JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 107, NO. C5, 10.1029/2000JC000683, 2002

Decadal variations in Labrador Sea ice cover and North
Atlantic sea surface temperatures
Clara Deser and Marika Holland
Climate and Global Dynamics Division, National Center for Atmospheric Research, Boulder, Colorado, USA

Gilles Reverdin
Laboratoire d’Etudes in Géophysique et Océnographie Spatiales, GRGS, CNES, Toulouse, France

Michael Timlin
CIRES Climate Diagnostics Center, Boulder, Colorado, USA
Received 25 October 2000; revised 9 July 2001; accepted 13 September 2001; published 1 May 2002

[1] The spatial and temporal evolution of winter sea ice anomalies in the Labrador Sea andassociated sea surface temperature (SST) variations in the North Atlantic are documented forthree periods of above-normal ice cover: 1972– 1974, 1983– 1985, and 1990 – 1992. These
events are notable for their winter-to-winter persistence, despite the fact that the ice margin
retreats to northern Baffin Bay each summer, and for their spatial evolution, progressing fromthe northern Labrador Sea to the southern tip of Newfoundland over a 3 year period. Abovenormal sea ice is consistently accompanied by below-normal SSTs in the subpolar Atlantic: thelatter persist 1 – 3 years after the decay of the ice anomalies and in some cases exhibit atendency for eastward movement across the gyre. Spring – summer freshwater anomalies at 100
m depth in the West Greenland Current are found to precede by 8 months the initial
occurrence of above-normal ice cover in the northern Labrador Sea. The role of atmosphericforcing in the joint evolution of anomalous sea ice and SST is assessed by means of an iceocean mixed layer model forced with observed air temperature and wind fields. The model
results indicate that thermodynamic atmospheric forcing accounts for much of the winter-towinter persistence and spatial evolution of the ice and concurrent SST anomaly patterns.
However, the subsequent persistence of SST anomalies in the subpolar region is not wellsimulated, suggesting that oceanic processes omitted from the simple slab mixed layer
formulation play a contributing role.
INDEX TERMS: 3339 Meteorology and Atmospheric
Dynamics: Ocean/atmosphere interactions (0312, 4504); 3349 Meteorology and Atmospheric
Dynamics: Polar meteorology; 4540 Oceanography: Physical: Ice mechanics and air/sea/ice
exchange processes; 9315 Information Related to Geographic Region: Arctic region; 9325
Information Related to Geographic Region: Atlantic Ocean; KEYWORDS: sea ice, decadal
variability, North Atlantic Ocean, sea surface temperature, Labrador Sea

1. Introduction[2] Sea ice is an integral component of the physical climate
system, modulating surface albedo, turbulent air-sea energy
exchange, and upper ocean stratification. Ice cover in the Labrador Sea exhibits substantial year-to-year variability, particularly
during the winter season, as shown by Walsh and Johnson[1979], Agnew [1993], Mysak and Manak [1989], Mysak et al.
[1990], Chapman and Walsh [1993], Fang and Wallace [1994],
Mysak et al. [1996], Slonosky et al. [1997], Prinsenberg et al.
[1997], Parkinson et al. [1999], and Deser et al. [2000a]. Thesestudies document that winter ice variations in the Labrador Sea
tend to be out of phase with those in the Greenland-BarentsNorwegian Seas. Such a configuration of sea ice anomalies has
been attributed to a recurring large-scale pattern of atmosphericcirculation changes broadly termed the North Atlantic Oscillation(NAO). It is likely that the prevailing positive polarity of the
NAO in recent decades has contributed to the retreat of the winterCopyright 2002 by the American Geophysical Union.
0148-0227/02/2000JC000683$09.00

ice edge in the Greenland-Barents-Norwegian Seas and to anadvance in the Labrador Sea [cf. Deser et al., 2000a].
[3] In addition to longer trends, decadal timescale fluctuations
are prominent in many physical variables within the Labrador
Sea, including upper ocean salinity, temperature, and sea ice[Deser and Blackmon, 1993; Marko et al., 1994; Houghton,
1996; Reverdin et al., 1997; Belkin et al., 1998]. An intriguinglag association between decadal fluctuations in ice and sea
surface temperature (SST) was reported by Deser and Blackmon[1993]. They found that periods of enhanced winter ice cover in
the northern Labrador Sea tend to precede colder than normal
SSTs east of Newfoundland by 1 – 2 years. Anomalous advectionof cold, fresh water by the Labrador Current was suggested as apossible mechanism linking the ice and SST variations. Subsequent studies by Houghton [1996], Reverdin et al. [1997], andBelkin et al. [1998] investigated the horizontal and verticalstructure of decadal-scale salinity and temperature fluctuationsin the northern North Atlantic and slope currents of theLabrador Sea. Their results confirmed a propagating signal ofcold, fresh anomalies from the Labrador Sea to the northeastern
subpolar Atlantic in the upper several hundred meters, with atransit time (4 – 5 yrs) roughly consistent with the mean advection speed of the gyre. Reverdin et al. [1997] also found a

3-1

3-2

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS
and Walsh [1993, and references therein]. For a recent analysis ofthese data on a hemispheric scale, see Deser et al. [2000a].
[6] The SST data are from the Comprehensive Ocean-Atmosphere Data Set (COADS), an extensive archive of surface marine
weather observations from merchant ships [see Woodruff et al.,1987]. COADS data are quality-controlled but not corrected forchanges in instrumentation and observing practice, and missing
data are not filled in. The monthly mean data are archived on a 2latitude by 2 longitude grid through 1997. We smoothed themonthly anomaly fields in both the zonal and meridional directions
with a three-point binomial filter.
[7] Throughout this study the term ‘‘monthly anomaly’’ refers to
the departure of a value for a given month from the long-termmonthly mean. Seasonal anomalies are averages of the monthly
anomalies. Unless stated otherwise, the statistical significance ofcorrelation coefficients is assessed using a two-tailed Student’s t test
taking into account the effective number of degrees of freedom inthe time series according to Trenberth [1984]. Only those correlations exceeding the 95% confidence level are discussed. A map ofgeographical sites referred to in this study is shown in Figure 1.

3. Results

Figure 1.

