Advertisement

Theoretical and Applied Climatology

, Volume 113, Issue 1–2, pp 305–315 | Cite as

Multidecadal variability of summer temperature over Romania and its relation with Atlantic Multidecadal Oscillation

  • Monica IonitaEmail author
  • Norel Rimbu
  • Silvia Chelcea
  • Simona Patrut
Original Paper

Abstract

We investigate the multidecadal variability of summer temperature over Romania as measured at 14 meteorological stations with long-term observational records. The dominant pattern of summer temperature variability has a monopolar structure and shows pronounced multidecadal variations. A correlation analysis reveals that these multidecadal variations are related with multidecadal variations in the frequency of four daily atmospheric circulation patterns from the North Atlantic region. It is found that on multidecadal time scales, negative summer mean temperature (TT) anomalies are associated with positive sea level pressure (SLP) anomalies centered over the northern part of the Atlantic Ocean and Scandinavia and negative SLP anomalies centered over the northern part of Africa. It is speculated that a possible cause of multidecadal fluctuations in the frequency of these four patterns are the sea surface temperature (SST) anomalies associated to the Atlantic Multidecadal Oscillation (AMO). These results have implications for predicting the evolution of summer temperature over Romania on multidecadal time scales.

Keywords

Empirical Orthogonal Function North Atlantic Oscillation Atlantic Multidecadal Oscillation Multidecadal Variability Atlantic Multidecadal Oscillation Index 
These keywords were added by machine and not by the authors. This process is experimental and the keywords may be updated as the learning algorithm improves.

1 Introduction

The variations of surface air temperature and precipitation are of vital importance for society and economy (Watson et al. 2001). Present-day weather conditions affect the natural, social, and economic systems all over the globe. Central and southern Europe, including Romania, is considered to be one of the most vulnerable regions affected by changes in the climate system (IPCC 2007). Regional climate simulations over Europe have revealed that most of the warming in the southern part of Europe is related to soil moisture deficit in summer (Goubanova and Li 2007). Moreover, these simulated changes in high temperatures, in summer, are larger than the corresponding changes in the mean state suggesting also changes in the temperature variability (Rowell 2005; Fischer and Schär 2009).

The atmospheric circulation is the principal factor that determines the climate variability in Europe. It can be characterized using circulation patterns or circulation types. The circulation patterns and their corresponding indices are frequently identified using the principal component analysis (e.g., Barnston and Livezey 1987; Thompson and Wallace 1998; Compagnucci and Richman 2008; Philipp 2009). On the other hand, circulation types can be identified using both subjective as well as objective classification methods (Kyselý and Huth 2006; Beck et al. 2007; Christiansen 2007; Fereday et al. 2008; Huth et al. 2008). Subjective manual classification of synoptic circulation patterns have been employed for single countries or limited regions (e.g., Yarnal 1993), for larger territories like Europe (e.g., Hess and Brezowsky 1969) and even for the whole hemisphere (Dzerdzeevski 1968).

Two of the most important phenomena that influence the temperature variability over Europe are the North Atlantic Oscillation (NAO) and the Atlantic Multidecadal Oscillation (AMO). NAO is one of the leading modes of climate variability over the Northern Hemisphere and consists of a north–south dipole of sea level pressure (SLP) anomalies, with one center located over Iceland and the other one over Azore. Changes in these large-scale modes have a strong influence on the temperature variability (Bárdossy and Caspary 1990; Xoplaki et al. 2003; Cahynová and Huth 2009). The climatic effects of NAO have been widely studied, reveling NAO to be the most important source of climate variability in Europe (Hurrell 1995; Osborn et al. 1999). The interannual to multidecadal climate variations over Europe have been related with variations in both phase and amplitude of NAO. The influence of NAO on the temperature variability over Europe has been intensively studied by different authors (Hurrell 1995; Slonosky and Yiou 2001; Dorn et al. 2003; Rauthe and Paeth 2004; Stephenson et al. 2006).

AMO is defined by the detrended Sea Surface Temperature (SST) anomalies over the North Atlantic from 0°N to 70°N (Enfield et al. 2001) and is characterized by a cycle of about 70 years. Knight et al. (2006) showed that AMO can explain 30–40 % of the low frequency of the Central England Temperature (CET) variance and that the climate effects of AMO, over Europe, are strongest in summer and autumn.

During the last decade, Romania has experienced the highest summer temperatures in the last 100 years. Just in July 2000, the daily maximum temperature was above 40 °C for more than 100 cases at meteorological stations situated over the Romanian territory. These extreme values might be triggered either by anthropogenic factors or by natural occurring changes in the climate system. Considerable attention has been paid lately on the understanding of the natural cycles, so that it may be correctly accounted for in the evolution assessments of greenhouse gases.

Romania is situated in the southeastern part of Europe (Fig. 1) and has a temperate continental climate. Various studies have shown certain changes in surface air temperature and precipitation regimes over Romania. Bojariu and Paliu (2001) found a significant connection between NAO phases and the Romanian temperature variability in winter, while Tomozeiu et al. (2002) showed that the mean maximum temperature over Romania presents a strong seasonal dependence on various large-scale circulation indices and the summer maximum temperature over Romania presents a significant increasing trend, with an upward shift in 1985.
Fig. 1

The topographic map of Romania and the location of the stations used in this study

A possible candidate to explain the decadal variability of summer temperature over Romania might be the SST from the Atlantic basin. It has been proposed that SST anomalies govern, at least partly, precipitation and air temperature anomalies in the neighboring continental regions (Hunt and Gordon 1988; Zorita et al. 1992; Rimbu et al. 2001). In addition, there are strong indications that fluctuations in SST, and hence fluctuations of surface fluxes, are intimately involved in decadal-scale climate variability (Trigo and DaCamara 2000). Many studies also suggested that the potential predictability of the climate system could be found in the decadal and longer cycles of SSTs (e.g., Rodwell et al. 1999).

