Articles | Volume 10, issue 4
Review article
21 Dec 2018
Review article |  | 21 Dec 2018

Reconciling North Atlantic climate modes: revised monthly indices for the East Atlantic and the Scandinavian patterns beyond the 20th century

Laia Comas-Bru and Armand Hernández

Climate variability in the North Atlantic sector is commonly ascribed to the North Atlantic Oscillation. However, recent studies have shown that taking into account the second and third mode of variability (namely the East Atlantic – EA – and the Scandinavian – SCA – patterns) greatly improves our understanding of their controlling mechanisms, as well as their impact on climate. The most commonly used EA and SCA indices span the period from 1950 to present, which is too short, for example, to calibrate palaeoclimate records or assess their variability over multi-decadal scales. To tackle this, here, we create new EOF-based (empirical orthogonal function) monthly EA and SCA indices covering the period from 1851 to present, and compare them with their equivalent instrumental indices. We also review and discuss the value of these new records and provide insights into the reasons why different sources of data may give slightly different time series. Furthermore, we demonstrate that using these patterns to explain climate variability beyond the winter season needs to be done carefully due to their non-stationary behaviour. The datasets are available at

1 Introduction

The spatial structure of regional climate variability follows recurrent patterns often referred to as modes of climate variability or teleconnections, which provide a simplified description of the climate system (Trenberth and Jones, 2007). For example, a considerable fraction of inter-annual climate variability in the Northern Hemisphere is often ascribed to the North Atlantic Oscillation (NAO), which represents the principal mode of winter climate variability across much of the North Atlantic sector (Hurrell, 1995; Wanner et al., 2001; Hurrell and Deser, 2010) and explains ca. 40 % of the winter sea-level pressure (SLP) variability in the region (Pinto and Raible, 2012). However, considering other modes of variability that have historically received less attention better explains the overall regional SLP and climate variability. In particular, the East Atlantic (EA) and the Scandinavian (SCA) patterns have been demonstrated to significantly influence the winter European climate (Comas-Bru and McDermott, 2014; Hall and Hanna, 2018) as well as the sensitivity of climate variables such as temperature and precipitation to the NAO. Furthermore, the interplay of these modes exerts a strong impact on climates at different spatio-temporal scales and has important ecological and societal impacts (e.g. Jerez and Trigo, 2013; Bastos et al., 2016) as well as impacts on the availability of, for example, wind energy resources (Zubiate et al., 2017).

In particular, the NAO consists of a north–south dipole of SLP anomalies resulting from the co-occurrence of the Azores High and the Icelandic Low (Hurrell, 1995) and modulates the extratropical zonal flow. Its varying strength is indicated by swings between positive and negative phases that produce large changes in surface air temperature, winds, storminess and precipitation across Eurasia, northern Africa, Greenland and North America (Hurrell and Deser, 2010). The NAO is commonly described by an index calculated as the difference in normalised SLP over Iceland and the Azores (Cropper et al., 2015; Rogers, 1984), Lisbon (Hurrell and van Loon, 1997) or Gibraltar (Jones et al., 1997), but there are a number of robust alternatives to this classical definition of the NAO index such as empirical orthogonal function analysis (EOF; Folland et al., 2009).

The second mode of climate variability in the North Atlantic region, the EA pattern, was originally identified in the EOF analysis of Barnston and Livezey (1987) and the exact representation of its EOF loadings is still a matter of debate. Some authors describe the EA as a north–south dipole of anomaly centres spanning the North Atlantic from east to west (Bastos et al., 2016; Chafik et al., 2017), while others characterise it as a well-defined SLP monopole south of Iceland and west of Ireland, near 52.5 N, 22.5 W (Josey and Marsh, 2005; Moore and Renfrew, 2012; Comas-Bru and McDermott, 2014; Zubiate et al., 2017). However, regardless of its exact spatial structure, the location of its main centre of action is, in all cases, along the nodal line of the NAO, often implying a southward shifted NAO with the corresponding North Atlantic storm track and jet stream also shifted towards lower latitudes (Woollings et al., 2010). The most common methods to obtain an index for the EA are EOF analyses (Barnston and Livezey, 1987; Comas-Bru and McDermott, 2014; Moore et al., 2013) or rotated principal component analysis (RPCA; CPC, 2012), but the SLP instrumental series from Valentia Observatory, Ireland (51.93 N, 10.23 W), has also been used in a limited number of studies (Comas-Bru et al., 2016; Moore and Renfrew, 2012). Here we use the positive phase of the EA as a strong centre of positive SLP anomalies offshore Ireland. This is associated with below-average surface temperatures in southern Europe, drier conditions over western Europe and wetter conditions across much of eastern Europe and the Norwegian coast (Moore et al., 2011; Rodríguez-Puebla and Nieto, 2010).

The SCA pattern is usually defined as the third leading mode of winter SLP variability in the European region and is equivalent to the Eurasia-1 pattern described by Barnston and Livezey (1987). It shows a vigorous centre at 60–70 N, 25–50 E, with some studies showing a more diffuse centre of opposite sign south of Greenland. As far as we are aware, only EOF analyses (Comas-Bru and McDermott, 2014; Crasemann et al., 2017; Moore et al., 2013; Hall and Hanna, 2018) and rotated principal component analysis (Bueh and Nakamura, 2007; CPC, 2012) have been used to obtain a temporal index of the SCA. The positive phase of the SCA is related to higher than average pressure anomalies over Fennoscandia, western Russia, and in some cases northern Europe, which may lead to a blocking situation that results in winter dry conditions over the Scandinavian region, below-average temperatures across central Russia and western Europe and wet conditions in southern Europe (CPC, 2012; Bueh and Nakamura, 2007; Crasemann et al., 2017; Scherrer et al., 2005).

To the best of our knowledge, while NAO indices are available from a wide variety of sources such as the Climate Prediction Center, CPC-NOAA (, last access date: 5 December 2018); the Climate Data Guide (, last access date: 5 December 2018); and the Climate Research Unit, University of East Anglia, CRU-UEA (, last access date: 5 December 2018), only the CPC-NOAA provides EA and SCA indices and, in both cases, they only cover the period since 1950. Along the same lines, the NOAA-CIRE (, last access date: 5 December 2018) provides a set of climate indices created with the Twentieth Century Reanalysis Project version 2c (20CRv2c) dataset (Compo et al., 2011), but the EA and the SCA are not included. This urges scientists willing to use a longer EA and/or SCA index to do their own EOF analyses, thereby increasing the likelihood that different studies will use EOF-based EA and SCA indices that may be based on a different geographical area (i.e. North Atlantic versus Northern Hemisphere), months (i.e. winter versus annual) or time periods, while at the same time increasing the likelihood of computational discrepancies. Therefore, making long monthly EOF-based indices of the EA and SCA readily available will probably contribute to an increased consistency across research studies such as those that aim at calibrating proxy-based records of past climate variability.

Table 1List of the meteorological stations used to construct the monthly instrumental indices. Daily data downloaded from the European Climate Assessment and Dataset (ECA&D; Klein Tank et al., 2002) are available at (last access: 6 February 2018). In April 2012 the manual station at Valentia was replaced by an automatic station at the same site (Met Éireann, personal communication, 2017).

