Impact of accelerated future global mean sea level rise on hypoxia in the Baltic Sea
Expanding hypoxia is today a major threat for many coastal seas around the world and disentangling its drivers is a large challenge for interdisciplinary research. Using a coupled physical-biogeochemical model we estimate the impact of past and accelerated future global mean sea level rise (GSLR) upon water exchange and oxygen conditions in a semi-enclosed, shallow sea. As a study site, the Baltic Sea was chosen that suffers today from eutrophication and from dead bottom zones due to (1) excessive nutrient loads from land, (2) limited water exchange with the world ocean and (3) perhaps other drivers like global warming. We show from model simulations for the period 1850–2008 that the impacts of past GSLR on the marine ecosystem were relatively small. If we assume for the end of the twenty-first century a GSLR of +0.5 m relative to today’s mean sea level, the impact on the marine ecosystem may still be small. Such a GSLR corresponds approximately to the projected ensemble-mean value reported by the Fifth Assessment Report of the Intergovernmental Panel on Climate Change. However, we conclude that GSLR should be considered in future high-end projections (>+1 m) for the Baltic Sea and other coastal seas with similar hydrographical conditions as in the Baltic because GSLR may lead to reinforced saltwater inflows causing higher salinity and increased vertical stratification compared to present-day conditions. Contrary to intuition, reinforced ventilation of the deep water does not lead to overall improved oxygen conditions but causes instead expanded dead bottom areas accompanied with increased internal phosphorus loads from the sediments and increased risk for cyanobacteria blooms.
KeywordsCoastal seas Baltic Sea Numerical modeling Climate change Global mean sea level rise Marine biogeochemical cycles Hypoxia
However, in all scenario simulations performed so far one effect has not been considered, the global mean sea level rise (GSLR) which may cause an increased flow of saltwater into the Baltic Sea due to increased water depth in the Danish straits (e.g., Gustafsson 2004; Hordoir et al. 2015; Arneborg 2016). According to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC 2013) global mean sea level has risen by about +0.19 m over the period 1901–2010 and is projected to rise further during this century (Church et al. 2013). Depending on the applied global general circulation model (GCM) and representative concentration pathway (RCP) the GSLR for 2081–2100 is projected to be in the range of +0.26 to +0.82 m relative to 1986–2005 (Church et al. 2013). For RCP8.5, the rise by the year 2100 is even in the range of +0.52 to +0.98 m. Semi-empirical model projections of GSLR are even higher (e.g., Pfeffer et al. 2008; Rahmstorf 2007) but whether these semi-empirical projections are physically plausible is a matter of debate. In general, projections of GSLR are very uncertain because the reaction of ice sheets to global warming is poorly known. Nevertheless, GSLR of about one meter at the end of this century might be possible (Church et al. 2013). From paleoclimate studies it is known that due to the interplay between land uplift and GSLR a larger cross section in the Sound (for location see Fig. 1) 6000 years ago caused much higher salinity in the Baltic than today (Gustafsson and Westman 2002). Indeed, there is evidence from sediment cores that in the Baltic Sea during that time and during other periods in the past hypoxia prevailed (Zillén et al. 2008, Zillén and Conley 2010). However, whether the higher salinity was the driver of past hypoxia is unknown.
GSLR may have significant consequences for the Baltic Sea ecosystem because larger salt water flow across the shallow sills in the Danish straits will result in higher salinity in the Baltic Sea (Gustafsson 2004) and in stronger vertical stratification (Meier 2005) affecting vertical nutrient flow. Especially internal phosphorus fluxes between the sediment and the water column are known to be oxygen and hence stratification dependent (e.g., Conley et al. 2009). However, whether the Baltic Sea will be more or less saline in future climate will depend on several competing drivers, like changes in river runoff, changes in wind patterns, GSLR and land uplift. In the northern Baltic land uplift might exceed or in the case of high-end scenarios neutralize GSLR whereas land uplift in the entrance area of the Baltic Sea is negligible on a 100-year time scale (Ekman 1996).
