A dynamical downscaling of the 6-hourly 1948–2006 NCEP/NCAR re-analyses for the subarctic region of the North Atlantic has been used to derive a climatology of polar lows by means of a tracking algorithm based on the simulated bandpass filtered MSLP-fields. This climatology is consistent with the limited observational evidence in terms of frequency and spatial distribution. The climatology exhibits strong year-to-year variability but weak decadal variability and a negligible trend. A Canonical Correlation Analysis describes the conditioning of the formation of polar lows by characteristic meridional seasonal mean flow regimes, which favor cold air outbreaks and upper air troughs.
 Polar lows [Rasmussen and Turner, 2003] are severe maritime mesoscale storms in sub polar regions with wind speed around and above gale force.
 Since the availability of comprehensive observations supported by satellite imagery, a couple of authors dealt with climatological issues of polar lows [Businger, 1985; Wilhelmsen, 1985; Noer and Ovhed, 2003; Blechschmidt, 2008]. However these observation based studies lack a sufficiently long enough time series of polar low occurrences and might also suffer from inhomogeneities due to the subjective way of data recording for robust statements on trends and variability of polar lows.
 So far the requirement of a sufficiently long and homogeneous time series is only fulfilled by numerical reanalysis data. Thus a number of further authors have applied global reanalysis data to investigate characteristics of polar lows statistics recently. Condron et al.  located the Laplacian of the pressure field or geopotential height in relatively coarsely gridded reanalysis data to detect mesocyclones and investigate their frequency. To overcome the problem of too coarsely resolved data in the global reanalysis products Kolstad  identifies low static stability and reverse wind shear conditions in the ERA40 reanalyses [Simmons and Gibson, 2000] indicative for reverse shear polar lows. Similarly Claud et al.  made use of different indicators for polar lows in reanalysis fields (NCEP and ERA40), which they related to various low frequency patterns of the atmosphere. By applying a cold air outbreak indicator and a vorticity constraint to numerical weather prediction data, Bracegirdle and Gray  managed to identify individual polar low events in the North Atlantic. However, their data spanned a short time (2000–2004) and it was not possible to track polar lows in the 12 hourly output fields. A cold air outbreak indicator was also used as an indirect measure of polar low activity by Kolstad et al. .
 In this paper we make use of the coarsely resolved large scale atmospheric fields of the NCEP/NCAR global reanalyses [Kalnay et al., 1996], but we downscale them with a higher resolution local area model (LAM) for a period of almost 60 years. That individual polar low cases are by and large reproducible with such an approach has been shown [Zahn et al., 2008]. However, the core pressures are too high compared to synoptic analyses but considerably deeper than in the driving re-analyses. The same is true for wind speeds.
Zahn and von Storch  (hereinafter referred to as ZvS08) exploited two dimensional digital bandpass filters [Feser and von Storch, 2005] to develop an automated detection procedure to track polar lows over a two year period and showed that statistics of polar lows in terms of frequency and spatial distribution can be derived with such an approach. Here we use the same algorithm to extend this work to a longer time period, from 1948 through 2006. This enables the compilation of a long term data base of polar lows for the first time. In this paper we use this data base to investigate trends and variability of polar low occurrences in the North Atlantic and their linkage to the large scale pressure situation over the last 60 years.
2. Data and Methodology
 The LAM we applied in this study is the CLM, the climate version of the “Lokal Modell” of the German Weather service [Böhm et al., 2006]. As initial and lateral boundary values, we used the NCEP/NCAR re-analyses [Kalnay et al., 1996]. The NCEP-large scale situation is enforced through spectral nudging [von Storch et al., 2000] to prevent CLM significantly deviating from the analyzed large scale state. Sea surface temperature and sea ice extent were also prescribed according to the NCEP/NCAR re-analyses. The simulation period starts 1 January 1948 and lasts through February 2006. The simulation area covers the whole North Atlantic including the Labrador Sea west of Greenland and the Barents Sea in the East, the ice edge prone to shallow baroclinicity in the North and about the position of the Polar Front in the South (cf. Figure 1 of ZvS08).
 The objective detection procedure of ZvS08 was applied to the simulated output fields. The detection procedure searches for the minima in the bandpass filtered mean sea level pressure (MSLP) fields and concatenates the minima in consecutive time steps to tracks. Along these tracks, the fulfillment of further criteria are requested: (1) strength of the minimum (≤−2 hPa once along the track), (2) wind speed (≥13.9 once along the track), (3) air-sea temperature difference (SST − T500 hPa ≥ 43 K), (4) north south direction of the track, and (5) limits to allowable adjacent grid boxes.
