Baltic Sea Environment Fact Sheet 2017, Published on 16 April 2018
Author: Lena Viktorsson, Swedish Meteorological and Hydrological Institute
The Baltic Sea is a sensitive sea area. The region is characterised by its natural formation as an enclosed estuary with high freshwater input and restricted access to oceanic high saline water. The stratification and fjord-like conditions, in combination with eutrophication and other factors, form the basis for a problematic oxygen situation in the deep water.
Anoxic conditions are characterised by the total absence of oxygen. When all oxygen is consumed by microbial processes hydrogen sulphide (H2S) is formed, which is toxic for all higher marine life. Anoxic conditions lead to release of phosphate and silicate from the sediments to the water column, which, through vertical mixing, can reach the surface layer and the photic zone. A surplus of phosphate in relation to nitrate favour cyanobacteria growth in the Baltic Sea during summer.
This fact sheet gives an overview of the development of salinity since 1990 to 2017 and oxygen from 1960 to 2017 and describes recent changes in these variables. The most notable changes since the major Baltic inflow in 2014 are:
Salinity, temperature and oxygen are physical background parameters, constraining biodiversity, fish recruitment and water quality in a semi-enclosed water body as the Baltic Sea.
Surface waters in the Baltic are strongly influenced by land run-off of freshwater. Changes in run-off alter the surface salinity while inflows through the Sound and the Belt Sea control the salinity of the deeper waters. Stratification between the upper and lower layers inhibits surface and deep waters mixing together, and thus preventing the oxygenated surface water penetrating to deep water. The strength of the stratification is indicated by the salinity difference between the surface and deep water.
Oxygen depletion is widely used as an indicator of the indirect effects of nutrient enrichment due to increased oxygen consumption. Lowest oxygen levels are experienced at the end of summer, between August and October, when detritus from biological activity in the surface waters has sank, and is decomposed by bacteria. This process consumes the oxygen. When oxygen is depleted bacteria start to use anaerobic processes for degradation of organic matter, producing toxic hydrogen sulphide. Oxygen levels above 4.6 mg/l (3.2 ml/l) are considered to cause no problems for most macroscopic animals and this limit could be considered as a precautionary limit to avoid catastrophic mortality events (Vaquer-Sunyer and Duarte (2008)).
Oxygen levels are used as an indicator of eutrophication by both HELCOM and OSPAR. It is listed as a core variable of the HELCOM COMBINE programme. Oxygen is delivered to the deep waters of the Baltic in the saline inflows that come through the Sound and Belt Sea. Hydrographic measurements (temperature and salinity) allow us to trace these inflows, and other water movements within the Baltic.
Time series of winter surface salinity between 1990 and 2017 (Figure 1)
show stable winter average (Dec-Feb) salinities in the surface waters (0-10 m)
of the Baltic Proper. Surface winter salinity (Figure 1) has remained fairly
constant in the southern Baltic Proper since 1990, around 8 psu in the Arkona and
Bornholm basins to around 7 psu in Eastern, Northern and Western Gotland basins
of the Baltic Proper. In the Eastern Gotland Basin the surface salinity decreased
between 2011 and 2014, but has risen again during the past three years and is
currently close to 8 psu. In the Bothnian Sea salinity in the surface water has
decreased by about 0.5 psu since 1990. Deep water salinity has increased in the
Eastern, Northern and Western Gotland basins of the Baltic Proper reaching new
peaks after every inflow since 1990. At present it is close to 14 psu in the
bottom water of the Eastern Gotland Basin. The effect of the winter 2002-2003
inflow is visible in the deep water salinity data from Arkona and Bornholm that
same winter. But it was not seen in the winter-averaged data from the Eastern
Gotland Deep until the following winter, 2003-2004. Smaller salinity increases after
this inflow can also be tracked in the Northern and Western Baltic Proper but
are not very clear in the winter averaged data. After the inflow in the winter
2002-2003 the deep water salinity in the Baltic Proper slowly decreases until
the next large inflow in the winter 2014-2015. This inflow is one of the
largest inflows recorded and is well described in Naumann et al. (2018), as well as a
series of smaller inflows 2014-2016. The 2014 inflow is seen in as a small
increase in winter mean salinity already in the winter 2014-2015 but it is not
until the following winter (2015-2016) the increase in salinity is clear. The
difference between surface and deep water salinity, in the main part of the
Baltic Proper, is much greater than at the start of the 1990s, and this will
hinder vertical mixing.