Geographical locations referred to in this study.

strong anticorrelation between ice cover and salinity fluctuationsin the Labrador Sea and briefly noted that sea ice anomalies in
the northern Labrador Sea tend to precede those in the south by
6 months to 1 year.
[4] The purpose of this study is to examine in greater detail the
spatial and temporal evolution of decadal-scale sea ice anomalies
in the Labrador Sea during winter. Is the southward progression
noted by Reverdin et al. [1997] a robust feature? What is the role ofatmospheric forcing in the evolution of anomalous sea ice cover?
What is the nature of the lag association between sea ice and SST
anomalies, and what is the role of atmospheric forcing in theircoevolution? What is the temporal relation between sea ice andsalinity anomalies within the Labrador Sea? To answer thesequestions, we perform simple analyses on gridded observational
data sets of sea ice concentration, SST, and surface wind during
1953 – 1997. We also make use of a sea ice-ocean mixed layer
model simulation forced by observed time-varying surface atmospheric fields. The data and analysis techniques are described in
section 2. The observational and modeling results are reported in
section 3 and discussed in section 4.

3.1. Winter Sea Ice Variability[8] The climatological distribution of SIC in the Labrador Sea
during winter (December – March) is shown in Figure 2a. The
marginal ice zone (concentrations between 0 and 100%) extends
from the Davis Strait to the southwestern tip of Greenland andalong the Labrador coast to Newfoundland. The interannual standard deviations of winter SIC (Figure 2b) are largest within themarginal ice zone, with maximum values 22% directly south of
the Davis Strait and 14% along the coast of Newfoundland.
[9] To define the dominant structure of interannual variability of
ice cover in the Labrador Sea, we apply empirical orthogonal
function (EOF) analysis to the area-weighted covariance matrix of
winter SIC anomalies during 1953 – 1997. The leading EOF and its
associated principal component (PC) time series are shown in
Figure 3. The EOF, which accounts for 56% of the variance overthe domain shown, is depicted in terms of the local correlation
coefficient between the PC time series and the sea ice anomaly
time series at each grid point. The EOF exhibits uniform polarity,
indicating that winter sea ice anomalies tend to fluctuate in phasewithin the entire Labrador Sea (Figure 3a). Local correlation

2. Data[5] The sea ice concentration (SIC) data set is an updated
version of that described by Chapman and Walsh [1993] containing end of month SIC values during 1953 – 1997. For this study theoriginal 110 km equal area grid was interpolated to a 1 latitude by1 longitude grid and smoothed in both the zonal and meridional
directions with a three-point binomial filter. Thus only the grossfeatures of interannual ice cover variability are resolved by our
analyses. Further information concerning data sources and issues
relating to homogeneity and quality control are given by Chapman

Figure 2. (a) Mean and (b) interannual standard deviation of
winter (December – March) sea ice concentrations (percent) in the
Labrador Sea based on the period 1953 – 1997. The contour
interval is 20% (4%) for the mean (standard deviation) field. The
circle in Figure 2b denotes the position of the Fylla Bank
hydrographic station.

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONSa3-3[10] Sequences of sea ice anomaly maps for 1972 – 1974, 1983 –
1985, and 1990 – 1992 are shown in Figure 4. No temporalsmoothing has been applied to these maps other than seasonal
averaging. In 1972 the largest SIC anomalies are located south of
the Davis Strait (values exceeding 50%), with weaker anomalies
extending along the southern Labrador and Newfoundland coasts;
this pattern closely resembles the EOF. In 1973, positive anomalies
recur but with diminished amplitude in the Davis Strait andincreased magnitude east of Newfoundland relative to 1972. In
1974, positive anomalies reappear off the southern tip of Newfoundland, with near-normal ice cover elsewhere. The ice anomaly
sequences during 1983 – 1985 (Figure 4(middle)) and 1990 – 1992
(Figure 4(bottom)) exhibit many features in common with thatduring 1972 – 1974. Above-normal SIC occurs initially in the Davis
Strait, followed in the next winter by a southward expansion and/or
intensification of the positive anomalies along the southern coast ofLabrador and in the third winter by positive anomalies off the Islandof Newfoundland. It should be noted that sea ice retreats to northwestern Baffin Bay during the intervening summers (not shown).
[11] Two other periods of above-normal SIC are evident in theice PC record: 1957 – 1959 and 1993 – 1994. The spatial evolutionof winter SIC anomalies for these years is shown in Figure 5.
Neither sequence conforms to the evolution of the three high ice
events just shown. In particular, the positive SIC anomalies in 1957
are followed by near-normal conditions in 1958 and by weak
positive anomalies in 1959. The positive SIC anomalies in 1993
are followed by weaker anomalies in 1994 (but no evidence for asouthward expansion, although a distinct maximum occurs off
Newfoundland) and near-normal conditions in 1995.

b

Figure 3. (a) Leading EOF of winter sea ice concentration
anomalies in the Labrador Sea and (b) its PC time series. The EOF,
which accounts for 56% of the variance over the domain shown, is
depicted in terms of the local correlation coefficient between the PC
time series and the sea ice anomaly time series at each grid point.

coefficients exceed 0.9 directly south of the Davis Strait and 0.7 off
Newfoundland; that is, the EOF accounts for nearly all of theinterannual variability in the Davis Strait and approximately half ofthe variability along the Newfoundland coast. The PC time series(Figure 3b) exhibits three distinct periods of extreme positive
values (1972 – 1973, 1983 – 1984, and 1990 – 1993); a period of
weaker positive values (relative to the years immediately before
and after) occurs in 1957 – 1959.

Figure 4. Sequences of winter sea ice concentration anomalies
for three periods of high ice cover in the Labrador Sea. The contour
interval is 5%; values >5% are shaded; the zero contour has been
omitted; and the dashed contour is 5%.

3-4

Figure 5.
ice cover.

