ICES
C.H. 1986/C:23
HYDROGRAPHIC CONDITIONS "IN
THE ICELAND SEA IN LATE WINTER
1971, 1975 and 1982
by
S.A. Malmberg, J. Olafsson and S.S. Kristmannsson
Marine Research Institute, Reykjavik, Ieeland
ABSTRACT
This paper deals with hydrographie observations in
the Ieeland Sea in late winter 1971, 1975 and 1982. Main
emphasis is laid on water mass eharaeteristies as regards
deep water formation, their variability, and possible
reasons and eonsequenees of the observed variability.
The observations in 1971 revealed that both the
elassieal model of eooling at the sea surfaee and the
double diffusion model eould be valid for deep water
formation not only in the Greenland Sea but also in the
Ieeland Sea. Due to lower salinities in the surfaee layer
as well as inthe intermediate layer in 1975 than in 1971,
eonditioning for deep water formation in the Ieeland Sea
were less favoured in 1975 than in 1971.
The 1982 observations in the Ieeland Sea revealed
ehanged water mass eharaeteristies from 1971 and 1975.
The Intermediate Water in 1982 was eolder and less saline
with salinity beldw 34.90 eompared with 34.93-34.94 in
1971 and 1975; thus no intermediate salinity maximum was
observed in 1982. Also the Bottom Water was in 1982 less
saline (<.34.92) than in 1971 and 1975 (>34.92), but
slightly warmer too (6) -1:0 °Cversus < -1.0 °C) and thus
slightly less dense.
These results from the Ieeland Sea in February 1982
may be the first reported showing a deerease in density
in deep water aeeompained with the salinity anomaly of
the late seventies in the northern North Atlantie and the
Subaretie Sea.
Introduetion
The waters bounded by Ieeland, Greenland and'Jan Mayen
are known as the Ieeland Sea (Fig. 1).
The region hasmueh
in eommon with the neighbouring Greenland and Norwegian Seas,
ineluding an interplay between Atlantie and polar influences
whieh not only makes the region lively and variable but, also
provides its importanee to the weather and elimate of northwestern Europe. The most outstanding publieations dealing
with the Ieeland Sea are those of Stefansson (1962) and, Swift
(1980; see also Swift et ale 1980 and Swift and Aagaard 1981).
The eyelonie eurrent system andthe differentwater
masses in the Ieeland and Greenland Seas are indieated in a
XBT seetion between northeast Ieeland and Spitzbergen earried
out in August 1972 (Fig. 2)
In February 1971 hydrographie investigations were
earried out.in the Ieeland and Greenland Seas (Fig. 1).
The main purpose of these investigations was to study the
late winter distribution of salinity in the East Ieelandie
Current northeast of Langanes (Malmberg 1984) and in the
Jan Mayen Polar Current northeast of Jan Mayen.
observations
were apart of a study of iee eonditions in
the sea north of Ieeland.
•
The
The hydrographie eonditions in
the area in the Greenland Sea where deep bottom water
formation is supposed to take plaee were also investigated.
In February 1975 (Ieeland Sea Projeet; Swift 1980) and1982
(Deep Water Projeet of ICES) again hydrographie investigations were earried out in the Ieeland Sea on seetions
between northeast Ieeland and Jan Mayen (Fig. 3).
The
present paper deals with these investigations from late
winter 1971, 1975 and 1982 mainly as regards water mass
e~araeteristies
and their variability, and possible reasons
and eonsequenees of the observed variability.
Material
Figs. 1 and 3 show the loeation of the hydrographie
stations dealt with in this paper. The data eolleeted are
- 2 -
kept on file at the Marine Research Institute in Reykjavik.
-The data- are based on standard hydrographie observations
withwater bottles and reversing thermometers (Hydro- Bios
I.
I
and Gohla, Kiel). The salinity was determined by conductivity (Australian Auto-Lab Salinometer in 1971 and 1975
and a Guildline Salinometer in 1982, using ros standard
·seawater and Unesco International Qceanographic Tables)'.