So far GSLR was neglected in both long hindcast and transient scenario simulations of the Baltic Sea because the effect was assumed to be small (e.g., Meier et al. 2006, 2011, 2012). However, the impact of GSLR has never been quantitatively assessed. From other coastal seas like Chesapeake Bay a statistically significant increase of salinity due to past sea level rise was reported (Hilton et al. 2008). In this study, for the first time the potential impact of past and accelerated future GSLR on stratification, phosphorus cycling and eutrophication is investigated using a coupled physical-biogeochemical model for the Baltic Sea (Meier et al. 2003; Eilola et al. 2009). The study is timely because within the BONUS BalticAPP project (http://www.bonusportal.org/projects/research_projects/balticapp) new scenario simulations based upon IPCC (2013) are under development.
We use the three-dimensional coupled physical-biogeochemical model RCO-SCOBI which consists of the physical Rossby Centre Ocean (RCO) model (Meier et al. 2003) and the Swedish Coastal and Ocean Biogeochemical (SCOBI) model (Eilola et al. 2009; Almroth-Rosell et al. 2011). RCO-SCOBI has been previously evaluated and applied for numerous long-term climate studies (e.g., Meier and Kauker 2003; Meier et al. 2003, 2011, 2012).
Within RCO the ocean circulation model is coupled to a Hibler-type sea ice model and the subgrid-scale mixing in the ocean is parameterized using a k-ɛ turbulence closure scheme with flux boundary conditions (Meier et al. 2003). A flux-corrected, monotonicity preserving transport (FCT) scheme is embedded without explicit horizontal diffusion. In the northern Kattegat (Fig. 1) open lateral boundary conditions are used, where in case of inflow temperature and salinity values are nudged towards observed climatological profiles and in case of outflow a modified Orlanski radiation condition is used. Horizontal and vertical resolutions amount to 3.7 km and 3 m, respectively. For further details, the reader is referred to Meier et al. (2003).
SCOBI describes the dynamics of nitrate, ammonium, phosphate, three phytoplankton species, zooplankton, detritus, oxygen and hydrogen sulfide (Eilola et al. 2009). The sediment contains nutrients in the form of benthic nitrogen and benthic phosphorus. Processes like assimilation, remineralization, nitrogen fixation, nitrification, denitrification, grazing, mortality, excretion, sedimentation, resuspension and burial are considered. With the help of a simplified wave model resuspension of organic matter is calculated (Almroth-Rosell et al. 2011). For further details and an evaluation of the SCOBI model the reader is referred to Eilola et al. (2009, 2011) and Almroth-Rosell et al. (2011).
The baseline of this study is a historical simulation for the period 1850–2008 using reconstructed atmospheric, hydrological and nutrient load forcing and daily sea levels at the lateral boundary as described by Gustafsson et al. (2012) and Meier et al. (2012). In the following, a brief summary of the forcing data is provided. Using regionalized reanalysis data for 1957–2007 together with historical station data of daily sea-level pressure and monthly air temperature observations, multivariate daily atmospheric forcing fields were reconstructed based upon the analog-method (Schenk and Zorita 2012). For the calculation of monthly mean river flows three data sets were merged. For 1850–1900, 1901–2004, 2005–2008 reconstructions by Hansson et al. (2011) and by Meier and Kauker (2003) and hydrological model data by Graham (1999) were used, respectively. For 1970–2006, nutrient loads from rivers and point sources were compiled from the Baltic Environmental and HELCOM databases (Savchuk et al. 2012). Estimates of pre-industrial loads for 1900 are based upon Savchuk et al. (2008). Between these two environmental states nutrient loads were linearly interpolated between selected reference years taking the intensified agriculture since the 1950s into account. Similarly, atmospheric loads were estimated (Ruoho-Airola et al. 2012). Nutrient loads contain both organic and inorganic phosphorus and nitrogen, respectively. Sea level elevations at the lateral boundary were calculated from the reconstructed, meridional sea level pressure gradient across the North Sea following Gustafsson and Andersson (2001). To avoid the underestimation of extremes the correlations were calculated for various frequency bands using Empirical Orthogonal Functions (EOFs) (Gustafsson et al. 2012). Finally, initial conditions were estimated based upon Savchuk et al. (2008). After a spin-up simulation for 1850–1902 utilizing the reconstructed forcing as described above, the calculated physical and biogeochemical variables at the end of the spin-up simulation were used as initial condition for 1850.
