Validation of HIROMB during 1995-96

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'

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SMHI

OCEANOGRAFI

Nr 67, 1997

Validation of HIROMB <luring

1995-96

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SMHI

OCEANOGRAFI

Nr 67, 1997

.•. --·. . -

-Validation of HIROMB <luring

1995-96

Lennart Funkquist and Patrik Ljungemyr

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Table of contents

Abstract

Introduction ... 1

Mod el configuration and forcing ... 1

V alidation ... 2

Closely related validation exercises ... 7

Conclusions ... 8

Recornrnendations ... 9

References ... 10 Figures 1-26

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Abstract

HIROMB (High Resolution Operational Mode! of the Baltic Sea) is the result of a combined effort between BSH (Bundesamt för Seeschiffahrt und Hydrographie) and SMHI (Swedish Meteorological and Hydrological Institute) aiming at a common operational model for the North Sea/Baltic Sea region. The present resolution is 3 nautical miles in the horizontal and 24 levels in the vertical and will increase with available computer capacity.

This report presents results from a continous verification exercise, where model results are compared to observations of water level, surface temperature, ice thickness and salinity and temperature profiles. The times series data are taken from the period September-November 1996 while the ice thickness data are from November and December 1996 and the sea surface temperature data are taken from August, November and December 1996.

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lntroduction

HIROMB (High Resolution Operational Model of the Baltic Sea) is the result of a combined effort between BSH (Bundesamt för Seeschiffahrt und Hydrographie) and

SMHI (Swedish Meteorological and Hydrological Institute). In its present form, the

model is a modified version of the BSH operational model (Kleine, 1994) with identical boundaries to the North Atlantic. The cooperation started in summer 1994 when the model was set up at SMHI. The first operational runs started in the sumrner 1995 and since then the model has been running daily except fora limited number of periods when there were no meteorological input from the HIRLAM (atmospheric) model available because of computer problems. During the first months, some occasions with stability problems occurred, leading toa restart from the climatological fields.

This report presents results from a continous verification exercise, where model

results are compared to observations of water level, surface temperature, currents, ice

thickness and salinity and temperature profiles. The times series data are taken from the period September-November 1996 while the ice thickness data are from November and December 1996 and the sea surface temperature data are taken from August, November and December 1996.

For a detailed description of the model, the reader is referred to a forthcoming report by Funkquist and Kleine.

Model configuration and forcing

In the Baltic Sea, a minimum resolution, which resolves the baroclinic Rossby radius,

mesoscale eddies, interna! waves and mixing, would be 500 m to 1 km in the

horizontal and from 1 m for the pycnocline to 10 m for more inactive layers.

However, in reality the resolution of the model has to be chosen in order to fit into the

available computer memory and CPU-time. For the horizontal, this has resulted in a

12 nautical miles grid covering the whole North Sea and Baltic Sea region. East of 6

E, a 3 nautical miles grid for the Skagerrak, Kattegat, Belt Sea and Baltic Sea is

nested into the larger grid. In the vertical, there is a variable resolution of 4 m for the

mixed Iayer and gradually increasing to 60 m for the deeper layers.

In a first attempt to set up the model configuration, a horizontal grid of 1 nautical mile

was nested into the 3 nautical miles grid with the boundary at the western part of the

Skagerrak. That version also included the two largest lakes in Sweden, Lake Vänern

and Lake Vättern, with a vertical resolution of 50 layers with 2 m resolution in the

mix.ed layer. While this grid was impossible to fit into the computer, a subset

containing only the lakes was extracted in order to test various lake-specific

phenomena like seiches and lake-ice dynarnics. The lake subset has also been tested

operationally fora limited period of time.

The main forcing comes from an atmospheric model in the form of 10 m wind, sea

surface pressure, 2 m temperature, 2m hurnidity and cloudiness. River runoff is

specified for 73 rivers and 17 tidal constituents are specified at the open boundary to

the Atlantic. HIROMB also consists of a NE Atlantic storm surge model, which gives

the storm surge at the open boundary.

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temperature, surface salinity and ice thickness. Besides these, a few examples of salinity and temperature profiles will be compared with ship observations.

Water level

Water leve! data from 7 stations (see Table 1) have been chosen as representative of the model area. In general, the three northernmost stations have a similar response reflecting the large-scale pressure and wind-dependent variation in the Baltic Sea. Landsort is representative of the mean water volume in the Baltic Sea with a much smaller variation. Simrishamn has a similar response as the first three stations, but with an opposite sign. Viken and Göteborg both have a relatively strong tidal component and with the largest variation in sea level.

Table 1. Water leve! stations usedfor verification against mode/ data.

Station Longitude Latitude

Furögrund 64°55' 21 °14' Ratan 64°00' 20°55' Spikarna 62°22' 17°32' Landsort 58°45' 17°52' Simrishamn _55°33' 14°21' Viken 56°09' 12°34' Göteborg 57°41' 11 °48'

As the datum for the computed water level depends on the initial density distribution and water level, there is no exactly defined value to be used in transforming the model data to the reference level used for the water level stations. Further, the steric effect caused by the density difference between stations in the southern and northern Baltic Sea may differ between the model state and real values, mainly because of wrong initial density field. Therefore, to exclude this effect, separate rnean values for both the observed and the computed water level data were subtracted from each time

series. First the rnean values for September was picked out to be used for all

subsequent months. However, due to a two days stop in September (18-19) and six

days stop in October (17-22) when the model's water level was left at the old value, a marked difference at all stations was observed after the restart. Therefore it was considered necessary to redefine the mean values that should be subtracted. To summarize, the mean values for September have been used for both the September and October plots, while new mean values were used for the November plots. These

problems could easily be removed if some kind of data assimilation procedure for

water level was incorporated into the model. Then it also should be more meaningful

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to look at the bias, a scalar error estimate that has not been addressed in the present study.

When comparing the time series one should have in mind that the model is forced by data from 12 to 36 hours forecast from the 55 km HIRLAM model. A limited validation study of the 10 m wind velocity in HIRLAM at Swedish coastal stations shows that for October-November the correlation range from 0.77 to 0.87 for forecasts up to 24 hours. However it is not straitforward to couple wind correlation to water level correlation, because the water level setup also depends on the sea level pressure, which probably gets a higher score in the HIRLAM forecast compared to wind velocity. There is also a dependence on variations in the density but it is only effective on a longer time scale.

In Figures 1-3 the observed water level is plotted against the computed one. In the rniddle of September there seems to have been problems with the data at Spikarna. Note also the different vertical scale for Landsort.

For September (Figure 1) the interruption of the model is evident from 12:00 the 17 to 12: 00 the 19. It is also clear that this has the effect that there is a marked bias for the rest of the month. However, in all the Baltic Sea stations, the model seems to adjust to the real state after 8 days. This means that there should have been an increased outflow from the Baltic Sea in the model as at all the stations the bias is positive.