Reported oxygen values were determined by Winkler titration.
Results and discussion
The main results of the investigations in 1971 were
the following (Malmberg 1983):
1. The t-s diagrams from the rceland and Greenland Seas
were similar (Figs. 4,5), showing only the slight but not
insignificant differences in the water mass characteristics
, (Table 1). The main water masses are (see Stefansson 1962,
Lee 1963, Carmack and Aagaard 1973, Swift and Aagaard 1981):
a) relatively cold and low saline water in the surface
layer in the soutnern parts of the seas (East Icelandic
Current and Jan Mayern Polar Current; Fig. 2),
b) relatively warm and saline intermediate waters below the
cold and low saline waters, and c) cold and saline deep or
bottom water _in the deepest and central parts of the seas,
more or less connected with the upper layers in these seas
of cyclonic current systems (Fig. 2).
2. As regards the observations from the Greenland Sea in
1971 it should be repeated here (Malmberg 1983) that a
salinity of 34.874 was reached in the surface layer of the
northernmost station in the Greenland Sea (Figs. 1, 5, 6;
stat. 139 at long 0°, 75°N). As far as known to the first
author of this paper in 1983 this was the highest w.inter
salinity observed in the area. Norwegian investigations
in 1958 revealed similar values (Odd H. $~len, pers. comm.).
This value of 34.874 is still slightly too low to allow
surface water to sink to greater depths bycooling at the
•
-
sea surface.
3 -
It was however stated (Malmberg 1983), that
the homogeneity in salinity and sigma-e from near surface
layers d~wn to the deepest observations at 3500 m (34.8734.90 and 28.08-28.09) indicates a deep reaching convection
with formation of deep or bottom water prior to the
observation time.
After that some lateral advection ofless
saline water may have taken place in the surface layers.
The oxygen values of the northernmost stations in the Greenland Sea (Fig. 1) were also relatively high and homogenous
from surface layers to the deepest observations at 3500 m
(7.75-7.40 ml/L or 93-89%). Farther south (stat. 135, 137
•
in Figs. 1, 5, 6), in the intermediate layer below the cold
surface layer of the Jan Mayen Polar Current, the observed
salinity distribution also permits water mass transformation
involving double diffusion and deep vertical convectionin
the very homogenous study area (Carmack and Aagaard 1973).
3.
In the Iceland Sea in February 1971 the salinity in
surface layers south of Jan Mayen (Fig. 7) was indeed high
enough (34.92-34.94) to permit the water to sink by cooling
(Stefansson 1962, Swift and Aagaard 1981), but the vertical
temperature distribution did not however reveal such
conditions to greater depths since the temperature decreased
with depth, ca .. loC from the sea surface down to bottom
(sigma - e of 28.05-28.09), and neither did the oxygen
distribution show such conditions (Fig. 8). Further south,
at station 124, relatively high oxygen values were found
from the sea surface (8.0 ml/L,> 95%) to bottom (7.25 ml/L,
> 88%). This might indicate a degree of vertical convection
in the area, possibly in connection with low temperatures
in the surface layers and high salinities in t~e intermediate water with salinity values of about 34.94 (Fig. 7,
lateral advection and diffusion; Carmack and Aagaard 1973).
4.
Thus the hydrographie data obtained in the Iceland Sea
and in the Greenland Sea in late winter 1971 showed the
generally known features of permanent net cyclonic circulation in these seas accompained by a doming of isopycnals
on a hundred of km length scale (Figs. 2, 6, 7). These
- 4 -
eonditions are believed to be important in the produetion
of deep water in the Greenland Sea at least.
The data
revealed that both the elassieal model of eooling (HellandHansen and Nansen 1909) at the sea surfaee and the double
diffusion model (Carmaek and Aagaard 1973) eould be valid
for deep water formation not only in the GreenlandSea, but
also in the Ieeland Sea.
Also small seale and/or non-
stationary eyelonie eireulation (eddies, ehimneys) together
with physieal
proeess~s
like intense winter eooling at the
surfaee and water mass transformation involving double
diffusion in intermediate waters eould lead to vertieal
eonveetion or deep water formation (Killworth 1979).
