Intermittency of Arctic–mid-latitude teleconnections: stratospheric pathway between autumn sea ice and the winter North Atlantic Oscillation
- 1Geophysical Institute, University of Bergen, Bergen, Norway
- 2Bjerknes Centre for Climate Research, Bergen, Norway
- 3NORCE, Bergen, Norway
Correspondence: Peter Yu Feng Siew (firstname.lastname@example.org)
There is an observed relationship linking Arctic sea ice conditions in autumn to mid-latitude weather the following winter. Of interest in this study is a hypothesized stratospheric pathway whereby reduced sea ice in the Barents and Kara seas enhances upward wave activity and wave-breaking in the stratosphere, leading to a weakening of the polar vortex and a transition of the North Atlantic Oscillation (NAO) to its negative phase. The Causal Effect Networks (CEN) framework is used to explore the stratospheric pathway between late autumn Barents–Kara sea ice and the February NAO, focusing on its seasonal evolution, timescale dependence, and robustness. Results indicate that the pathway is statistically detectable and has been relatively active over the 39-year observational period used here, explaining approximately 26 % of the interannual variability in the February NAO. However, a bootstrap-based resampling test reveals that the pathway is highly intermittent: the full stratospheric pathway appears in only 16 % of the sample populations derived from observations, with individual causal linkages ranging from 46 % to 84 % in occurrence rates. The pathway's intermittency is consistent with the weak signal-to-noise ratio of the atmospheric response to Arctic sea ice variability in modelling experiments and suggests that Arctic–mid-latitude teleconnections might be favoured in certain background states. On shorter timescales, the CEN detects two-way interactions between Barents–Kara sea ice and the mid-latitude circulation that indicate a role for synoptic variability associated with blocking over the Urals region and moist air intrusions from the Euro-Atlantic sector. This synoptic variability has the potential to interfere with the stratospheric pathway, thereby contributing to its intermittency. This study helps quantify the robustness of causal linkages within the stratospheric pathway, and provides insight into which linkages are most subject to sampling issues within the relatively short observational record. Overall, the results should help guide the analysis and design of ensemble modelling experiments required to improve physical understanding of Arctic–mid-latitude teleconnections.
Autumn sea ice is a potential source of skill in predicting the winter North Atlantic Oscillation (NAO) and hence the European climate (Scaife et al., 2014; Wang et al., 2017; Hall et al., 2017). One proposed mechanism for the relationship focuses on the Barents and Kara seas, a region with seasonal ice cover that has exhibited strong negative trends during the cold season over the last decades (Cavalieri and Parkinson, 2012; Serreze and Stroeve, 2015; Onarheim and Årthun, 2017). According to this mechanism, reduced Barents–Kara sea ice triggers a wave response that constructively interferes with the climatological stationary wave pattern (Peings and Magnusdottir, 2014; Kim et al., 2014; Sun et al., 2015; Nakamura et al., 2016; Wu and Smith, 2016; Hoshi et al., 2017; Zhang et al., 2018a; De and Wu, 2019), enhancing upward propagation of planetary waves, which weakens the stratospheric polar vortex (Nishii et al., 2009; Garfinkel et al., 2010; Smith et al., 2010). Downward coupling from the stratosphere to the troposphere subsequently produces circulation anomalies that resemble the negative phase of the NAO or Arctic Oscillation (AO) (Baldwin and Dunkerton, 1999; Polvani and Waugh, 2004), along with its attendant climate effects (Hurrell, 1995).
A delayed stratospheric pathway linking sea ice and the NAO is suggested by observations, but its exact nature is somewhat unclear. The observational evidence (e.g. García-Serrano et al., 2015; King et al., 2016; Koenigk et al., 2016) hinges on lagged correlations, such as the one shown in Fig. 1a (similar to Fig. 10c in García-Serrano et al., 2015, and Fig. 6b in King et al., 2016): less Barents–Kara sea ice in November is associated with higher polar cap heights in the stratosphere (i.e. polar vortex weakening) and a subsequent downward propagation of the height anomalies into the troposphere through the winter season, consistent with the appearance of negative NAO conditions several months later. However, the stationarity and statistical significance of this signal have both been questioned when using longer records that extend back to before the satellite era (Hopsch et al., 2012; Kolstad and Screen, 2019). In fact, the strength and timing of the signal can change when the observational period in Fig. 1a is extended by several additional winters, showing a statistically insignificant autumn sea ice connection to the winter NAO via the stratosphere (Fig. 1b).
Evidence from modelling experiments is even more difficult to interpret because the relationship between Barents–Kara sea ice and the NAO is not robust in simulations. Some studies find a clear stratospheric signal after removing sea ice, leading to a weakening of the polar vortex and a negative NAO (Kim et al., 2014; Nakamura et al., 2015; Sun et al., 2015). A negative NAO response to sea ice loss is also possible, although much weaker, if the stratospheric pathway is not well represented or artificially suppressed (Liptak and Strong, 2014; Sun et al., 2015; Wu and Smith, 2016; Nakamura et al., 2016; Zhang et al., 2018a; De and Wu, 2019). However, other modelling studies show a weak or even positive NAO response when sea ice is reduced (Singarayer et al., 2006; Strey et al., 2010; Orsolini et al., 2012; Cassano et al., 2014; Screen et al., 2014), and we lack a comprehensive understanding of why model results are so different (Screen et al., 2018). One reason may be that the atmospheric response depends on where and when sea ice is removed; for example, some studies have shown that sea ice loss in the Pacific sector leads to a strengthening of the polar vortex (Sun et al., 2015; Screen, 2017; McKenna et al., 2018) and that winter ice loss may be more influential than autumn ice loss in weakening and shifting the jet stream (Blackport and Screen, 2019). Other possible reasons include non-linearities with respect to the amplitude of sea ice loss (Petoukhov and Semenov, 2010; Semenov and Latif, 2015; Chen et al., 2016; Overland et al., 2016) and dependence of the atmospheric response on the background state (Smith et al., 2017, 2019; Labe et al., 2019).
Overall, isolating the sea ice influence on the mid-latitudes remains a challenge in part because it is a search for causal drivers in a tightly coupled system with large internal variability (Shepherd, 2016). This internal atmospheric variability itself has well-known effects on Arctic climate over a range of timescales. Synoptic weather systems carry heat and moisture poleward from the North Atlantic and are associated with moist intrusions that have been shown to warm the Arctic and melt sea ice (Woods et al., 2013; D.-S. R. Park et al., 2015; H.-S. Park et al., 2015; Gong and Luo, 2017; Kim et al., 2017; Lee et al., 2017). Feedbacks between sea ice and the NAO acting on intraseasonal timescales can yield opposite-signed relationships depending on the time lag considered: anomalously low Barents–Kara sea ice concentrations are favoured by positive NAO conditions (Fang and Wallace, 1994; Deser et al., 2000) but are also part of an ice perturbation pattern that has been found to produce negative NAO conditions (Magnusdottir et al., 2004; Deser et al., 2004; Kvamstø et al., 2004; Strong et al., 2009; Deser et al., 2010; Wu and Zhang, 2010). The causality problem with respect to sea ice extends beyond the NAO to other mid-latitude phenomena, such as Eurasian cooling, for which one finds numerous studies arguing both for (Outten and Esau, 2012; Mori et al., 2014, 2019) and against (McCusker et al., 2016; Sorokina et al., 2016; Ogawa et al., 2018; Blackport et al., 2019) sea ice loss being responsible for the recent spate of extreme winters.
In the present study, we revisit the observed relationship between autumn Barents–Kara sea ice and the winter NAO with the goal of quantifying the robustness of the stratospheric linkage. In other words, we ask how systematically the stratospheric linkage has appeared during the satellite period. While sampling issues are unavoidable when using a short observational record with large internal variability, our analysis attempts to account for this by exploring the idea that weak but statistically significant signals may arise from a teleconnection pathway that is only intermittently active.