As we anticipate a long response time scale of the phosphorus cycle to GSLR (e.g., Gustafsson et al. 2012; Radtke et al. 2012), we chose a 159-year long simulation as reference (henceforth referred to as REF). In addition to REF, sensitivity experiments were carried out with the same setup as in REF but with externally prescribed, time-independent sea level anomalies relative to present-day, mean sea surface height (SSH). For the simulated distribution of SSH the reader is referred to Meier et al. (2003). Technically the water depth in the entire model domain was increased or decreased depending on the change in global mean sea level and the thickness of the uppermost model layer was modified accordingly. Hence, in the sensitivity experiments only the mean sea level was altered whereas the temporal variability on all time scales remained unchanged compared to REF.
Past eustatic sea level rise in the Baltic Sea was estimated to be 1.5 ± 0.53 mm year−1 (Gornitz 1995) or about 0.24 m during 1850–2008. Hence, we investigate in a sensitivity experiment how biogeochemical cycling might have developed without the impact of past sea level rise assuming a 0.24 m lower sea level than today (henceforth referred to as PAST).
Further, we study how the projected future ensemble-mean sea level rise of about +0.5 m and a high-end scenario of about +1 m compared to present-day sea level (Church et al. 2013) may affect biogeochemical cycling assuming nutrient loads and eutrophication status of the twentieth century. Henceforth, these sensitivity experiments mirroring perhaps sea level conditions at the end of the twenty-first century are referred to as S50 (+0.5 m) and S100 (+1.0 m), respectively. In our sensitivity studies other possible changes of future climate like warming, increasing runoff and acidification are neglected.
Changes in sea surface and bottom salinities at Gotland Deep (ΔSSS and ΔBS in g kg−1), volume averaged salinity of the entire Baltic Sea (ΔSave in both g kg−1 and % of the mean salinity averaged for the entire Baltic Sea of 7.4 g kg−1), annual maximum hypoxic area (ΔHA in %) and volume averaged dissolved inorganic phosphate concentrations (ΔDIP in %) in the sensitivity experiments, PAST, S50 and S100, with specified sea surface height anomalies (ΔSSH in m)
ΔSSS (g kg−1)
ΔBS (g kg−1)
ΔSave (g kg−1)
Applying a 0.5 m higher sea level (S50) causes surface and bottom salinities at Gotland Deep to increase by about 0.7 and 0.9 g kg−1 compared to REF, respectively (Table 1; Fig. 2), due to increased salt inflows. The corresponding salinity increase averaged for the entire Baltic Sea amounts to 0.7 g kg−1 or 10 %. Surface salinity changes are somewhat smaller than bottom salinity changes indicating an increase in stratification. The e-folding time scale of surface salinity changes at Gotland Deep as response to changes in saltwater inflows amounts to about 21 years (Fig. 2). This finding confirms earlier results of sensitivity experiments by Meier (2005) who investigated salinity changes as a consequence of increased salt water transports into the Baltic Sea by increasing the amplitude of sea level variations at the lateral boundary in Kattegat. However, for the temporal evolution of bottom salinity, in particular during the first years of the simulation, an e-function is not a good approximation indicating that non-diffusive processes like advection are important as well. After about 60 years a new quasi steady-state will be reached (Fig. 2). Hence, the relevant time scale for the salinity response to GSLR is relatively large as we anticipated.
Applying a 1 m higher sea level (S100) causes surface and bottom salinities at Gotland Deep to increase by about 1.3 and 1.8 g kg−1 compared to REF, respectively (Table 1; Fig. 2). The corresponding increase in mean salinity averaged for the Baltic Sea including Kattegat amounts to 1.4 g kg−1 or 19 %. Our results support earlier findings by Gustafsson (2004) who used a process-oriented model to study salinity in the Baltic Sea as function of freshwater supply and mean sea level change. Gustafsson (2004) found that a GSLR of +1 m would lead to a sea surface salinity increase of 1 g kg−1 in the southern Baltic proper.