The difference at the Landsort station <luring days 6-9 and 13 rnay have been caused by a poorly forecasted wind which on these occasions happened to have a large local influence, but this can not be conclusive as no comparisons on observed and modelled wind are done on a routine basis. By studying available data from Falsterbo, it is although evident that HIRLAM has a relatively large error in the wind speed during both periods.

The dominant tide (M2) at Viken and Gothenburg is surprisingly well captured by the model, especially regarding the phase. After the restart the 19 September, it only takes a few cycles before the water level reach the right phase again.

The correlation for October (Table 2) is highly influenced by the one week's stop in the model run, but <luring this period the change in the water volume for the Baltic Sea is not as large as for the September stop. On the other hand there is an underestimate of the water volume that shows up at all Baltic Sea stations starting at the 6 to 7 October (Figure 2). From the 13 October the underestimate increases at the Bothnian Bay stations.

Notably for Viken and Gothenburg, is that the peak at the end of the month is almost perfectly forecasted.

For November when there were no interruptions, it is clear that the correlation (Table 2) has drastically increased. A further explanation is that the result of a subjective comparison of the observed and the HIRLAM winds, also gives a higher score for this month.

During 5-6 November a heavy storm caused an unusually high water level at Gothenburg (Figure 3). This is rather well captured by the mode!, though the difference is about 25 cm.

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Station September 1996 October 1996 November 1996 Furuögrund 0.86 0.87

_*

Ratan 0.88 0.84 0.91 Spikarna 0.56 0.72 0.83 Landsort 0.40 0.52

_*

Simrishamn 0.85 0.81 0.93 Viken 0.74 0.87 0.77 Göteborg 0.76 0.79 0.89

Vertical salinity and temperature profiles

Vertical profiles of salinity and temperature from the model results have been compared with measurements from U/F Argos at five locations during the June 1996 cruise (Table 3). It is obvious that the last initial stratification used for the mode! start (March 1996) at all these locations (Figures 4 and 5) is very weak or almost absent. Then a quantitative comparison between model data and observations should not be very fruitful. However, looking at the model results for June 1996, well established pycnoclines and thermoclines have developed and except fora thin surface layer, both salinity and temperature are very close to what has been observed.

The model temperature for stations BY15 and BY20 clearly shows the effect of the absence of a vertical density gradient in the initial data. The whole water column has been mixed during late winter resulting in too low temperatures below the summer thermocline. However, the thermocline is well developed and in agreement with observations though the surface layer (0-5 m) is too warm. At the Bornholm Deep, inflowing warmer water has started to reestablish the temperature stratification in the deep water. In general, a significant amount of heat has been lost from the Baltic Sea.

For the Skagerrak and Kattegat stations the heat loss is srnaller and the thermocline evolution seems to be limited by the halocline. The observed thermocline is deeper which probably is the result of non-local processes which will need longer time to create the observed vertical temperature structure. As long as there is no data assimilation in the model, the only way to correct for the temperature stratification error is to restart the model from more realistic initial data. This will in fäet be done as new initial fields soon will be available as part of an analysis project at SMID.

At the Gotland Deep and Fårö Deep stations, a weak halocline has been established at 10 m depth and the salinity has increased for the whole water column. At station BY5 (Bornholm Deep ), the salinity of the bottom water has increased by almost 2 PSU because of inflowing salt water creating a halocline at a depth of 50 to 60 m. For the other two stations, the corresponding increase is between 0.2 and 0.6 PSU. Though

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inflowing water has started to increase the deep water salinity at the Bornholm Deep, it will take too long to correct for the wrong initial data. The development of the halocline is much faster at the Skagerrak: and Kattegat stations and for SKl 7 the salinity increase is about 3.5 PSU at 100 m depth. For all five stations the further development of salinity for July to September is marked with dashed lines. The gradually increase of bottom water salinity is most clearly seen at BY5 and SKl 7 which are more exposed for a continous supply of more saline bottom water from the Arkona Sea and the North Sea. The new initial fields mentioned above will hopefully correct for the salinity error in the same way as for temperature.

Table 3. Geo graphical position for five vertical stations

Station Longitude

Gotland Deep (BT15) 20°03' Fåry Deep (BT20) _19°57' Bornholm Deep (BYS) 15°59' Kattegat (KA29) 56°40' Skagerrak: (SKl 7) _58°16'

M onthly means and standard deviation

Temperature and salinity

Latitude 57°20' 58°35' 58°80' 12°07' 10°43.5'

We have calculated the monthly means and standard deviations for surface temperature and surface salinity using the output fields from every 6th hour. This has been done for August and November 1996 (Figures 6 - 14). The August pictures show large temperature deviations (see Figure 10) along coastal areas where uppwelling occurs and the largest deviation occurs outside the coast of Östergötland and along the southern coast of Norrland.The surface temperature deviation picture (Figure 11) shows smaller deviations in November and the largest deviations are around the coasts in the southwest and also at the very northern top of the Bay of Bothnia where the coastal water reaches zero degrees toards the end of November. The mean salinity pictures (Figures 8 and 9) shows the large salinity differences between the N orth Sea and the Baltic Sea. The Baltic Current is visible and in november also the Norwegian Coastal Current. Some river outflows can be seen on the November picture because the river discharge has been added to the model after the end of August.The largest salinity deviations (Figure 12) in August 1996 can be seen in the Sound, the Great Belt and the Fehmarn Belt. The area northeast of Skagen also shows larger salinity deviations. In November there are not as large deviations as

in August. The salinity deviations (Figure 13) are much smaller but if one changes the scale (Figure 14) there is a complex pattern with the largest deviations around the Swedish westcoast, near the outflows of some rivers and in shallow areas. The two surface salinity deviation pictures from November (Figures 13 and 14) also has same areas with zero salinity deviation and these areas appear as white spots (extra islands).

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currents and water level for November 1996. The water level mean fields (Figure 15) show the Baltic Sea leaning towards the south with a water level difference of about 35 cm between the Bay of Bothnia and the Arcona basin and about 15 cm difference

between the Arcona basin and the eastern North Sea. This is a combined effect of

dominating southerly winds, inflow and river runoff and corresponds well to

observations (Ekrnan and Mäkinen, 1996). The water level standard deviation (Figure

17) has a minimum in the rniddle of the Baltic Proper and a great maximum in the German Bight.

The current mean fields (Figure 16) show maximum currents in the southeastern Baltic Sea and in the North Sea and the prevailing direction is towards northeast. The current standard devation for November (Figure 18) shows minimas around the coasts

and in the Gulf of Finland and the Gulf of Riga. The maximas are in the German

Bight, north of Denmark and also smaller maximas in the Baltic Sea inflow regions and in the southeastem part of the Baltic Sea.

Ice and temperature verification

The surface temperature and ice cover output fields from the HIROMB model was

verified by eye during spring 1996 against the ice and SST-maps created by SMHI.

The result was prornising both for the temperature and ice case but when the ice

began to melt the modelled ice was to thick and had a to high concentration. This has

been considered by Ekhard Kleine and Lennart Funkquist who now has changed the

ice model to allow for more ice deformation. This new part of the icemodel in

HIROMB will be tested during the winter 96/97.