We begin with a description of data and methods (Sect. 2), including a Causal Effect Networks (CEN) approach that provides a statistical framework for assessing causality (applied to climate problems by studies such as Ebert-Uphoff and Deng, 2012; Runge et al., 2014; Kretschmer et al., 2016, 2018). Results showing that the pathway is indeed detectable but exhibits a high level of intermittency are presented in Sect. 3, and the implications for understanding present-day Arctic–mid-latitude teleconnections are discussed in Sect. 4. We end with some concluding remarks in Sect. 5.
2.1 Reanalysis data
The Causal Effect Networks (CEN) approach requires indices (time series) of variables representing key processes in the dynamical mechanism being studied. In our study, we use sea ice area fraction, surface sensible heat flux, surface latent heat flux, sea level pressure, meridional wind, temperature, geopotential height, and downward thermal radiation at the surface. Raw daily data for the period 1979 to 2018 are from the European Centre for Medium-Range Weather Forecasts (ECMWF) ERA-Interim reanalysis (Dee et al., 2011). The seasonal cycle is removed at each grid point by subtracting the climatological daily mean to obtain anomalies of each variable, and the data are then detrended. The trend is removed through all the days of the year (1 January, 2 January, etc.). The following indices are then calculated from the reanalysis data from September to March.
Barents–Kara sea ice (ICE): sea ice area fraction averaged over 70–80∘ N, 30–105∘ E (Fig. 2a);
Barents–Kara turbulent heat flux (THF): sum of surface sensible and latent heat flux averaged over 70–80∘ N, 30–105∘ E (Fig. 2b), with positive defined as heat flux from the ocean to the atmosphere;
stratospheric polar vortex strength (SPV): negative of geopotential height poleward of 60∘ N (Fig. 2c) averaged between 10 and 100 hPa, as defined by Kretschmer et al. (2016), such that positive values of the index indicate a stronger polar vortex;
Urals sea level pressure (URALS): sea level pressure averaged over 45–70∘ N, 40–85∘ E (Fig. 2d);
downward longwave radiation (IR): downward thermal radiation at the surface averaged over 70–90∘ N (Fig. 2e);
poleward eddy heat flux (): product of V∗ and T∗ at 100 hPa averaged over 45–75∘ N (Fig. 2f), where V and T denote the meridional wind velocity and air temperature, respectively, and the superscript ∗ indicates deviations from the zonal mean;
North Atlantic Oscillation index (NAO): taken from the Climate Prediction Center, based on Rotated Principal Component Analysis of 500 hPa geopotential height (see details at https://www.cpc.ncep.noaa.gov/products/precip/CWlink/pna/nao.shtml, last access: November 2019).
Finally, the daily indices are averaged up to monthly, half-monthly and pentad means for the different analyses carried out in this study.
2.2 Causal Effect Networks (CEN)
The CEN algorithm is a causal inference framework (Runge et al., 2014, 2019) aimed at identifying causal relationships between variables of interest. It was previously used to study Arctic–mid-latitude teleconnections by Kretschmer et al. (2016, 2018). Essentially, given a set of indices such as the ones described above, a CEN is constructed following three steps: (1) identifying potential causal drivers of each index (condition selection), (2) identifying the causal drivers using these potential causal drivers as a “conditioning set”, and (3) quantifying the strength of the causal relationship. We will illustrate the algorithm using January stratospheric polar vortex strength (SPVJan) as an example. Readers are referred to Kretschmer et al. (2018) and Runge et al. (2019) for a full description of the CEN algorithm, also known as PCMCI.
In the first step, we find all possible drivers for SPVJan. A preliminary list of drivers is generated by calculating the Pearson correlation r between SPVJan and all other indices (including SPV itself) in the preceding months, up to a maximum lag of 2 months (i.e. November and December for this example). Indices with significant correlations are retained, where an optimal significance level is determined using the Akaike information criterion (AIC). The AIC results in the selection of a 20 % significance level for the case of SPVJan (note that the AIC allows for these rather liberal significance levels in the first step, but more stringent levels are used later in the second step). This leaves us with the following possible drivers: , URALSDec, SPVDec and URALSNov. This list is sorted in descending order according to the absolute value of the Pearson correlation coefficient. Next, we test for the conditional independence of all four possible drivers with SPVJan by calculating partial correlations, controlling for the effect of each driver one at a time, starting from the top of the sorted list. If a driver passes the partial correlation test, it is retained in the list of possible drivers; if it does not pass, it is removed from the list, meaning it is no longer in the conditioning set. For example, the partial correlation between URALSNov and SPVJan controlling for is, following the notation of Kretschmer et al. (2016):
The partial correlation is significant at the 20 % level (p value =0.105); therefore, URALSNov is retained as a possible driver of SPVJan. After going through the entire list, SPVDec is eliminated, leaving us with three possible drivers of SPVJan: URALSNov, URALSDec, and .
In the second step, we retest all possible links (for all indices in the preceding 2 months, including those rejected in the first step) with SPVJan, controlling for the combined effect of the possible drivers (conditioning set) identified in the first step. This step helps account for false positives when working with highly interdependent time series (as is often the case with climate indices) and enhances detection power (Runge et al., 2019). Specifically, the test for SPVJan is as follows:
where X represents all indices of ICE, THF, URALS, , SPV, and NAO in both November and December. Any X producing a significant partial correlation in Eq. (3) is regarded as a causal driver of SPVJan. The conditioning set excludes X when X is being tested, for example:
which is significant at the 5 % level (p value =0.00629). Testing all of X leaves us with three causal drivers of SPVJan: URALSNov, URALSDec and . Note that these are the same causal drivers identified in the first step, meaning that no new drivers are reintroduced in the second step in this case. As an additional refinement, the Hochberg–Benjamini false discovery rate (FDR) control may be used to account for the multiple testing problem (Kretschmer et al., 2018; Runge et al., 2019).
In the third step, we use a multiple regression equation to quantify the influence of causal drivers and simultaneous influences on SPVJan:
where the β values are regression coefficients for the standardized regressors , , , , and the superscript s indicates a standardized index. The inclusion of Y allows us to check for significant simultaneous relationships between all indices. By standardizing, the interpretation is that changing a certain regressor by one standard deviation changes SPVJan by β standard deviations, provided that all other variables are held fixed.
A two-tailed t test is used for significance testing. For the AIC in step one, a significance set of (5 %, 10 %, 20 %) is used. There are no substantial changes to the main messages when using other significance sets (Fig. S4 in the Supplement). A significance level of 5 % is used in the second and third steps.
The above example illustrates how the CEN algorithm identifies and evaluates causal drivers of SPVJan. In order to construct the complete monthly and half-monthly CENs, we identify causal drivers for all our chosen indices (ICE, THF, URALS, , SPV, and NAO) during the extended winter season (NDJFM). September to December (January to March) indices are taken over the period of 1979 to 2017 (1980 to 2018). All Pearson correlations and partial correlations (first and second steps) and the multiple regressions (third step) are thus based on indices with a sample size of 39 winter seasons. A similar procedure is used for the pentad CEN but with a maximum lag of two pentads to capture processes occurring on synoptic timescales.
This section describes results from our exploration of the ICE–NAO stratospheric pathway using the CEN framework (Sect. 3.1), including an assessment of its strength (Sect. 3.2) and intermittency (Sect. 3.3) in the observational record. We also explore processes occurring on shorter timescales and discuss how these effects may reinforce or interrupt the stratospheric pathway (Sect. 3.4).
3.1 Seasonally evolving ICE–NAO pathway
We begin by examining pathways from Barents–Kara sea ice to the NAO proposed by previous studies. The CEN analysis follows the approach of Kretschmer et al. (2016) but keeps individual months separate rather than considering the DJF period as a whole. This allows us to capture the seasonal evolution of pathways through the cold season.