According to Table 1, the relationship between salinity and sea level change is approximately linear, indicating that changes in salt transports through the Danish straits alter with the changes in cross section.
Although MBIs usually consist of oxygen-rich winter water (Matthäus and Franck 1992), we found in S50 and S100 only small increases of the mean (median) bottom oxygen concentration at Gotland Deep averaged for the entire period 1850–2008 of about 0.07 (0.06) and 0.08 (0.04) mL L−1, respectively (Fig. 3b, c). In S50 oxygen anomalies at the bottom of Gotland Deep amount to up to 2.8 mL L−1. Most of the additional oxygen in inflowing water pulses is lost either on the way into the Baltic interior due to diffusion (mixing with oxygen-poor surrounding water) or in the deep water due to oxygen consumption by organic matter degradation and oxidation of earlier reduced compounds (Fig. 3b, c). In agreement with observations (Feistel et al. 2008) the time scale of oxygen depletion at Gotland Deep after an MBI amounts to about 18 months on average under present eutrophication conditions (at least until the 1990s). Hence, in the deep water at Gotland Deep the effect of a 1 m higher global mean sea level as shown in S100 on oxygen renewal is relatively small on average. Nonetheless, in S50 and S100 mean and median changes in bottom oxygen concentrations are significantly positive whereas in PAST these changes are significantly negative (Fig. 3c). The relative frequency distributions of bottom oxygen concentration changes in S50 and S100 show larger positive extremes compared to PAST.
As under anoxic conditions internal phosphorus fluxes from the sediments increase (e.g., Eilola et al. 2009), in S50 and S100 the volume integrated dissolved inorganic phosphorus (DIP) contents in the water column of the entire Baltic Sea increase during 1988–2007 relative to REF by about 5 and 9 %, respectively (Table 1; Fig. 5). In the sediments of the shallow Baltic Sea, organic phosphorus is transformed to inorganic phosphorus and on long time scales phosphorus is even removed from the biogeochemical cycling in the water column (Eilola et al. 2009). It is proposed that a fraction of the deposited organic phosphorus is transformed to mineral bound inorganic phosphorus (e.g., Almroth-Rosell et al. 2015). Phosphorus can be released from the sediment pool to the overlaying water or become adsorbed from the water into the sediment depending on the oxygen concentrations. In case of anoxic conditions, phosphorus is released from the sediments and under oxic conditions the flux is reversed. For details of the relevant sediment chemistry, the reader is referred to Almroth-Rosell et al. (2015). In the SCOBI version of the present study, a salinity and oxygen dependent parameterization of the phosphorus release capacity is used to calculate the sediment–water fluxes (Eilola et al. 2009).
The increased phosphate concentration in the euphotic zone results in increased primary production (not shown). In addition, the risk for the occurrence of nitrogen-fixing cyanobacteria blooms during summer might increase enhancing the so-called “vicious” cycle that amplifies eutrophication in the Baltic Sea (Vahtera et al. 2007; Conley et al. 2009). Our findings are qualitatively similar to simulation results with a dredged Sound using two different coupled physical-biogeochemical models (Gustafsson et al. 2008).
4.1 Shortcoming of the experimental set-up
In this study, three sensitivity simulations are analyzed to investigate the impact of (1) past GSLR, (2) an ensemble-average scenario for GSLR of +0.5 m, and (3) a high-end scenario for GSLR of +1 m on biogeochemical cycling assuming present eutrophication conditions. We cover with our experiments the whole range of future sea level evolutions until 2100 as projected by Church et al. (2013). However, the simulations are idealized sensitivity experiments with added time-independent sea level anomalies instead of transient simulations with continuously rising sea level. Although our idealized experiments are neither plausible scenario simulations for future climate nor realistic reconstructions of past climate, respectively, they have the advantage that we were able to study steady-state conditions and response time scales without overlying long-term trends.