We have chosen the period 21 November until 19 December 1996 to show how the

SST and the initial ice develops in the HIROMB model compared to observations.

See figures 19 - 26.

The surface temperature fields from HIROMB (Figures 19b - 26b) show a very good

accordance with the SST maps (Figures 19a - 26a) and the differences are rarely more

than 1 degree in most areas but can be great in regions where HIROMB simulates

uppwelling which is not seen on the SST map.

The ice fields from HIROMB (Figures 21c -26c) show a quite good accordance with

the ice maps (Figures 21a - 26a) but have a tendency to form too much ice which can be seen on the figure from 19 December where the Gävle Bight and parts of the

Northern Quark is ice covered by HIROMB but not on the ice map. The ice growth in

the inner Gulf of Finland is though well simulated.

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Closely related validation exercises

Validation exercise for the Kattegat and the Skage"ak

In 1994, the Nordic Council of Ministers (NMR) conducted a model intercomparison for the Skagerrak - Kattegat region consisting of 6 invited models. A horizontal grid of 5 km was assumed but with no restrictions on the vertical resolution. Three more or less artificial cases were considered where the first only dealt with wind-driven flow with closed boundaries, the second with no wind and specified in- and outflow and the third with both kinds of forcing.

As there were no real data or even a real situation available to campare with the test cases, the outcome of the exercise can be kept in a short summary. A general experience from the intercomparison was that the models responded similar to the applied forcing. Clear differences could be related to physical and numerical formulations in the models. Differences in the mixing parameters were also clear and

same shortcomings of some models were noticed. The whole intercomparison is described in Gustafsson and Jönsson (1994) and the HIROMB application is reported in Funkquist (1996).

DYNOCS

DYNOCS (Dynamics of connected seas) is a MAST-Il project concentrating on the flow characteristics in the seas that connect the N orth Sea and the Baltic Sea. It contains field measurements, process studies and numerical as well as laboratory modelling. In the numerical modelling part, three different type of models are applied in a local area bounded by the southern Kattegat and the eastern Bornholm Basin. One of the models is identical to HIROMB with the addition of a flow relaxation scheme for the open boundaries. The model is run for three different periods each lasting for about two weeks. Boundary and initial data is given by a regional model covering the North Sea and the Baltic Sea. There will be an intercomparison between all models as well as comparisons with field data.

At present, only data reports and a few data analysis reports are available. Results from the model exercise will be reported soon after the finish of the project, i.e. in March 1997.

Vänern and Vättern

With the aim to learn more about the BSH-model the lakes Vänern and Vättern have been set up as a 3D-model. There was already an existing grid with 1 nm resolution covering the Baltic Sea including Lake Vänern and Lake Vättern and the area covering these lakes were cut out to form a smaller grid with 98x98 horisontal gridpoint and 35 vertical levels with 2 meters resolution the first 27 layers and then increasing every second layer to 4,6, 8 and 10 meters down to the maximum depth 110 meters (in Lake Vättern). The time step is 3 minutes and the discharge from the rivers Klarälven and Göta älv is considered. After some tests it was discovered that the grid was not complete, the western part of Lake Vänern was missing but the work to complete the grid has started and will be ready in the early 1997.

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been tested as an operational mode! during June 1996. It uses HIRLAM-fields as input data and works stable without numerical problems. It has been verificated aginst the SST-maps (which covers Vänern but not Vättern) from 960616 and 960620

which shows that the model surface temperature is up to 5 degrees to high. This

implies that Lake Vänern is to quickly heated or the vertical diffusion is to low.

Seiches in lake Vättern

The barotropic part of the Vänern-Vättern model has been thoroughly investigated. The Lake Vättern is known for the seiches going in the north-south direction and

there are measurements done by Bergsten 1926. In 1989 Björk and Lundberg did

some measurements and found three north-south seiche modes which they also found

in their calculations. We tried to find these periods, of which the 3-hour (179.5 min)

period is bye far the strongest, and with different methods we rnanaged to find all three of them.

Lake Vättern has a length of 111 km in our medel (with the narrow bay south of Askersund not included in the grid) and has a rnean depth of about 40 meters. A

seiche moves with the speed v=sqrt(g*h)

~

20.2 m/s which rneans that a journey back

and fourth will take about 183 minutes. When the model was started with a tilted watersurface (in north-south direction) the 3 hour period is very clearly seen and is damped with a damping coefficient of about 30 hours. The 3 hour period is also easily found if the model is forced with a sinusshaped wind with a 3 hour period.

The second strongest period is 97 rninutes but is 10 times weaker than the dominating 3 hour period. It can be found by either initiating the mode! with a ridge of water in the rniddle of the lake(as seen from east or west) or by forcing the medel with a sinusshaped wind with a 97 rninute period.

The 80.5 minute period is almost as strong as the 97 minute period and was found by

forcing the model with a sinusshaped wind with a 80.5 rninute period.

In the paper by Björk and Lundberg there were some rneasurements of the waterlevel in Jönköping (at the southern end of Lake Vättern) from 6-8 December 1985. In a test our model was forced by SYNOP-data every third hour from the Baltic database

from 1. to 9. December but did not reproduce the rnesurement at all. The amplitudes

were about the same size but in the simulation the 3 hour period dominated totally and there were no small timescale varations like in the observations. We tried to change the bottomfriction and other parameters in the model but without result. When we later added a random part and let the wind change every half an hour, instead of every third hour, the waterlevel answer was slightly better but there were no major difference.

Conclusions

A general conclusion from this validation is that the medel results to a !arge extent suffer from the poor initial data, where the vertical stratification is too weak or almost

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absent. This is well illustrated by the comparisons of vertical profiles. Consequently the vertical mixing has been too large leading to an excessive cooling of the Baltic Sea with implications on the start of the ice formation. However, since the last restart from initial data in March 1996, both thermoclines and haloclines have started to form and seem to continously approach the observed structures, which means that the model, if run long enough, is capable of producing the Baltic Sea estuarian structure.

An SMHI oceanographic analysis project which ends in February 1997 will produce

monthly values of gridded salinity and temperature data. Then it is most likely that the model performance will increase and more baroclinic features will appear in the model

results.

Most of the water level variations are reproduced by the model and the correlation for

November 1996 is in the range 0.77 to 0.93. Also the tidal component which

dominates the stations in Kattegat and Skagerrak is right in phase and almost right in amplitude. The mean water level for November 1996 (Figure 15) agrees well with the corresponding data from observations.

Although the water level is well captured by the model, the perforrnance could easily

be increased by including a data assimilation routine. Then also the effect caused by a several days break in the simulation, which is well demonstrated in the October data, could be removed.

The surface salinity looks reasonably and the surface temperature is very close to observations. The ice results are rather good but there are some overestirnation of the icecoverage which probably depends on the too cold deeper water caused by the absence of a halocline. The seiches in Lake Vättern are well simulated and all three measured seichmodes are seen in the model simulations but measured variations with much smaller timescale than 3 hours are not caught by the model.