The CEN (Fig. 3) shows evidence for a stratospheric pathway leading from autumn sea ice perturbations in the Barents and Kara seas to a late winter NAO response. This pathway appears using both monthly (Fig. 3a) and half-monthly (Fig. 3b) averages as input to the CEN, albeit with slight differences in timing. The half-monthly CEN in Fig. 3b is displayed such that individual half-monthly linkages (shown in Fig. S2) are aggregated into full months to allow for direct comparison to Fig. 3a.
Coloured arrows in the network diagrams highlight the ICE–NAO stratospheric pathway, where red indicates positive relationships and blue indicates negative relationships (the exact values correspond to the beta coefficients in the multiple regression equation, e.g. Eq. 5). Grey arrows show other linkages that are statistically significant, including some tropospheric pathways that also contribute to the ICE–NAO relationship. A figure including all the identified causal linkages and autocorrelations appears in the Supplement (Fig. S1). For the monthly CEN, the stratospheric pathway is
where we use the notation A⇒B to indicate index A as a “driver” of index B and ↓ and ↑ to represent a decrease or increase, respectively, of the indices. The pathway is described for the case of a negative sea ice perturbation leading to a negative NAO. For the half-monthly CEN, the pathway may be summarized as follows:
Using the finer half-monthly resolution in the CEN prevents shorter timescale processes (such as linkages through THF) from being averaged out.
The CEN results illustrate how the stratospheric pathway unfolds through the winter season. The timing is in general agreement with previous observational studies, suggesting that the involvement of the stratosphere introduces a few months' delay in the NAO response to Barents–Kara sea ice variability (Kim et al., 2014; García-Serrano et al., 2015; Jaiser et al., 2016; King et al., 2016; Kretschmer et al., 2016; Yang et al., 2016). The causal linkages are consistent with the idea that Arctic sea ice reduction enhances upward wave activity through constructive interference between forced Rossby waves and the climatological stationary waves (Garfinkel et al., 2010; Smith et al., 2010). The resulting increase in wave-breaking in the stratosphere decelerates the polar vortex (Charney and Drazin, 1961), which in turn leads to tropospheric circulation anomalies and surface impacts via downward coupling (Baldwin and Dunkerton, 1999). Some features of the pathway, such as the relatively long lagged relationship of autumn sea ice to December Urals sea level pressure, are not well understood, an issue that will be further discussed in Sect. 4.
We will focus on the stratospheric pathway from ICEOct to NAOFeb in the monthly CEN, as this timing yields the strongest negative ICE–NAO correlation (Fig. S5). The correlation between ICENov and NAOJan is equally strong, but the causal pathway goes through the troposphere only (Fig. S1b) and is not a focus of this study. Results from the half-monthly CEN yield consistent messages and will be brought into the discussion where relevant.
3.2 Strength of the pathway
An interesting question is how to assess the strength of the ICE–NAO stratospheric pathway as a whole, and what insights may be gained by such an assessment.
The CEN analysis yields a set of beta coefficients (colours of the arrows in Fig. 3) that describe the strength of individual causal linkages in our network. Following Runge et al. (2015), the total causal effect of the stratospheric pathway from ICEOct to NAOFeb may be calculated by summing over the product of beta coefficients along the two relevant chains of linkages from Fig. 3a.
The total causal effect () tells us that a single standard deviation perturbation in ICEOct yields a like-signed response of 8 % of a standard deviation in February NAO (Runge et al., 2015). One might question the interpretation of the contemporaneous linkage in the first chain as a causal effect, but the fact that it also shows up in the half-monthly CEN as a linkage from the first half of the December to the second half of December (Fig. S2) supports the point.
A comparison between the stratospheric and tropospheric ICE–NAO pathways shows that the latter are generally stronger in the CEN framework. Table 1 summarizes the causal effect of the three full pathways (Fig. S6). Our main stratospheric pathway of interest from ICEOct to NAOFeb is comparable in strength to the pathway from ICEOct to NAOMar (0.0823 and 0.0872). The latter has both stratospheric and tropospheric chains, accounting for 30 % () and 70 % () of the total causal effect, respectively. The tropospheric pathway is the strongest in terms of the total causal effect (0.137), primarily because it involves fewer linkages. Overall, the larger causal effect of the tropospheric pathways is perhaps unsurprising, given that the stratospheric pathway may be disrupted by internal variability (noise) from both the troposphere and the stratosphere.
An alternative view of the pathway strength comes from considering the amount of February NAO variance explained by the various linkages along the pathway using a multiple linear regression framework. This gives a sense of the relative importance of each linkage and how information passes through the pathway. The full pathway can be represented by the following regression equation:
where κ0 is a constant and κ1, κ2, κ3, and κ4 are the regression coefficients for the standardized regressors ICEOct, URALSDec, and SPVJan, respectively. The importance of the regressors may be quantified in the following different ways.
NAOFeb variance explained by individual regressors, calculated via a simple bivariate regression between each regressor and NAOFeb (blue bars), e.g. for :
reduction in NAOFeb variance explained when individual regressors are removed, calculated by removing the term from the regression equation (green bars), e.g. for :
Both the blue and green bars in Fig. 4 provide a measure of the contribution of individual regressors, while comparison of these with the orange bars gives some indication of whether information from a given regressor is redundant.
The stratospheric pathway explains 26 % of the variance in the February NAO (Fig. 4). The cumulative variance explained (orange bars) increases from 11 % to 26 % as regressors are added (moving from left to right), indicating that each linkage in the pathway adds some useful information. This result is consistent with other estimates from observations but likely represents an upper limit as the Barents–Kara sea ice and NAO relationship is shown to be particularly strong during the current reanalysis period compared to the rest of the 20th century (Kolstad and Screen, 2019).
While successive linkages in the pathway add explanatory power, they are not independent. Comparing the orange and blue bars, we see that the increase in cumulative explained variance moving from left to right is much lower than the explained variance from each individual regressor. For example, while SPVJan explains the most NAO variance of any individual regressor (18 %), its removal from the full regression does not have much effect (3 % reduction in explained variance). However, we know that variability in upward wave activity and variability in the polar vortex are closely related, and thus in a sense it is not physically meaningful to consider one in isolation of the other. Removing both and SPVJan from the regression equation results in a 8 % reduction (not shown) in explained variance, which is perhaps a more representative estimate of the stratosphere's contribution. Sea ice appears to impart information that cannot be explained by the other three regressors (6 % reduction in explained NAO variance when removed), but this may also be a result of atmosphere–ice feedbacks explored in Sect. 3.4.
Overall, these analyses show a role for the stratosphere in connecting autumn ICE to late winter NAO, but it is one that accounts for a modest fraction of the total NAO variance. However, the pathway strength reported here should be considered an estimate, as there remain uncertainties associated with analysis choices, such as the time resolution of the input data and the relevant lags to include. In the next section, we will further explore reasons for this relatively weak ICE–NAO covariability.
3.3 Intermittency of the pathway
The ICE–NAO stratospheric pathway identified by the CEN comprises statistical relationships inferred from a relatively short observational record of only 39 winters. It is meaningful to ask how robust the pathway is, i.e. how systematically the relevant statistical relationships occur in the record. To assess the robustness, we perform a bootstrapping test, where bootstrap samples are created by randomly selecting 39 winters with replacement from the entire reanalysis period. The CEN of each sample is then constructed. This procedure is repeated 10 000 times.
The bootstrapping results (Fig. 5) indicate that the stratospheric pathway is intermittent. Percentages show the occurrence rate of individual segments in the pathway within the bootstrap sample population (see Fig. S7 for occurrence rates of other statistically significant linkages). By this measure, it is clear that individual segments have varying levels of intermittency, ranging from 46 % for the segment to 84 % for the segment . The full stratospheric pathway (the sequence of all four segments) is detected in only 16 % of the samples, suggesting that it does not occur systematically during every winter season. An alternative three-segment pathway is slightly less intermittent (22 % occurrence rate), but its physical interpretation is unclear given that there is no linkage through to the polar vortex, as expected from theory. These intermittency results are a likely reason why detection of the pathway is sensitive to the choice of observational period (Fig. 1), and suggests that it may be favoured in certain background states (Overland et al., 2016; Smith et al., 2017).