Primarily, this deep water may be formed in the Greenland
Sea and the Norwegian Sea where its presenee and eharaeter:isties maintain seeondary eonditions for deep water
;formation in the Ieeland Sea.
5.
The investigations in the Ieeland Sea in late winter
1975 (Swift 1980, Swift and Aagaard 1981, Halmberg 1984)
again revealed the threi'above mentioned water masses
(Table
1, Figs. 9, 10).
The low-saline and eold water in
the surfaee layers was now slightly fresher (~34.80) than
in 1971 «34.90). The intermediate water was above O°C
in temperature along the whole seetion between Northeast
Ieeland and Jan Mayen eontrary to 1971 (Fig. 7) ,but both
eolder and less saline in the southern and northern parts
of the seetion.
The bottom water was in 1975 similar in
temperaturri (6( - 1.0°) as in 1971 and so was the salinity,
though with slightly higher values (>34.92) in the southern
part of the area than in the northern one
(~34.92).
This
may indieate a different origin of the deep water, the
former being Norwegian Sea Bottom Water and the ~atter
Greenland Sea Bottom Water (Aagaard et ale 1985).
Due to
lower salinities in the surfaee layer as weIl as in the
intermediate layer in 1975 than in 1971 eonditioning for
deep water formation in the Ieeland Sea ean be eonsidered
still less favoured in 1975 than in 1971.
6. The observations in,February 1982 in the Ieeland Sea
revealed ehanged water mass eharaeteristies from 1971 and
..
- 5 .
f'
197~ -except for the surface layer (Table 1, Figs. ~il,;12).
The Intermediate Water in 1982 was colder and less saline
with salinity below 34.90 compared with 34.93-34.94 in 1971
and 1975; thus no intermediate maximum in salinity was
observed.
The potential temperature in the intermediate
layer in 1982 was below oOe instead of 0-1°e in 1971 and
1975.
However, the Bottom Water was in 1982 less saline
( (. 34.92) than in 1971 and 1975 and slightly warmer
(0) - 1. 0 oe versus e< - 1. 0 Oe).
It was thus slightly less
dense, possibly indicating effects of the low-saline
Intermediate Water on the Bottom Water.
•
These conditions of the Intermediate and Bottom Water
in the Ieeland Sea in February 1982 may be coupled to the
so-called mid-seventies salinity anomaly (Dooley et al.
1984, Dickson and Blindheim 1984, Dickson et al. 1984),
i.e. a decrease in salinity observed in the northern North .
Atlantic and the European Subarctic Sea in the late
seventies.
It may either be directly connected to an in-
creased outflow of Polar Water from the European Arctic
and Subarctic Seas during the late sixties (Dickson et al.
1984, Malmberg 1985, 1986) or indirectly through atmospheric variations (Dooley et al. 1984, Gammelsröd and Holm
1984, Dickson et al. 1975, Malmberg and Svansson 1982),
traced from the Denmark Strait (1968) to Labrador (1972)
and from there back to the coasts of Europe (1976) and into
the European Subarctic Sea (1979-1981; see also Aarkrog et
al. 1983).
As previously shown (Dickson and Blindheim 1984), not
only a decrease in salinity was observed during these years,
but also a cooling found place in the European Subarctic Sea
so densities remained close to normal.
This i8 also true
for the Intermediate Water in the Ieeland Sea in 1971, 1975
and 1982 (Table 1; densities around 28.03-28.04), but in
the Deep or Bottom Water a slight increase
in temperature
was observed in 1982 compared with the findings in 1971 and
1975, together with a decrease in salinity, leading to a
slight decrease in density (28.08 versus 28.09) of the
- 6 -
Bottom Water (Figs. 9, 11).
These conditions should lead,
toa decrease both in salinity and temperature of the
Denmark Strait Overflow which consists of 80-90% of Intermediate Water partly formed in the Iceland Sea (Swift et
al. 1981, Ross 1984), which again is in accordance with
findings by Swift (1984).