Recommendations

This validation study clearly points at potential improvements that could be implemented in the model.

Realistic monthly means of temperature and salinity will be extracted to be used for initialization and operational control of the model. The analysis project mentioned in the validation section is a first step to solve this problem.

The weak mixing in the surface layer has to be corrected by looking for a possible error in the model code or modifying the turbulence model.

Data assimilation of water level could be incorporated by applying e.g. a variational method.

Concentration and thickness of ice only affects the surface layer and a suitable data

assimilation method for these parameters should rather easily be implemented. As a

consequence of changing the ice variables, the sea surface temperature also should be modified according to a suitable assirniliation scheme.

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At present, the light attenuation coefficient is held constant. But as there are significant variations both in time and space, this coefficient could be variable.

In the original setup of the model, the river runoff for all 73 rivers is constant in time.

However, monthly mean values are available and will be transferred to the model.

References

Bergsten, F. 1926.

The seiches of Lake Vetter. Geof. Ann. 8, 1-73.

Björk, G. and Lundberg, P. 1990.

A re-examination of the seiche periods of Lake Vättern. Tellus, 42A, 615-626.

Ekman, M. and Mäkinen, J. 1996.

Mean sea surface topography in the Baltic Sea and it's transition to the North Sea: A geodetic solution and comparison with oceanographic models. J. Geophys. Res., 101,

C5, 11993-11999

Funkquist, L., 1995.

The Skagerrak-Kattegat model experiment, application of HIROMB. In manuscript. Funkquist, L. and Kleine, E.

HIROMB, an introduction toan operational baroclinic model for the North Sea and Baltic Sea. In manuscript.

Gustafsson, B and Jönsson, A., 1995.

Verification of hydrodynamic models applied to Kattegat-Skagerrak, Report, Department of Oceanography, Göteborg University,.

Kleine, E., 1994.

Oas operationelle Modell des BSH för Nordsee und Ostsee, Konzeption und Obersicht. Bundesamt för Seeschiffahrt und Hydrographie, Hamburg.

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1a I I 80. 40. 0. -40. -80. I 24 72 120 168 216 264 312 360 408 456 504 552 600 648 696

- - - COUPUTEO_FVR\JOGRUNO(O•wlev_,ep) T

Water level at Furuogrund (sep 96)

1b 80. 40. 0. -40. -80. 24 72 120 168 216 264 312 360 408 456 504 552 600 648 696 - - - COIAPUTED_RATAN[D=wlev_sep) T

Water level at Ratan (sep 96)

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-40.

-80.

I

24 72 120 168 216 264 312 360 408 456 504 552 600 648 696

- - - CCI.IPUTED_SPll(ARNA[D=wlev_seo] T

Water level

al

Spikarna (sep 96)

20.

0.

-20.

24 72 120 168 216 264 312 360 408 456 504 552 600 648 696

- - - COIAPUTED_LANOSORT[O•wlev_sep] T

Water level at Landsort (sep 96)

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1e I I 80. 40. 0. -40. -80. 24 72 120 1 68 21 6 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_SIMRISHA1,CN(D=wlev_sep] T

Water level at Simrishamn (sep 96)

1f

80. 40. 0. -40. -80. 24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_VIKEN[D;wlev_sep] T

Water level at Viken (sep 96)

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40. 0. -40. -80. 24 72 120 1 68 216 264 .312 .360 408 456 504 552 600 648 696 - - - COMPUTED_GOTE80RG(D=wlev_sep] T

Water level at Goteborg (sep 96)

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2a

80. 40. 0. -40. -80. 24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696

- - - COMPU_TEO_FURUOGRUNO[D=wlev_oct] T

Water level at Furuogrund (oct 96)

2b

80. 40. 0. -40. -80. 24 72 120 168 216 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_RATAN[D;wlev_oct] T

Water level at Ratan (oct 96)

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40. 0. -40. -80. 24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_SPIKARNA{D=wlev_ocl] T

Water level at Spikarna (oct 96)

24 72 120 168 216 264 312 360 408 456 504 552 600 648 696

- - - COMPUTED_LANDSORT[D=wlev_ocl] T

Water level at Landsort (oct 96)

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2e

80. 40. 0. -40. -80. 24 72 120 168 216 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_SIMRISHAMN[D=wlev_octJ T

Water level at Simrishamn ( oct 96)

2f

80. 40. 0. -40. -80. 24 72 120 168 216 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_VIKEN[D=wlev_oct] T

Water level at Viken (oct 96)

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24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696

- - - COt.4PUTED_GOTEBORG[D-wlev_oct] T

Wa ter level a t Gote borg ( oct 96)

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Jo

80. 40. 0. -40. -80. 24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696 - - - COUPUTED_FURUOCRUNO[D:wlev_nov] T

W a ter level a t Furuogrund (N ov 96)

· Jb

80. 40. 0. -40. -80. 24 72 120 168 216 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_RATAN[D=wlev_nov) T

Water level at Ratan (Nov 96)

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40. 0. -40. -80. 24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696 - - - C0!.4PUTED_SPIKARNA[D=wlev_nov] T

Water level at Spikarna (Nav 96)

24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696

- - - C0!.4PUTED_u\NDSORT(D=wlev_nov] T

Water level at Landsort (Nav 96)

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3e

I I 80. 40. 0. -40. -80. 24 72 120 168 216 264 312 360 408 456 504 552 600 648 696 - - - CO,..PUTED_Sl"RISHAUN[D=wlev_nov] T

Water level at Simrishamn (Nov 96)

3f

80. 40. 0. -40. -80. 24 72 120 1 68 21 6 264 312 360 408 456 504 552 600 648 696 - - - COMPUTED_VIKEN[D=wlev_nov) T

Water level at Viken (Nov 96)

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80. 40. 0. -40. 24 72 120 1 68 216 264 312 360 408 456 504 552 600 648 696 - - - CO~PUTEO_GOTEBORG[D=wlev_nov) T

Wa ter level a t Gote borg (N ov 96)

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Station BY 15 0 -50 g-100 .. . ,', .-..

.s

0.

Ö

-150 -200 : .. ·. ,•, •'• -1 0 1 2 3 4 5 6 7 8 910111213141516 Temperature (0_C) 0 -50 g-100 .c::

2-0 -150 -200 6 7 8 ..._...._...._. ... . . . _.. . . ~ ' . . . ,• _.. . . •, . . . . ,' .... •'_.• ....

.

· ... •_.' 9 10 11 12 13 Salinity (psu) Station BY 20 0 -50 ,..._ 5-100

i

Ö

-150 . ,•. -200 ... -1 0 1 2 3 4 5 6 7 8 910111213141516 Temperature (0_C) 0 -50 g-100

.s

fr O -150 -200 6 . . . ~ . . . _.·. . . _.. . . . •, _.. . . 7 8 9 10 I I 12 13 Salinity (psu)

Figure 4.a: Temperature and salinity data: initial-green, calculated-red and observed-blue from June 26 1996, whereas the red dashed lines is from July, August and September 24.

