of the cumulative chla was reached during the year, advanced by 1–2 days/year. A similar trend was observed for the month in which the maximum bloom was observed, with the exception of station WS1. All stations showed an earlier initiation of the bloom, whereas the day at which the phytoplankton bloom was terminated also moved forward in time excepted for WS11. As a result, the bloom length decreased at station WS1, remained the same at station WS6, and increased at WS11. This complicated pattern in bloom phenology demonstrates the complex nature of ecosystem functioning in estuaries.
KeywordsChlorophyll aTimes seriesPhenologyPhytoplankton biomassWestern Scheldt estuary
The influence of climate change is well documented in marine ecosystems. Regime shifts have been observed in many oceans and seas like the North Pacific (Chiba et al. 2008; Hare and Mantua 2000), the Atlantic (Beaugrand 2004a), the Baltic (Hakanson and Lindgren 2008), the North Sea (Edwards et al. 2002; McQuatters-Gollop et al. 2007; Weijerman et al. 2005), as well as in many lakes (Scheffer et al. 2001). These regime shifts are often driven by changes in large-scale weather patterns like the Pacific decadal oscillation or the North Atlantic Oscillation (NAO). Because of the semicyclic pattern of these changes, they might obscure changes induced by human-induced climate change. Climate-induced warming events are well documented as changes in phenology in terrestrial systems (Walther et al. 2002). Marine systems are less well documented, especially with regard to the lowest levels of the foodweb. Edwards and Richardson (2004) noticed a significant earlier start in the development of dinoflagellates and zooplankton in the North Sea, whereas the timing of diatom blooms in general did not change. The Helgoland Road (German Bight, North Sea) time series, with its high temporal resolution, also did exhibit a long-term change in the timing of the spring bloom, although the spring bloom seemed to be delayed in warm years (Wiltshire et al. 2008).
Estuaries have been less well studied with respect to phenology and climate change. Because estuarine ecosystem function is heavily influenced by land-use changes, it might be very hard to actually detect signals due to climate change. Nevertheless, regime shifts have been observed in estuaries. In North San Francisco Bay, the introduction of the Asian clam (Potamocurbula amurensis) drastically reduced the magnitude of the phytoplankton blooms (Cloern 2001). Climate change causes migration of benthic marine species, but often, these sorts of introductions are caused by man with species migrating in ballast tanks of ships.
The heterotrophic Western Scheldt estuary is a turbid, well-mixed, macro-tidal eutrophic estuary. In the last two decades, the water quality of the estuary has improved considerably, due to gradually increased efforts since the end of the 1970s to treat wastewater before it is discharged into the Schelde River (Soetaert et al. 2006). Changes in nutrient concentrations have been recently summarized by Soetaert et al. (2006). In addition, there is regular dredging to remove sills in order to allow large ships to enter the port of Antwerp. Despite the large changes in nutrient loads and dredging activity, primary production does not seem to have changed significantly between 1991 and 2001 (Kromkamp and Peene 2005). This is probably due to the fact that even though phosphate concentrations might have reached potentially limiting concentrations for short periods in spring in the mouth of the estuary, it is the high turbidity that is still mainly causing light-limited growth of the phytoplankton.
The objective of this paper was to determine if long-term changes in phytoplankton biomass and the timing of the phytoplankton bloom in this heavily anthropogenically influenced estuary occur as a result of climate change. We observed complex changes in the phenology of the bloom initiation and bloom termination during the period 1978–2006.
