The warming trend at Helgoland Roads, North Sea: phytoplankton response
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We combine the temperature and phytoplankton data from one of the longest aquatic data sets in history, the Helgoland Roads (North Sea, 54°11.3’N, 7°54.0’E) timeseries to evaluate the effects of climate change on the base of marine food webs. The data shows that, despite an obvious warming of 1.1°C since 1962, the mean diatom day of the algal spring bloom is delayed and shifted to the end of the first quarter of the year. This is apparently related to a warming of the autumn (October–December) temperatures. It is the first indication of a warming related shift in phytoplankton succession, the consequences of which would range from lifecycle/food resource mismatches to regime shifts in the North Sea system.
KeywordsDiatoms Spring bloom German Bight Global warming
We have little information on how the warming trends of the last 10–20 years have affected the food webs of aquatic systems (Cushing 1995; Walther et al. 2002). However, knowledge of how climate warming affects phytoplankton, in its important position at the base of the aquatic food chain, is vital. In contrast, the fingerprints of global warming on terrestrial animals and plants have been well documented (Walther et al. 2002; Parmesan and Yohe 2003; Root et al. 2003).
A pole-ward extension of species ranges and earlier and later onset of spring and autumn events, respectively, have been shown for terrestrial systems. Examples include the flowering of trees, leaf-loss, and bird migration and breeding, (Walther et al. 2002; Hüppop and Hüppop 2003; Parmesan and Yohe 2003; Root et al. 2003). There is some evidence for the persistence of warm-water species and changes in the distribution of zooplankton and phytoplankton in aquatic environments (Straile 2000; Walther et al. 2002). In lakes it has been shown that a warming trend has moved the spring diatom bloom forward by up to 1 month (Weyhenmeyer et al. 1999; Weyhenmeyer 2001). Although fundamental to food web considerations, almost no information exists on the relationship between phytoplankton processes and long-term temperature trends in marine systems, and to date none have been documented for the North Sea. In the past it has been difficult to provide conclusive evidence of a warming trend for the North Sea from real-time measurements (Becker and Pauly 1996; Edwards et al. 2001). This has mainly been because the data series used were relatively short, or because the emphasis was laid on large areas with thermoclines interpolated between the measurement points of sea surface temperature and oceanographic division of water masses. However, since 1873 the surface water temperature of the North Sea at Helgoland (54°11.3’N, 7°54.0’E) has been recorded on an almost daily basis and provides an excellent basis for the analysis of long-term trends. In addition, in 1962 a long-term pelagic monitoring program, including plankton species composition, was started at the same location by the Biologische Anstalt Helgoland on a work-daily basis (Biologische Anstalt Helgoland 1873–1962; Hickel et al. 1993). Thus, we combined the unique timeseries data for phytoplankton and temperature in the German Bight to assess the effect of a potential warming on the patterns of phytoplankton occurrence.
Surface water samples were taken (usually before 9 a.m.) on workdays at the Cable buoy site (54°11.3’N, 7°54.0’E) between the two islands at Helgoland using a bucket. The temperature in the sample was measured immediately. This sample was well-mixed and sub-sampled into a glass bottle for future analyses of nutrients and phytoplankton. The phytoplankton samples taken from this were preserved with Lugols’ solution. Using the Utermöhl method and an inverted microscope, 25 ml of samples were counted daily to species level.
Phytoplankton and temperature analyses
Since the timing of the spring bloom is mostly determined using the day of maximum diatom abundance, see e.g. Weyhenmeyer (2001), we first of all evaluated the data to determine a significant maximum. This, however, proved unsupportable as no significant maxima could be calculated. An insignificant positive trend was found. Hence, the maximum diatom day is a poor representation of the actual situation.