(32)

6

.__,, -40

i

Q -60 ,--.._

5

.c:: 15.. <!) Q -80 . : _... ·. . · .... _.: .. · .. · . . . : .. · .. · .. . -100 '--'-~--'---'----'...L...L_._~~~--'---'----'--'-__,__, -1 0 1 2 3 4 5 6 7 8 910111213141516 Temperature (0C) 0 ... ... ·.·. ·: .. ·.· .. : ... ·: .. ·.· .. . -20 -40 .. ·,. • .. : .. ·,. · .. : ' .. ·,·. . •. ,• .. •, . -60 -80 . ' .. ·:. !\· ' .. ·: ... ' . . . ' . . . . . · ...

Il

:

-100 .__~.c....,___.__JJJ...,_~__.__~__._~~..___. 6 7 8 9 10 11 12 13 14 15 16 17 Salinity (psu)

Figure 4.b: Temperature and salinity data: initial-green, calculated-red and observed-blue

(33)

Station SK 21 0 -20

g

-5 -40 0.. Q) Cl

g

-60 4 6 8 I O 12 14 16 I 8 20 Temperature (0_C) 0 -20 -5 -40 0.. Q) Cl -60 ... •,• ... . , .... , ... •. ·· ... ·. -· ...

·--so~--'--~-~~-~--'---~~

20 22 24 26 28 30 32 34 36 Salinity (psu) 0 -50 I-100 -5 0.. Ö -150 -200 0 -50 I-100 ..c

fr

Cl -150 -200 28 Station SK 17 4 6 8 I O 12 14 16 18 20 30 Temperature (0_C) '\·:· &.i ... _ ll:1 ... il1 ·111 .. ·_-11i. : 111 · · · ·:· -1\1· 32 Salinity (psu) 34 36

Figure 5: Temperature and salinity <lat~: initial-green, calculated-red and observed-blue

(34)

□

30.

23. □

23.00

22.00 □

22.00

21.00

)

□

21.00 ,.

20.00 □

20.00

19.00

18.00

17.00

. ···•

■

17.00

16.00 ■

16.00

15.00 ■

15.00

. . ... -.. ..

14.00

(35)

HIROMB mean surface-temperature November 1996

□

12.00

11.00 □

11.00

10.00 □

10.00

9.00 □

8.00

9.00 □

8.00

7.00

6.00

5.00 ■

5.00

4.00 ■

4.0 0.1

(38)

□

5 .

00

4 .

00 □

4 .

00

3.00 □

3 .

00

2 .

50

2 .

50

2 .

00

2 .

0

1.

50

1 .50

1.00 ■

1.

0

0.50 ■

0

0 .5

.1

■

0.

1

0 ' - - - '

0 .

00

(39)

. -· ·•--- . -. ----. ---~ . --. . --- ..

HIROMB standard deviation surface-temperature November 1996

□

5.00

4.00 □

4.00

3.00

3.00 □

2.50 □

2.50

2.00

1.50

1.00 ■

1.00

0.50 ■

0.5

0.1 ■

0.10

0.00

Figure 11. Standard deviation, surface temperature (colourscale, °C), november

(40)

Figure 12. Standard deviation, swface salinity, august 1996

□

5.00

4.00 □

4.00

3.00 □

3.00

2.50 □

2.50

2.00

1.50

1.00 ■

1.00

0.50 ■

0.5

0.1

0.10 ■

0.00

(41)

HIROMB standard deviation surface-salinity November 1996

Figure 13. Standard deviation, su,face salinity, november 1996

5.00

0

4.00 □.

4.00

3.00 □

3.00

2.50 □

2.50

2.00

1.50

1.00 ■

1.00

0.50 ■

0.5

0.1 ■

0.10

0.00

(42)

□

1.00

0.60 □

0.60

0.50 .

□

0.50

0.40 □

0.40

0.30

0.20 ■

0.

20

0 .10

■

0.10

0.05 ■

0.05

0.

0

1

0 .

01 ■

0.00

(43)

HIROMB mean waterlevel 80. 75. 75. 70. 70. 65. 65. 50. 50. 45. 45. 40. 40. 35. 35. 30.

■

3025. . 25. 20. 20. 15.

■

1510. .

■

105. .

■

5.0 0.0

(44)

~

40.

35. □

35

30. .

□

30.

25.

20. ■

20.

15. ■

15.

10.

5. ■

5.

1 .

■

0.01

1.00

(45)

HIROMB standard deviation waterlevel

0.5 5. 10. 15. 20. 25. 30. 35. 40. 45. 50. 55. 60. 65. 70. 100.

(46)

□

100.

40. □

□

■

40.

35 .

35.

30.

25.

20.

15.

10.

5. ~---~

■

5 1 .

.

(47)

,.

..

.

.,.

sa•

,. ,..

SMHI

The Swedish Meteorological and Hydrological lnstitute©

YTVATTENTEMPERATURER SEA SURFACE TEMPERA TURES

SYMBOLS

2 ./ Vaucn1cm~ra1ur isotcnn ··c

,..- \Vilttr 1ri11pmllrlft iJOttn11, 'C

w Varmt maximum

Wunn11uuinmm

C _{Co/d miniuu,m}K.:1111 minimum

NR 93 1996-11-21

90

Figure 19a. SST and ice map from 21. november

,..

...

.,

.

---+- - - ·1-- -Sl' LIEPAJA J - - - + - - - + -- - - + - - - - t - - - - t - - - 5 ' ' 1 - - - - + - - - - t - - -- - l - - - - t - ----+r---SS' ,..

(48)

SMHI WED 20 NOV 96 12Z +024

VT: THU 21 NOV 96 12Z

-1.00 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 8.00 9.00 10. 12. 14. 16. 30.

(49)

,. 11' I'

SMHI

The Swedish Meteorological and Hydrological lnstitute©

YTVATTENTEMPERATURER

SEA SURFACE TEMPERATURES Nr 94 1996-11-25

21' ,.. 65'---+---~--~---~--~---~--~---~--~---~---,.---'---+---+---'i' SYMBOLS

..

.

..

.

2./ Vaucmcmp,.?ratur iso1mn ~c ,,,- \\'111u 1r:nrpm11uu i1oltn/J, 'C w Varmt m.uimum IV11m1 maxinuuu C K:illl minimum 63' Co/dmini11w111 63' 62' 61'- --+-- - - + - - - - + - - - -+ - - -- + - - -- + - - - - +- - - + - - - - + _ , . sa•

(l

8' ,,, GA w UEPAJA 56' l - - - l - - - - + - - - - f - - - + - - - t - - - - 5 5' I' ,. I' I' 2' 2' 2'

(50)

SMHI SUN 24 NOV 96 12Z +024

VT: MON 25 NOV 96 12Z

-1.00 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 8.00 9.00 10. 12. 14. 16. 30.

(51)

,,.

SMHI

The Swedish Meteorological and Hydrological lnstitute

©

/SLÄGE & YTVATTENTEMPERATURER NR 95 1996-11-28

... /GE COND/T/ONS AND SEA SURFA GE TEMPERA TURES

SYMBOLS

~ F:istis

...