Materials and Methods
The estuary is sampled for monitoring by the Netherlands Institute of Coastal and Marine Management (RIKZ), which has four sites in the estuary: Vlissingen (Flushing, WS1), a station in the mouth of the estuary with an average salinity of ~30, Hansweert (WS6) halfway the estuary (salinity ~ 17), Bath (WS10, salinity ~ 11), and one near the Dutch–Belgian Border (Doel, WS11, salinity ~ 7). Data from these sites were retrieved from the database www.waterbase.nl maintained by Rijkswaterstaat (RWS). Chla and total suspended matter (SPM, mg L−1) data were obtained from 1978 onwards, although data for 1980 and 1981 are missing for WS1 and WS6. For station Bath (WS10), data were obtained from 1988 to 1995. In addition, the Netherlands Institute of Ecology, Centre for Estuarine and Marine Ecology (NIOO-CEME) has a water quality monitoring program in the same region with 17 stations from Vlissingen in the mouth of the estuary to station Temse (WS17), which is located upstream of Antwerp in the tidal freshwater region. Eleven stations are located in the Dutch part. For station Bath (WS10), we combined data from the RWS database and the NIOO-CEME database, which is not publicly accessible yet. Sampling frequency varied from 11 to 34 times a year and also varied between stations but was in general biweekly apart from the period 1982–1992 when sampling was monthly. In the years 2002–2004, sampling frequency was reduced to monthly in the winter months.
Light data (PAR, µmol photons m−2 s−1) is measured continuously by the NIOO-CEME since 1994 using a LiCor LI190 2π light sensor connected to a LiCor LI1000 datalogger. Hourly averaged data were logged, and total daily light was computed (mol photons m−2). Total daily irradiance data (from J cm−2 day−1, obtained with a pyranometer) from 1978 to 1994 were obtained from the Royal Netherlands Meteorological Institute from the nearby station Vlissingen. These data were converted to micromole photons per square meter per second by multiplying by a factor 5.5274 (r2 = 0.96) which was based on a comparison of data from 1994 (n = 365).
Phytoplankton biomass is expressed as chlorophyll a (chla, µg L−1) and was extracted in 90% acetone. In 1986, both the NIOO-CEME and RIKZ changed analyses method from spectrophotometry to reverse-phase HPLC. An analysis of NIOO-CEME data of the 1 year of overlapping techniques demonstrated that this did not influence the estimates of annual mean chla concentrations, although individual samples did show some differences (P. Herman, personal communication). A comparison of the time series from the respective stations did not reveal any systematic changes that could be attributed to changes in the chlorophyll methodology. Particularly strong peaks around 1984–1987 occurred in at least two of the three stations. Wavelet transformations (Maximal Overlap Discrete Wavelet Transform) of the respective time series, which can help in identifying strong sudden changes, demonstrated isolated peaks during this period but no consistent changes throughout the stations (data not shown). This is what one would expect from a methodology-induced shift. In addition, a simple variance analysis of yearly weighted average chla data did not reveal significant differences between the periods 1978–1985 and 1986–2005, corroborating the statement that the methodological change did not affect the results. It should be mentioned that the phenological patterns were not affected at all.
Annual average chlorophyll concentrations were calculated using linear interpolation between the sampling dates and were thus weighted. In general, the weighted mean was close to the arithmetic mean as the sampling interval was quite regular.
Changes in the timing of the phytoplankton blooms at stations WS1, WS6, and WS11 were also analyzed with the statistical package R (R Development Core Team 2008) using discrete wavelet coherence analysis on monthly averaged data for the period 1982–2005. A wavelet transformation converts the time representation of a series (measurements as function of time) to a time/scale representation. We used the Maximal Overlap Discrete Wavelet Transformation (MODWT), which essentially gives for each scale a new time series of wavelet coefficients of the same length as the original time series. Each new time series only contains variations at that particular scale. In the case of monthly data, the first wavelet vector will contain all the short-term variations up to 4 months. The second vector groups the 4- to 8-month scales, and the third vector presents the 8- to 16-month scales. The latter also contains the 12-month periodicity (seasonality). The variation is thus filtered and separated into a number of individual scale-specific component signals (scale bands), using so-called wavelet filters. We used the “k3l3” Hilbert wavelet filter pair from the Waveslim package (Whitcher 2007) for R (R Development Core Team 2008). This combination is further referred to as a MODHWT, following Whitcher and Craigmile (2004). This MODHWT gives a complex-valued time/scale representation of time series, containing information on the strength (cfr. modulus of a complex number) and phase (cfr. argument of a complex number), similar to the amplitude and phase of, for example, a sine wave. We refer the interested reader to the specialized literature for more technical details (e.g., Percival and Walden 2000; Selesnick 2001, 2002; Whitcher and Craigmile 2005).