Figure 1. Surface (orange) and
deep water (blue) salinity from 1990 to 2017 at selected monitoring stations in
the HELCOM marine area. Depth for surface water is
0-10 m at all stations, deep water values are calculated from a mean of all
values at and below the depths specified in the title of each plot.
Figure 2. Map
showing the HELCOM marine area and the basins and stations in them that are
used in this fact sheet. In Figure 1 the southernmost station (BSC-III-10) in
the Eastern Gotland Basin is presented as South-Eastern Baltic Proper while the
northernmost station (BY15 Gotland deep) is representing the Eastern Gotland
For each of
the basin in Figure 2 oxygen profiles from 1960 – 2016 were examined using data
from the autumn months (August, September and October). The profiles were
interpolated to 1 m depth resolution and the depths at which the oxygen
concentration fell below 4 ml/l, 2 ml/l (hypoxia) and 0 ml/l (anoxia) were
selected. The volume of each depth was calculated using data from the Baltic
Sea Bathymetry Data Base (Baltic Sea
Hydrographic Commission, 2013) and an estimate of the volume of water below each oxygen limit could
thereby be calculated. This method takes into account oxic waters that remain
below layers of anoxic waters after inflow events. The values were interpreted
in terms of the proportion of the volume of each basin affected by reduced
oxygen levels. Results are presented as time series in Figure 3. The figure for
each basin is based on oxygen profiles from the deepest monitoring station in
that basin. The positions of the basins are shown on the map in Figure 2.
Figure 3. Autumn oxygen conditions as
a percentage of the total volume of the basins. Grey areas in the panels mark
periods with either no data available or too little data to make a reliable
evaluation of the situation. Volume percentages below 0, 2 and 4 ml/l are shown
in red, orange and yellow colours respectively.
Kattegat very rarely experience anoxia but has oxygen concentrations below 4
ml/l in between 30-40% of its volume more or less every year in the autumn
which is what is presented here. In the Arkona Basin anoxia is a sparse
phenomenon, while in the Bornholm Basin it is a more seasonal feature occurring
almost every year. The volume affected by anoxia has decreased to only a few
percent after the inflow 2004. The Northern Baltic Proper as well as the
Eastern and Western Gotland basins are the basins most affected by anoxia. The
Western Gotland basin shows the largest percentages of its volume with anoxia. Here
the volume of anoxic waters steadily increased after the inflow 1994 and has
been fairly constant around 30% since the beginning of 2000. Despite this the severity
of anoxia is in a way lower in the Western Gotland basin than in the Eastern
Gotland Basin. Hydrogen sulphide concentrations are lower in the southern part
of the Western Gotland basin and oxygen conditions varies over the year,
tending to show a seasonal cycle with the highest sulphide concentrations
during the autumn and the lowest at the end of the winter season. At some
occasions oxygen has been measured in the whole water column even during the 21st
century. Note that the conditions differ notably between the northern parts of
this basin and the southern parts with less variable oxygen conditions in the
northern part compared to the southern. The Northern Baltic Proper rarely
experienced large volumes of anoxic water until the beginning of the 21st
century. However oxygen conditions were still severe being well below 2 ml/l in
a large part of the basin. After year 2000 the anoxic volume in the Northern
Baltic Proper lays around 20% of the basins total volume until the effects of
the inflow 2014 are seen in 2016. The offshore Gulf of Bothnia, including the
Åland Sea does not suffer from low oxygen levels. The data coverage for the
Gulf of Finland is poor in the 1990’s in this dataset. The Bothnian Bay and
Bothnian Sea are not included in figure 3 since they do not show any oxygen
deficiency. However, there are indications that the oxygen conditions in the
Bothnian Sea may also be declining (Ahlgren et al., 2017).
of the areal extent of hypoxia was produced by using gridded linear
interpolation of a larger dataset and shows the area of bottoms affected by
anoxia in 2017 in Figure 4. For a more detailed description of the dataset and
method see Hansson et al 2018. The map shows that the Western Gotland Basin and
the Northern Baltic Proper still suffer from a large areal extent of anoxia.