Va.lllrllChupp1omlllis

fostict RiJgtd or liummocUd ict

SairulLlllfru.-cn.1.:nmp;oo lsbm

~ dkrmyd\1tl1Jri1is lrttdJt DmsolidtlUd. compaa or Upptl;an:ulisbntclkr

65" 1·uyclou ictt9-/(J//O/ _isgrans .,.

§ Totilii\is E.stinwuJ iu tJJt or Clostictf7-&IIOJ icebour.dnry ~ _"'

rn

Si-ii.lddri1·is ,.,,, Opeiiiet/-1-MO/ .JL Sump1.,1ll \Villdroll',jamintd ~ Mycl:ctspriddJrhis brashbarrirr Vtf)'Optn ict/l-J/10/ 6 lshumlingar ... _{Flotbtijl4fotbitJ} ...

D

Op(ll.11-:UlCJI Optnll'attr/< I/JO/

5J

Uppm:i11is1joctld; 111icJ.:,1wniLumrtdi,1cm

□

Nyis

Ntwict _{Vaucnicm~r.uur}_iso1trrn_·_c

2/

,,.. \Vaser ltmpmuurt iwum1. 'C

~ l!imois lcrtlict w V:irmt maximum 63" _{IVam1m11.tU11w11} .,. nn Hup>kjw~nis C K:illl minimwn

lwjltdict Cold 111i1Jim11111

C = Koncentr.itioo I tiondel.Dr Conwuration in 1whs

.,.

S = lstjocklck 62'

S, S,S, S111_,t of dmlopmrnJ

t' = Fonn a\' i~akstorlck

Fom1 oj iet/jl()(Ji:.t

Cod, Codc Om/

<l O(Wlct

"

<ID <~ J 10-JO 20--100

'

10-15 100-500 5 15-JO 500-2000

'

30--200 2ll00-10000 7 J0-70 ,10000 8 J0-50 F:öt[ct

..

.

_'

50-70 unknown I. 70-l!O 1 - - 1 - - - + - - - s a· ,r-- -,-- - - ,- ~_.flitl,1,,·~--+- -- +-- -l---+----+----+---+----+--56" \----t---+----+----J---+---SS• ... ,. 2. ,..

(52)

SMHI WED 27 NOV 96 12Z +024 VT: THU 28 NOV 96 12Z

-1.00 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 8.00 9.00 10. 12. 14. 16. 30.

(53)

HIROMB (3 nm) ice concentration (%)

SMHI WED 27 NOV 96 12Z +024

VT: THU 28 NOV 96 12Z

D

Figure 21c. HIROMB icefieldfrom28. november

100.

80.

80 .

60 .

60.

30.

10 .

10 .0

0.0

(54)

(55)

..

.

65'

..

.

.,. 62' 61' 60'

..

.

S

MHI

/SLÄGE & YTVATTENTEMPERATURER

/GE CONDITIONS AND SEA SURFACE TEMPERATURES

SYMBOLS

~ F:i.stis

...

forJiu

Sammanfru.-.:1L kump.ili

~ dkrm)'ch'ttll<lrivis CnTWJ/;JnuJ. rompact or 1·ttJ c/ose ice (9-/0//0J § Ta1Jri1is Clou ice /7-81/0J ~ ~ Spridddri1·is

Optn iet t./-6/IOJ

_J!_

~ Mych.1spridlldri1is

Vuyopen ict/ 1-JIIOJ

t,

D

Öpfl'.1 valtl!n Vptn ll'GIU t< 11/0/

5J

□

Nyis Ntwice 2/ ,r ~ fäm11is U:1·dict w JUl Hop.!il;:ju1enis

C Fwf1t1lia C = Konc,:nlration i tiondelar 1 - - - - ~ Cot1ClJllfO/io1t ill ltlllhs c,cbc, s, SbS C Codc nc11·ict < IO J 10-30

'

10-15 5 1$-30 6 30-200 1 30-70 8 JO-JO 9 50-70 I. 70-120 S = lsljocklek Stagt oj dtwlopmtnt F = Form av isnlak51orlek Fon11 oficdflotsi:e CodcOm/ <l

"

<20 20-100 100-500 ; 500-2000 6 2000-10000 1 >10000 8 Fasticc X unknown Valllfochupptom:itlis RidgtJ or /u1mmncl:td iu lsl:.lnl latdgt Upp~!JJ isbnl dkr isgr.ins F.stimaud ice tJgt ur ictbmmda')· 1W; L,,u/ Sumpvall \\'i11droll', jammtd brwhbarriu Jsbumlingu F/oebugSQlotbiu Uppm:iu istjockkk T//icblm mtamrtd i11 cm

Vau~n~ml),!r:Uurisocenn 'C

\Vaur umpmu11re iwumL 'C

Varmt m:iximum

\Vun1111ratinJ11J11

K:L11t minimwn

Coldmini1111un

NR 97 1996-12-05

Figure 22a. SST and ice mapfrom 5. december

21' ,.. ,.,

©

65'

"-..

.

., . / ----,- - - - + - - - 5 8 ' -- -- - - - t - -- 57' \---+-- ---l-- --+---l----+---56' \ - - - t- ---+---,f-- ---j---,r---55' 2' 24' ,.

(56)

SMHI WED 04 DEC 96 122 +024 VT: THU 5 DEC 96 122

/

-1.00 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 8.00 9.00 10. 12. 14. 16. 30.

(57)

SMHI WED 04 DEC 96 12Z +024 VT: THU 5 DEC 96 12Z

D

Figure 22c. HIROMB icefieldfrom 5. december

100.

80.

60.

30.

10.

10.0

0.0

(58)

(59)

65'

...

63' 61' 60' "'

SMHI

/SLÄGE & YTVATTENTEMPERATURER

/GE CONDITIONS AND SEA SURFA GE TEMPERA TURES

SYMBOLS ~ F:is1is AÅ. Fiwia Sanuiunfru.~llkornp.ili ~ cllcrmrck.:11:11dri\is OJ11toliJaud. compac1 or

l'tf)' c/uu ict (9-Ull/OJ

§ T.11llri1is C/ou ia (7-PJ/0/ ~

rn

SpriJJtlri\'is Opt11ict/4-61/0J _ff_ ~ M)'cki.1spri<lt.liirhis Vtt)' opm ice (/-3110/ t,

D

Öppt.'l\'al\CII

Optn 1ru1u / < 1/I0J

5]

RidgtJ ur lu,mmncttd ict

lsbm latdgt Uppibnad isbnl dkr isgr.ui.~ Eslima1r1Jicttd.~tor icrboiuuillry ""' Ltod Sumpvall \Viudrow, Jammtd bauhbarrirr lsbumlinglf Flaebt~1(f/otbits Uppn\111 isljod:ld:

Tl,icknas meunmd i11 cm

V;rncntcm~r.llurisotcrm ·c

IVUltr 1tmpu1J1urt isottm1. 'C

Vannt mnimum \Vam1nwit111m1 Kallt minimwn Cold minimum I' NR 98 1996-12-09 I' I' I'

Figure 23a. SST and ice map ji·om 9. december

21' ,,, ,.. 2'

©

65'

..