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS

As in Figure 4 but for two additional periods of high[12] To document further the temporal relation between winter
SIC anomalies in the northern and southern portions of the Labrador
Sea, we constructed regional indices for the Davis Strait (58 – 67N,
64 – 52W) and for the area directly east of Newfoundland (45 –54N, 54 – 45W); these records are shown in Figure 6. The Davis
Strait ice index is nearly identical to the PC time series: its correlation
coefficient is 0.98. The Newfoundland ice index tends to fluctuate inphase with and also lags the Davis Strait ice index, consistent withthe results shown in Figure 4. This behavior is particularly evident
during the periods of extreme ice cover in the 1970s, 1980s, and1990s. The lag cross-correlation curve between the two records(Figure 7) confirms this tendency: maximum correlation coefficients(significant at the 99% confidence level) occur at zero and 1 year lag(0.73 and 0.77, respectively). The Newfoundland ice index exhibits
higher persistence than the Davis Strait ice index, with a 1 year lag
autocorrelation of 0.56 compared to 0.37.
3.2. Relation of Winter Sea Ice Variability to SST Anomalies
in the North Atlantic[13] One of the motivations for this study was to investigate
further the link found by Deser and Blackmon [1993] between sea

Figure 6. Regional winter sea ice concentration anomaly indices:
Davis Strait (58 – 67N, 64 – 52W) (solid curve) and Newfoundland (45 – 54N, 54 – 45W) (dashed curve). Both curves arenormalized by their respective standard deviations, and no
temporal smoothing has been applied other than seasonal
averaging.

Figure 7. Lag cross-correlation curve between the Davis Strait
and Newfoundland Ice Indices, based on data smoothed with athree-point binomial filter. Positive lags indicate Davis Strait leads
Newfoundland.

ice variations in the Labrador Sea and subsequent SST fluctuationsin the subpolar North Atlantic. Here we present a composite
analysis of the joint spatial and temporal evolution of winter SIC
and SST anomalies associated with extreme ice conditions in the
Labrador Sea. Figure 8 shows a sequence of lag correlation maps
formed by correlating the leading ice PC (nearly identical results
are obtained with the Davis Strait ice index) with the gridded SIC
and SST anomaly fields at lags 0 – 3 years. The analysis is based on
the period after 1965 to diminish the influence of the long-term
SST cooling trend from the 1950s to the 1990s (see Figure 10)
upon the correlations (beginning the analysis in 1961 or 1968
produces nearly identical results). SST anomalies are based on theextended cold season December – May in view of the strong
persistence of winter SST anomalies through spring (not shown).
Correlation values in excess of 0.30 (0.35) in absolute value are
significant at the 95% confidence level for SIC (SST). For
convenience we shall use the terms subpolar gyre (subtropicalgyre) to refer to the portion of the North Atlantic Ocean poleward(equatorward) of 45N, just south of Newfoundland.
[14] The sequence of lag correlation maps depicts a southward
progression of SIC anomalies from the Davis Strait to Newfoundland over a 2 year period (lag 0 to lag 2), as expected fromthe results shown in section 3a. Negative SST anomalies in the
subpolar gyre are associated with positive ice cover anomalies at
all lags shown, with some evidence for an eastward progression
over time (note that only the far eastern portion of the gyrecontains significant correlations at lag 3 years). The SST patterns
at lag 1 and 2 years, with negative values in the subpolar gyreand positive values in the western subtropical gyre, resemble thesecond EOF of winter SST anomalies shown by Deser andBlackmon [1993], confirming that their SST EOF is most closely
associated with winter SIC anomalies in the Davis Strait 1 – 2years earlier (note that Deser and Blackmon’s study period ended
in 1988).

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS

3-5[15] To what extent do individual high-ice events follow thecomposite evolution depicted in Figure 8? Joint sequences of
winter sea ice and SST anomaly fields during 1972 – 1976,
1983 – 1987, and 1990 – 1994 are shown in Figure 9. Enhanced
ice cover is consistently accompanied by below-normal SSTs over
the western subpolar gyre in all the years shown, indicating that
this aspect of the lag correlation analysis is robust. The persistenceof negative SST anomalies 1 – 3 yrs after the decay of positive ice
cover anomalies is also evident in many years, for example, 1974 –1976, 1985 – 1987 (although we note that the SST anomalies in1986 are more intense than those in 1985, suggesting more thansimple persistence in this case), 1992, and 1994, confirming the lagcorrelation results. However, eastward movement of negative SST
anomalies in the subpolar gyre is discernible only during 1972 –1976 and 1990 – 1992, and positive SST anomalies near the Gulf
Stream are evident only in 1983 – 1985 and 1993 – 1994: these
aspects of the composite evolution are thus considered less reliable.
[16] The temporal association between sea ice anomalies in the
Labrador Sea and SST anomalies in the subpolar North Atlantic isfurther illustrated in Figure 10, which shows the (inverted) Davis
Strait ice index and the record of winter SST anomalies averaged
over the eastern two thirds of the subpolar gyre (50 – 62N, 46 –12W) where the lag 2 correlations in Figure 8 are strongest. No
temporal smoothing has been applied to either record. As expectedfrom Figure 9, below-normal SSTs accompany and persist 1 – 3years beyond each period of severe ice conditions in the 1970s,
1980s, and 1990s. The weaker ice event in the late 1950s does notappear to be linked directly to below-normal SSTs, although arelative minimum in the SST index occurs in 1960 – 1963. A similar
pair of curves was presented by Deser and Blackmon [1993; seealso Deser and Timlin, 1996] for the period 1953 – 1988, although
the indices are slightly different from those used here.
[17] The main results of section 3.1 and section 3.2 aresummarized as follows. Three periods of anomalously high winterice cover are identifiable in the Labrador Sea after 1953: 1972 –
1974, 1983 – 1985, and 1990 – 1994 (a weaker episode occurs in1957 – 1959). The high-ice events during the winters of 1972 –
1974, 1983 – 1985, and 1990 – 1992 are notable for their persistence, despite the fact that the ice margin retreats to northern Baffin
Bay each summer, and for their spatial evolution, progressing fromthe northern Labrador Sea to the southern tip of Newfoundlandover a 3 year period. Positive ice cover anomalies are consistently
accompanied by below-normal SSTs in the subpolar Atlantic andless consistently by positive SST anomalies in the western subtropical gyre. The subpolar SST anomalies persist 1 – 3 years after
the decay of the ice cover anomalies and in some cases exhibit atendency for eastward movement.

Figure 8. Lag correlation maps (lag in years) between the ice PC
and winter anomaly fields of SST (thin contours) and sea ice
concentration (thick contours) based on the period 1965 – 1997.
The thin solid (dashed) contours denote positive (negative) SST
correlations (contour interval = 0.2; zero contour is omitted);values  0.4 are shaded. Only the 0.4 and 0.8 contours areshown for the sea ice correlation fields.