The existence of intermittency in the stratospheric pathway is consistent with previous suggestions that internal variability modulates the influence of Arctic sea ice on the mid-latitude circulation (Screen et al., 2014; Overland et al., 2016; Shepherd, 2016). An examination of where in the pathway the intermittency is strongest provides clues to its origins. For example, the upward coupling from sea ice to the stratosphere includes the segments , and , whose occurrence rates are 50 % and 74 %, respectively. The occurrence of these two linkages together is seen in about 41 % out of 10 000 bootstrap samples, meaning that most of the time when the linkage is detected, the subsequent linkage to follows. Conversely, when the linkage is detected, it is preceded by the linkage in only about half the cases. An obvious source of the intermittency in both segments (individually and in terms of their “combined” occurrence rate) is regional sea level pressure (SLP) variability over the Urals related to atmospheric internal variability. Similarly, the downward coupling from SPV to NAO is vulnerable to both stratospheric and tropospheric internal variability, leading to a relatively low occurrence rate of 46 %. This is consistent with the idea that not all polar vortex strengthening and weakening events affect the tropospheric circulation (Karpechko et al., 2017). Most robust is the linkage (84 %), which arises from well-known physical processes related to upward planetary wave flux and polar vortex weakening. Sea ice variability can also contribute to intermittency in the pathway through higher-frequency synoptic processes, a topic we will explore in Sect. 3.4.
The strength of the segments in the pathway also exhibits large variability among the bootstrap samples. This can be seen in histograms of the beta coefficients for all segments in the pathway (Fig. 5). While the beta coefficients exhibit ranges of up to 0.5 for any given segment, the sign is always the same, indicating that the sign of the relationship between variables is robust. The observed beta coefficients (black lines) for the reanalysis period itself fall within the spread of the distributions. Note that the distributions are composed only of samples in which the linkage of interest is detected by the CEN algorithm (i.e. a beta coefficient can be calculated from Eq. 5), which is why some of the distributions appear skewed. This is particularly true for the linkages that are least robust (the first and last segments, for which the observed beta coefficients are towards the weaker end of the distributions). Overall, these results indicate that even when the stratospheric pathway is active, there is substantial interannual variability in how it manifests.
3.4 Synoptic linkages and interactions across timescales
In the monthly CEN analysis, there are simultaneous relationships between Barents–Kara sea ice, Urals sea level pressure, and the NAO (Fig. 6) that point to linkages through shorter timescale synoptic processes. For example, the NAO shows significant negative simultaneous relationships with Barents–Kara sea ice (positive NAO with reduced ice) in December and March, reflecting a well-known pattern of atmospheric forcing on sea ice via anomalies in surface heat fluxes driven by wind and temperature variability (Fang and Wallace, 1994; Deser et al., 2000). Additional simultaneous relationships between sea ice, turbulent heat flux, and Urals sea level pressure are consistent with synoptic features related to cyclones (Boisvert et al., 2016; Wickström et al., 2019) and moist intrusions (Woods et al., 2013; H.-S. Park et al., 2015) entering the Arctic. Moist intrusions in particular appear to occur preferentially during the positive phase of the NAO (Luo et al., 2017) and have been shown to lead to enhanced downward longwave radiation, surface warming, and sea ice reductions (Gong and Luo, 2017; Chen et al., 2018). We explore the possible influences of such events within the CEN framework by using higher-frequency data to capture the relevant synoptic processes. The input data are pentad (5 d) means of Barents–Kara sea ice (ICE), Urals sea level pressure (URALS), and downward longwave radiation (IR). The maximum lag is set to two pentads (10 d) to isolate the synoptic timescale. The results are summarized in Fig. 7 by summing the number of times a linkage appears in each month from Fig. S8. The maximum count for a given linkage in a month is 12 (6 pentads in a month and up to 2-pentad lag considered). Autocorrelation is strong on these short timescales and thus is not used to reject causal linkages in the partial correlation tests.
The CEN detects synoptic-scale influences from the Arctic to the mid-latitudes that reinforce linkages found in the monthly analysis. A linkage from ICE to URALS appears regularly throughout the winter season (Fig. 7a), both indirectly through IR and as a direct connection and in the correct sense to contribute to the linkage shown in the monthly and half-monthly CENs (Fig. 3). The linkage (blue bars, first histogram in Fig. 7a) follows from the idea that sea ice retreat exposes open ocean, which is a local evaporative source for water vapour, leading to a moister, optically thicker atmosphere (Kim and Kim, 2017; Zhong et al., 2018). The linkage (red bars, second histogram in Fig. 7a) is consistent with a suggested mechanism, whereby the resulting surface warming weakens zonal wind locally and promotes blocking over the Urals (Luo et al., 2016). These synoptic processes, if habitually occurring, can imprint onto longer timescales but may also produce interference effects, as seen by the appearance of opposite-signed causal relationships from those described above from time to time through the winter season.
At the same time, causal effects from the mid-latitudes to the Arctic are also detected, consistent with an influence from moisture transport by cyclones or synoptic moist intrusions (Fig. 7b). This is represented by the linkage (most frequently observed in October, January and February) and the linkage (most frequently observed in November, January and February), which reflect the transport of moist air into the dry Arctic atmosphere by the large-scale flow or by cyclones tracking into the Barents Sea. These mid-latitude-to-Arctic linkages have a uniform sign (all red bars in first histogram, all blue bars in second histogram), suggesting that the effect of the relevant processes is rather systematic despite exhibiting month-to-month variability. We also detect a direct linkage from the Urals to Barents–Kara sea ice that can be of either sign. In the slightly more frequent negative sense (), it can be interpreted as a direct effect of warm air advection and mechanical forcing of the ice cover from enhanced southerlies over the Barents–Kara region (Sorokina et al., 2016; McCusker et al., 2016). Together, these synoptic linkages show how Urals SLP variability, which has a large internally generated component, can reinforce or interrupt the ICE–NAO stratospheric pathway.
Given that our understanding of Arctic–mid-latitude teleconnections must account for the combined influences of such linkages across regions and timescales, it is no surprise that we have yet to identify a definitive set of mechanisms. Implications of such scale interactions and how they relate to viewpoints presented in previous studies are further discussed in Sect. 4.
This study quantifies the robustness of atmospheric teleconnections between the Arctic and mid-latitudes, documenting their high level of intermittency in the observational record. In a bootstrapping test, the full stratospheric pathway emerges in only 16 % of the sample populations derived from the observations (Fig. 5). The existence of intermittency is likely why studies using various analytical approaches and time periods find teleconnections that differ in pattern, timing, robustness, and apparent mechanisms (Overland et al., 2016; Francis, 2017; Cohen et al., 2018; Overland and Wang, 2018; Cohen et al., 2020). In this section we discuss some of the factors that may contribute to the intermittency. Of course, anything that influences polar vortex strength is a potential source of intermittency (including internal variability, anthropogenic forcing, tropical variability, etc.), but we focus the discussion on factors that are most directly related to our CEN results.
To be more concrete, the intermittency of the stratospheric pathway stems from the fact that it can be reinforced or interrupted by other processes. For example, reinforcement can come from tropospheric pathways also detected by the CEN algorithm (see Fig. S1a and b):
All these tropospheric and stratospheric pathways lead from the reduction of sea ice to a negative NAO, although they differ slightly in timing. The existence of the tropospheric pathway is supported by sea ice and surface heating perturbation experiments, where negative NAO and AO responses are simulated even when the stratospheric pathway is suppressed (Wu and Smith, 2016) or not well represented (Sun et al., 2015). However, the NAO/AO response is stronger when the stratospheric pathway is active than when it emerges through the tropospheric pathway alone (Nakamura et al., 2016; Zhang et al., 2018a, b).