4.2 Model shortcomings
Model response to changing GSLR is assumed to be realistic because RCO-SCOBI was earlier thoroughly evaluated. For instance, the evolution of salinity and the frequency of MBIs in REF were evaluated by Schimanke and Meier (2016) who found that the model gives reasonably good results compared to observations although the atmospheric and hydrological forcing fields are only reconstructed (Gustafsson et al. 2012). However, salinity of the deep water at Gotland Deep is somewhat lower than in observations.
Also the evolution of oxygen is well simulated (Fig. 3a) but modeled oxygen concentrations in the Gotland Deep water during the 1960s are somewhat too high. This seems to be a common problem among historical simulations driven by reconstructed forcing (Meier et al. 2012) indicating either a general problem of biogeochemical models under oligotrophic conditions or unrealistically high nutrient loads during the 1950s and 1960s in the reconstruction.
Simulated and from observations derived hypoxic and anoxic areas have been analyzed by Väli et al. (2013). They found only small model biases when they applied the same methodology for their calculations as was applied for observations.
Finally, volume and salt water flows through the Danish straits as function of sea level changes have previously been evaluated by Meier et al. (2003). They found that the volume transports through one of the connecting straits, the Sound (Fig. 1), are very well simulated compared to volume transports calculated from ADCP measurements during 1992 and 1993 indicating that in RCO the flow resistance to sea level changes is well calibrated (Meier et al. 2003). As also volume changes in the Baltic Sea are realistically simulated (compared to observations from tide gauges, e.g. at Landsort station), the volume flows through the second connecting strait, the Great Belt, where the calculation of transports from ADCP measurements is more difficult due to the more complicated topography, are consequently simulated realistically as well. For the MBI in 1993 Meier et al. (2003) showed that simulated volume and salt transports through each of the connecting straits are within the error bar of corresponding figures estimated from available observations during that period.
Nevertheless, the simulated response to GSLR might be biased due to model deficiencies. In particular, changes in halocline depth and halocline strength are simulated differently in different models (Meier et al. 2011). Further, sediment–water fluxes of nutrients are not well known (Eilola et al. 2011). Hence, we propose to investigate sediment–water fluxes of phosphorus in more detail to reduce uncertainty of simulated changes in phosphorus cycling. For this purpose, Almroth-Rosell et al. (2015) recently developed a new sediment module that takes oxygen penetration depths (OPDs) and inorganic phosphorus pools within the vertically integrated sediment model into account. Although the new sediment module may improve the simulated sediment–water fluxes, more research is still needed.
4.3 Other drivers of hypoxia
According to Schrum et al. (2016) GSLR is approximately representative for the North Sea region because around 70 % of the world’s coastline is located in an area with a projected sea level rise that falls within a 20 % range of the GSLR (Church et al. 2013). Further, it was concluded that future changes in wind speed and storm surge height over the North Sea are either statistically insignificant or relatively small (e.g., Christensen et al. 2015; Meier 2015; Schrum et al. 2016). There is also no evidence of significant trends in annual wind statistics since the nineteenth century (Rutgersson et al. 2015). These findings support our assumptions that GSLR may be applied together with unchanged sea level variations at the northern boundary in Kattegat.
However, a northeastward shift in storm tracks and an increase in the deep lows over Scandinavia were found (e.g. Lehmann et al. 2011; Feser et al. 2014; Rutgersson et al. 2015). If these atmospheric changes in extreme conditions persist in the future, this may be an additional factor potentially affecting MBIs and consequently hypoxia. Although Schimanke et al. (2014) concluded that atmospheric variability favorable for MBIs may intensify in future climate, there is nevertheless no strong evidence from available scenario simulations (which do not take GSLR into account) that intensity or frequency of saltwater inflows may change significantly (Meier 2015). Therefore, in future climate GSLR and changes in river runoff to the Baltic Sea, as suggested by Meier et al. (2006), might be the two dominating and competing drivers of the water exchange between North Sea and Baltic Sea. However, the role of GSLR for the future water exchange is still unclear because of the large uncertainty of projected GSLR. In addition, changes in frequency and intensity of small and medium inflows and MBIs cannot be ruled out.