3.3. Relation of Winter Sea Ice Anomalies
to Atmospheric Forcing[18] Numerous studies have shown that anomalous atmosphericconditions play an important role in forcing anomalous winter SIC
in the Labrador Sea [cf. Ikeda et al., 1988; Ikeda, 1990; Agnew,
1993; Fang and Wallace, 1994; Mysak et al., 1996; Prinsenberg etal., 1997]. In particular, the strength of the northwesterly (offshore)surface geostrophic wind component and accompanying surface airtemperature anomaly are strong determinants of winter sea ice
conditions in the Davis Strait (Labrador and Newfoundland
coasts). However, none of these studies explicitly examined therole of atmospheric forcing in terms of its contribution to theobserved persistence and southward evolution of winter sea ice
anomalies during the periods of enhanced ice cover in the 1970s,
1980s, and 1990s.
[19] Figure 11 shows the sequence of winter (December –February) geostrophic wind anomalies during 1972 – 1974,
1983 – 1985, and 1990 – 1992, superimposed upon the ice anomaly
fields. The wind anomalies were derived from an updated versionof the sea level pressure data set of Trenberth and Paolino [1980]

3-6

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS

Figure 9. Sequences of winter sea ice concentration anomalies (thick contours) and SST anomalies (thin contours
and shading) for three periods of high ice cover in the Labrador Sea. For sea ice, only the 10% isopleth is shown. For
SST the contour interval is 0.35 K beginning at ±0.15 K, and solid (dashed) contours indicate positive (negative)
anomalies, with values 0.15 shaded. Anomalies are with respect to the period 1965 – 1997.
archived on a 5 longitude by 5 latitude grid. In both 1972 and1973 a coherent pattern of northwesterly geostrophic wind anomalies overlies the positive SIC anomalies in the Labrador Sea, while
in 1974, anomalous offshore flow prevails over the region ofenhanced ice cover directly east of Newfoundland. In 1983 and1984, anomalous northwesterly flow occurs over the eastern
portion of positive SIC anomalies in the northern Labrador Sea,
while in 1985 the circulation is near-normal, although very weak
offshore flow anomalies occur east of Newfoundland. The wind
anomaly patterns over the Labrador Sea in 1990 – 1992 are similar
to those in 1972 – 1974, with enhanced northwesterly flow over theextended ice margin in 1990 and 1991 and moderate offshore wind
anomalies in the region of enhanced ice cover east of Newfoundland in 1992.
[20] These qualitative comparisons between the wind and ice
anomaly fields lend support to the notion that atmosphericcirculation conditions may be partially responsible for theobserved spatial patterns and winter-to-winter persistence of
positive SIC anomalies during 1972 – 1974 and 1990 – 1992, andto a lesser extent during 1983 – 1985. Rogers et al. [1998] have

Figure 10. Winter Davis Strait ice index (inverted; solid curve)
and SST anomalies in the subpolar North Atlantic (51 – 61N,
45 – 13W; dashed curve). Both records are normalized by theirrespective standard deviations, and no temporal smoothing has
been applied other than seasonal averaging.

also documented the persistent nature of atmospheric circulation
anomalies over the Labrador Sea during the early 1970s and mid1980s, not only from winter to winter but extending into otherseasons as well. The extent to which the southward evolution of
positive SIC anomalies during the three episodes of high ice
cover is attributable to atmospheric forcing is more difficult toassess from the general qualitative comparisons presented in
Figure 11. For a more quantitative assessment of the role ofatmospheric forcing we examine next a sea ice model simulation
forced by observed surface atmospheric fields for the period1948 – 1998.
3.4. Sea Ice Model Simulation[21] The model used in this study is an early version of the newsea ice component in the National Center for AtmosphericResearch (NCAR) Community Climate System Model (CCSM),
documented in full detail by B. P. Briegleb et al. (manuscript in
preparation, 2002). It employs an elastic-viscous-plastic rheology[Hunke and Dukowicz, 1997] to solve the ice dynamics. Thisrheology approaches the viscous-plastic solution [Hibler, 1979] on
the timescales associated with the wind forcing. A subgridscale ice
thickness distribution [Bitz et al., 2001] is used that allows for fiveice and one open water category within each grid cell. This
represents the high spatial variability present in the observed ice
cover. The thermodynamics of each ice category is solved separately using the formulation of Bitz and Lipscomb [1999]. This
results in different surface conditions for each category and thus
different ice/atmosphere exchange. The ice model is run on a
global grid that has the North Pole rotated into Greenland, allowing
us to avoid the problem of converging meridians in the Arctic
basin. The model resolution is 3.6 longitude by 1.8 latitude in thepolar region.
[22] The sea ice model is coupled to a very simple slab
mixed layer ocean model to allow for variable ocean temperatures and ice/ocean heat exchange. This slab model is notintended to be a physically complete formulation of the processes affecting ocean mixed layer temperatures but rather ismeant to serve as a simple lower-boundary condition for the sea
ice model. The mixed layer ocean model consists of independent
columns beneath each grid cell in the ice model. The column

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS

3-7

Figure 11. As in Figure 4 but for geostrophic surface wind anomalies. Ice anomalies >10% (10%) are indicatedwith light (dark) shading.

depths vary seasonally as well as spatially, as described below.
The governing equation for the T isðr Cp HÞ dT=dt ¼ Qatm þ Qice þ Qocn ;ð1Þ

where r is the density of seawater, Cp is the heat capacity ofseawater, H is the mixed layer (column) depth, Qatm is the sum ofradiative (longwave plus shortwave) and turbulent (sensible plus
latent) heat fluxes at the ocean-atmosphere interface, Qice is the iceocean heat exchange, and Qocn is the lateral and vertical oceanic
heat exchange not explicitly accounted for in the slab ocean model(e.g., due to ocean currents, entrainment, etc.).
[23] The specifications of H, Qocn, and current velocities in theslab ocean model were obtained as follows. A separate ‘‘equilibrium’’ run was carried out with the ice model coupled to the ocean
general circulation model component of CCSM (see Smith et al.
[1992] for details of the ocean model). This coupled model was run
for 100 years, forced by repeating cycles of observed 6 hourly
surface atmospheric fields during 1984 – 1987 [Large et al., 1997].
Mean annual cycles of H, Qocn, and current velocities at the top
level of the ocean model were computed by averaging the datafrom the last 4 years of the 100 year integration. These quantities
were then employed as lower-boundary conditions for the coupled
ice slab ocean model integration used in this study. The simulated
mixed layer depths and ocean current velocities in the North
Atlantic are in reasonable agreement with observations (notshown).
[24] The coupled ice slab ocean mixed layer model used in thisstudy is driven by observed interannually varying atmosphericforcing: specifically, near-surface air temperatures, humidities, andwinds at 6 hourly resolution from 1948 to 1998 based on data fromthe National Centers for Environmental Prediction (NCEP)/NCAR
Reanalysis Project [Kalnay et al., 1986]. Climatological annual