Another example of a factor that may contribute to intermittency is the El Niño–Southern Oscillation (ENSO). El Niño winters are associated with a deepened Aleutian low, which enhances upward propagating waves, weakens the polar vortex, and favours negative NAO conditions (Domeisen et al., 2019). As such, the stratospheric pathway may be reinforced if an El Niño develops following a low autumn ice season (both are associated with a weakened polar vortex, e.g. winter 1986/87 or 2009/10, Fig. 8); if a La Niña develops instead, the stratospheric pathway may be weakened (e.g. winter 2007/08 or 2010/11, Fig. 8). The relationship between wintertime ENSO and the NAO is rather weak (Brönnimann, 2007; Domeisen et al., 2019), consistent with Fig. 8, which shows high and low NINO3.4 values in both the lower (negative NAO) and upper (positive NAO) quadrants of the scatter plot. Given that we find no systematic phasing of ENSO with Barents–Kara sea ice variability during the reanalysis period, it is likely that ENSO contributes to intermittency in the ICE–NAO pathway.
In terms of reinforcing the stratospheric pathway, blocking over the Urals region seems to play a particularly important but not fully understood role. Enhanced Urals sea level pressure is closely linked to the Scandinavian pattern in Euro-Atlantic climate variability and is related but not directly equivalent to the occurrence of atmospheric blocking. The Urals linkage appears in the monthly CEN ( in Fig. 3a). The latter segment from Urals sea level pressure to poleward eddy heat flux is fairly systematic (appears in 74 % of the bootstrap samples in Fig. 5) and is grounded in the idea that tropospheric precursors over the Urals lead polar vortex weakening (Cohen and Jones, 2011; Cohen et al., 2014). However, the first segment from Barents–Kara sea ice to Urals blocking is more intermittent (appears in 50 % of the bootstrap samples), and whether it is in fact a causal linkage has been questioned by a recent modelling study using ensemble nudging experiments (Peings, 2019). Interestingly, not only Barents–Kara sea ice (Fig. 5e in King et al., 2016) but also ENSO (Fig. 5e and f in King et al., 2018) has been linked to the Scandinavian pattern, which suggests another avenue for ENSO to contribute to intermittency.
The ICE–URALS relationship highlights the complexity of interactions between atmospheric internal variability and Barents–Kara sea ice over a range of timescales. On synoptic scales, the pentad CEN (Fig. 7) shows linkages from reduced sea ice to enhanced Urals sea level pressure but also linkages in the opposite direction (), with Urals sea level pressure altering ice cover via changes in poleward moisture transport that have been tied to synoptic moist intrusions (Woods et al., 2013; Luo et al., 2016; Gong and Luo, 2017; Lee et al., 2017). This chain of linkages can act as a positive feedback on sea ice perturbations but also provides a pathway by which blocking variability (internal to the atmosphere) may interrupt the expected troposphere–stratosphere coupling in response to autumn sea ice (for example, imagine a case where atmospheric conditions inhibit Urals blocking after a low-ice autumn). Furthermore, enhanced Urals blocking and moist intrusions can lead to highly transient perturbations in turbulent heat flux over the Barents and Kara seas. Initially, turbulent heat loss from the ocean is suppressed near the sea ice edge where moist intrusions act to weaken temperature and moisture contrasts between the atmosphere and ocean (Woods et al., 2013; Gong and Luo, 2017). But the heat flux anomaly can become positive (enhanced heat loss from the ocean) after the sea ice melts back in response to the moist intrusion, 1 to 2 weeks later (Woods and Caballero, 2016; Lee et al., 2017). On longer (monthly to seasonal) timescales, there is evidence that atmospheric variability is the main driver of heat flux variability over the Barents and Kara seas both in observations and models (Sorokina et al., 2016; Blackport et al., 2019). This perhaps explains why turbulent heat flux does not show up in the monthly CEN (Fig. 3a) but does show up in the half-monthly CEN (Fig. 3b). Across synoptic to seasonal timescales, it appears that sea ice is best thought of as an intermediary rather than a true boundary forcing, as is implied by prescribed sea ice (e.g. AGCM) experiments.
One outstanding issue involves the mechanisms that have been proposed to explain the linkage, which act on timescales that are inconsistent with the 2-month delay found in observations. For example, reduced sea ice may allow more heating of the atmosphere by the ocean to produce a Rossby wave train with an anomalous high over the Urals region (Honda et al., 2009), but this would be expected to manifest within a matter of days to a week. Alternatively, reduced ice may reduce local baroclinicity, which discourages cyclones from tracking into the Barents and Kara seas and produces an anomalous high due to the relative absence of low-pressure systems (Inoue et al., 2012). This mechanism could introduce some delay between the ice perturbation and sea level pressure perturbation, but a 2-month persistence of such a pattern is unlikely. Finally, reduced ice may increase atmospheric moisture content, leading to increased Eurasian snow cover, diabatic cooling, and anomalously high sea level pressure over the continent (Liu et al., 2012; Cohen et al., 2014; Garcia-Serrano and Frankignoul, 2014). Though this would plausibly lead to persistence on the required timescale, recent observational and modelling studies do not support a role for Eurasian snow in this teleconnection pathway (Kretschmer et al., 2016; Peings et al., 2017; Henderson et al., 2018), and we chose not to include it in our main analyses. Note that these mechanisms may still be responsible for contemporaneous forcing of the winter atmospheric circulation by winter sea ice variability, which has been suggested to be a stronger influence than the forcing by autumn sea ice variability (Blackport and Screen, 2019).
Lastly, our experience with the CEN offers some cautionary notes about its application to climate problems. The CEN approach was designed for hypothesis testing, i.e. to test causal pathways that are thought or known to exist, either from theory or existing evidence. It should not be used as an exploratory data analysis tool to search for causal pathways because the statistics behind the CEN do not know whether relationships are physically meaningful. One specific problem we encountered is that the algorithm may drop an existing causal linkage if a new variable is added. For example, when we introduce downward longwave radiation into the monthly CEN, its strong correlation with sea ice overrides the linkage (see Fig. S9 compared to Fig. S1a). Since many climate variables are highly correlated but not necessarily directly related via specific processes, the CEN’s ability to identify physically meaningful linkages depends critically on the careful selection of input variables.
This study uses the Causal Effect Networks (CEN) framework to quantify the robustness of the stratospheric pathway between late autumn Barents–Kara sea ice and the February NAO, documenting its high level of intermittency in the observational record. The pathway has been relatively active over the satellite period, explaining approximately 26 % of the interannual variability in the February NAO. However, this result is highly sensitive to which winters are included in the analysis. Results from a bootstrapping test show that the full stratospheric pathway appears in only 16 % of the sample populations derived from the observations. The result reflects the strong internal variability of the mid-latitude atmosphere and the likelihood that Arctic–mid-latitude teleconnections may require certain background flow conditions. On synoptic timescales, we identify two-way interactions between Barents–Kara sea ice and the mid-latitude circulation, suggesting a role for atmospheric blocking over the Urals region and moist intrusions, both of which can reduce Barents–Kara sea ice. These synoptic processes can reinforce or interrupt the stratospheric pathway, contributing to intermittency. Finally, we cannot rule out that the causal linkages found on longer timescales may be artefacts of averaging over the synoptic processes or even the result of entirely different mechanisms (Smith et al., 2017; Hell et al., 2020).
Coupled interactions between sea ice and the mid-latitude circulation involve complicated lead–lag feedbacks over a range of timescales. Applying causal inference frameworks such as the CEN can help clarify some of the important physical processes at play, but, in the end, models are required to improve our understanding. A complication is that the fidelity of climate models in representing the relevant processes is difficult to ascertain (King et al., 2016; Smith et al., 2017; Mori et al., 2019), especially those processes at fine spatial and temporal scales and their interactions across scales. However, ways forward are indicated by this study, as well as others (McCusker et al., 2016; Sun et al., 2016; Peings, 2019), that provide insight into which linkages are most robust and which are subject to sampling issues within the relatively short observational record.