We then computed the mean diatom day (MDD) and the mean diatom count (MDC) in a quarter of each year (January–March, April–June, July–September and October–December). The MDD in a quarter of the year was defined as MDD=Σ f i d i /Σ f i , where f i is the diatom count on day d i of the quarter, and the sum is over the available samples in the quarter. The second measure, MDC was the mean of the logarithm to base 10 of the count in a quarter of the year. These two measures of the diatom distribution were used to examine how diatom abundance is related to temperature.
The MDD data were related to temperature of that quarter and all previous quarters through a multiple regression. Non-significant effects at the 5% level were removed from the equation to produce the final fitted model. In most cases, no effects were significant. However, where significant relationships were found then a check was made for autocorrelation in the regression residuals. Where autocorrelation was found, the equation was refitted allowing for this. Similar analyses were carried out with the MDC data. All calculations were carried out in GenStat (Lawes Agricultural Trust 2002).
The yearly minimum, mean and maximum water temperatures (°C) measured are shown as moving averages with standard deviations in Fig. 1. These show a decline in yearly mean temperatures from 1873 to 1893, no change between 1907 and 1985, and an increase from 1985 to 2001. The years 1994, 1995 and 1997 had the three highest monthly maximum temperatures. Very cold winters (monthly minimum temperature of −1°C or less) occurred about every 10 years up to 1944, but only once since 1960.
Relationship between temperature and the parameters MDD and MDC—fitted equations with significant effects. Temp mean temperature in the MDD/MDC quarter; TempB1 value in the previous quarter; TempB2 value in the quarter before that; TempB4 value two quarters before that
Quarter 1 MDD = 17.3 − 2.27 (Temp) + 5.06 (TempB1)
Quarter 1 MDC = 1.67 − 0.098 (Temp) + 0.242 (TempB1)
Quarter 2 MDC = 3.85 + 0.149 (TempB4)
Quarter 3 MDC = 1.21 + 0.251 (Temp)
The temperature increase of 1.13°C for the 40 years since 1962 in the North Sea at Helgoland is substantial. This concrete increase is new information for the North Sea and conclusively demonstrates the warming trend using data from in situ measurements. It updates the first evaluations made on the warming trend in the North Sea by Becker and Pauly (1996). It compares with a rise in average global temperatures of about 0.6°C in the past 100 years (Houghton 2001) and is in line with the warming trends evinced for the measurements in the English Channel (Hawkins et al. 2003), North Sea (Edwards et al. 2002) and North Atlantic (Edwards et al. 2001). The climate anomalies (cold periods) described in the literature for the late 1970s and 1980s are clearly to be seen from the data, although it is also clear that the really cold period was in the early 1960s.
There is a large body of literature relating zooplankton abundances to fish recruitment and how this is affected by climate change in marine systems (Southwood et al. 1988; Conover et al. 1995; Beaugrand et al. 2003; Hawkins et al. 2003; Reid et al. 2003). However, there has been no link between the primary producers and temperature, which, because of their pivotal position at the bottom of the food chain function, is crucial. Although there has been some work on phytoplankton abundances in the North Sea inferred from the secondary data related to colour of samples in the continuous Plankton Recorder Surveys (Edwards et al. 2002), our work for the first time combines algal counts from a marine system with the concurrent temperature measurements.
Our work relates the timing and abundance of the spring bloom of diatoms to temperature. We found that, in the German Bight, the MDD of the spring bloom was shifted backwards in cold quarters when the previous quarter was warm, which in terms of biomass emphasis is a shift towards the end of the first quarter. The diatom abundance was high at the beginning of the year, when temperatures are cold, but the previous quarter was warmer. This may be related to the winter trigger mechanisms, such as mixing/stability, which are required for ending dormancy (Itakura et al. 1997; Lewis et al. 1999). It also may be related to the qualitative information we have for Helgoland and for the North Sea of a longer persistence of zooplankton grazers in autumn and early winter which may depress the crucial biomass-building phase leading up to a phytoplankton bloom, thus delaying the bloom. The shape of the diatom abundance curve seems to have changed in the first quarter, with a lower lift-off and a sharper angle of increase shifting all the emphasis of the biomass in the first quarter to the end of the quarter (Wiltshire et al. in preparation).