 When the strength of the minimum in the bandpass filtered MSLP field decreases below −6 hPa once, and there are not too many coastal grid boxes around that location, a polar low is recorded independent of the other criteria.
 Polar lows are winter phenomena which in general occur in the period from October through May. Therefore, we use the term “Polar Low Season” (PLS) to describe the one year period from July through June the following year. A polar low season is addressed by the second year, e.g. the PLS 1950 begins in July 1949 and ends June 1950. PLSs 1948 and 2006 are omitted from our statistical analysis, as they do not contain the whole number of 12 months.
3.1. Trends and Variability
Figure 1 shows the yearly time series of the number of detected polar lows per PLS. 3313 polar lows resulted in a mean number of approx. 56 polar lows for each PLS with a strong year-to-year variability indicated by a standard deviation of σ ≈ ±13. Maximum and minimum numbers of detected cases are found in PLS 1981 with 100 cases and 1964 with only 34 cases.
 The decadal variability is weak. The overall trend in the frequency of polar lows is negligible with −0.024 cases/year. Also, the slope of the trend strongly depends on the number of cases of the first/last PLSs.
 The annual cycle of monthly numbers of detected polar lows reveals highest frequency in winter with maxima in December and January and almost no polar low activity in summer (not shown). Contrary to other authors [e.g., Wilhelmsen, 1985; Lystad, 1986; ZvS08; Noer and Ovhed, 2003] no secondary minimum of polar low activity in February compared to January and March is found in our investigations for the whole period. However Wilhelmsen  and Lystad  only focused on the northern North Atlantic close to Norway during a few winters. When we extract activity in equivalent periods and regions these secondary minima become visible in our data too, (not shown). Similarly a secondary minimum is evident for polar low activity in PLSs 1993 through 1995 (cf. ZvS08), but not for period and region used by Noer and Ovhed .
 The spatial distribution of polar low occurrences is plotted in Figure 2. The location of each polar low is defined as the location at which its track is detected for the first time. Highest absolute frequency and frequency per maritime area are found in the region south and east of Iceland in accordance with investigations of Harold et al.  or Condron et al. . Although Bracegirdle and Gray  mainly focus their investigations on the North Atlantic around Norway, they also detect a maximum of possible polar lows in the Iceland-Greenland region.
 A second maximum in counts per maritime area unit is found in the northern North Atlantic regions, R7 and R2, which is also in accordance with the above mentioned studies and with Kolstad .
 Also for the different regions, only negligible trends and high year-to-year variability for polar low frequency are found. Almost all regions (apart from R5 and R8) have PLSs without polar low activity but also PLSs with high activity (not shown).
 We further examined the sensitivity of the time series regarding the thresholds prescribed in the algorithm. On the one hand, we used lower and higher thresholds for wind speed (≥10.8 and ≥17.2 ) and “air-sea temperature difference” (≥39 K and ≥45 K) and on the other hand we left out the “air-sea temperature difference” and the “north south direction of the track” criterion, respectively. There is a strong effect on the yearly numbers of detected polar lows (up to three times more cases when leaving the “north south direction of the track” criterion out), but no changes in the statistics: negligible trends and strong variability persist and the courses of the time series remain similar. Correlation coefficients are above ρ > 0.9 between the times series gained with the varied thresholds and ρ ≈ 0.8 with the others.
3.2. Links to Large Scale Pressure Patterns
 Here we investigate how PLS-mean MSLP patterns are related to the distribution of yearly numbers of polar low occurrences. The PLS-mean MSLP fields are calculated consistently to the PLSs, namely as the mean field from July through June the following year. We consider this quantity because it is a large-scale, reliably and homogeneously analyzed field.
 Note that we do not compare the synoptic situation, as given by an instantaneous air pressure field, directly with the probability of a polar low to occur. Instead we indirectly relate the statistic of the “PLS mean MSLP field” with the statistic of the “number of Polar Lows” formed in different regions. Hence the mean state favors synoptic situations which condition polar low formation as a random realization of the short-term variability [cf. Branstator, 1995; von Storch and Reichardt, 1997].
 We quantify the linkage between the yearly mean MSLP-fields and the various regions' polar low time series by means of Canonical Correlation Analysis (CCA) [von Storch and Zwiers, 1999]. CCA is a method to calculate correlation between several multidimensional sets of variables. To exclude noise in each set we used the first 5 Empirical Orthogonal Functions (EOFs) of both the polar low time series on the one hand and the PLS-mean MSLP (representing 77% and 85% of the variance, respectively). We excluded the time series of R13 and R14, because there were too few polar lows occurring in these regions.