The code to construct the figures in this study is available upon request.
ERA-Interim data are provided by European Centre for Medium-Range Weather Forecasts (ECMWF) available online at https://www.ecmwf.int/en/forecasts/datasets/reanalysis-datasets/era-interim (Dee et al., 2011).
The supplement related to this article is available online at: https://doi.org/10.5194/wcd-1-261-2020-supplement.
PYFS conducted the analysis, prepared the figures, and wrote the paper with contributions from all co-authors. CL and SPS conceived of the original idea. CL, SPS, and MPK provided guidance on the interpretation of results.
Camille Li is a member of the editorial board of the journal.
This work was supported by the Research Council of Norway projects 255027 (DynAMiTe) and 272721 (Nansen Legacy). We acknowledge the European Centre for Medium-Range Weather Forecasts for providing the ERA-Interim data. Finally, we thank two anonymous reviewers for insightful suggestions and the Bjerknes storm tracks group for the stimulating discussions, all of which helped improve this study.
This research has been supported by the Research Council of Norway (grant nos. 255027 and 272721).
This paper was edited by Yang Zhang and reviewed by two anonymous referees.
Boisvert, L. N., Petty, A. A., and Stroeve, J. C.: The impact of the extreme winter 2015/16 Arctic cyclone on the Barents–Kara Seas, Mon. Weather Rev., 144, 4279–4287, 2016. a
Cassano, E. N., Cassano, J. J., Higgins, M. E., and Serreze, M. C.: Atmospheric impacts of an Arctic sea ice minimum as seen in the Community Atmosphere Model, Int. J. Climatol., 34, 766–779, 2014. a
Charney, J. G. and Drazin, P. G.: Propagation of planetary-scale disturbances from the lower into the upper atmosphere, J. Geophys. Res., 66, 83–109, 1961. a
Chen, H. W., Zhang, F., and Alley, R. B.: The robustness of midlatitude weather pattern changes due to Arctic sea ice loss, J. Climate, 29, 7831–7849, 2016. a
Chen, X., Luo, D., Feldstein, S. B., and Lee, S.: Impact of winter Ural blocking on Arctic sea ice: short-time variability, J. Climate, 31, 2267–2282, 2018. a
Cohen, J. and Jones, J.: Tropospheric precursors and stratospheric warmings, J. Climate, 24, 6562–6572, 2011. a
Cohen, J., Zhang, X., Francis, J., Jung, T., Kwok, R., Overland, J., Tayler, P. C., Lee, S., Laliberte, F., Feldstein, S., Maslowski, W., Henderson, G., Stroeve, J., Coumou, D., Handorf, D., Semmler, T., Ballinger, T., Hell, M., Kretschmer, M., Vavrus, S., Wang, M., Wang, S., Wu, Y., Vihma, T., Bhatt, U., Ionita, M., Linderholm, H., Rigor, I., Routson, C., Singh, D., Wendisch, M., Smith, D., Screen, J., Yoon, J., Peings, Y., Chen, H., and Blackport, R.: Arctic change and possible influence on mid-latitude climate and weather, US CLIVAR Report, 1, CLIVAR Project Office, Washington, D.C., USA, https://doi.org/10.5065/D6TH8KGW, 2018. a
Cohen, J., Zhang, X., Francis, J., Jung, T., Kwok, R., Overland, J., Ballinger, T. J., Bhatt, U. S., Chen, H. W., Coumou, D., Feldstein, S., Gu, H., Handorf, D., Henderson, G., Ionita, M., Kretschmer, M., Laliberte, F., Lee, S., Linderholm, H. W., Maslowski, W., Peings, Y., Pfeiffer, K., Rigor, I., Semmler, T., Stroeve, J., Taylor, P. C., Vavrus, S., Vihma, T., Wang, S., Wendisch, M., Wu, Y., and Yoon, J.: Divergent consensuses on Arctic amplification influence on midlatitude severe winter weather, Nat. Clim. Change, 10, 20–29, 2020. a
Dee, D. P., Uppala, S. M., Simmons, A. J., Berrisford, P., Poli, P., Kobayashi, S., Andrae, U., Balmaseda, M. A., Balsamo, G., Bauer, P., Bechtold, P., Beljaars, A. C. M., van de Berg, L., Bidlot, J., Bormann, N., Delsol, C., Dragani, R., Fuentes, M., Geer, A. J., Haimberger, L., Healy, S. B., Hersbach, H., Hólm, E. V., Isaksen, L., Kållberg, P., Köhler, M., Matricardi, M., McNally, A. P., Monge-Sanz, B. M., Morcrette, J.-J., Park, B.-K., Peubey, C., de Rosnay, P., Tavolato, C., Thépaut, J.-N., and Vitart, F.: The ERA-Interim reanalysis: Configuration and performance of the data assimilation system, Q. J. Roy. Meteor. Soc., 137, 553–597, https://doi.org/10.1002/qj.828, 2011 (data available at: https://www.ecmwf.int/en/forecasts/datasets/reanalysis-datasets/era-interim, last access: November 2019). a, b
Deser, C., Magnusdottir, G., Saravanan, R., and Phillips, A.: The effects of North Atlantic SST and sea ice anomalies on the winter circulation in CCM3. Part II: Direct and indirect components of the response, J. Climate, 17, 877–889, 2004. a
Deser, C., Tomas, R., Alexander, M., and Lawrence, D.: The seasonal atmospheric response to projected Arctic sea ice loss in the late twenty-first century, J. Climate, 23, 333–351, 2010. a
Ebert-Uphoff, I. and Deng, Y.: Causal discovery for climate research using graphical models, J. Climate, 25, 5648–5665, 2012. a
Francis, J. A.: Why are Arctic linkages to extreme weather still up in the air?, B. Am. Meteorol. Soc., 98, 2551–2557, 2017. a
Garcia-Serrano, J. and Frankignoul, C.: Retraction: High predictability of the winter Euro–Atlantic climate from cryospheric variability, Nat. Geosci., 7, E2, https://doi.org/10.1038/ngeo2118, 2014. a
García-Serrano, J., Frankignoul, C., Gastineau, G., and De La Càmara, A.: On the predictability of the winter Euro-Atlantic climate: lagged influence of autumn Arctic sea ice, J. Climate, 28, 5195–5216, 2015. a, b, c
Hall, R. J., Scaife, A. A., Hanna, E., Jones, J. M., and Erdélyi, R.: Simple statistical probabilistic forecasts of the winter NAO, Weather Forecast., 32, 1585–1601, 2017. a
Hell, M. C., Schneider, T., and Li, C.: Atmospheric Circulation Response to Short-Term Arctic Warming in an Idealized Model, J. Atmos. Sci., 77, 531–549, 2020. a
Henderson, G. R., Peings, Y., Furtado, J. C., and Kushner, P. J.: Snow–atmosphere coupling in the Northern Hemisphere, Nat. Clim. Change, 8, 954–963, 2018. a
Hopsch, S., Cohen, J., and Dethloff, K.: Analysis of a link between fall Arctic sea ice concentration and atmospheric patterns in the following winter, Tellus A, 64, 18624, https://doi.org/10.3402/tellusa.v64i0.18624, 2012. a
Hoshi, K., Ukita, J., Honda, M., Iwamoto, K., Nakamura, T., Yamazaki, K., Dethloff, K., Jaiser, R., and Handorf, D.: Poleward eddy heat flux anomalies associated with recent Arctic sea ice loss, Geophys. Res. Lett., 44, 446–454, 2017. a
Hurrell, J. W.: Decadal trends in the North Atlantic Oscillation: regional temperatures and precipitation, Science, 269, 676–679, 1995. a