Download Print Version | Download XLSX

On the other hand, station-based indices have the advantage of providing continuous records that may extend back beyond the 20th century, when reanalysis data are more scarce (Cropper et al., 2015). However, the main compromises of such methodology are that (i) using station-based indices implies a fixed location of the mode's centres of action, even though non-stationarities in the geographical location of such centres, in particular those of the NAO, have been widely demonstrated (Blade et al., 2012; Lehner et al., 2012); (ii) the SLP recorded by meteorological stations may not be regionally representative due to local biases (i.e. artificial changes in their local environments; Pielke et al., 2007); and (iii) early SLP recordings may be compromised by the use of less reliable old instrumental devices (Aguilar et al., 2003; Trewin, 2010). By contrast, while EOF-based indices better capture the inter-annual variability in an area larger than the exact location of the centres of action (Folland et al., 2009), they are constrained by (i) the accuracy of the reanalysis products from which they are derived, (ii) the non-stationarity of the EOF pattern, (iii) the orthogonality imposed by the EOF technique, (iv) the fact that the constructed EOFs are influenced by the region selected and (v) having to repeat the analysis every time an update is required, which may change previously obtained time series (Wang et al., 2014; Cropper et al., 2015). It is also worth noting that the EOFs are statistical constructs and are not always associated with climate physics (Dommenget and Latif, 2002). Here, we present a compilation of monthly indices of the EA and the SCA based on meteorological stations and from five reanalyses products. The instrumental series go back to 1866 and 1901, respectively, while the EOF-based series go back to 1851. To the best of our knowledge, these are the longest EA and SCA datasets made available to the scientific community. We also provide a comprehensive comparison of the instrumental and EOF-based indices, including their ability to capture seasonal changes of the SLP field in the region.

2 Data and methods

2.1 Instrumental data

A set of meteorological stations were selected according to their proximity to the EA and SCA centres of action shown in our EOF analyses: Ireland for the EA and Norway for the SCA. Only one meteorological station with SLP measurements in Ireland could be used in this study: Valentia Observatory. On the other hand, five Norwegian stations with SLP data were located in the region of interest. The most suitable Norwegian station was further selected according to three criteria: (i) length of the record, (ii) continuity (i.e. the least missing data, the better) and (iii) correlation with the EOF-based SCA time series. Bergen Florida (Norway) was the station which better fulfilled these criteria. Details of all meteorological stations are available in Table S1.

Thus, daily records from Valentia Observatory (Ireland; 1 October 1939–31 December 2016) and Bergen Florida (Norway; 1 January 1901–31 October 2016) as well as monthly data from Valentia Observatory (January 1866 to December 2013; Table 1) have been used to calculate the monthly series that form our instrumental indices. Only 1 day (14 November 2012) and 4 months (December 1938 and May 1872, 1873 and 1874) were missing from the Valentia SLP data. Filling the gap in the daily time series with its long-term average does not improve the accuracy of the corresponding monthly mean, and so this day has been omitted in the calculations. Datasets were tested for inhomogeneities already by their sources (Table 1). A long continuous record of monthly SLP for Valentia was obtained by merging the monthly averages from January 1866 to December 2016 and the computed monthly means for the period since November 1939 on the basis that the overlapping period (1939–2013) showed a correlation ρ>0.99. Hereafter, standardised monthly SLP anomalies for these stations are named ValSLP and BerSLP.

Table 2Details of the reanalysis products used in this study.

Download Print Version | Download XLSX

Figure 1EOF loadings based on monthly SLP data (20CRv2c dataset; Compo et al., 2011). Each column represents a 3-month season. The percentages at the bottom right of each map are the variability explained by the corresponding EOF (rows) at any given season (columns) as shown in Table S2. The text at the bottom of each map identifies the observed pattern. Pink (purple) dots show the location of Bergen Florida (Valentia Observatory) stations as listed in Table 1. Figures S1–S4 show the same maps for the other four reanalysis products in Table 2.


2.2 Empirical orthogonal function (EOF) analysis

Five reanalyses datasets have been used in this study (Table 2). ERA-40 (Uppala et al., 2005) is a conventional-input reanalysis used in many studies that require long-term atmospheric data. ERA-Interim (Dee et al., 2011) improves ERA-40 in that it assimilates a more complete set of observations and therefore achieves more realistic representations of the hydrologic cycle and the stratospheric circulation relative to ERA-40, and it also improves the consistency of the reanalysis products over time. ERA-20C (Poli et al., 2016) directly assimilates surface pressure and surface wind observations, enabling it to extend back in time to cover the entire 20th century. 20CRv2c (Compo et al., 2011) is also a surface-input reanalysis with a different assimilation procedure than that of ERA-20C. The main limitation of 20CRv2c is that it does not correct for biases in surface pressure observations from ships and buoys, which results in the anomalous SLP observed for the period 1850–1865. Finally, the NCEP/NCAR (Kalnay et al., 1996) was the first modern reanalysis of extended temporal coverage (1948 to present) and it is still widely used. For an extensive review on the quality of these datasets, the reader is referred to Fujiwara et al. (2017).

Empirical orthogonal function (EOF) analysis was performed on the above-mentioned five reanalyses datasets of monthly SLP for a constrained Atlantic sector (100 W–40 E, 10–80 N; Table 2) using the pca function of Matlab© R2018a (which is equivalent to prin_comp in R and the PCA function from the sklearn library in Python). As in previous studies, the SLP anomalies were geographically equalised prior to the analyses by multiplying them by the square root of the cosine of its corresponding latitude (North et al., 1982). The percentage of variance explained by each EOF is shown in Table S2.

To maximise the representation of each pattern across seasons, and because the relative strength of the three main modes of variability is not constant throughout the year, all EOFs have been calculated for each 3-month season (DJF, MAM, JJA and SON). Although we only used SLP fields, these patterns are also recognisable if using different levels of the atmosphere. See Wallace and Gutzler (1981) and Cradden and McDermott (2018) for patterns using 500 mb heights and Barnston and Livezey (1987) for 700 mb heights.

The polarities of the derived EOF time series have been fixed to correspond to our definitions of the EA and the SCA (see Sect. 1), which coincide with positive centres of action offshore Ireland and over Scandinavia, respectively (Figs. 1 and S1–S4). This is consistent with the expected climate patterns and in the case of the EA, is compatible with the usage of SLP data from Valentia Observatory (Ireland) as an instrumental EA index (Comas-Bru et al., 2016; Moore and Renfrew, 2012; see Sect. 3.1).

2.3 Composite time series

Monthly composite series of the NAO, EA and SCA patterns have been calculated for each 3-month season independently. Each individual month was given the average of the available EOF-based series with a confidence interval that corresponds to their standard deviation. The number of EOF-based series used for any given month is provided here, along with the composite series. Since the EA and the SCA do not always correspond to the second and third EOF, respectively, a selection of what series to include in each composite based on their spatial patterns was done in advance (see Table 3 for a list of individual EOFs included in each composite).

2.4 Data analysis

All correlations have been computed using Spearman rank coefficients (rho, ρ) to avoid assumptions about normally distributed data that are inherent in some other correlation coefficients. The Spearman rank correlation coefficient is generally expressed as Eq. (1):

(1) ρ = 1 - 6 i = 1 n d i 2 n n 2 - 1 ,

where n is the number of measurements in each of the two variables in the correlation and di is the difference between the ranks of the ith observation of the two variables.