.

63' J----,---+--sa· .--1- -- + - -- ,I' f---+--f--f----+---f---+--ss· \----,----+---,f----+----t---55' 2' ,..

(60)

SMHI SUN 08 DEC 96 12Z +024 VT: MON 9 DEC 96 12Z

-1.00 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 8.00 9.00 10. 12. 14. 16. 30.

(61)

SMHI SUN 08 DEC 96122 +024 VT: MON 9 DEC 96 12Z

D

100 .

80 .

60.

30.

10.

10 .0

0.0

(62)

(63)

,,. 2J' 24• ,. ,..

SMHI

©

/SLÄGE & YTVATTENTEMPERATURER NR 99 1996-12-12

66' /GE CONOIT/ONS AND SEA SURFA GE TEMPERA TURES

SYMBOLS

~ Fa.stis

...

Valbr ud1 upp!umJd is

Foslict RiJ.eed vr /umwrncl:td iet

S.'.lllllnlllf~rL komplb lsb.Ju ~ clkr myck1.'t lal drh·is latdgt

Con.w/idaud, con1pac1 or _{Uppsbu:ul ishtu dia}

65'

65' 1·u)· cl ost ice (9-/0//0J _LSgrans

§ T:u<lrivis Es1imatediceed.~tnr irt boundary

C/auict(l-lVJOJ

~ lill

L,ad

w

SpriddJtivis

0pe,1 ia f./-6//0J

_ff_ Sumpvall Windrow. jam11ud

~ Mydcl spridtl dri\is brashlwria

Vuy optn iu I/-1/IOJ

t,. lsbumling:ir

..

.

FlotbugS.,1otbiis

..

.

D

Orp,'1 vani:n Optnirnttrt< 1//0)

5]

Uppm'inistjodld T/1icLtt'.SS111tusurtdit1c111

□

N}is Newice 2 / Vancmcm~ra1ur isoicnn "C / \Varu 1e111per11111rt ismeml •c

~ fämnis I.erdice w V;lmlt ma.,;imum .,. \Van1111w.riJ111u11 .,

.

JlJl Hopskjutcnis C Kall! minimum

Ruftedict Co/d 111i11i11uu1t

C = Konccnlrullon I tiondelar Co11wuratio11ii11t111/Js

·~

S=lstjocklek StogtojdmlopmttU F = Form av ist1lakstorltk Funu of icrlj1ouiu .,, _Cod, _{Codc Om /} d ncwicc d '" <20 3 10-]) 20-100 I 10-15 100-500 5 15-30 ; 500-2000 6 30-.?00 6 .?000-10000 7 30-70 7 > 10000 8 J0-5-0 8 F:istict "' 9 50-70 X unkno\\n I. 70-1.?0 1---f--f---+-- - s a' UEPAJA w )---+---t- - - + - ----t---t---56' \----t---+---t---+----1---55' 5'' ,. ,. ,. ,. 2'

(64)

-1.00 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 8.00 9.00 10. 12. 14. 16. 30.

(65)

SMHI WED 11 DEC 96 122 +024

VT: THU 12 DEC 96 122

D

■

100.

80 .

80.

60.

30.

10 .

10.0

0.0

(66)

(67)

SMHI

©

ISLÄGE & YTVATTENTEMPERATURER NR 100 1996-12-16

"' /GE CONDJTJONS AND SEA SURFA GE TEMPERA TURES

SYMBOLS

~ Fast is

...

VJ.11:lr och upp1omad is

Fustict Ridgtd or fwmmocUd iu

Samrrunfru:ic!n.l:omp.ili lsl:an1

§fl c!lkrmy<:kctt.11.tlrivis lurdgt

Consolit!Dud. compact or Uppsbnad isbnt clkr

65' myclostice(9-HVJO/ _isgrtinS § Taldsl\is Esli111Llltd ice tdgt or

C/ose ice (7-81/0J ictbotuidary

~ Rlk

rn

Spridddri\'is L,ad

Opt11ice(-l-6/JOJ

_ff_ Swnpv.1.11 Windroll',jwnmtd

~ Mych.1spritJd<lri\is brashbarritr

Vtry·opt11ict(I-JIJO) t:.

lsbumling:u-..

.

Flothugsffeotbiu

D

Oppc.'1 Yll(CU Oprn1ra1t1(< 1/10}

~

Uppm!inis1jockli!k 771ictne.ss mtusmtd in cm

□

Nyis Newice 2 / Vaucntcmp!ratur iso1~rm °C

/ \Vlllu ltmpu1J11,rt isortm~ 'C

~ J:imois

Le1·tlice _w Varmt maximum

63' \Vam1 maximum

J1.fl Hopil.:j111cnis

C Kallt minimum

Rilfttdict Co/d minimum

0&;::;o'~

SMHI SUN 15 DEC 96 12Z +024

VT: MON 16 DEC 96122

D

■

100 a

80. 80a

60.

60 a

30 .

30 a

1 O

a

10.0

0 .

0

(69)

,,. 22' ,,. ,.. ,..

SMHI

The Swedish Meleorological and Hydrological lnstilule

©

/SLÄGE & YTVATTENTEMPERATURER NR 101 1996-12-19

ICE CONDITIONS AND SEA SURFACE TEMPERATURES

SYMBOLS

~ Flstis

...

VJll:1rodiupp1om:itlis

Fuslict Ridgtd or lumur,nckd ice

Samm:infru.~n. kompakt lsbru

~ clkrm)ål'tl.lldrh'is lcredgt

tl-=.. .. Cun.sofidaud. compac/ or _Uppiblllll_i_sl:Jn_l_l!lli!r

65' _1·uy_c/ose_{iet: /9-/0/10!}

isgt'.ins 65'

§ T:11dri\is C/ou ice /7-&'IOJ

Es1im11ud ice tdge or

iceboundary

~ lill

rn

Spriddilri\'is L,ad

Open ice r~-6//0/

_ff_ SIJlllpvall Willdro11·. jan111ud

~ Mych.,spridddr1\is brashbarrirr Vu:,-upmice(/-J/10) t,, lsbumlingar

..

.

F/oebug~1oebiu

..

.