Inoue, J., Hori, M. E., and Takaya, K.: The role of Barents Sea ice in the wintertime cyclone track and emergence of a warm-Arctic cold-Siberian anomaly, J. Climate, 25, 2561–2568, 2012. a
Jaiser, R., Nakamura, T., Handorf, D., Dethloff, K., Ukita, J., and Yamazaki, K.: Atmospheric winter response to Arctic sea ice changes in reanalysis data and model simulations, J. Geophys. Res.-Atmos., 121, 7564–7577, 2016. a
Karpechko, A. Y., Hitchcock, P., Peters, D. H., and Schneidereit, A.: Predictability of downward propagation of major sudden stratospheric warmings, Q. J. Roy. Meteor. Soc., 143, 1459–1470, 2017. a
Kim, B.-M., Son, S.-W., Min, S.-K., Jeong, J.-H., Kim, S.-J., Zhang, X., Shim, T., and Yoon, J.-H.: Weakening of the stratospheric polar vortex by Arctic sea-ice loss, Nat. Commun., 5, 4646, https://doi.org/10.1038/NCOMMS5646, 2014. a, b, c
Kim, B.-M., Hong, J.-Y., Jun, S.-Y., Zhang, X., Kwon, H., Kim, S.-J., Kim, J.-H., Kim, S.-W., and Kim, H.-K.: Major cause of unprecedented Arctic warming in January 2016: Critical role of an Atlantic windstorm, Sci. Rep., 7, 40051, https://doi.org/10.1038/srep40051, 2017. a
Kim, H.-M. and Kim, B.-M.: Relative contributions of atmospheric energy transport and sea ice loss to the recent warm Arctic winter, J. Climate, 30, 7441–7450, 2017. a
King, M. P., Hell, M., and Keenlyside, N.: Investigation of the atmospheric mechanisms related to the autumn sea ice and winter circulation link in the Northern Hemisphere, Clim. Dynam., 46, 1185–1195, 2016. a, b, c, d, e
King, M. P., Herceg-Bulić, I., Bladé, I., García-Serrano, J., Keenlyside, N., Kucharski, F., Li, C., and Sobolowski, S.: Importance of late fall ENSO teleconnection in the Euro-Atlantic sector, B. Am. Meteorol. Soc., 99, 1337–1343, 2018. a
Koenigk, T., Caian, M., Nikulin, G., and Schimanke, S.: Regional Arctic sea ice variations as predictor for winter climate conditions, Clim. Dynam., 46, 317–337, 2016. a
Kolstad, E. and Screen, J.: Non-Stationary Relationship between Autumn Arctic Sea Ice and the Winter North Atlantic Oscillation, Geophys. Res. Lett., 46, 7583–7591, https://doi.org/10.1029/2019GL083059, 2019. a, b
Kretschmer, M., Coumou, D., Donges, J. F., and Runge, J.: Using causal effect networks to analyze different Arctic drivers of midlatitude winter circulation, J. Climate, 29, 4069–4081, 2016. a, b, c, d, e, f, g
Kretschmer, M., Cohen, J., Matthias, V., Runge, J., and Coumou, D.: The different stratospheric influence on cold-extremes in Eurasia and North America, npj Climate and Atmospheric Science, 1, 1–10, 2018. a, b, c, d
Kvamstø, N. G., Skeie, P., and Stephenson, D. B.: Impact of Labrador sea-ice extent on the North Atlantic Oscillation, Int. J. Climatol., 24, 603–612, 2004. a
Labe, Z., Peings, Y., and Magnusdottir, G.: The Effect of QBO Phase on the Atmospheric Response to Projected Arctic Sea Ice Loss in Early Winter, Geophys. Res. Lett., 46, 7663–7671, 2019. a
Lee, S., Gong, T., Feldstein, S. B., Screen, J. A., and Simmonds, I.: Revisiting the cause of the 1989–2009 Arctic surface warming using the surface energy budget: downward infrared radiation dominates the surface fluxes, Geophys. Res. Lett., 44, 10–654, 2017. a, b, c
Liptak, J. and Strong, C.: The winter atmospheric response to sea ice anomalies in the Barents Sea, J. Climate, 27, 914–924, 2014. a
Liu, J., Curry, J. A., Wang, H., Song, M., and Horton, R. M.: Impact of declining Arctic sea ice on winter snowfall, P. Natl. Acad. Sci. USA, 109, 4074–4079, 2012. a
Luo, B., Luo, D., Wu, L., Zhong, L., and Simmonds, I.: Atmospheric circulation patterns which promote winter Arctic sea ice decline, Environ. Res. Lett., 12, 054017, https://doi.org/10.1088/1748-9326/aa69d0, 2017. a
Luo, D., Xiao, Y., Diao, Y., Dai, A., Franzke, C. L., and Simmonds, I.: Impact of Ural blocking on winter warm Arctic–cold Eurasian anomalies. Part II: The link to the North Atlantic Oscillation, J. Climate, 29, 3949–3971, 2016. a, b
Magnusdottir, G., Deser, C., and Saravanan, R.: The effects of North Atlantic SST and sea ice anomalies on the winter circulation in CCM3. Part I: Main features and storm track characteristics of the response, J. Climate, 17, 857–876, 2004. a
McKenna, C. M., Bracegirdle, T. J., Shuckburgh, E. F., Haynes, P. H., and Joshi, M. M.: Arctic sea ice loss in different regions leads to contrasting Northern Hemisphere impacts, Geophys. Res. Lett., 45, 945–954, 2018. a
Mori, M., Watanabe, M., Shiogama, H., Inoue, J., and Kimoto, M.: Robust Arctic sea-ice influence on the frequent Eurasian cold winters in past decades, Nat. Geosci., 7, 869–873, 2014. a
Mori, M., Kosaka, Y., Watanabe, M., Nakamura, H., and Kimoto, M.: A reconciled estimate of the influence of Arctic sea-ice loss on recent Eurasian cooling, Nat. Clim. Change, 9, 123–129, https://doi.org/10.1038/s41558-018-0379-3, 2019. a, b
Nakamura, T., Yamazaki, K., Iwamoto, K., Honda, M., Miyoshi, Y., Ogawa, Y., and Ukita, J.: A negative phase shift of the winter AO/NAO due to the recent Arctic sea-ice reduction in late autumn, J. Geophys. Res.-Atmos., 120, 3209–3227, 2015. a
Nakamura, T., Yamazaki, K., Iwamoto, K., Honda, M., Miyoshi, Y., Ogawa, Y., Tomikawa, Y., and Ukita, J.: The stratospheric pathway for Arctic impacts on midlatitude climate, Geophys. Res. Lett., 43, 3494–3501, 2016. a, b, c
Nishii, K., Nakamura, H., and Miyasaka, T.: Modulations in the planetary wave field induced by upward-propagating Rossby wave packets prior to stratospheric sudden warming events: A case-study, Q. J. Roy. Meteor. Soc., 135, 39–52, 2009. a
Ogawa, F., Keenlyside, N., Gao, Y., Koenigk, T., Yang, S., Suo, L., Wang, T., Gastineau, G., Nakamura, T., Cheung, H. N., Omrani, N., Ukita, J., and Semenov, V.: Evaluating impacts of recent Arctic sea ice loss on the northern hemisphere winter climate change, Geophys. Res. Lett., 45, 3255–3263, 2018. a
Onarheim, I. H. and Årthun, M.: Toward an ice-free Barents Sea, Geophys. Res. Lett., 44, 8387–8395, 2017. a
Orsolini, Y. J., Senan, R., Benestad, R. E., and Melsom, A.: Autumn atmospheric response to the 2007 low Arctic sea ice extent in coupled ocean–atmosphere hindcasts, Clim. Dynam., 38, 2437–2448, 2012. a
Outten, S. and Esau, I.: A link between Arctic sea ice and recent cooling trends over Eurasia, Climatic Change, 110, 1069–1075, 2012. a
Overland, J. E. and Wang, M.: Arctic-midlatitude weather linkages in North America, Polar Sci., 16, 1–9, 2018. a