He reported a decrease in
salinity of 0.02 and in temperature of 0.15°C in deep ,
waters of the North-East Atlantic.
The same was stated,by
Swift (1984) as regards the Iceland-Scotland overflow
water.
This overflow consists of Norwegian Sea Deep or
Bottom Water at least in the Faroe-Shetland Channel but
more of intermediate waters farther north on the IcelandFaroe Ridge (Stefansson 1967, Meincke 1978).
On the other hand the results of the investigation in
the Iceland Sea, dealt with in this paper, show a decrease
in salinity of approximately 0.01 of the Bottom Water from
1971, 1975 to 1982 but a slight increase in potential
temperature of O.Ol°Cand hence a decrease in density of
0.01.
Thus the data from the Iceland Sea in February 1982
may possibly be the first reported showing a decrease in
density in deep waters accompanied with the salinity anomaly
of the late seventies.
7. A data series from spring in deep waters east of
Iceland (Fig. 14) reveals the same trend (Fig. 13).
The
data are from 600 m depth and cover the period 1975-1984.
The locality can be regarded as upstream for the flow of
Deep or Bottom Water along or across the Iceland-Faroe
Ridge and through the Faroe-Shetland Channel.
It is
evident from the series that a freshening of 0.02 took
place in the Deep Water at this,location east of Iceland
together with a decrease in density.
There was not as
clear a trend in temperature at this location and only of
secondary importance to the density.
During this period,
which may be coupled to the seventiessalinity anomaly in
the Subarctic Sea, the hydrobiological conditions in North
Icelandic waters also changed to the most unfavourable
primerly due to a cold arctic water mass (t=1-3°; S""'34.8)
dominating in North Icelandic waters in spring 1981-1983
tt
- 7 -
contrary to the usual Atlantic and/or polar influence in
the area (Fig. 15).
Conclusion
It can be concluded that both the classical model of
cooling at the sea surface and the double diffusion model
could be valid for deep water formation in the Ieeland Sea
in late winter 1971, but these conditions were less favoured
in 1975 due to lower salinities in the surface layer as weIl
as in the intermediate layer than in 1971.
The 1982 observations in the Ieeland Sea revealed changed
water mass characteristics from 1971 and 1975, the Intermediate
Water was colder and less saline and no intermediate salinity
maximum was observed.
Also the Bottom Water was in 1982 less
saline than in 1971 and 1975, but also slightly warmer and thus
slightly less dense.
The results from the Ieeland Sea in
February 1982 may be the first reported showing a decrease in
density in deep water accompained with salinity anomaly of
the late seventies in the northern North Atlantic and the
European Subarctic Sea.
- 8 -
Referenees
Aagaard, K., J.H. Swift and E.C. Carmaek 1985.
Thermohaline
eireulation in rhe Aretie Mediterranean seas. Journal
of Geophysieal Res., 90:4833-4846.
Aarkrog, A., H. Dahlgaard, L. Hallstadius, H. Hansen and
E. Holm 1983.
Radioeaesium from Sellafield effluents
in Greenland waters.
Nature 304, 5921:49-51.
Carmaek, E.C. and K. Aagaard 1973.
the Greenland Sea.
On the deep water of
Deep-Sea Res. 20:687-715.
Diekson, R.R., H.H. Larnb, S.A. Malrnberg and T.M. Colebrook
1975.
Climatie reversal in the northern North-Atlantie.
Nature 256:479-482.
Diekson, R.R. and J. Blindheim 1984.
On the abnormal
hydrographie eonditions in the European Aretie during
the 1970's.
Rapp. P.-v. Reun. Cons. int. Explor. Mer,
185:201-213.
Diekson, R.R., S.A. Malrnberg, S.R. Jones and A.J. Lee 1984.
An investigation of the earlier Great salinity Anomaly
of 1910-1914 in waters west of the British lsles.
C.M. 1984/GEN:4.
lCES
Minisyrnposium (mimeo).
Dooley, H.D., J.H.A. Martin and D.J. Ellett 1984.