When computing the 30-year running correlations, the significance of the correlations for each time window was done using a Monte Carlo approach following the methodology described in Ebisuzaki (1997). Each time window is defined from i to i+30, where i is the oldest year of overlap between the time series.

Decadal variability of the time series (Sect. 3.2.3) has been explored after filtering the time series with a second-order low-pass Butterworth filter with a cut-off frequency of 1∕10 (as implemented in the butter function of Matlab© R2018a).

Table 3Summary of the geographical structures of the EOF loadings across datasets (columns) and seasons (rows).

Superindices indicate which EOFs are included in the composite series: 1 NAOcomp, 2 EAcomp, 3 SCAcomp and 4 WAcomp.
(i) The NAO in DJF and MAM presents a southern pole extending towards Europe. In JJA, the southern pole is weak and predominantly shifted northwards. The same pattern is found in SON, except for 20CRv2c and ERA-20C. (ii) “EA with secondary pole” means that a negative pole over Scandinavia is evident. (iii) “Extended SCA” refers to the classic SCA with the positive pole extending towards Ireland and the UK. (iv) The western Atlantic (WA) pattern in MAM/EOF2 is a dipole with a main centre over the N. Atlantic Ocean and a second weak centre over Scandinavia (both negative). (v) Note that no EA pattern is observed in 20CRv2c during JJA, which results in a shorter EAcomp for this season. See Figs. 1 and S1–S4 for the corresponding maps.

Download Print Version | Download XLSX

3 Results and discussion

3.1 Instrumental versus EOF-based series

In order to identify the most suitable meteorological station to reconstruct each teleconnection index, we first need to investigate the robustness of their spatial structures across reanalyses datasets (Figs. 1 and S1–S4). For example, while the geographical patterns are very stable across datasets during winter (Table 3), some discrepancies are observed during summer (JJA; see EOF2 or EOF3).

Moore and Renfrew (2012) used SLP data from Valentia Island (Ireland; Table 1) to derive an EA station-based index and, even though this meteorological station is not located at EA centre of SLP anomalies, the correlation coefficients between its winter values (when the mode is strongest) and EOF2 are very high (0.7<ρ<0.9; Fig. 2a; Table 4). Furthermore, our results show that when an EA pattern is identified in the reanalysis products, the location of Valentia Observatory lies within the main area of SLP anomalies. For an example, see the relative location of the purple dot and the yellow centre of anomalies of EOF2 in Fig. 1. This indicates the suitability of using Valentia Observatory data as a proxy of EA variability.

Figure 2Monthly (DJF) EOF time series and their equivalent instrumental records. (a) EOF2 and normalised SLP data from Valentia Observatory (ValSLP); (b) same as (a) with the EOF3 and SLP data from Bergen Florida (BerSLP). Correlation coefficients between these time series are given in Table 4.


Table 4Correlation coefficients between the three monthly EOFs for winter (DJF), spring (MAM), summer (JJA) and autumn (SON) and the corresponding monthly ValSLP and BerSLP.

Note that all correlations are with p value  0.01 except a 0.01 <p value  0.05; b 0.05 <p value  0.1; and c p value > 0.1.

Download Print Version | Download XLSX

After an exhaustive investigation to find a long and continuous instrumental SLP dataset in Fennoscandia as a measurement of the strength of the Scandinavian pattern, we suggest using the SLP record from Bergen Florida (Norway; Table 1), which falls on the SCA's centre of action as shown by the pink dots in Fig. 1. This decision is further supported by the high resemblance between this meteorological dataset and the third EOF of the winter SLP field (0.7<ρ<0.8; Fig. 2b; Table 4). This EOF3 corresponds to the SCA pattern defined by Barnston and Livezey (1987) that extended towards Ireland and UK and, in some cases, most of northern Europe (ERA-20C, ERA-40, ERA-Interim and NCEP/NCAR; see Figs. 1 and S1–S4). Due to the spatial extent of the winter's EOF3 positive centre of anomalies covering from Scandinavia to SW Ireland, ValSLP (purple dot in Figs. 1 and S1–S4) is unsurprisingly correlated with all winter EOF3s (0.5<ρ<0.6; Table 4).

Consistent with previous studies (e.g. Hurrell et al., 2013; Moore et al., 2013) EOF1 represents the NAO across seasons and datasets, albeit with slight changes in the extension and/or intensity of its southern pole (Figs. 1 and S1–S4). However, EOF2 and EOF3 are far from showing a homogeneous pattern over the course of the four seasons and across the five reanalysis datasets.

During spring, the spatial structure of the EA (Figs. 1 and S1–S4) is recognised in EOF3. This is consistent with the moderate to high correlations between EOF3 and ValSLP (0.6<ρ<0.7; Table 4). However, due to the observed (in some cases weak) negative pole over Scandinavia, BerSLP is poorly correlated to EOF3 (-0.4<ρ<-0.1; Table 4). As the spatial patterns of EOF2 show a predominant centre over the N. Atlantic Ocean (ca. 40 N) in all datasets, their time series are uncorrelated with our instrumental records (Figs. 1 and S1–S4, Table 4). This mode of variability is similar to the Western Atlantic (WA) pattern defined by Wallace and Gutzler (1981).

Not surprisingly, the overall picture over the course of summer is a bit more complicated than in other seasons, when most datasets are consistent. In this case, ValSLP shows moderate to high correlations with EOF2 (0.6<ρ<0.7; Table 4) except for ERA-Interim, for which the strongest correlations are observed with EOF1 and EOF3 (ρ=0.6). However, most of these EOF2s represent an extended Scandinavian pattern (Table 4), the centre of which covers the location of Valentia Observatory, instead of the EA. A clear EA pattern is only observed for EOF3 ERA-20C and a northwardly shifted EA pattern is found in EOF2 ERA-Interim and EOF3 NCEP/NCAR (Table 3). These discrepancies between ERA-Interim and the other datasets arise because (i) EOF1 depicts a NAO pattern with a southern pole shifted towards northern Europe, (ii) EOF2 represents a pattern similar to a northwardly shifted EA and (iii) EOF3 is equivalent to the extended SCA pattern also found in winter across all datasets (see Figs. 1 and S1–S4).

Correlations between summer BerSLP and EOF3 are only moderate to high for 20CRv2c and ERA-40 (ρ>0.6; Table 4) because they represent the classical SCA pattern, with a centre of anomalies only over Fennoscandia and the North Sea. However, as a result of this spatial pattern, moderate correlations are also found with EOF2 across datasets (0.5<ρ<0.7, except ERA-Interim). Regarding ERA-Interim's EOF2, the weak correlation with BerSLP (ρ=0.3) is due to the EA having migrated northwards. In contrast with the rest of the seasons, and as previously noted for ValSLP, a range of moderate to high correlations are observed between summer EOF1 and BerSLP as a result of the observed summer NAO pattern already defined in previous studies (Blade et al., 2012; Folland et al., 2009).