cycles of cloud cover and precipitation are specified on the basis ofdata from Hahn et al. [1987] and Rossow and Schiffer [1991], andXie and Arkin [1996], respectively. A climatological annual cycleof shortwave radiation is computed according to Bishop et al.
[1997]. Further details on the atmospheric conditions used to force
the model are given by Large et al. [1997].
[25] The imposed wind and air temperature variations impact
the distribution of sea ice thermodynamically through the surface
turbulent energy fluxes, while the imposed wind stresses modify
the ice through dynamical processes such as advection andridging. An additional simulation is performed in which the airtemperature is kept at a climatological annual cycle to isolate therole of direct dynamical wind forcing upon the sea ice field. In all
simulations, ocean mixed layer salinity variations resulting fromice formation and melt do not feed back upon the sea ice
distribution.
[26] It is important to note that in this simulation, sea ice
anomalies may be advected by ocean currents, but the latter containno interannual variability. Mixed layer temperature anomalies, on
the other hand, cannot be advected by ocean currents since there isno lateral communication between adjacent grid cells in the ocean
model (note that the effect of lateral and vertical ocean heatadvection upon the mean annual cycle of mixed layer temperatures
is implicitly accounted for by Qocn). It should also be noted that theformulation of the slab mixed layer model does not allow for any
interannual ‘‘memory’’ in the ocean because of the neglect ofphysical processes such as entrainment and anomalous heat storage
within the permanent and seasonal thermoclines.
[27] Figure 12 shows the modeled sequences of winter sea
ice concentration anomalies during 1972 – 1974, 1983 – 1985, and1990 – 1992, which may be compared to their observationalcounterparts shown in Figure 4. It is immediately apparent thatthe simulated ice anomalies are displaced south and east of theobserved anomalies. This is due to an overly extensive climato-

3-8

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS
ice cover anomalies. Strictly speaking, wind anomalies impact sea
ice through both thermodynamic and dynamic processes; however,
without the accompanying air temperature anomalies the thermodynamic effect of the wind anomalies is negligible compared totheir dynamic influence (not shown). Comparing the simulations
with full and ‘‘wind-only’’ forcing indicates that the direct dynamical effect of anomalous winds accounts for 8% (2%) of thesimulated winter sea ice concentration anomalies in the Davis
Strait (Newfoundland) regions. Thus, in this model, interannual
variations in winter ice cover forced by atmospheric circulation
anomalies are predominantly thermodynamically as opposed to
dynamically driven. This result is consistent with the model
simulations of Ikeda et al. [1988].
[30] As mentioned earlier, the surface wind and air temperature anomalies used to drive the sea ice model may themselves
include a component due to air-sea interaction. In particular, theair temperature anomalies may implicitly contain a direct thermodynamic feedback from the sea ice anomalies (note that
surface air temperatures in the NCEP reanalyses are determined
prognostically over sea ice, with the presence of ice specified
from the same observational archives used in this study). Thus, if
in reality ice cover anomalies result from oceanic processes, their
feedback upon surface air temperatures would be subject tomisinterpretation in our model simulation. Additional experiments, such as a simulation that incorporates anomalous wind
forcing advecting climatological air temperature gradients or one
that couples an atmospheric boundary layer to the ice-ocean
model, are needed to isolate the direct role of atmospheric
thermodynamic forcing.

Figure 12.

As in Figure 4 but for the standard model simulation.

logical mean winter ice cover in the model compared toobservations (not shown). Despite the shift in position themodeled ice anomaly sequences bear a strong resemblance toobservations, both in terms of amplitude and spatial pattern. For
example, a positive ice anomaly extends from the southwest
coast of Greenland to east of Newfoundland in 1972, followedby persistence of the anomaly in the north and enhancement of
the anomaly in the south in 1973, followed by a single positive
anomaly center east of Newfoundland in 1974. This sequence
follows the observations closely. The evolution of ice anomalies
during 1983 – 1985 is also similar to observations, although thesouthward expansion in 1984 relative to 1983 is less pronounced. The observed southward progression of positive ice
anomalies during 1990 – 1992 is not well simulated, although themodel is realistic in terms of persisting the high-ice conditions
through all three winters.
[28] A further comparison of the model and observations isgiven in Figure 13, which shows the winter ice anomaly time series
for the Davis Strait and Newfoundland regions. The correlation
between the observed and simulated ice records is 0.77 for theDavis Strait and 0.72 for Newfoundland, indicating good overall
agreement between the model and observations. In summary, themodel simulates much of the observed winter-to-winter persistence
and spatial evolution of the three main periods of enhanced ice
cover in the Labrador Sea after 1953, suggesting that atmosphericvariability is the main forcing for the sea ice anomaly patterns. This
result is in keeping with the previous studies cited above.
[29] An additional simulation was performed in which the airtemperatures are kept at their climatological annual cycles toisolate the role of direct dynamical wind forcing upon interannual