In order to investigate the phenology of the phytoplankton bloom, an average seasonality of the chla concentration was obtained by averaging chla values per month of the year. This average seasonal profile was replicated 24 times to obtain a time series of the same length as the original chla time series. The time-dependent phase difference between the original time series and the replicated annual signal was calculated in a coherence analysis, which is basically a comparison of the MODHWT of the original signal with that of the average seasonal signal. Phenological changes in the chla concentration are detectable as variation in the phase differences between the original time series and the average seasonal chla signal. Two relevant time scales are obtained; the first describes variability in the scale interval of 4–8 months with a periodicity optimum close to 6 months (second wavelet vector), the second encompasses the variability at scales from 8 to 16 months with a periodicity optimum close to 12 months (third wavelet vector). The time-dependent phase differences in both of these scale bands were averaged per year to eliminate the majority of the interdependence between these values. This allowed for the use of simple regression analysis in assessing the secular trend in these phase differences at each of the scales, without further correction for interdependence of observations. Theoretically, the use of average data might make the data sensitive to extreme values. A repeat of the coherence analyses using a median seasonality led to nearly identical seasonal profiles, and there was no difference in significance.
Seasonal Patterns in Chlorophyll a
Interannual Trends in Average Annual Chlorophyll a: Periodicity
Chlorophyll Fulcrum in chla
Statistics of the fulcrum and wavelet analyses on changes in chlorophyll a
From sigmoidal fits
From wavelet analysis
Results Phase Shift Analysis
The differences in phenology between the stations, as mentioned in the previous section, were supported by pairwise coherence (phase) analyses of the WS1, WS6, and WS11 stations. We discuss station WS6 as an example. The result of the other stations can be found in Table 1. The phase difference at the scale of 4 to 8 months showed a significant positive trend (linear regression, T = 3.859, p = 0.001), indicating an initial lag of the original series with respect to its average signal (the phase difference is negative). The slope of this time-dependent phase difference was 0.06 radians. If we used the optimum periodicity (±6 months) of the filter set for this particular scale to convert this phase difference to a time shift, we obtained an average shift of 0.057 (±0.015 SE) months/year or a total shift over the entire measurement period of 1.367 (±0.354 SE) months. Translated to days, this amounted to an advance of 1.71 (±0.45) days/year or 41.0 (±10.6) days between 1982 and 2005 (Table 1). In general, the findings from the phase analyses qualitatively corroborated the results of the fulcrum analyses, except for WS1, which showed a much smaller and no significant change in phenology compared to the fulcrum analysis (Table 1). This was in agreement with the results obtained for the timing of the maximum of the bloom. Quantitative differences were most likely attributable to the fact that the fulcrum analyses focused on a specific point in the distribution, while the phase analyses emphasized an overall temporal shift of the periodic signal in a particular scale band. No specifics were derived concerning the distribution of chla throughout the year from the latter analyses (20%, 50%, and 80% points, cfr. below).
The deviating result for the phase analysis of WS1 compared to the fulcrum analysis had two potential causes (not mutually exclusive). First, the fulcrum analyses used a more precise time localization in the estimation of fulcrum (to the day), while the wavelet-based analysis was performed using monthly averaged chla values because observations need to be equidistant for these wavelet analyses. The fact that the wavelet analysis did not show a significant phase shift can thus in part be due to a loss of time resolution. This was supported by a nonsignificant result from a fulcrum analysis on monthly averaged chla concentrations. Secondly, the fulcrum analysis is more sensitive to increases in the annual maximum concentration. This was tested using an artificially constructed time series, consisting of the average annual profile of the WS1 signal, but with a linearly increasing maximum of the bloom peak similar to that found in the original series. The fulcrum advanced linearly over time with an increasing bloom maximum, which means that, with an increasing bloom maxima, the fulcrum can advance without any real change in phenology. However, the sensitivity for this process was too small to explain the significant advance of the fulcrum for WS1.