In the case of autumn, a more coherent picture across datasets is observed: EOF1 represents a NAO with a weak southern pole that, in some cases, migrates towards Europe; EOF2 is equivalent to the EA with a weak negative pole over Scandinavia; and EOF3 shows a SCA pattern similar to the one obtained for the winter months. Consequently, ValSLP is correlated with EOF2 (0.6<ρ<0.7) and BerSLP with the EOF3 (0.6<ρ<0.8) for all the reanalysis products. However, due to the extended SCA in EOF3, ValSLP is also moderately correlated to it for all datasets except ERA-Interim, in which Valentia Observatory lies at the edge of the centre. In addition, ValSLP is also moderately correlated with ERA-Interim's EOF1 as a result of the NAO's southern pole being shifted towards northwestern Europe (Fig. S3).

In summary, it has been shown that winter and autumn ValSLP and BerSLP indices correlate with EOF2 and EOF3, respectively. In contrast, the summer EA and SCA patterns swap their order in some datasets, but good correlations are found when the geographical representation of the EOFs is taken into account. During spring, the EA pattern is represented by EOF3 across all datasets, and EOF2 shows the WA pattern. In this case, the SCA pattern is not reflected in any of the first three components of the EOF analysis.

Figure 3Monthly series of EAcomp, the instrumental data (ValSLP) and the EA from the CPC (EACPC; CPC, 2012) for each 3-month season. Note that the CPC series have been inverted for an easy visual comparison.


Figure 4Same as in Fig. 3 for SCAcomp, instrumental data (BerSLP) and the SCAfrom the CPC (SCACPC; CPC, 2012).


3.2 New monthly EA and SCA time series

3.2.1 Monthly composites

Each reanalysis dataset has advantages and shortcomings when it comes to its ability to reproduce the different climate modes, and outlining objective indicators to select the reanalysis dataset that performs best is outside of the scope of this study. Instead, since the correlations amongst datasets are very high (DJF: ρ<0.9; MAM: ρ>0.8; JJA: ρ>0.6; SON: ρ>0.9; Table S3), we have created robust composite series of each climate mode on the basis of their geographical representations as described in Table 3. This was done by averaging the overlapping EOF-based time series that display either the NAO, EA or SCA (WA for MAM). See Sect. 2.2 for further details.

Figures 3 and 4 show the monthly time series of EAcomp SCAcomp, ValSLP BerSLP and EACPC SCACPC (the longest available records from CPC, 2012). Spearman rank coefficients between these series are in Tables 5 and 6. For winter, ValSLP is robustly correlated with EAcomp (ρ=0.8) and moderately correlated with SCAcomp (ρ=0.5; Table 5). This results from the fact that the datasets forming SCAcomp all show an extended SCA pattern (which covers UK and Ireland, and therefore Valentia Observatory; see Figs. 1 and S1–S4). On the other hand, BerSLP exhibits a very high correlation (ρ=0.8) with SCAcomp and is uncorrelated with EAcomp, even though all EA spatial patterns show a weak secondary pole of negative SLP anomalies over Scandinavia (Figs. 1 and S1–S4). It seems therefore that only the main centre of action is reflected in the correlations (Table 5).

Table 5Monthly correlations of our composite indices (EAcomp and SCAcomp) and the instrumental records (ValSLP and BerSLP).

* Spring (MAM) pattern is that of WA. See text for details. Note that all correlations are with p value  0.01 except a 0.01 <p value  0.05; b 0.05 <p value  0.1; and c p value > 0.1.

Download Print Version | Download XLSX

With regard to spring, ValSLP is moderately correlated with EAcomp (ρ=0.7) and uncorrelated with the WAcomp (ρ=0.1). On the other hand, BerSLP is uncorrelated with either EAcomp or the WA index (Table 5) because Bergen Florida lies at the edge of the SLP dipole, resulting in this station being insensitive to these climate patterns (purple dot in Figs. 1 and S1–S4).

For summer, ValSLP shows a low (ρ=0.4) and medium–high (ρ=0.5) correlation with EAcomp and SCAcomp, respectively. The low correlation between ValSLP and EAcomp for this season reflects the inconsistency of the EA pattern across the different reanalysis datasets (note that the degree of correlations amongst EOFs is the lowest in summer; Table S3). Consequently, only three datasets – ERA-20C, ERA-Interim and NCEP/NCAR – were used to construct the summer EAcomp (Table 3), with the last two showing a clear northern migration of its anomaly centre that leaves Valentia Observatory outside the area sensitive to this pattern (pink dot in Figs. S3 and S4). By contrast, the observed relatively high correlation between ValSLP and SCAcomp is due to the extended SCA (Figs. 1 and S1–S4). Regarding BerSLP, this is poorly correlated with EAcomp (ρ=0.2) and moderately correlated with SCAcomp (ρ=0.6; Table 5) as a result of the robust extended SCA patterns used to create SCAcomp (Table 3).

As far as autumn is concerned, ValSLP displays similar moderate correlations with EAcomp and SCAcomp (ρ=0.5), again as a result of the similarity between the EA and the extended SCA patterns. Moreover, BerSLP is negatively correlated with EAcomp (ρ=-0.2) because of the negative secondary pole of the EA (see Figs. 1 and S1–S4) and highly correlated with SCAcomp (ρ=0.7).

Figure 5Running correlations between our composite series and the instrumental records. (a) EAcomp and ValSLP; (b) SCAcomp and BerSLP. The window size is 30 years and is defined from i to i+30, where i is the oldest month. Dashed lines indicate the 0.01 significance thresholds. Note that spring in panel (b) corresponds to the WA index instead of the SCA.


3.2.2 Consistency of the correlations

To assess the temporal stability of the correlations discussed above, we have calculated 30-year moving correlations between EAcomp SCAcomp and ValSLP BerSLP. As evident in Fig. 5, these relationships are only stationary (and constantly significant at ρ>0.7) during winter, when the two atmospheric climate modes are more robustly expressed. During spring, correlations between EAcomp and ValSLP vary across a large range of values: from non-significant correlations during the 1880s and the early and mid-20th century (ca. 1950–1965) to moderate–high correlations (ρ>0.6) during the 1930s and 1990s. By contrast, the correlations between SCAcomp and BerSLP are non-significant for almost the entire time interval (1901–2016), with only two small windows – between ca. 1925 and 1935 and around 1970 – exhibiting significant correlations (ρ∼0.5). This results from the spring composite in Fig. 5 representing the WA instead of the SCA. The EA correlations during summer (Fig. 5a) show the largest variability, with correlations peaking in the 1940s (ρ>0.6) and after 1980. Non-significant correlations are found for the reminding periods. Regarding summer, SCAcomp and BerSLP are moderately correlated in the interval 1930–1980 and for a short period at the end of the 20th century. Autumn EAcomp moderately correlates with ValSLP except for 1895–1920 and after ca. 1990, while SCAcomp is only significantly correlated with BerSLP in the period before ca. 1935 and after ca. 1965.

These results demonstrate that the station-based indices may be used as reference during the winter season but, beyond that, they ought to be used with caution due to the non-stationary behaviour of the EA and SCA patterns. For these non-winter seasons, almost opposite patterns of significance versus non-significance are found (i.e. EAcomp and ValSLP show significant correlations when the SCAcomp and BerSLP correlations are not significant and vice versa). This may result from a displacement of their respective centres of action through time, similarly to what has been suggested for other climate modes of variability (i.e. NAO, AMO, ENSO and PDO) during these seasons for the last two centuries in the North Atlantic sector (Hernández et al., 2016).