3.5. SST Simulation[31] Although the ocean model used in this study is highly
simplified, it is of interest to compare the simulated SST anomalies
with observations. What aspects of the observed winter SST
anomaly fields are consistent with the process of anomalous
atmospheric forcing of a simple fixed depth slab mixed layer
ocean? Figure 14 shows the lag correlation maps between theDavis Strait ice index and the SST anomaly fields from the model
for lags 0 – 3 years (see Figure 8 for the maps based uponobservations). At lag 0 the model correlation pattern is similar toobservations, with negative values in the subpolar gyre and positive
values in the western subtropical gyre, although the magnitudes arelarger (we speculate that sampling fluctuations and intrinsic oceanic
mesoscale variability reduce the signal-to-noise ratios and hence
lower the correlations in the observed data). Unlike observations,the model correlations weaken with lag, and by the third year (lag2), only the region directly east of Newfoundland contains significant negative correlations. Thus the simulated correlation map at alag of 2 years deviates substantially from its observational counterpart, which exhibits robust negative correlations in the eastern two
thirds of the subpolar gyre, in addition to a less consistent signal of
positive correlations along the Gulf Stream. The differences in thelagged SST signal in subpolar gyre may reflect the contribution ofoceanic processes not included in the simple slab ocean model. In
particular, we conjecture that anomalous heat storage within the
deep winter mixed layer, which can be reentrained during subsequent winters [cf. Bhatt et al., 1998; Watanabe and Kimoto, 2000;
Deser et al., 2000b], coupled with advection of temperature
anomalies by mean and anomalous ocean currents, may be important for prolonging SST anomalies in the subpolar gyre. Further
simulations are planned with a full ocean general circulation model
to evaluate this scenario.
3.6. Relation of Winter Sea Ice Variability to Upper Ocean
Salinity Anomalies[32] Evidence for decadal variations in upper ocean salinity atsites within the subpolar Atlantic has been presented by several

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS

3-9

Figure 13. Observed (open circles) and simulated (solid circles) winter sea ice indices for (top) Davis Strait and(bottom) Newfoundland. All curves are normalized by their respective standard deviations, and no temporalsmoothing has been applied other than seasonal averaging.
studies, including Dickson et al. [1988], Houghton [1996], Belkin
et al. [1998], and Reverdin et al. [1997]. These studies support thenotion of an advective pathway for freshwater anomalies from theLabrador Sea to the eastern subpolar gyre with a transit time of 4 –5 years. Reverdin et al. [1997] also compared a spatially integrated
measure of salinity anomalies in the subpolar gyre, which incorporates lag associations between the various sites, and winter ice
conditions in the Labrador Sea. They found a strong out-of-phaserelation between this spatially integrated salinity index and Labrador ice cover, such that periods of above-normal ice covercorrespond to freshwater anomalies in the upper ocean and viceversa. Two interpretations were offered for this result: (1) low
salinity in the Labrador Sea is directly (but not causally) associatedwith cold water flowing from the East Greenland Current or
Canadian Arctic, which in turn is conducive to sea ice formation,and (2) low salinity contributes to the near-surface stratificationand therefore winter surface cooling and ice formation [see also
Houghton, 1996]. Here we report on the relation between winter
SIC anomalies in the Davis Strait and salinity variations at 100 m
depth in spring-summer (April – July; data in other months are notconsistently available) off Fylla Bank (64N, 54W), which islocated in the slope region influenced by the West Greenland
Current (see Figure 2 for the location of Fylla Bank; the data
sources are described by Reverdin et al. [1997]). Note that salinity
variations at this site are coherent from 50 to 200 m depth (e.g.,beneath the summer pycnocline) [Reverdin et al., 1997].
[33] As shown in Figure 15, spring – summer freshwater anomalies off Fylla Bank tend to precede and sometimes also follow
winters of above-normal ice cover in the Davis Strait during the1950s, 1970s, 1980s, and 1990s. For example, below-normal
salinity occurs in spring – summer of 1970 and 1971, while
above-normal winter ice cover does not occur until 1972; these
freshwater anomalies persist in spring – summer of 1972 and 1973,
directly following winters of above-normal ice cover. Belownormal salinity also occurs in spring – summer of 1982 and 1989,
6 months before the initial occurrence of above-normal winter ice
cover; these freshwater anomalies then persist in spring – summer
1983 and 1990, respectively (data for 1991 are missing). Similar
behavior is evident during 1993 and 1994 when freshwater
anomalies follow positive SIC anomalies during the previous
winter. Because salinity data are missing in 1956, we cannot
determine whether low salinity leads the high-ice event in 1957 –

3 - 10DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS

Figure 15. Inverted winter Davis Strait ice index (open circles)
and April – July salinity anomalies at 100 m depth in the West
Greenland Current (offshore of Fylla Bank; solid circles). Bothcurves are normalized by their respective standard deviations, andno temporal smoothing has been applied other than seasonal
averaging.
1959; however, below-normal salinity follows above-normal SIC
in spring – summer of 1957 and 1958.
[34] Figure 16 shows the lag cross-correlation curve between
the sea ice and salinity records shown in Figure 15; negative(positive) lags indicate salinity leads (lags) sea ice. Note that thelags are offset from integer years because of the implicit 4 monthlag between the April – July salinity record and the December –March ice index. The strongest negative correlations (significant at
the 95% confidence level) are found at 20, 8, and +4 months,
with a peak value of 0.83 at 8 months.
[35] A plausible physical interpretation of the results is thatspring – summer upper ocean salinity anomalies precondition thewater column for anomalous winter sea ice growth, as well as

Figure 14. As in Figure 8 but for the model simulation.

Figure 16. Lag cross-correlation curve between the Davis Strait
ice index and the April – July salinity record at Fylla Bank based ondata smoothed with a three-point binomial filter. Negative lags
indicate the salinity record leads the ice index.

DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONS
respond to anomalous local ice melt. Specifically, a freshwater
anomaly, by stabilizing the upper ocean, may promote excess
winter cooling, thereby facilitating sea ice growth, all other factors
being equal. The enhanced winter ice cover will then freshen theupper ocean during the ensuing melt season. A similar conclusion
was reached by Marsden et al. [1991], although their lag crosscorrelations were not as strong as those shown here [see also
Mysak et al., 1990; Dickson et al., 1988]. However, as we haveseen, atmospheric forcing appears to be the dominant factor
controlling interannual sea ice variability in the Labrador Sea.
Thus the apparent 8 month lead of freshwater anomalies relative toenhanced ice conditions may not necessarily reflect any causal
connection; rather, we conjecture that anomalous large-scaleatmospheric circulation conditions are responsible for both thesalinity and the ice anomalies.
[36] Additional research is needed to understand the origin of
upper ocean salinity anomalies off Fylla Bank in the West
Greenland Current and their role, if any, in the development ofenhanced winter sea ice cover in the Labrador Sea. The freshwater
anomalies in 1970 and 1971 were likely due in part to the arrivalof the ‘‘Great Salinity Anomaly,’’ a freshwater pulse resulting
from excess wind-driven export of Arctic sea ice through Fram
Strait during the late 1960s, which was subsequently advected into
the Labrador Sea by the East and West Greenland Currents[Dickson et al., 1988]. The causes of the freshwater anomalies
in 1982 and 1989 off Fylla Bank have not been definitively
established: Reverdin et al. [1997] and Belkin et al. [1998] suggestthat their origin may be local to the Labrador Sea/Baffin Bay
region.