Abnormal
hydrographie eonditions in the north-east Atlantie
during the nineteen-seventies. Rapp. P.-v. Reun. Cons.
int. Explor. Mer, 185:179-187.
Gamrnelsröd, T. and A. Holm 1984.
Variations of temperature
med salinity at Station M (66°N, 02°E). Rapp. P.-v.
Reun. Cons. int. Explor. Mer, 185:188-200.
Helland-Hansen, B. and F. Nansen 1909.
The Norwegian Sea.
lts physieal oeeanography based upon the Norwegian
researehes 1900-1904. Rep. Norwegian Fishery Mar.
lnvestigations, 2.
-
9 -
Killworth, P.D. 1979. On "ehimney" formations in the oeean.
Journ. Physieal Oeeanogr. 9:531-554.
Lee, A. 1963. The hydrography of the European Artie and
Subaretie Seas. Oeeanogr. Mar. Biol. Ann. Rev.:47-76.
Malmberg, S.A. 1983.
Hydrographie Investigations in the
Ieeland and Greenland Seas in late winter 1971. "Deep Water Projeet".
Malmberg, S.A. 1984.
J6kull 33:133-140.
Hydrographie eonditions in the East
Ieelandie Current and sea iee in North Ieelandie
waters 1970-1980.
Mer, 185:170-178.
Rapp. P.-v. Reun. Cons. int. Explor.
Malmberg, S.A. 1985. The water masses between Ieeland and
Greenland. Rit Fiskideildar 9:127-140.
Malmberg, S.A. 1986.
The Eeologieal Impact of the East
Greenland Current on the North leelandie Waters. The
Role of Freshwater Outflow in eoastal marine eeosystems.
Ed. S. Skreslet.
NATO ASI Series. Vol. 67:389-404.
Malmberg, S.A. and A. Svansson 1982.
Variations in the
physieal marine environment in relation to elimate.
lCES C.M. 1982/GEN:4. Minisymposium (mimeo).
Meineke, J. 1978.
On the distribution of low saline inter-
mediate waters around the Faroes.
Dt. hydrogr. Z.
31:50-64.
Ross, C.K. 1984.
Temperature-salinity eharaeteristies of
the overflow water in Denmark Strait during "Overflow
'73". Rapp. P.-v. Reun. Cons. int. Explor. Mer, 185:
111-119.
Stefansson, U. 1962.
North leelandie Waters.
Rit Fiski-
deildar 3, 219 pp.
Stefansson, U. 1967.
The overflow of north lcelandic winter
water aeross the Ieeland-Faroe Ridge.
Cons. int. Explor. Mer, 157:135-137.
Rapp. P.-v. Reun.
- 10 -
Swift, J.H. 1980.
Seasonal Processes in the Iceland Sea
with special reference of their relationship to the
Denmark Strait overflow.
University of Washington:
296 pp.
Swift, J.H. 1984. Arecent 6-S shift in the deep water of
the northern north Atlantic. In J.E. Hanson and T.
Takahashi (Eds) , Climate"Processes and Climate
Sensitivity, Geophys. Monogr. 29, Maurice Ewing Vol.
5, 47 AGU, Washington D.C.:39-47.
Swift, J.H., K. Aagaard and S.A. Malmberg 1980.
The
contribution of the Denmark Strait overflow to the deep
North Atlantic. Deep Sea Res. 274:29-42.
Swift, J.H. and K. Aagaard 1981.
Seasonal transitions and
water mass formation in the Iceland and Greenland Seas.
Deep-Sea Res. 20A(10) :1107-1129.
•
- 11 'Tab1e 1a. Water masses in the leeland Sea in February 1971, 1975
and 1982.
1971
tOC
Surface water
Intermediate water
e
tOC
S
<-
0.5
0-1
.9
34.94
~34
> 34.92
Deep and bottom water"""-1
Table Ib.