The southern parts of the Eastern Gotland Basin remains oxygenated after the
2014 inflow, although with oxygen concentrations <2ml/l. Hydrogen sulphide
was removed in large parts of the Eastern Gotland basin after the inflow 2014 but
are now slowly building up again. In the map (Figure 4) this means that the
central part of the Eastern Gotland Basin is still coloured black indicating
Figure 4 shows the regional distribution of the bottom
areas where oxygen concentrations are below the critical level of 2 ml/l. The
spatial change over time follows the changes discussed above.
The surface water layer is defined as the average of 0-10 m and the bottom water is defined so it includes the deepest measurements at each station and is the depths used for each basin are given in Figure 2 above. The winter is defined as December, January and February with December data from the year previous to January and February. The winter data is presented as belonging to the year of January and February.
Data for each station was selected by including all profiles within a 0.1 degree radius from the positions given in the map in Figure 2.
This study has made use of the official HELCOM COMBINE-programme dataset. Data is from the HELCOM data archive held at the International Council for the Exploration of the Sea (http://www.ices.dk). Data to ICES is normally reported by contracting parties on annual basis and all data for 2016 will therefore not be available until the upcoming year.
The map in Figure 2 and its basins are drawn from the shapefile "HELCOM subbasins with coastal and offshore division 2018" downloaded from the HELCOM map service, http://maps.helcom.fi/website/mapservice/. With exception of the Northern Baltic Proper and the Western Gotland Basin where the older version of the basin divisions are used so that the deep station BY31 can be used for the Northern Baltic Proper.
To calculate the volume of anoxic water in each basin, hypsographs were created from the Baltic Sea Bathymetry Database 500 m gridded bathymetry together with the HELCOM shapefile using the offshore basins shown in Figure 2.
Data collected for the HELCOM COMBINE programme is collected and analysed according to agreed methods (COMBINE Manual). Laboratories participate in quality assurance consortia such as QUASIMEME and are almost uniformly ISO accredited for good laboratory practice.
Ahlgren J., Grimvall A., Omstedt A., Rolff C. and Wikner J. (2017). Temperature, DOC level and basin interactions explain the declining oxygen concentrations in the Bothnian Sea. Journal of Marine Systems. 170. . 10.1016/j.jmarsys.2016.12.010.
Baltic Sea Hydrographic Commission. (2013). Baltic Sea Bathymetry Database version 0.9.3. Downloaded from http://data.bshc.pro/
Hansson M., Viktorsson L., Andersson L. (2018). Oxygen Survey in the Baltic Sea 2017 - Extent of Anoxia and Hypoxia, 1960-2017. SMHI Report Oceanography no. 63.
Michael Naumann, Volker Mohrholz and Joanna J. Waniek. (2018). WATER EXCHANGE AND CONDITIONS IN THE DEEP BASINS. HELCOM Baltic Sea Environment Fact Sheets. Online. 8 February 2018, http://www.helcom.fi/baltic-sea-trends/environment-fact-sheets/.
Vaquer-Sunyer, R. and Duarte, C. M. (2008). Thresholds of hypoxia for marine biodiversity, P. Natl. Acad. Sci. USA, 105, 15452–1545.
For reference purposes, please cite this Baltic Sea environment fact sheet as follows:
[Author's name(s)], [Year]. [Baltic Sea environment fact sheet title]. HELCOM Baltic Sea Environment Fact Sheets. Online. [Date Viewed], http://www.helcom.fi/baltic-sea-trends/environment-fact-sheets/.
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