4. Summary[37] We have described the evolution of winter ice conditions in
the Labrador Sea during three periods of above-normal ice cover:1972 – 1974, 1983 – 1985, and 1990 – 1992. These winter high-ice
events are notable for their persistence, despite the fact that the ice
margin retreats to northern Baffin Bay each summer, and for their
spatial evolution, progressing from the northern Labrador Sea tothe southern tip of Newfoundland over a three winter period.
Although evidence was found for spring – summer freshwater
anomalies at 100 m depth in the West Greenland Current toprecede by 8 months the occurrence of each period of abovenormal winter ice cover, atmospheric conditions appear to play a
determining role in the anomalous SIC distributions. In particular,
each event of above-normal ice cover is accompanied by stronger
than normal northwesterly winds within the Labrador Sea andoffshore flow east of Newfoundland, consistent with the results ofprevious studies. A sea ice-ocean mixed layer model simulation
was used to quantify the role of surface wind and air temperature
forcing of the anomalous ice conditions during these three events.
Surface atmospheric forcing was found to account for much of thepersistence and spatial evolution of the anomalous ice conditions,with thermodynamic processes dominating over dynamical mechanisms. However, we caution that the use of observed air temperature anomalies (and to a lesser extent observed wind anomalies) todrive the ice-ocean model implicitly incorporates any direct thermodynamic feedback effects of the ice/SST anomalies upon theatmospheric boundary layer. Additional experiments in which
variable wind forcing advects climatological air temperature gradients or a simulation in which an atmospheric boundary layer iscoupled to the ice-ocean model are needed to isolate the direct roleof atmospheric forcing upon sea ice cover.
[38] The observational results indicate that below-normal SSTs
in the subpolar gyre accompany periods of enhanced ice cover.
These SST anomalies persist 1 – 3 years after the decay of ice coveranomalies in the Davis Strait. The ice-ocean model simulates theconcurrent association between ice cover anomalies in the Davis
Strait and SST anomalies over the North Atlantic, suggesting that3 - 11the joint ice/SST anomaly patterns are due to a common large-scaleatmospheric forcing. However, the high persistence of SST anomalies in the subpolar gyre is not well simulated by the simple slab
ocean mixed layer model. This shortcoming may indicate that
oceanic processes not included in the model, such as horizontal
advection and the seasonal cycle of vertical entrainment throughthe base of the mixed layer that can tap the anomalous heat stored
at depth, contribute to the observed SST persistence characteristics.
Comparison of the slab ocean mixed layer simulation to an ocean
general circulation model is required to test these ideas.
[39] Acknowledgments. This study was supported in part by grants
from NSF Physical Oceanography Atlantic Circulation and Climate Experiment to C. Deser and M. Alexander and from the French Programme
National d’Etude du Climat to G. Reverdin. The graphics were producedwith the GrADS software package developed by Brian Doty. We thankMichael Alexander and three anonymous reviewers for helpful comments.

References
Agnew, T., Simultaneous winter sea-ice and atmospheric circulation anomaly patterns, Atmos. Ocean, 31, 259 – 280, 1993.
Belkin, I. M., S. Levitus, J. I. Antonov, and S.-A. Malmberg, ‘‘Great Salinity Anomalies’’ in the North Atlantic, Prog. Oceanogr., 41, 1 – 68, 1998.
Bhatt, U. S., M. A. Alexander, D. S. Battisti, D. D. Houghton, and L. M.
Keller, Atmosphere-ocean interaction in the North Atlantic: Near-surface
variability, J. Clim., 11, 1615 – 1632, 1998.
Bishop, J. K. B., W. B. Rossow, and E. G. Dutton, Surface solar irradiancefrom the international satellite cloud climatology project 1983 – 1991,
J. Geophys. Res., 102, 6883 – 6910, 1997.
Bitz, C. M., and W. H. Lipscomb, An energy-conserving thermodynamic
model of sea ice, J. Geophys. Res., 104, 15,669 – 15,677, 1999.
Bitz, C. M., M. M. Holland, M. Eby, and A. J. Weaver, Simulating the icethickness distribution in a coupled climate model, J. Geophys. Res., 106,2441 – 2463, 2001.
Chapman, W. L., and J. E. Walsh, Recent variations of sea ice and airtemperature in high latitudes, Bull. Am. Meteorol. Soc., 74, 33 – 47, 1993.
Deser, C., and M. Blackmon, Surface climate variations over the North
Atlantic Ocean during winter: 1900 – 1989, J. Clim., 6, 1743 – 1753, 1993.
Deser, C., and M. S. Timlin, Decadal Variations in Sea Ice and Sea Surface
Temperature in the Subpolar North Atlantic: Proceedings of the Atlantic
Climate Change Program Principal Investigators Meeting, edited by
A.-M. Wilburn, Woods Hole Oceanogr. Inst., Woods Hole, Mass., 1996.
Deser, C., J. E. Walsh, and M. S. Timlin, Arctic sea ice variability in thecontext of recent atmospheric circulation trends, J. Clim., 13, 617 – 633,
2000a.
Deser, C., M. A. Alexander, and M. S. Timlin, Re-emergence of winter SST
anomalies in the North Atlantic: 2000 U.S. WOCE report, U.S. WOCE
Implement. Rep.12, 60 pp., U.S. WOCE Off., College Station, Tex., 2000b.
Dickson, R. R., J. Meincke, S.-A. Malmberg, and A. J. Lee, The ‘‘GreatSalinity Anomaly’’ in the northern North Atlantic, 1968 – 1982, Prog.
Oceanogr., 20, 103 – 151, 1988.
Fang, Z., and J. M. Wallace, Arctic sea ice variability on a timescale ofweeks: Its relation to atmospheric forcing, J. Clim., 7, 1897 – 1913, 1994.
Hahn, C. J., S. G. Warren, J. London, R. L. Jenne, and R. M. Chervin,
Climatological data for clouds over the globe from surface observations,
Rep. NDP-026, 56 pp., Carbon Dioxide Inf. Cent., Oak Ridge, Tenn., 1987.
Hibler, W. D., A dynamic thermodynamic sea ice model, J. Phys. Oceanogr., 9, 815 – 846, 1979.
Houghton, R. W., Subsurface quasi-decadal fluctuations in the North Atlantic, J. Clim., 9, 1363 – 1373, 1996.
Hunke, E. C., and J. K. Dukowicz, An elastic-viscous-plastic model for sea
ice dynamics, J. Phys. Oceanogr., 27, 1849 – 1867, 1997.
Ikeda, M., Decadal oscillations of the air-ice-ocean system in the Northern
Hemisphere, Atmos. Ocean, 28, 106 – 139, 1990.
Ikeda, M., T. Yao, and G. Symonds, Simulated fluctuations in annual Labrador Sea ice cover, Atmos. Ocean, 26, 16 – 39, 1988.
Kalnay, E., et al., The NCEP/NCAR reanalysis project, Bull. Am. Meteorol.
Soc., 77, 437 – 471, 1986.
Large, W. G., G. Danabasoglu, S. C. Doney, and J. C. McWilliams, Sensitivity to surface forcing and boundary layer mixing in a global ocean model:
Annual-mean climatology, J. Phys. Oceanogr., 27, 2418 – 2447, 1997.
Marko, J. R., D. B. Fissel, P. Wadhams, P. M. Kelly, and R. D. Brown,
Iceberg severity off eastern North America: Its relationship to sea ice
variability and climate change, J. Clim., 7, 1335 – 1351, 1994.
Marsden, R. F., L. A. Mysak, and R. A. Myers, Evidence for stability
enhancement of sea ice in the Greenland and Labrador Seas, J. Geophys.
Res., 96, 4783 – 4789, 1991.