D

OpJ11.'I \'Jll~n Optflll'a/tr/< 1//0/

~

Uppnunistjocklck Tl,icbim 111tasured i11 cm

□

Nyis

Ne11·ice VaUl!nl~mp:rJtur iso1mn 'C

"

2 /

/ \Vuur u111pua1uu iJfJ/tmt. 'C

~ fämnis

Lere/ire

w V:irmt maximum

.,. _{\V1m11m,uinm111} GJ'

.fUl Hopskjwl!nis

C Kallt minimwn

Rufudice Co/J mi11i11uu11

C = Koncrn[radon i tiondelar c, cbc, Co11umra1io11 in umhs 62' S = lstjocklek

·~

s. SbS C Sragr af dmlopmolf f= Fonn av Wflakstorltk Fonu of icelf/ouiu Cod, Codc Om / fi d ncwict I

,,

<lfi

'

<20 J 10-JO 20-100 i 10-15 10()....500 5 15--JO ; 500-2000 6 J0-,00 6 2000-10000 7 30-70 7 , lllOOO 8 JO-W 8 Fasticc 60' 9 50-70 X unkmnrn I. 70-120 ss· - - + - - -+---58' - -+- - ---- -57' UEPAJA 11----+---+----+---+----+--58' ss· From 25 December 1996

54' "1---=+==-:!-.✓--«:,;.:_-+---+---~"""-::..-~"'-l----+---4---+--+----ITo ports,.in Bay of Bolhnia 2000 dwt lce Class 1C ,..

In Gäla Alv and lo ports in Vänern 1000 dwt lce Class

,. ,,. ,..

(70)

-1.00 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 8.00 9.00 10. 12. 14. 16. 30.

(71)

SMHI WED 18 DEC 9612Z +024 VT: THU 19 DEC 96 12Z

D

100.

80.

60.

30.

10.

10.0

0.0

(72)

(73)

SMHis publiceringar

SMHI ger ut sex rapportserier. Tre av dessa, R-serierna är avsedda för internationell publik och skrivs därför oftast på engelska. I de övriga serierna används det svenska

språket.

Seriernas namn

RMK (Rapport Meteorologi och Klimatologi) RH (Rapport Hydrologi)

RO (Rapport Oceanografi) METEOROLOGI

HYDROLOGI OCEANOGRAFI

I serien OCEANOGRAFI har tidigare utgivits:

1 Lennart Funkquist (1985)

En hydrodynamisk modell för spridnings-och cirkulationsberäkningar i Östersjön S lu trapport.

2 Barry Bro.man och Carsten Pettersson. (1985)

Spridningsundersökningar i yttre fjärden Piteå.

3 Cecilia Ambjörn (1986).

Utbyggnad vid Malmö hamn; effekter för Lommabuktens vattenutbyte.

4 Jan Andersson och Robert Hillgren (1986). SMHis undersökningar i Öregrundsgrepen perioden 84/85.

5 Bo Juhlin (1986)

Oceanografiska observationer utmed sven-ska kusten med l"Ustbevakningens fartyg 1985.

6 Barry Broman (1986)

Uppföljning av sjövärmepump i Lilla

Vär-tan.

7 Bo Juhlin (1986)

15 års mätningar längs svenska kusten med kustbevakningen (1970 - 1985).

8 Jonny Svensson (1986)

Vågdata från svenska kustvatten 1985. 9 Barry Broman (1986)

Oceanografiska stationsnät - Svenskt Vat-tenarkiv. 12 13 14 15 16 17 18 19

Publiceras sedan

1974 1990

1986

1985

Bo Juhlin (1987)

Oceanografiska observationer utmed sven-ska kusten med kustbevakningens fartyg 1986.

Jan Andersson och Robert Hillgren (1987) SMHis undersökningar i Öregrundsgrepen 1986.

Jan-Erik Lundqvist (1987)

Impact of ice on Swedish offshore ligh-thouses. Ice drift conditions in the area at Sydostbrotten - ice season 1986/87. SMHJ/SNV (1987)

Fasta förbindelser över Öresund - utredning av effekter på vattenmiljön i Östersjön. Cecilia Ambjörn och Kjell Wickström (1987)

Undersökning av vattenmiljön vid utfyllna-den av Kockums varvsbassäng.

Slutrapport för perioden 18 juni - 21 augusti 1987.

Erland Bergstrand (1987)

Östergötlands skärgård - Vattenmiljön. Stig H. Fonselius (1987)

Kattegatt - havet i väster.

Erland Bergstrand (1987)

Recipientkontroll vid Breviksnäs fiskodling 1986.

(74)

21 Cecilia Ambjörn (1987) 33b Eleonor Marmefelt och Jonny Svensson

Förstudie av ett svenskt modellsystem för (1990)

kemikaliespridning i vatten. Nwnerical circulation models for the

Skagerrak - Kattegat. Preparatory study.

22 Kjell Wickström (1988)

Vägdata från svenska kustvatten 1986. 34 Kjell Wickström (1990)

Oskarshamnsverket - kylvattenutsläpp i 23 Jonny Svensson, SMHI/National Swedish havet - slutrapport.

Environmental Protection Board (SNV)

(1988) 35 Bo Juhlin (1990)

A permanent traffic link across the Oceanografiska observationer runt svenska

öresund channel - A study of the hydro-en- kusten med kustbevakningens fartyg 1989. vironmental effects in the Baltic Sea.

36 Bertil Håkansson och Mats Moberg (1990) 24 Jan Andersson och Robert Hillgren (1988) Glommaälvens spridningsomräde i

nord-SMHis undersökningar utanför Forsmark östra Skagerack.

1987.

37 Robert Hillgren (1990)

25 Carsten Peterson och Per-Olof Skoglund SMHis undersökningar utanför Forsmark

(1988) 1989.

Kylvattnet från Ringhals 1974-86.

38 Stig Fonselius (1990)

26 Bo Juhlin (1988) Skagerrak - the gateway to the North Sea.

Oceanografiska observationer runt svenska

k"Usten med k"Ustbevakningens fartyg 1987. 39 Stig Fonselius (1990)

Skagerack -porten mot Nordsjön.

27 Bo Juhlin och Stefan Tobiasson (1988)

Recipientkontroll vid Breviksnäs fiskodling 40 Cecilia Ambjörn och Kjell Wickström

1987. (1990)

Spridningsundersökningar i norra

Kalmar-28 Cecilia Ambjörn (1989) sund för Mönsterås bruk.

Spridning och sedimentation av tippat ler

-material utanför Helsingborgs hamnområ- 41 Cecilia Ambjörn (1990)

de. Strömningsteknisk utredning avseende

ut-byggnad av gipsdeponi i Landskrona.

29 Robert Hillgren (1989)

SMHis undersökningar utanför Forsmark 42 Cecilia Ambjörn, Torbjörn Grafström och

1988. Jan Andersson (1990)

Spridningsberäkningar -Klints Bank. 30 Bo Juhlin ( 1989)

Oceanografiska observationer runt svenska 43 Kjell Wickström och Robert Hillgren kusten med kustbevakningens fartyg 1988. (1990)

Spridningsberäkningar för EKA-NOBELs 31 Erland Bergstrand och Stefan Tobiasson fabrik i Stockviksverken.

(1989)

Samordnade kustvattenkontrollen i Öster- 44 Jan Andersson (1990)

götland 1988. Brofjordens kraftstation -

Kylvattensprid-ning i Hanneviken.

32 Cecilia Ambjörn (1989)

Oceanografiska förhållanden i Brofjorden i 45 Gustaf W estring och Kjell Wickström

samband med kylvattenutsläpp i Tromme- (1990)

kilen. Spridningsberäkningar för Höganäs