Phytoplankton Bloom Initiation, Termination, and Bloom Length
Statistics of the secular trends in bloom initiation (defined as the day when the cumulative chla reached 20% of the total), bloom termination (day at which 80% of the chla is reached), and the length of the bloom
The situation for station WS6 was different. Here, both the time when the bloom started and when it ended occur earlier in the year, and as a result, the length of the bloom did not change and lasted about 100 days, which was significantly shorter than the bloom at station WS1.
Again, station WS11 showed a different pattern. As in the other stations, the initiation of the bloom occurred earlier in the year, but the termination date of the bloom phase did not change significantly (Table 2). As a result, there was a significant increase in the length of the bloom. Thus, the situation at station WS11 was opposite to those in WS1, and station WS6 exhibited an intermediate pattern. Interestingly, the periodicity observed in the annual chla concentrations was also visible in the bloom initiation data. Spectral analyses revealed a clear periodicity with a period of 9.3 years for stations WS1 and WS11 and a periodicity of 7 years for WS6.
Suspended Matter, Secchi Depth, and Temperature
Average, minimum, and maximum nutrient concentrations (µM) for stations WS1 and WS11 for the periods 1978–1980 and 2004–2006
We also looked at differences in incident irradiance (Eo). No significant secular trend was observed in the yearly average irradiance nor in the average irradiance during the spring period (April–May). We also investigated the timing of the maximum in annual irradiance in a fulcrum analysis (data not shown). As might be expected, the fulcrum was very constant and occurred on 23 June ±3 days. The day at which 20% of the cumulative irradiance was reached was only slightly more variable, 21 April ±4 days. A Fourier analysis revealed no clear periodicity in the yearly variations in both the average in April–May or Eo (data not shown).
Interannual Variability in Phytoplankton Biomass
Two main time scales were observed showing variability, one with a period of 12 months and one with a period of about 7 years. Of course, the former one is the time scale describing the spring or summer bloom which clearly showed one single peak each year. A smaller second autumn bloom, often presented in many marine systems, was sometimes observed, and it was often more pronounced in the primary production data (Kromkamp and Peene 1995a). The initiation of the spring bloom was earlier in the marine stations, exemplified by station WS1, where the light conditions were better than in the more turbid inner stations where the spring bloom moved toward a single summer bloom (e.g., WS11). It is hard to explain the individual difference in the magnitude of the bloom. It may be limited by nutrients (not very likely, but it cannot be ruled out for the recent years for station 1), but the fact that there was no overall trend in chla concentrations suggested that nutrient limitation did not play a prominent role. Blooms might also be terminated by grazing, settling/sinking, viral infections, or periods with low solar irradiance, and since no information about most of these factors is available, it is not very fruitful to speculate further.
More interesting is the reason behind the apparent periodic behavior. All stations showed a 7-year periodicity in the average annual chla concentration according to the spectral Fourier analysis. Periodicity was also observed in the onset of the bloom, although the time scales did not exactly match for stations WS1 and WS11 but did match for station WS6, and the climatologies were also approximately synchronous. Large El Niño events were observed in 1982–1983 and 1997–1998, and during these occasions, we observed that the chla climatologies switched from positive to negative, suggesting teleconnections to the atmosphere. The Scheldt estuary is a rain-fed river, and rainfall and river discharge might thus be important drivers for the phytoplankton. As rainfall is influenced by the North Atlantic Oscillation (the pressure difference between Iceland and the Azores), we might expect a relationship between the NAO, rainfall, and river discharge. In 1988, the NAO index increased to the highest values that have been observed thus far this century (Reid et al. 2001), causing large-scale changes in the hydrodynamic regime and a rise in temperature. It is thought to be the driving force behind the observed regime shift in the North Sea (Beaugrand 2004b; Beaugrand and Ibanez 2004; deYoung et al. 2004; Weijerman et al. 2005) and Baltic Sea (Beaugrand 2004b). We calculated the average value of the NAO index for the period 1978–2006 and compared these NAO deviations from the average (climatologies) to the deviations in annual rainfall (measured at station WS1), discharge (measured near station WS11), and the annual chla of station WS1 (Fig. 13). Generally, it appears that when the rainfall is higher than the 1978–2006 average, then the NAO index is smaller than the mean for this period (Fig. 6). This is unexpected because a positive NAO coincides with more rainfall in North Western Europe and more severe dry periods in Southern Europe. Despite the low r2 of 0.15 for the regression analyses, the relationship was significant (ANOVA, p = 0.036). No relationship was found between the NAO and annual river discharge or annual chla. Interestingly, a time series analysis on the average annual data revealed a strong 7-year periodicity for both rainfall and river discharge, the same frequency as was observed for the periodic interannual variation in chla.