Eilola et al. (2014) showed with the help of tracer experiments that the overall direct impact of MBIs on the annual uplift of nutrients from below the halocline to the surface waters is small because vertical transports are comparably large also during periods without MBIs. Further, they suggested that phosphorus released from the sediments between 60 and 100 m depth in the eastern Gotland Basin may contribute to eutrophication. These results support our findings that the direct impact of GSLR like increased frequency and intensity of MBIs on the phosphorus cycling is small. Instead, a shallower halocline and extended hypoxic areas due to GSLR are the important factors that affect the reduced phosphorus retention in the sediments.
We propose to perform new multi-model ensemble scenario simulations for the Baltic Sea taking GSLR and also new, improved regional and global models, and the latest greenhouse gas emission (RCPs) and nutrient load scenarios into account. Further, new evaluation data sets and more realistic initial conditions may help to improve scenario simulations.
Our model simulations suggest that GSLR will cause increases in (1) frequency and magnitude of saltwater inflows, (2) salinity and (3) phosphate concentrations in the Baltic Sea as a direct or indirect consequence of increased cross sections in the Danish straits, and will contribute to (4) increased hypoxia and anoxia amplifying the previously reported future impacts of increased external nutrient loads due to increased runoff, reduced oxygen flux from the atmosphere to the ocean and intensified internal nutrient cycling due to increased water temperatures in future climate (Meier et al. 2011). Although GSLR will cause more intense inflows of high-saline, oxygen-rich water, hypoxic bottom areas will increase because of increased stratification. However, the impact of historical GSLR since 1850 on hypoxic area and mean DIP concentrations was small and long-term changes in both variables were mainly governed by changes in anthropogenic nutrient loads. Also future GSLR will very likely have only a small effect on biogeochemical cycles when a projected ensemble-mean GSLR of about +0.5 m until the end of the twenty-first century and present-day eutrophication status is assumed. However, applying a high-end scenario with a GSLR of +1 m will result in an increase in mean salinity of about 19 % and in increased hypoxic bottom area of about 43 % in maximum. Hence, GSLR should be considered as potential driver in climate change scenario simulations for the Baltic Sea and other coastal seas with similar hydrographical conditions.
The research presented in this study is part of the Baltic Earth program (Earth System Science for the Baltic Sea region, see http://www.baltic.earth) and was funded by the Swedish Research Council for Environment, Agricultural Sciences and Spatial Planning (FORMAS) within the project “Impact of accelerated future global mean sea level rise on the phosphorus cycle in the Baltic Sea” (Grant No. 214-2009-577), by the Stockholm University’s Strategic Marine Environmental Research Funds “Baltic Ecosystem Adaptive Management (BEAM)”, and by the Swedish Research Council (VR) within the project “Reconstruction and projecting Baltic Sea climate variability 1850–2100” (Grant No. 2012-2117). Additional financial support from the Danish Agency for Science, Technology and Innovation (# 09-067259/DSF) is acknowledged. We thank three anonymous reviewers for their comments that helped to improve the manuscript.