Figure 6Seasonally averaged EAcomp (dashed blue line) and SCAcomp (dashed red line) and decadal EAcomp (blue solid line) and SCAcomp (red solid line). (a) Winter (DJF); (b) spring (MAM); (c) summer (JJA); (d) autumn (SON). A 10-year bandpass filter has been used to obtain the decadal series. Note that in (b) the red lines correspond to WAcomp instead of SCAcomp. Note the different y scale for summer indices. The grey band indicates the period of low confidence of our composite series (see Methods section for details).


3.2.3 Decadal variability of new EA and SCA time series

Figures 3 and 4 show that most variability in EAcomp and SCAcomp is observed at inter-annual scales, but some decadal variability is also evident in Fig. 6. Overall, all 10-year filtered indices fluctuate around the zero line with no evident trend, except for one period when both series are persistently positive: during winter at the end of the 19th century (Fig. 6a). During this season, both indices show similar trends between 1880 and 1920, when a decoupling occurs. In addition, the SCA experiences a large change of sign during the first three decades of the 20th century. Focusing on spring (Fig. 6b), we observe different patterns for both the EA and the WA, with an EA absolute maximum at ca. 1915 and two SCA minima at ca. 1930 and ca. 1960. The extreme absolute minima at the start of the summer SCAcomp record (Fig. 6) seems to result from a low-pressure bias in marine records (Woodruff et al., 2005; Wallbrink et al., 2009) that has affected 20CRv2c fields such as the sea-level pressure from 1851 to ca. 1865 (further information on this can be found here:, last access: 5 December 2018). Since the 20CRv2c is the only reanalysis dataset covering that early period, we cannot provide an alternative. Instead, this period of low confidence has been highlighted in all our figures with a grey band. During the rest of the period, EAcomp and SCAcomp alternate between similar (e.g. 1965–2000) and opposite patterns (e.g. 1910–1925), with amplitudes that gradually decrease towards present. Autumn EAcomp and SCAcomp alternate between in-phase (e.g. 1990–2000) and out-of-phase (e.g. 1955–1965) states.

Figure 7Running correlations as in Fig. 5 between our composite series and the CPC indices. (a) EAcomp and EACPC; (b) SCAcomp and SCACPC. The window size is 30 years and is defined from i to i+30, where i is the oldest month. Dashed lines indicate the 0.01 significance thresholds.


Table 6Monthly correlations between the CPC indices (NAOCPC, EACPC and SCACPC) and our composites (NAOcomp, EAcomp and SCAcomp.

Note that all correlations are with p value  0.01 except a 0.01 <p value  0.05; b 0.05 <p-valve 0.1; and c p value > 0.1. The SCA has only been compared to the composites for DJF, JJA and SON because spring is showing the WA pattern (see Table 4 and Figs. 1 and S1–S4 for further details).

Download Print Version | Download XLSX

3.3 Composite versus CPC series

To further check the performance of our composite series, we have compared them to the most widely used series from the CPC (CPC, 2012; Figs. 3 and 4; Table 6).

Table 7Monthly correlations between the EACPC and SCACPC and our station-based indices (ValSLP and BerSLP).

Note that all correlations are with p value  0.01 except a 0.01 <p value  0.05; b 0.05 <p value  0.1; and c p value > 0.1.

Download Print Version | Download XLSX

Figure 8Correlation distribution maps between the monthly precipitation (a) and surface air temperature (b) and our monthly composites (EAcomp and SCAcomp) between 1902 and 2016. Climate data from the CRU-TS4.01 global climate data set (Harris et al., 2014). Positive correlations are shown in red and negative correlations are shown in blue (see colour bar). Correlation coefficients are Spearman rank coefficients. SCAcomp MAM maps (marked with an asterisk) correspond to the WA pattern.


The NAO index from CPC (NAOCPC) is moderately to very highly correlated with our NAO composite across all seasons (Table 6; 0.6<ρ<0.8). The EA index (EACPC) shows a moderate negative correlation with winter EAcomp (ρ=-0.6) and low negative correlations with the other seasons (ρ=-0.3; Table 6). These negative correlations are due to the fixed polarity of the EA pattern: the main anomaly centre of our EA is positive, while that of the CPC is negative. This can be seen contrasting the spatial patterns of their teleconnection patterns, found at, last access: 5 December 2018, for the EA and, last access: 5 December 2018, for the SCA, as well as in our Figs. 1 and S1–S4. Comas-Bru and McDermott (2014) provide an extensive discussion on this. These negative correlations are consistent with the correlations between EACPC and ValSLP (Table 7) as well as the running correlations discussed below. Regarding the SCA index, SCACPC exhibits a low correlation with SCAcomp for all seasons (ρ<0.4; note that the composite for spring is reflecting the WA pattern and hence it has not been compared with the CPC indices). The moving correlations (30-year sliding window) between the seasonal EAcomp EACPC (Fig. 7a) and SCAcomp SCACPC (Fig. 7b) are consistent with the correlations in Table 6. For winter and summer, the correlations between EAcomp and EACPC are fairly constant (ρ<-0.5). However, non-significant correlations are obtained for autumn during the entire time period (1950–2016), and, during spring, only the period between 1970 and 2000 is significant (ρ<-0.4), with the exception of a few time windows at the end of the 1980s. Regarding the temporal variability of the correlations between SCAcomp and SCACPC, these are only significant (ρ>0.4) after 1990 for the winter season (Fig. 5b).

Overall, these results suggest that the difference in methodology between our EOFs and the one followed by the CPC, and/or the difference in the reanalysis products used, is not relevant for the NAO, but it becomes critical for the EOFs that account for a smaller percentage of the total SLP variance (>30 % versus 10 %–20 %; Table S2). The low correlations observed beyond the winter season could be linked to a non-stationary behaviour of the EA and SCA, resulting in migrations of their centres that are not adequately captured by our methodology and/or that employed by the CPC, or in the reanalyses products from which the indices are derived.

This is further supported by the geographical displays of seasonal EACPC and SCACPC (see URLs above). The EACPC consists of a dipole with negative anomalies that spans from the central North Atlantic Ocean to central Europe (leaving Valentia Observatory at its margin) and positive anomalies in the middle subtropical Atlantic. According to their maps, the negative pole remains geographically fixed throughout the year, only varying in intensity, whereas the positive pole varies both in strength and position, being less intense and displaced towards the centre of the subtropical Atlantic in summer. On the other hand, the SCACPC is essentially a primary positive centre located over northern Scandinavia at ∼70 N (for reference, Bergen Florida station is at 60 N), with weaker negative centres over western Europe and Russia. In this case, both poles present an almost spatial stationary behaviour, with their highest intensity occurring in winter. Thus, the low correlations obtained for the CPC indices and the station-based data (Table 7) could be attributed to the distance between the meteorological stations and their centres of action.

The discrepancies observed between our composite-EOFs and those from the CPC may also be attributed to (i) the different and shorter time period considered by CPC when performing the RPCA; (ii) the fact that the CPC considers data from all 12 calendar months, whereas the EA/SCA patterns are more distinctly developed in wintertime; (iii) the fact that the region over which CPC computed the RPCA covers all longitudes from 20 to 90 N, whereas we have limited our computations to the N. Atlantic region (100 W–40 E, 10–80 N); (iv) the non-orthogonality of the RPCA; and (v) differences related to the use of SLP or 500 mb heights and/or the accuracy of the reanalysis datasets used.