Another reason for the observed interannual variability with a quasi 7 year period in chla concentrations might be the variation in light availability, temperature, or nutrient concentrations. However, no significant relationship could be detected with incident irradiance, with the average incident irradiance in April–May (the period of the start of the spring bloom) or with Secchi depth. No periodicity was observed in phosphate concentrations. Also, there was no relationship between the fluctuation in temperature and chla concentrations. Thus, it seems reasonable to suggest that interannual changes in rainfall leading to varying rates of discharge are the drivers behind the 7-year periodic behavior in phytoplankton biomass in the Scheldt estuary.
Shifts in the Timing of Bloom Characteristics
Secular trends were observed in the bloom characteristics. All three stations for which we have a 30-year record in chla concentrations showed that the fulcrum (i.e., the day at which 50% of the cumulative chla distribution was reached) moved forward with time at a rate of 1–2 days/year. These changes were highly significant and thus resulted in a shift in 1 to 2 months during this period! The results were corroborated by the time series analysis which investigated which month the phytoplankton bloom reached its maximum by wavelet analysis. Only station WS1 showed a complex result, and this was mainly due to the higher sensitivity of the fulcrum analysis to higher spring peak concentrations compared to the wavelet coherence analysis.
Further analyses of the bloom dynamics showed a complicated pattern. The onset of the bloom (defined as the day when the cumulative chla concentrations reached 20%) showed the blooms started earlier with approximately 0.5 day/year for station WS1 and nearly 2 days/year for stations WS6 and WS11. The termination of the bloom showed a different pattern. In both stations WS1 and WS6, the bloom terminated earlier at a rate of 1.7–1.9 days/year. Station WS11 showed no significant change in the time of the bloom termination. As a result, the length of the bloom decreased by ~1 day/year for station WS1 (i.e., the sigmoidal rise in cumulative chla became steeper). In station WS6, the bloom started and ended earlier at about the same rate, leaving the bloom length unchanged. Station WS11 again showed a different pattern. Because the bloom started earlier but did not change its termination date, the length of the bloom actually increased by 1.4 days/year. These different patterns in bloom dynamics demonstrate the complex nature of estuarine ecosystems and how difficult it is to predict changes accurately.
How can we explain these secular trends in the timing of the different bloom events? In a turbid eutrophic estuary like the Western Scheldt, two main bottom–up factors can probably explain an earlier initiation of the bloom, an increase in the light climate, or an increase in temperature. The former one would allow the day the critical depth is exceeded to move to an earlier date, whereas the latter one would stimulate the growth rate, although the effect of temperature on light-limited growth rate is very limited (Post et al. 1985). A vertical stabilization of the water column is one way to improve the light climate, but it does not play a role in the well-mixed macro-tidal Western Scheldt estuary. No long-term trends were observed in incident irradiance. With respect to light availability for phytoplankton growth, we conclude that the underwater light climate at station WS1 hardly changed. For station WS11, we observed a significant decrease in SPM, suggesting a decrease in turbidity. However, this was not corroborated by the Secchi disk data. Whether this discrepancy is due to noise or to the fact that there was a significant change in colored dissolved organic matter (CDOM), which does influence Secchi depth but not SPM, remains to be resolved. Our time series of CDOM started in 2004, and hence, it is too short to draw conclusions, although we observed a clear increase during these few years. Therefore, following Sverdrups' critical depth hypothesis (Sverdrup 1953), we would not expect an earlier start of the bloom at stations WS1 and WS6. Other studies also did not reveal an earlier phytoplankton spring bloom, which mainly consists of diatoms (Edwards and Richardson 2004; Wiltshire et al. 2008), and it has been suggested that this might be related to the fact that germination of diatoms resting spores is related to photoperiod length (Eilertsen et al. 1995) and that this might explain the consistency in the timing of the spring bloom observed in other studies. Hence, our results for stations WS1, WS6, and perhaps WS11 clearly did not follow this pattern.