- Bergström S, Carlsson B (1994) River runoff to the Baltic Sea: 1950–1990. Ambio 23:280–287Google Scholar
- Christensen OB, Kjellström E, Zorita E (2015) Projected change: atmosphere. In: BACC II author team, second assessment of climate change for the Baltic Sea Basin. Reg Clim Stud Springer Berlin Chapter 11, pp 217–233Google Scholar
- Church JA, Clark PU, Cazenave A, Gregory JM, Jevrejeva S, Levermann A, Merrifield MA, Milne GA, Nerem RS, Nunn PD, Payne AJ, Pfeffer WT, Stammer D, Unnikrishnan AS (2013) Sea level change. In: IPCC, climate change 2013: the physical science basis, working group I contribution to the fifth assessment report (AR5). Intergovernmental panel on climate change, chapter 13, pp 1137–1216Google Scholar
- Eilola K (1998) Oceanographic studies of the dynamics of freshwater, oxygen and nutrients in the Baltic Sea. Ph.D. thesis A30, Dept of Oceanography, Göteborg University, Sweden, pp 1–22Google Scholar
- Feistel R, Nausch G, Wasmund N (eds) (2008) State and evolution of the Baltic Sea, 1952–2005. A detailed 50-year survey of meteorology and climate, physics, chemistry, biology, and marine environment. Wiley, HobokenGoogle Scholar
- Graham LP (1999) Modeling runoff to the Baltic Sea. Ambio 27:328–334Google Scholar
- Gustafsson BG, Westman P (2002) On the causes for salinity variations in the Baltic Sea during the last 8500 years. Paleoceanography 17:12-2–12-14. doi: 10.1029/2000PA000572
- Gustafsson BG, Meier HEM, Savchuk OP, Eilola K, Axell L, Almroth E (2008) Simulation of some engineering measures aiming at reducing effects from eutrophication of the Baltic Sea. Report Series C82, Earth Sciences Centre, Göteborg University, SwedenGoogle Scholar
- IPCC (2013) Climate change 2013: the physical science basis, working group I contribution to the fifth assessment report (AR5). Intergovernmental panel on climate change. http://www.ipcc.ch
- Matthäus W, Dietwart N, Feistel R, Nausch G, Mohrholz V, Lass H-U (2008) The inflow of highly saline water into the Baltic Sea. In: Feistel R, Nausch G, Wasmund N (eds) State and evolution of the Baltic Sea 1952–2005. Wiley, HobokenGoogle Scholar
- Meier HEM (2015) Projected change: marine physics. In: BACC II author team, second assessment of climate change for the Baltic Sea Basin. Reg Clim Stud Springer Berlin Chapter 13, pp 243–252Google Scholar
- Meier HEM, Andersson HC, Arheimer B, Blenckner T, Chubarenko B, Donnelly C, Eilola K, Gustafsson BG, Hansson A, Havenhand J, Höglund A, Kuznetsov I, MacKenzie B, Müller-Karulis B, Neumann T, Niiranen S, Piwowarczyk J, Raudsepp U, Reckermann M, Ruoho-Airola T, Savchuk OP, Schenk F, Weslawski JM, Zorita E (2012) Comparing reconstructed past variations and future projections of the Baltic Sea ecosystem—first results from multi-model ensemble simulations. Environ Res Lett 7:034005. doi: 10.1088/1748-9326/7/3/034005 CrossRefGoogle Scholar
- Quante M, Colijn F (eds) (2016) North Sea region climate change assessment. Springer, Berlin (in press)Google Scholar
- Rutgersson A, Jaagus J, Schenk F, Stendel M, Bärring L, Briede A, Claremar B, Hanssen-Bauer I, Holopainen J, Moberg A, Nordli Ø, Rimkus E and Wibig J (2015) Recent change: atmosphere. In: BACC II author team, second assessment of climate change for the Baltic Sea Basin. Reg Clim Stud Springer Berlin Chapter 4, pp 69–98Google Scholar
- Savchuk OP, Gustafsson BG, Rodriguez-Medina M, Sokolov AV, Wulff FV (2012) Nutrient loads to the Baltic Sea 1970–2006, Baltic Nest Institute technical report no. 5, StockholmGoogle Scholar
- Schrum C, Lowe J, Meier HEM (2016) Projected change: North Sea. In: Quante M, Colijn F (eds) North Sea region climate change assessment. Springer, BerlinGoogle Scholar
- Sonnenborg TO (2015) Projected change: hydrology. In: BACC II author team, second assessment of climate change for the Baltic Sea Basin. Reg Clim Stud Springer Berlin Chapter 12, pp 235–241Google Scholar
- Vahtera E, Conley DJ, Gustafsson BG, Kuosa H, Pitkänen H, Savchuk OP, Tamminen T, Viitasalo M, Voss M, Wasmund N, Wulff F (2007) Internal ecosystem feedbacks enhance nitrogen-fixing cyanobacteria blooms and complicate management in the Baltic Sea. Ambio 36:186–194. doi: 10.1579/0044-7447 CrossRefGoogle Scholar
Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.