1975
<. -0.5
;V'
1982
S
tOc
< 34.8
-0.5
0-0.2 34.93
-1
"-'34.92
S
<. 34.8
<0
34.90
> -1
<. 34.92
Water masses in the Greenland Sea in February 1971.
tOC
Surface water
~
-
S
1.5 -----34.87-
Intermediate water
0-1.5
34.95
Deep and bottom water
-
34.90
1.3
_._------
- 12 -
Figure 1.
Loeation of hydrographie stations in the Iee1and
and Greenland Seas earried out on R/V Bjarni
S~undsson in February 1971 (+), and a XBT seetion
earried out in August 1972 (X).
(Halmberg 1983)
200
)00 ' - - _ - ' -
o ...
ICHAND
JANMAYEN
ICELAND SfA
Figure 2.
Temperature distribution in a XBT seetion from
Ieeland to Spitsbergen from August 1972.
The
eyelonie eurrent systems and the different water
masses in the Ieeland and Greenland Seas are
indieated. For loeation see Fig. 1.
(Malmberg
1983) .
I
o
1975
e 1982
ell4
-
ello
el08
560.106
el04
59
o
68 0
-
el02
-
e 061
94
t-
e92
90
I-
e062
e88
66
lt>86
-
e84
e 8 :3
p
D
660 -..A
15°
Figure 3.
I
I
I
I
10°
Loeation of hydrographie stations in the Ieeland
Sea earried out on R/V Bjarni
1975 and 1982.
S~undsson
in February
14
5%0
34.9
34.8
0.0·
0.0·
-1.0·
-1.0·
S'Yoo
34.9
34.8
Potential temperature - sa1inity diagrams at
Figure 4.
selected stations in the Ice1and Sea in February
1971. For location see Fig. 1. (Malmberg 1983).
34.8
34.7
34.6
1.0·
I
~
/1
0.0·
~
• I
I
I
I
I
I
I
/
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
I
28.00
I
I
/
/
I
I
I
I
I
i,,'"//
I
""
~
\~ "I'
.,v-"
Figure 5.
"
"",
0.0·
," "
,"
,//
I
I ,
I
I
I
I
I
"
I
",'
I
II
I
I
I
'
I
I
34.7
-1.0·
l·
I
,"
I
34.6
,,
,"
II
"
"
"
"
,
"
,
I,'
,,'
I
,,
,.f
, I
"" /
,,'"
I
I
I
I
I
t~C
I
/1
I
-1.0·
-2.0·
I
I
I
/
I
35.0
1.0·
27.90
t:C
5%0
34.9
/
I
I
I
I
I
I
28.10
/28.11
I
I
34.8
Potential temperature
-2.0·
34.9
-
5%0
35.0
sa1inity diagrams at
stations in the Greenland Sea in February 1971.
For location see Fig. l .
(Ma1mberg 1983) •
e
- 15 -
O.
po
• -1
000
bOO
I
'<'00
: 120::1
.. 00
• lfiQQ
WOll
· zooo
2400 _
aoo
• IbOO
1
loe
~
"00
.I
i
• )I,JO
I
,
~--
-<
'0
Figure 6.
I
'00
_ l_-.J
"0
o ".
'00
'0
Temperature and sa1inity distribution in a section
along the 0 0 meridian from 72°24'N to 75°00'N in
the Green1and Sea in February 1971.
see Fig. 1.
For location
Notice differences in cruise stat.
numbers he re used and consecutive stat. numbers
used elsewhere in this paper.
(Malmberg 1983).
120
125
129
o
m
500
o
n.m.
Figure 7.
100
Temperature and sa1inity distribution in a section
between Iceland and Jan Mayen in February 1971.
For location see Fig. 1.
(Malmberg
1983).
16 120
o
129
125
125
120
129
o
m
m
500
500
1000
1000
1500
1500
2000
2000
o
n.m
100
Figure 8.
200
300
0
n.m.
\00
200
300
Oxygen distribution in the same section as shown in
Fig. 7.
(Malmberg
1983).
1.0 ,---,--..,----,--,--,-~---.-r__._-_,______,r__.__-,____.,
9
27/2-1/3 1975
0·5
34.85
Figure 9.