3 - 12DESER ET AL.: DECADAL LABRADOR SEA ICE AND SST VARIATIONSMysak, L. A., and D. K. Manak, Arctic sea ice extent and anomalies,
1953 – 1984, Atmos. Ocean, 27, 376 – 405, 1989.
Mysak, L. A., D. K. Manak, and R. F. Marsden, Sea ice anomalies
observed in the Greenland and Labrador Seas during 1901 – 1984 andtheir relation to an interdecadal Arctic climate cycle, Clim. Dyn., 5,
111 – 133, 1990.
Mysak, L. A., R. G. Ingram, J. Wang, and A. Van Der Baaren, The anomalous sea-ice extent in Hudson Bay, Baffin Bay and the Labrador Sea
during three simultaneous ENSO and NAO episodes, Atmos. Ocean, 34,
313 – 343, 1996.
Parkinson, C. L., D. J. Cavalieri, P. Gloersen, H. J. Zwally, and J. Comiso,
Arctic sea ice extents, areas and trends, 1978 – 1996, J. Geophys. Res.,
104, 20,837 – 20,856, 1999.
Prinsenberg, S. J., I. K. Peterson, S. Narayanan, and J. U. Umoh, Interaction
between atmosphere, ice cover and ocean off Labrador and Newfoundland from 1962 – 1992, Can. J. Aquat. Sci., 54, 30 – 39, 1997.
Reverdin, G., D. Cayan, and Y. Kushnir, Decadal variability of hydrography in the upper northern North Atlantic in 1948 – 1990, J. Geophys.
Res., 102, 8505 – 8531, 1997.
Rogers, J., C.-C. Wang, and M. J. McHugh, Persistent cold climatic episodes around Greenland and Baffin Island: Links to decadal-scale sea
surface temperature anomalies, Geophys. Res. Lett., 25, 3971 – 3974,
1998.
Rossow, W. B., and R. A. Schiffer, ISCCP cloud data products, Bull. Am.
Meteorol. Soc., 27, 2 – 20, 1991.
Slonosky, V. C., L. A. Mysak, and J. Derome, Linking arctic sea ice andatmospheric circulation anomalies on interannual and decadal time scales,
Atmos. Ocean, 35, 333 – 366, 1997.
Smith, R. D., J. K. Dukowicz, and R. C. Malone, Parallel ocean circulation
modeling, Physica D, 60, 38 – 61, 1992.

Taylor, A. H., and J. A. Stephens, Seasonal and year-to-year variations insurface salinity at the nine North Atlantic Ocean weather stations, Oceanol. Acta, 3, 421 – 430, 1980.
Trenberth, K. E., Some effects of finite sample size and persistence on
meteorological statistics, part I, Autocorrelations, Mon. Weather Rev.,
112, 2359 – 2368, 1984.
Trenberth, K. E., and D. A. Paolino, The Northern Hemisphere sea-levelpressure data set: Trends, errors and discontinuities, Mon. Weather Rev.,
108, 855 – 872, 1980.
Walsh, J. E., and C. M. Johnson, An analysis of arctic sea ice fluctuations,1953 – 1977, J. Phys. Oceanogr., 9, 580 – 591, 1979.
Watanabe, M., and M. Kimoto, On the persistence of decadal SST anomalies in the North Atlantic, J. Clim., 13, 3017 – 3028, 2000.
Woodruff, S. D., R. J. Slutz, R. L. Jenne, and P. M. Steurer, A comprehensive atmosphere-ocean data set, Bull. Am. Meteorol. Soc., 68, 1239 –
1250, 1987.
Xie, P., and P. A. Arkin, Analyses of global monthly precipitation using
gauge observations, satellite estimates, and numerical model predictions,J. Clim., 9, 840 – 858, 1996.



C. Deser and M. Holland, Climate and Global Dynamics Division,
NCAR, PO Box 3000, Boulder, CO 80307-3000, USA. (cdeser@ucar.edu)
G. Reverdin, Laboratoire d’Etudes in Géophysique et Océnographie
Spatiales (LEGOS), GRGS, CNES, 14 Av. E. Belin, 31401 Toulouse Cx 4,France.
M. Timlin, NOAA-CIRES Climate Diagnostics Center, R/CDC1, 325
Broadway, Boulder, CO 80305, USA.