3.4 Climate impact of the composite EA and SCA series

Figure 8 illustrates the monthly correlation distribution maps between our composite series (EAcomp and SCAcomp) versus surface air temperature and precipitation amount for the four seasons (DJF, MAM, JJA and SON) between 1901 and 2016 using the CRU-TS.4.01 dataset (Harris et al., 2014). The strongest correlations are found in winter, when these patterns are more prominent, and are consistent with previous studies (Moore et al., 2011; Comas-Bru and McDermott, 2014; Lim, 2015).

The only European regions for which the EA impacts on precipitation are strong and robust (i.e. in the same direction) throughout the year are the UK and Ireland. The predominantly weak correlations observed in other regions, far from the main centres of action, could arise from the low percentages of variability explained by each EOF pattern (<20 % for EA; Table S2). Nevertheless, consistent patterns are observed in terms of precipitation amount across all seasons except in EAcomp JJA, which also shows an anomalous relationship with temperature. We interpret this to be caused by the northerly shift of the EA centre of action in JJA (i.e. between Scotland and Iceland instead of offshore Ireland; see Table 3 and Figs. S3 and S4) that hampers its influence on the western Mediterranean region, which in turn becomes wetter with positive EA modes. Regarding the impact of the SCA on precipitation, a similar pattern with negative correlations in northern Europe and predominantly positive correlations in the circum-Mediterranean region is observed across seasons, albeit with different strengths. We observe a strong seasonality on the impact of both climate modes on surface air temperature. Weak correlations are found for the all seasons except JJA for the EA with non-significant correlations across all Europe in SON. The opposite is observed for SCA, where the strongest impact on air temperature is shown in DJF (predominantly negative) and SON (predominantly positive).

Due to the low variance explained by both climate modes, they are not expected to imprint a very strong signal on the climate, and thus the extent to which these correlations would be reflected in the absolute precipitation and temperature values will primarily depend on the concomitant state of the NAO, the main driver of climate variability in the region (Hurrell and van Loon, 1997; Hurrell and Deser, 2010). In addition, the impact of these atmospheric modes on the climate is not robust throughout the year. For example, none of the datasets used in this study showed a SCA pattern within the three leading EOFs in spring.

Individual EOFs such as the EA and the SCA are statistical constructs that do not necessarily represent a physically independent phenomenon linked (i.e. correlated) to climate variables in a robust manner. Full characterisation of the regional atmospheric dynamics therefore requires multiple EOFs to be taken into account (Roundy, 2015). To thoroughly characterise the climate in the region, the impacts of the EA/SCA should be investigated in conjunction with the NAO (Moore et al., 2011; Comas-Bru and McDermott, 2014; Hall and Hanna, 2018) but this is outside the scope of this study. As far as we are aware, such an investigation does not exist outside the winter months.

4 Data availability

The datasets consisting of the instrumental data and the monthly composite indices of NAO, EA and SCA are available at (Comas-Bru and Hernández, 2018).

5 Conclusions

This study presents a new set of indices for the second and third modes of climate variability in the North Atlantic sector (EAcomp and SCAcomp). These indices were constructed after identifying the main patterns of variability across five different reanalysis products and were then compared to the two meteorological stations identified as instrumental series for the EA and the SCA pattern: Valentia Observatory (Ireland) and Bergen Florida (Norway). The high resemblance between our EOF-based indices and these instrumental SLP records during winter allows both indices to be readily updated as required. Beyond this season, however, a more complex picture arises. For example, the Scandinavian pattern is not included within the first three modes of climate variability during spring, and instead, the Western Atlantic pattern as described by Wallace and Gutzler (1981) dominates SLP variability after the NAO, leaving the EA as the third pattern for this season.

Our results also suggest that the difference in methodology and/or reanalysis products between our composite EOF-based indices and those provided by NOAA-CPC (CPC, 2012) is not relevant for the NAO, but it becomes critical for the second and third EOF. However, despite the differences, both sets of indices display very similar and recognisable spatio-temporal patterns at inter-annual timescales (Figs. 3 and 4).


The supplement related to this article is available online at:

Author contributions

AH identified the meteorological stations used. LCB developed the scripts and performed the data analyses. LCB and AHH designed the calculations and carried them out. The manuscript was collaboratively written by both co-authors.

Competing interests

The authors declare that they have no conflict of interest.


We would like to thank Met Éireann and the European Climate Assessment & Dataset project (ECA&D) for making the meteorological datasets of Valentia Observatory (Ireland) and Bergen Florida (Norway) publicly available. Support for the Twentieth Century Reanalysis Project version 2c (20CRv2c) dataset is provided by the U.S. Department of Energy, Office of Science Biological and Environmental Research (BER), and by the National Oceanic and Atmospheric Administration Climate Program Office. We acknowledge use of ECMWF reanalysis datasets (ERA-40, ERA-20C and ERA-Interim) for which documentation is found at (last access: 5 December 2018). NCEP Reanalysis data are provided by the NOAA/OAR/ESRL PSD, Boulder, Colorado, USA, on their website at (last access: 5 December 2018). Armand Hernández was supported by a Beatriu de Pinós–Marie Curie COFUND contract within the framework of the FLOODES2k (2016 BP 00023), PaleoModes (CGL2016-75281-C2) and HOLMODRIVE (PTDC/CTA-GEO/29029/2018) projects.

Edited by: David Carlson
Reviewed by: two anonymous referees


Aguilar, E., Auer, I., Brunet, M., Peterson, T., and Wieringa, J.: Guidelines on climate metadata and homogenization. World Climate Programme Data and Monitoring WCDMP-No. 53, WMO-TD No. 1186, World Meteorological Organization, Geneva, 55 pp., 2003. 

Barnston, A. G. and Livezey, R. E.: Classification, Seasonality and Persistence of Low-Frequency Atmospheric Circulation Patterns, Mon. Weather Rev., 115, 1083–1126,<1083:CSAPOL>2.0.CO;2, 1987. 

Bastos, A., Janssens, I. A., Gouveia, C. M., Trigo, R. M., Ciais, P., Chevallier, F., Peñuelas, J., Rödenbeck, C., Piao, S., Friedlingstein, P., and Running, S. W.: European land CO2 sink influenced by NAO and East-Atlantic Pattern coupling, Nat. Commun., 7, 10315,, 2016. 

Blade, I., Liebmann, B., Fortuny, D., and van Oldenborgh, G. J.: Observed and simulated impacts of the summer NAO in Europe: implications for projected drying in the Mediterranean region, Clim. Dynam., 39, 709–727,, 2012. 

Bueh, C. and Nakamura, H.: Scandinavian pattern and its climatic impact, Q. J. Roy. Meteorol. Soc., 133, 2117–2131,, 2007. 

Chafik, L., Nilsen, J. E. Ø., and Dangendorf, S.: Impact of North Atlantic Teleconnection Patterns on Northern European Sea Level, J. Mar. Sci. Eng., 5, 43,, 2017. 

Comas-Bru, L. and Hernández, A.: Reconciling North Atlantic climate modes: Revised monthly indices for the East Atlantic and the Scandinavian patterns beyond the 20th century, PANGAEA,, 2018. 