In lakes, the spring bloom is delayed in a cold winter by the formation of surface-water ice and, thus, the reduction of light and the comparably cold water temperatures. A warm winter will prevent this process and also cause changes in the mixing regime (Weyhenmeyer et al. 1999; Gerten and Adrian 2001; Weyhenmeyer 2001). Since the formation of sea ice is rare at Helgoland, a delay of the spring bloom caused by temperatures in the first quarter will only occur in very cold winters, of which there has only been one since 1962. The winters of 1985–1987 and 1996 were cold, but not cold enough to cause sea ice or to slow phytoplankton growth or affect the timing of the spring bloom. It is unlikely that this delay could be related to changes in stratification, as has been shown for lakes (Straile 2000; Scheffer et al. 2001), as the North Sea is only about 8 m deep at Helgoland Roads and is generally well mixed. It has been shown that the hydrography of the North Sea has changed (Beare et al. 2002), potentially due to a climate-related increased inflow of Atlantic water into the northern North Sea (Reid et al. 2003). This will also affect the sea around Helgoland. We know from our salinity data that there has been a significant increase in salinity at Helgoland Roads over the last 40 years (0.0077 per year) and that the light penetration has also increased by approximately 1–2 m over this time period. Corroborating this are the observations of the local people at Helgoland, who maintain that the currents at Helgoland and in the German Bight have changed. We are now dealing with clearer, more marine water and warmer conditions, all potentially related to climate changes and the North Atlantic Oscillation (Beare et al. 2002; Edwards et al. 2002; Reid et al. 2003).
Apart from the spring bloom, the timing of diatom occurrences does not generally appear to be related to the temperature at other times of the year. It is interesting that the abundance in the second quarter is strongly related only to the temperature in the same quarter 1 year before, which is perhaps due to the occurrences of the same species in this quarter in each year. The abundance in the third quarter has a simple relationship with the temperature at the same time suggesting that summer temperatures result in a growth of organisms without lags. The abundance in the fourth quarter appears to be unrelated to temperature and it could be expected that zooplankton grazing, for example, has a greater influence on the system.
Work by Edwards et al. (2002) on North Sea phytoplankton abundances inferred from the sample colour in the continuous Plankton Recorder Surveys suggests that the abundance of microalgae is going up in the North Sea. Our data, based on direct counts at Helgoland, does not confirm this. Unlike terrestrial plants, phytoplankton in temperate regions are perhaps the most adaptable of all organisms with regard to temperature shifts. Most of the species found at Helgoland Roads also have a large latitudinal range. It is clear that the temperature increase has not nearly reached the limits of the organisms, but that the trigger mechanisms governing phytoplankton events and seasonality have changed substantially. Studies in the Pacific and Atlantic systems showing climate-induced regime shifts (Lluch-Belda et al. 2001; Ottersen et al. 2001; Chavez et al. 2002; Lavaniegos et al. 2002; Link 2002; Marinovic et al. 2002) and the work by Beaugrand et al. (2003) indicate that we may, with this data, be providing the first evidence for regime shifts in the North Sea at the bottom of the food web.
This demonstration of the link between warming and the shift in MDD of the spring diatom bloom, a process that drives our temperate marine ecosystems, is an invaluable step forward. It starts to close one of the most serious gaps (Walther et al. 2002) in our understanding of climate change impacts at the base of aquatic food webs.
We gratefully acknowledge all those who measured the temperature and counted phytoplankton at Helgoland Roads and who archived their data for further use. In particular, we thank E. Hagmeier, H. Hickel, P. Mangelsdorf, A. Treutner, H. Spindler, S. Janisch and R. Scharek. We thank the crews of R.V. Aade and R.V. Ellenbogen for their dedication to long-term science.
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