•
Potential temperature
salinity diagrams at selected
stations in the Iceland Sea in February 1975. For
location see Fig. 3.
17 sr.
66
62
61
59
60
56
sr. 66
55
62
61
60
••
59
!
56
55
i /
34.8~.
---::=:;===:::::::::;:=3J;4;:;9i22:=~~:
:::::::-349: '
• ==-- :
500
. 500
1000
: 1000
8·
0
34.92
>34.92
~
I~OO
, 1500
-0.9
'-------/--'''-092--------.-- __ --~
..............................
tOe
27/2-2/3 1975
27/2 - 2/3 1975
2000l----..l-------L------=':-----'-:-----=-:---'
o n.m.
~o
100
150
200
250
Figure 10.
<34.92 .
s
2000'--------'-------'------''-----'-------L..---'
o n.m.
250
200
50
100
150
Temperature and salinity distribution in a seetion
between Ieeland and Jan Mayen in February 1975.
For loeation see Fig. 3.
1.0 r--r---,.--,---r----.--,--.-------r---,--,----r--r---,.---,
8
23-26/2 1982
0.5
o
o
00
00
I
°
<»0
°0
-0.5
o
o
o
0
00
o
-1.0
34.80 $%0
Figure 11.
34.85
34.92
.94
Potential temperature
salinity diagrams at seIeeted
stations' in the IeeIand Sea in February 1982. For
Ioeation see Fig. 3.
- 18 -
94
96
98
100 102
104 106
500
1000
..~
-0.8'
1500
1°C
2000
23-27/2 1982
o
n.m.
50
100
90.... 92
94
150
96
98
100
200
102
104 106
250
108
110
112
300
'14
500
1000
1500
s
2000
23-27/2
o n.m.
Figure 12,
50
100
150
200
250
300
Temperature and sa1inity distribution in a section
between leeland and Jan Mayen in February 1982.
For location see Fig. 3.
------------------------
-
-
-
- 19 i --
--
I
- I
I
--
---.
-,'
-·-r- . - - - - . - j
.-
~
I
I
[J
-.151
I
-. 2
\
~
\
\
-.25 ;
I
I
\
,
\
\ 0'-'\
-.31
\
\
-.35 ;
/'
//
~/
.
LJ
i
-.4:
\
I
i
'j
-.451
I
I
-.5:
I
78
H
I
_.
_
-r---.--
82
__
_ __
Oll
84
,--.-- --- -,-
1
,
34.925;
__ --1
-'--'1
1..._ _
BO
7B
34.93
•
_'
o
[J
\
34. 92 ~
\
I
I
34. gIS!
I
I
!
I
34.91 :
V
"
I
I
34. 005 1
28.07
1
I
I
7fl
34.9:
74
_ - - ---_.,
_ _ __
78
--
..
I. _ •
80
_
L
__
~
B2
- ._-,----------,--
._ .L.
. __ .
B4
B8
-~/----'
I
28. 065
[~
2a.OB
28.055
28.05 _
28.045 __
2B.
041
74
Figure 13.
_
1
76
_1_ _ .
m
.1-.
00
..1-..
~
L
~
_
00
Temperature, sa1inity and density in June 1975-1984
at 600 m depth east of Iceland.
Fig. 14.
For location see
-
20 -
K-6
•
64°
620 L..-..
30°
Figure 14.
---'
2S0
-..l.
20°
-l-_--:.:>JI
---..L.
ISO
10°
Main oeean eurrents in Ieelandie waters and Ioeation
of two standard hydrographie stations north of Ieeland
and east of Ieeland.
8
tOe
7
1924-1960
6
5
1961-1970
4
3
2
o
-I
Figure 15.
Mean temperature - salinity relationships in MayJune 1924-1960, 1961-1970 and. 1971-1980 and in 1981
at a station in North Ieeland waters. For Ioeation
see Fig. 14.
(Malmberg and Svansson 1982).
•
• r-
FJOLRITUNARSTOFA
OANIELS HALLOORSSONAR