Overland, J. E., Dethloff, K., Francis, J. A., Hall, R. J., Hanna, E., Kim, S.-J., Screen, J. A., Shepherd, T. G., and Vihma, T.: Nonlinear response of mid-latitude weather to the changing Arctic, Nat. Clim. Change, 6, 992–999, 2016. a, b, c, d
Park, D.-S. R., Lee, S., and Feldstein, S. B.: Attribution of the recent winter sea ice decline over the Atlantic sector of the Arctic Ocean, J. Climate, 28, 4027–4033, 2015. a
Peings, Y. and Magnusdottir, G.: Response of the wintertime Northern Hemisphere atmospheric circulation to current and projected Arctic sea ice decline: A numerical study with CAM5, J. Climate, 27, 244–264, 2014. a
Peings, Y., Douville, H., Colin, J., Martin, D. S., and Magnusdottir, G.: Snow–(N) AO teleconnection and its modulation by the Quasi-Biennial Oscillation, J. Climate, 30, 10211–10235, 2017. a
Petoukhov, V. and Semenov, V. A.: A link between reduced Barents-Kara sea ice and cold winter extremes over northern continents, J. Geophys. Res.-Atmos., 115, D21111, https://doi.org/10.1029/2009JD013568, 2010. a
Polvani, L. M. and Waugh, D. W.: Upward wave activity flux as a precursor to extreme stratospheric events and subsequent anomalous surface weather regimes, J. Climate, 17, 3548–3554, 2004. a
Runge, J., Petoukhov, V., and Kurths, J.: Quantifying the strength and delay of climatic interactions: The ambiguities of cross correlation and a novel measure based on graphical models, J. Climate, 27, 720–739, 2014. a, b
Runge, J., Petoukhov, V., Donges, J. F., Hlinka, J., Jajcay, N., Vejmelka, M., Hartman, D., Marwan, N., Paluš, M., and Kurths, J.: Identifying causal gateways and mediators in complex spatio-temporal systems, Nat. Commun., 6, 1–10, 2015. a, b
Runge, J., Nowack, P., Kretschmer, M., Flaxman, S., and Sejdinovic, D.: Detecting and quantifying causal associations in large nonlinear time series datasets, Sci. Adv., 5, eaau4996, https://doi.org/10.1126/sciadv.aau4996, 2019. a, b, c, d
Scaife, A. A., Arribas, A., Blockley, E., Brookshaw, A., Clark, R. T., Dunstone, N., Eade, R., Fereday, D., Folland, C. K., Gordon, M., Hermanson, L., Knight, J. R., Lea, D. J., MacLachlan, C., Maidens, A., Martin, M., Peterson, A. K., Smith, D., Vellinga, M., Wallace, E., Waters, J., and Williams, A.: Skillful long-range prediction of European and North American winters, Geophys. Res. Lett., 41, 2514–2519, 2014. a
Screen, J. A.: Simulated atmospheric response to regional and pan-Arctic sea ice loss, J. Climate, 30, 3945–3962, 2017. a
Screen, J. A., Deser, C., Simmonds, I., and Tomas, R.: Atmospheric impacts of Arctic sea-ice loss, 1979–2009: Separating forced change from atmospheric internal variability, Clim. Dynam., 43, 333–344, 2014. a, b
Screen, J. A., Deser, C., Smith, D. M., Zhang, X., Blackport, R., Kushner, P. J., Oudar, T., McCusker, K. E., and Sun, L.: Consistency and discrepancy in the atmospheric response to Arctic sea-ice loss across climate models, Nat. Geosci., 11, 155–163, https://doi.org/10.1038/s41561-018-0059-y, 2018. a
Semenov, V. A. and Latif, M.: Nonlinear winter atmospheric circulation response to Arctic sea ice concentration anomalies for different periods during 1966–2012, Environ. Res. Lett., 10, 054020, https://doi.org/10.1088/1748-9326/10/5/054020, 2015. a
Serreze, M. C. and Stroeve, J.: Arctic sea ice trends, variability and implications for seasonal ice forecasting, Philos. T. Roy. Soc. A, 373, 20140159, https://doi.org/10.1098/rsta.2014.0159, 2015. a
Singarayer, J. S., Bamber, J. L., and Valdes, P. J.: Twenty-first-century climate impacts from a declining Arctic sea ice cover, J. Climate, 19, 1109–1125, 2006. a
Smith, D. M., Dunstone, N. J., Scaife, A. A., Fiedler, E. K., Copsey, D., and Hardiman, S. C.: Atmospheric response to Arctic and Antarctic sea ice: The importance of ocean–atmosphere coupling and the background state, J. Climate, 30, 4547–4565, 2017. a, b, c, d
Smith, D. M., Screen, J. A., Deser, C., Cohen, J., Fyfe, J. C., García-Serrano, J., Jung, T., Kattsov, V., Matei, D., Msadek, R., Peings, Y., Sigmond, M., Ukita, J., Yoon, J.-H., and Zhang, X.: The Polar Amplification Model Intercomparison Project (PAMIP) contribution to CMIP6: investigating the causes and consequences of polar amplification, Geosci. Model Dev., 12, 1139–1164, https://doi.org/10.5194/gmd-12-1139-2019, 2019. a
Sorokina, S. A., Li, C., Wettstein, J. J., and Kvamstø, N. G.: Observed atmospheric coupling between Barents Sea ice and the warm-Arctic cold-Siberian anomaly pattern, J. Climate, 29, 495–511, 2016. a, b, c
Strey, S. T., Chapman, W. L., and Walsh, J. E.: The 2007 sea ice minimum: Impacts on the Northern Hemisphere atmosphere in late autumn and early winter, J. Geophys. Res.-Atmos., 115, D23103, https://doi.org/10.1029/2009JD013294, 2010. a
Strong, C., Magnusdottir, G., and Stern, H.: Observed feedback between winter sea ice and the North Atlantic Oscillation, J. Climate, 22, 6021–6032, 2009. a
Sun, L., Perlwitz, J., and Hoerling, M.: What caused the recent “Warm Arctic, Cold Continents” trend pattern in winter temperatures?, Geophys. Res. Lett., 43, 5345–5352, 2016. a
Wickström, S., Jonassen, M., Vihma, T., and Uotila, P.: Trends in cyclones in the high-latitude North Atlantic during 1979–2016, Q. J. Roy. Meteor. Soc., 146, 762–779, https://doi.org/10.1002/qj.3707, 2019. a
Woods, C. and Caballero, R.: The role of moist intrusions in winter Arctic warming and sea ice decline, J. Climate, 29, 4473–4485, 2016. a
Wu, Q. and Zhang, X.: Observed forcing-feedback processes between Northern Hemisphere atmospheric circulation and Arctic sea ice coverage, J. Geophys. Res.-Atmos., 115, D14119, https://doi.org/10.1029/2009JD013574, 2010. a
Yang, X.-Y., Yuan, X., and Ting, M.: Dynamical link between the Barents–Kara sea ice and the Arctic Oscillation, J. Climate, 29, 5103–5122, 2016. a
Zhang, P., Wu, Y., and Smith, K. L.: Prolonged effect of the stratospheric pathway in linking Barents-Kara Sea sea ice variability to the midlatitude circulation in a simplified model, Clim. Dynam., 50, 527–539, 2018a. a, b, c
Zhang, P., Wu, Y., Simpson, I. R., Smith, K. L., Zhang, X., De, B., and Callaghan, P.: A stratospheric pathway linking a colder Siberia to Barents-Kara Sea sea ice loss, Sci. Adv., 4, eaat6025, https://doi.org/10.1126/sciadv.aat6025, 2018b. a
Zhong, L., Hua, L., and Luo, D.: Local and external moisture sources for the Arctic warming over the Barents–Kara seas, J. Climate, 31, 1963–1982, 2018. a