Comas-Bru, L. and McDermott, F.: Impacts of the EA and SCA patterns on the European twentieth century NAO-winter climate relationship, Q. J. Roy. Meteorol. Soc., 140, 354–363,, 2014. 

Comas-Bru, L., McDermott, F., and Werner, M.: The effect of the East Atlantic pattern on the precipitation delta O-18-NAO relationship in Europe, Clim. Dynam., 47, 2059–2069,, 2016. 

Compo, G. P., Whitaker, J. S., Sardeshmukh, P. D., Matsui, N. , Allan, R. J., Yin, X. , Gleason, B. E., Vose, R. S., Rutledge, G. , Bessemoulin, P. , Brönnimann, S. , Brunet, M. , Crouthamel, R. I., Grant, A. N., Groisman, P. Y., Jones, P. D., Kruk, M. C., Kruger, A. C., Marshall, G. J., Maugeri, M., Mok, H. Y., Nordli, Ø., Ross, T. F., Trigo, R. M., Wang, X. L., Woodruff, S. D., and Worley, S. J.: The Twentieth Century Reanalysis Project, Q. J. Roy. Meteorol. Soc., 137, 1–28,, 2011. 

CPC: Northern Hemisphere Teleconnection Patterns, Climate Prediction Centre, US National Oceanic and Atmospheric Administration, available at: (last access: 26 February 2018), 2012. 

Cradden, L. C. and McDermott, F.: A weather regime characterisation of Irish wind generation and electricity demand in winters 2009–11, Environ. Res. Lett., 13, 054022,, 2018. 

Crasemann, B., Handorf, D., Jaiser, R., Dethloff, K., Nakamura, T., Ukita, J., and Yamazaki, K.: Can preferred atmospheric circulation patterns over the North-Atlantic-Eurasian region be associated with arctic sea ice loss?, Polar Sci., 14, 9–20,, 2017. 

Cropper, T., Hanna, E., Valente, M. A., and Jónsson, T.: A daily Azores–Iceland North Atlantic Oscillation index back to 1850, Geosci. Data J., 2, 12–24,, 2015. 

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, I., Biblot, J., Bormann, N., Delsol, C., Dragani, R., Fuentes, M., Greer, A. J., Haimberger, L., Healy, S. B., Hersbach, H., Holm, E. V., Isaksen, L., Kallberg, P., Kohler, M., Matricardi, M., McNally, A. P., Mong-Sanz, B. M., Morcette, J.-J., Park, B.-K., Peubey, C., de Rosnay, P., Tavolato, C., Thepaut, J. N., and Vitart, F.: The ERA-Interim reanalysis: Configuration and performance of the data assimilation system, Q. J. Roy. Meteorol. Soc., 137, 553–597,, 2011. 

Dommenget, D. and Latif, M.: A cautionary note on the interpretation of EOFs, J. Climate, 15, 216–225,<0216:ACNOTI>2.0.CO;2, 2002. 

Ebisuzaki, W.: A method to estimate the statistical significance of a correlation when the data are serially correlated, J. Climate, 10, 2147–2153,<2147:AMTETS>2.0.CO;2, 1997. 

Folland, C. K., Knight, J., Linderholm, H. W., Fereday, D., Ineson, S., and Hurrell, J. W.: The Summer North Atlantic Oscillation: Past, Present, and Future, J. Climate, 22, 1082–1103,, 2009. 

Fujiwara, M., Wright, J. S., Manney, G. L., Gray, L. J., Anstey, J., Birner, T., Davis, S., Gerber, E. P., Harvey, V. L., Hegglin, M. I., Homeyer, C. R., Knox, J. A., Krüger, K., Lambert, A., Long, C. S., Martineau, P., Molod, A., Monge-Sanz, B. M., Santee, M. L., Tegtmeier, S., Chabrillat, S., Tan, D. G. H., Jackson, D. R., Polavarapu, S., Compo, G. P., Dragani, R., Ebisuzaki, W., Harada, Y., Kobayashi, C., McCarty, W., Onogi, K., Pawson, S., Simmons, A., Wargan, K., Whitaker, J. S., and Zou, C.-Z.: Introduction to the SPARC Reanalysis Intercomparison Project (S-RIP) and overview of the reanalysis systems, Atmos. Chem. Phys., 17, 1417–1452,, 2017. 

Hall, R. J. and Hanna, E.: North Atlantic circulation indices: links with summer and winter UK temperatures and precipitation and implications for seasonal forecasting, Int. J. Climatol., 38, e660–e677,, 2018. 

Harris, I., Jones, P. D., Osborn, T. J., and Lister, D. H.: Updated high-resolution grids of monthly climatic observations – the CRU TS3.10 Dataset, Int. J. Climatol., 34, 623–642,, 2014. 

Hernández, A., Kutiel, H., Trigo, R. M., Valente, M. A., Sigró, J., Cropper, T., and Espírito-Santo, F.: New Azores archipelago daily precipitation dataset and its links with large-scale modes of climate variability, Int. J. Climatol., 36, 4439–4454,, 2016. 

Hurrell, J. W.: Decadal trends in the north atlantic oscillation: regional temperatures and precipitation, Science, 269, 676–679,, 1995. 

Hurrell, J. W. and Deser, C.: North Atlantic climate variability: The role of the North Atlantic Oscillation, J. Marine Syst., 79, 231–244,, 2010. 

Hurrell, J. W. and van Loon, H.: Decadal variations in climate associated with the north Atlantic oscillation, Clim. Change, 36, 301–326,, 1997. 

Hurrell, J. W., Kushnir, Y., Ottersen, G., and Visbeck, M. (Eds.): An Overview of the North Atlantic Oscillation, in: The North Atlantic Oscillation: Climatic Significance and Environmental Impact, Geophysical Monograph Series,, 2013. 

Jerez, S. and Trigo, R. M.: Time-scale and extent at which large-scale circulation modes determine the wind and solar potential in the Iberian Peninsula, Environ. Res. Lett., 8, 044035,, 2013. 

Jones, P. D., Jónsson, T., and Wheeler, D.: Extension to the North Atlantic Oscillation using early instrumental pressure observations from Gibraltar and south-west Iceland, Int. J. Climatol., 17, 1433–1450,<1433::AID-JOC203>3.0.CO;2-P, 1997. 

Josey, S. A. and Marsh, R.: Surface freshwater flux variability and recent freshening of the North Atlantic in the eastern subpolar gyre, J. Geophys. Res.-Oceans, 110, C05008,, 2005. 

Kalnay, E., Kanamitsu, M., Kistler, R., Collins, W., Deaven, D., Gandin, L., Iredell, M., Saha, S., White, G., Woollen, J., Zhu, Y., Chelliah, M., Ebisuzaki, W., Higgins, W., Janowiak, J., Mo, K. C., Ropelewski, C., Wang, J., Leetmaa, A., Reynolds, R., Jenne, R., and Joseph, D.: The NCEP/NCAR 40-Year Reanalysis Project, B. Am. Meteorol. Soc., 77, 437–472,<0437:TNYRP>2.0.CO;2, 1996. 