The observed earlier occurrence in the bloom initiation and the fulcrum fit may be linked to global warming. Phenological trends in terrestrial ecosystems have clearly shown an earlier development of plant growth and an increase in the length of the growing season as a result of global warming. We also did observe a significant rise in temperature at both WS1 and WS11 (Fig. 13), suggesting a temperature rise in the whole estuary with a rate of about 0.05–0.07°C/year. This is higher than the 0.043°C found near Helgoland (German Bight, North Sea) for the same period (Wiltshire et al. 2008) or for the western English Channel or the Bay of Biscay in the 1980–2000 period (Hawkins et al. 2003). Increased temperatures might have promoted higher winter phytoplankton stocks, but this was not observed, as the winter concentrations of chla in WS1 or WS6 did not change significantly (data not shown). This was of course not the case for station WS11, which showed an overall decrease in chla concentrations which also exhibited a decrease in winter concentrations due to the regime shift, and is a result of the improved oxygen conditions allowing grazers to enter the upstream part of the estuary (Appeltans et al. 2003). Despite these conditions, an earlier start of the season and an earlier date of the fulcrum were observed as well at this station. Our result deviated from those observed in the coastal North Sea by McQuatters-Gollop et al. (2007), who observed that a combination of sea surface temperature and winter and Secchi depth was the best predictor for the chla concentration and that, as a result, the chla concentrations in both the coastal and open North Sea increased after 1980.
The earlier termination of the bloom observed in WS1 and WS6 can be due to several factors. Nutrient depletion might play a role, but we think this is very unlikely in this eutrophic estuary where nutrients are in excess. Also, if nutrient reduction played a role, it might have reduced the overall productivity of the phytoplankton, but as the average yearly chla concentrations did not change significantly for stations WS1 and WS6, this was unlikely to have played a role. In addition, the phosphate concentrations at station WS1, the most likely station to be limiting, did not decrease after 1995.
In summary, we obtained evidence for a cyclic pattern in the annual mean chla concentrations which we could attribute to varying discharge rates. We observed in all stations that the day at which 50% of the annual cumulative chla was reached occurred earlier in the season. No significant trend was observed in the annual mean chla concentrations for stations WS1 and WS6, but chla concentrations for WS11 decreased due to improved oxygen conditions, allowing important pelagic grazers to have access to the upstream part of the estuary. All stations also showed an earlier initiation of the phytoplankton bloom, although the earlier shift was very limited for station WS1. The phytoplankton bloom also showed an earlier termination of the bloom, apart from station WS11, which did not show a change in the termination date. As a result, the length of the bloom decreased in WS1, remained the same for station WS6, and increased for station WS11. This demonstrates the complex nature of estuarine ecosystem functions. The earlier shifts in time coincided with a rise in temperature, showing an expected change in phenology, i.e., in the timing of the phytoplankton blooms.
We would like to thank the EU-program EUROCEANS for sponsoring JCK's visit to the AGU Chapman conference on long-term time series observations in coastal ecosystems in Rovinj, Croatia, which started this analysis. Thanks are due to Jim Cloern and Alan Jassby for providing us with stimulating ideas. We would also like to thank two anonymous reviewers for their helpful comments. This is NIOO publication 4604.
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