Figure 3 shows the two most important combinations of patterns in terms of MSLP and polar low occurrence anomalies. Their coefficient time series (Figures 3a and 3b) share a correlation of about 0.60 - and thus may be degenerate, so that any linear combination of the two patterns would qualify. They both together describe about 40% of the year-to-year variance of polar low occurrences.
 The first Canonical pattern (CCA1, Figure 3c) describes a bipolar pressure distribution - when the CCA coefficient is positive then on average there will be a southward flow across the Norwegian Sea, and consistently, more polar lows. A pressure contrast of about 2 hPa between Northern Scandinavia and the region south of Greenland is associated with 0.5 to 1.6 less polar lows in the regions around south of Greenland (R5,R10,R12). In the remaining regions of the North Atlantic, above normal polar low activity is found. Highest values of 1.7 and 2.0 appear in the regions in the pattern's central southward flow, R7 and R8. This pattern is reminiscent of the flow patterns found to be characteristic for marine cold air outbreaks in the these regions [Kolstad et al., 2008]. Skeie  suggests to call this anomalous circulation pattern “Barents Oscillation”, as its center is located over the Barents Sea. When the sign of the coefficient changes, the pattern of additional and less polar lows reverses as well.
 A similar co-variability is described by the second pattern (Figure 3d), with a unipolar pattern centered over the Norwegian Sea and negative values below 1.5 hPa. Now the mean southward flow is shifted farther west compared to the first pattern. Accordingly highest values of 3.2 more polar lows show up in the region between Greenland and Iceland, R5.
 When examining the time series in Figures 3a and 3b, it is evident that CCA1 dominates the PLSs 1953, 1981 and 2005. In these PLSs noticeably high numbers of polar lows occur contemporaneously in the regions basically contributing to CCA1, R7,R8 and R9. Accordingly, minima of the time series correspond to years (e.g., 1954, 1990) with few polar low in all these regions.
 The second Canonical pattern (CCA2) is dominated by the region between Iceland and Greenland, R5. Thus CCA2 dominates in 1951 and 1995 with high numbers of polar lows in R5 and with a negative sign in 1964, 1996 and 2003 with markedly less polar lows in this region.
 We conducted the same investigations applying the mean MSLP field for the periods in which most of the polar lows occur, October through March. The results qualitatively stay the same, but numbers change to higher values. Now the former CCA2 pattern shares a correlation 0.74 and CCA1 shares a correlation of 0.64. The explained variances remain similar. The such gained time coefficients are similar those obtained based on the whole PLS (ρ > 0.85).
 We conclude that a dynamical link exists between the occurrence of polar lows and time mean flow on time scales of years and longer, a significant link is associated only with anomalous meridional flow. The same analysis, with geopotential height at 500 hPa instead of MSLP, gave essentially the same results.
4. Summary and Outlook
 For the first time a multidecadal LAM simulation was done with the purpose of deriving a climatology of polar lows in the subpolar North Atlantic.
 The 1949–2005 climatology shows large inter annual variability, but little decadal variability of polar low occurrences and no significant long-term changes in overall or regional polar low activity.
 By means of Canonical Correlation Analysis we determined MSLP patterns, averaged across a polar low year, which favor or disfavor the formation of spatial polar low occurrence. Meridional southward/poleward mean flows were found to establish large-scale time mean environments within which less/more polar lows develop.
 An important caveat with this study is that the model did not reproduce all polar lows of the real world; instead relevant statistics of polar low dynamics are realistically reproduced - in particular the number of polar lows, their spatial distribution and the link to the time mean circulation are simulated consistently with the limited (typically: few years) observational evidence. The simulation is thus useful to analyze climatological issues of polar lows, but only to a limited extent for studying synoptic details of specific events.
 In this study we have used the data set only to assess year-to-year variability and possible trends. Beyond these issues, the space-time complete, digital data set has a high potential for the analysis of other issues, such as development mechanisms or the statistical linkage between polar low frequency and synoptic situations.
 Thanks to Eduardo Zorita for support with the statistical routines and to Dennis Bray for reading the manuscript. The work was conducted within the Virtual Institute (VI) EXTROP which is promoted by the “Initiative and Networking Fund” of the Helmholtz Association. NCEP Reanalysis data were provided by the NOAA/OAR/ESRL PSD, Boulder, Colorado, USA, from their Web site at http://www.cdc.noaa.gov/.