Klein Tank, A. M., Wijngaard, J. B., Können, G. P., Böhm, R., Demarée, G., Gocheva, A., Mileta, M., Pashiardis, S., Hejkrlik, L., Kern-Hansen, C., Heino, R., Bessemoulin, P., Müller-Westermeier, G., Tzanakou, M., Szalai, S., Pálsdóttir, T., Fitzgerald, D., Rubin, S., Capaldo, M., Maugeri, M., Leitass, A., Bukantis, A., Aberfeld, R., van Engelen, A. F., Forland, E., Mietus, M., Coelho, F., Mares, C., Razuvaev, V., Nieplova, E., Cegnar, T., Antonio López, J., Dahlström, B., Moberg, A., Kirchhofer, W., Ceylan, A., Pachaliuk, O., Alexander, L. V., and Petrovic, P.: Daily dataset of 20th-century surface air temperature and precipitation series for the European Climate Assessment, Int. J. Climatol., 22, 1441–1453,, 2002. 

Lehner, F., Raible, C. C., and Stocker, T. F.: Testing the robustness of a precipitation proxy-based North Atlantic Oscillation reconstruction, Quaternary Sci. Rev., 45, 85–94,, 2012. 

Lim, Y.-K.: The East Atlantic/West Russia (EA/WR) teleconnection in the North Atlantic: climate impact and relation to Rossby wave propagation, Clim. Dynam., 44, 3211–3222,, 2015. 

Moore, G. W. K. and Renfrew, I. A.: Cold European winters: interplay between the NAO and the East Atlantic mode, Atmos. Sci. Lett., 13, 1–8,, 2012. 

Moore, G. W. K., Pickart, R. S., and Renfrew, I. A.: Complexities in the climate of the subpolar North Atlantic: a case study from the winter of 2007, Q. J. Roy. Meteorol. Soc., 137, 757–767,, 2011. 

Moore, G. W. K., Renfrew, I. A., and Pickart, R. S.: Multidecadal Mobility of the North Atlantic Oscillation, J. Climate, 26, 2453–2466,, 2013. 

North, G. R., Bell, T. L., Cahalan, R. F., and Moeng, F. J.: Sampling Errors in the Estimation of Empirical Orthogonal Functions, Mon. Weather Rev., 110, 699–706,<0699:SEITEO>2.0.CO;2, 1982. 

Pielke, R. J., Prins, G., Rayner, S., and Sarewitz, D.: Lifting the taboo on adaptation, Nature, 445, 597–598,, 2007. 

Pinto, J. G. and Raible, C. C.: Past and recent changes in the North Atlantic oscillation, WIRES Clim. Change, 3, 79–90,, 2012. 

Poli, P., Hersbach, H., Dee, D. P., Berrisford, P., Simmons, A. J., Vitart, F., Laloyaux, P., Tan, D. G. H., Peubey, C., Thépaut, J.-N., Trémolet, Y., Hólm, E. V., Bonavita, M., Isaksen, L., and Fisher, M.: ERA-20C: An Atmospheric Reanalysis of the Twentieth Century, J. Climate, 29, 4083–4097,, 2016. 

Rodríguez-Puebla, C. and Nieto, S.: Trends of precipitation over the Iberian Peninsula and the North Atlantic Oscillation under climate change conditions, Int. J. Climatol., 30, 1807–1815,, 2010. 

Rogers, J. C.: The Association between the North Atlantic Oscillation and the Southern Oscillation in the Northern Hemisphere, Mon. Weather Rev., 112, 1999–2015,<1999:TABTNA>2.0.CO;2, 1984 

Roundy, P. E.: On the interpretation of EOF analysis of ENSO, atmospheric Kelvin waves, and the MJO, J. Climate, 28, 1148–1165,, 2015. 

Scherrer, S. C., Appenzeller, C., Liniger, M. A., and Schär, C.: European temperature distribution changes in observations and climate change scenarios, Geophys. Res. Lett., 32, L19705,, 2005. 

Trenberth, K. E. and Jones, P. D.: Observations: Surface and Atmospheric Climate Change, Cambridge University Press, New York, 2007. 

Trewin, B.: Exposure, instrumentation, and observing practice effects on land temperature measurements, WIRES Clim. Change, 1, 490–506,, 2010. 

Uppala, S. M., Kållberg, P. W., Simmons, A. J., Andrae, U., Da Costa Bechtold, V., Fiorino, M., Gibson, J.K., Haseler, J., Hernandez, A., Kelly, G. A., Li, X., Onogi, K., Saarinen, S., Sokka, N., Allan, R. P., Anderson, E., Arpe, K., Balmaseda, M. A., Beljaars, A. C. M., Van De Berg, L., Bidlot, J., Bormann, N., Caires, S., Chevallier, F., Dethof, A., Dragosavac, M., Fisher, M., Fuentes, M., Hagemann, S., Hólm, E., Hoskins, B. J., Isaksen, L., Janssen, P. A. E. M., Jenne, R., Mcnally, A. P., Mahfouf, J.-F., Morcrette, J.-J., Rayner, N. A., Saunders, R. W., Simon, P., Sterl, A., Trenbreth, K. E., Untch, A., Vasiljevic, D., Viterbo, P., and Woollen, J.: The ERA-40 re-analysis, Q. J. Roy. Meteor. Soc., 131, 2961–3012,, 2005.  

Wallace, J. M. and Gutzler, D. S.: Teleconnections in the Geopotential Height Field during the Northern Hemisphere Winter, Mon. Weather Rev., 109, 784–812,<0784:TITGHF>2.0.CO;2, 1981. 

Wallbrink, H., Koek, F., and Brandsma, T.: The US Maury Collection Metadata 1796–1861, KNMI-225/HISKLIM-11, available at: (last access: 5 December 2018), 2009. 

Wang, Y. H., Magnusdottir, G., Stern, H., Tian, X., and Yu, Y. M.: Uncertainty Estimates of the EOF-Derived North Atlantic Oscillation, J. Climate, 27, 1290–1301,, 2014. 

Wanner, H., Bronnimann, S., Casty, C., Gyalistras, D., Luterbacher, J., Schmutz, C., Stephenson, D. B., and Xoplaki, E.: North Atlantic Oscillation – Concepts and studies, Surv. Geophys., 22, 321–382,, 2001. 

Woodruff, S. D., Diaz, H. F., Worley, S. J., Reynolds, R. W., and Lubker, S. J.: Early ship observational data and ICOADS, Clim. Change, 73, 169–194,, 2005. 

Woollings, T., Hannachi, A., Hoskins, B., and Turner, A.: A Regime View of the North Atlantic Oscillation and Its Response to Anthropogenic Forcing, J. Climate, 23, 1291–1307,, 2010. 

Zubiate, L., McDermott, F., Sweeney, C., and O'Malley, M.: Spatial variability in winter NAO-wind speed relationships in western Europe linked to concomitant states of the East Atlantic and Scandinavian patterns, Q. J. Roy. Meteorol. Soc., 143, 552–562,, 2017. 

Short summary
This review presents new EOF-based monthly indices of the east Atlantic and the Scandinavian patterns covering the period from 1851 to present. The paper also includes a comparison with their analogous instrumental indices, provides insights into the reasons why different sources of data may give slightly different time series and demonstrates that using these patterns to explain climate variability beyond the winter season needs to be done carefully due to their non-stationary behaviour.