In recent decades, Europe has experienced unprecedented rate of summer warming (Klein Tank and Können 2003; Luterbacher et al. 2004; Klein Tank et al. 2005). Recent studies (Sutton and Hodson 2005) have looked at the mechanisms that contribute to the formation and prediction of such extreme warm events and they attribute the long-term variability of summer average temperature to a mode of SST called the AMO (Enfield et al. 2001). The AMO is believed to be caused by the North Atlantic thermohaline circulation (Knight et al. 2005) and it has been linked with the occurrence of Sahel drought (Folland et al. 1986; Rowell et al. 1995), variability in the North Brazilian rainfall (Folland et al. 2001), North American climate (Sutton and Hodson 2005), US river streamflow variability (Enfield et al. 2001), and the frequency of Atlantic hurricanes (Goldenberg et al. 2001). This pattern has showed marked fluctuations in the twentieth century, with intervals between successive peaks and troughs of roughly 70 years (Mann and Park 1994; Schlesinger and Ramankutty 1994).

The aim of this study is to search for the physical mechanisms responsible for the multidecadal variability of summer temperature over Romania in connection with SST and large-scale atmospheric circulation. It is important to study such connections because the possibility of predicting temperature anomalies months or years in advance is of great interest to regional economies. Characterization of temperature variability on long time scales and identification of connections to climate forcings provide potential improvement for forecasts when the climate forcings are predictable or slowly evolving (Croley and Luukkonen 2003).

2 Data and methods

Our study is based on four data sets:
  1. 1.

    Monthly mean air temperature (TT) at 14 stations over Romania, for the summer months (June, July, and August [JJA]). The name and coordinates of the stations are presented in Table 1. The temperature data set is quality controlled (Busuioc et al. 2007).

     
  2. 2.

    The Extended Reconstructed SST (ERSST.v3, Smith et al. 2008), with a 2° × 2° resolution.

     
  3. 3.

    AMO time series index, which was taken from http://www.cdc.noaa.gov/Timeseries/AMO. The AMO index is defined as the SST averaged over 0°–60°N, 0°–80°W minus SST averaged over 60°S–60°N (Enfield et al. 2001).

     
  4. 4.

    The frequency of daily circulation patterns published by Philipp et al. 2007 (available online at http://www.cru.uea.ac.uk/cru/projects/emulate/). The daily mean SLP data set used to compute the daily patterns was taken from the data reconstructed by Ansell et al. (2006) within the European project EMULATE. Within the EMULATE project, a new reconstruction of daily mean SLP, based on instrumental data has been obtained (Ansell et al. 2006). This data set offers the possibility to extend the view of daily resolved circulation variability back to the year 1850.

     
Table 1

Geographical coordinates, altitude, mean annual temperature, and annual precipitation of the 14 stations used in the analysis

Name

Latitude (N)

Longitude (E)

Altitude (m)

Mean annual temperature (°C)

Annual precipitation (mm)

Bistrita

47° 09′

24° 31′

366

8.2

689

Baia Mare

47° 40′

23° 30′

216

9.5

921

Brasov

45° 42′

25° 32′

534

7.6

680

Bucureti Filaret

44° 25′

26° 06′

82

11.1

591

Calarasi

44° 12′

27° 20′

19

11.3

501

Constanta

44° 13′

28° 38′

13

11.4

386

Iasi

47° 10′

27° 38′

102

9.5

544

Ocna Sugatag

47° 47′

23° 57′

503

7.9

744

Roman

46° 58′

26° 55′

216

8.5

520

Sibiu

45° 48′

24° 09′

443

8.8

642

Sulina

45° 10′

29° 44′

3

11.2

319

Targu Jiu

45° 02′

23° 16′

203

10.3

749

Timisoara

45° 46′

21° 15′

86

10.8

599

Turnu Severin

44° 38′

22° 33′

77

11.6

672

All data sets were processed in the same way. First, the summer means (June, July, and August [JJA]) were calculated from the monthly means. Then, the summer standardized anomalies with respect to their mean and their standard deviation, estimated for the period 1899–2003, were produced. Since our focus is the multidecadal character of the data sets, we applied a 21-year running mean to the standardized time series for all data sets.

The dominant modes of summer temperature variability are based on Empirical Orthogonal Function (EOF) analysis (von Storch and Zwiers 1999). The aim of the EOF method is to find a new set of variables that capture most of the observed variance from the data through a linear combination of the original variables. The patterns provided by the EOF method show the main spatial features of summer temperature, while their time coefficient describes the dominant temporal variability in the data set. EOF analysis was performed for summer temperature anomalies at 14 stations using the normalized and detrended time series.

In order to analyze the temporal structure (interannual and decadal variability) of summer temperature variability over Romania, we applied a wavelet power spectrum. The wavelet analysis used in this paper follows the methods of Torrence and Compo (1998). Statistical significance is determined against a red noise null hypothesis using a chi-squared test. By decomposing a time series into a time–frequency space, it is possible to determine the dominant modes of variability, as well as, how these modes vary in time. The wavelet transform is designed to analyze time series that contain nonstationary power over many different frequency scales (Daubechies 1990). The wavelet transform breaks up a signal into scaled versions of a wavelet function, where the scale of the wavelet (the window) varies with frequency. Thus, the wavelet is narrow in time at high frequencies and the scale of the wavelet increases with decreasing frequency. The wavelet transform, therefore, expresses a time series in a three-dimensional space: time (x), scale/frequency (y), and power (z).

3 Results

3.1 Dominant pattern of summer temperature and its relationship with Atlantic Multidecadal Oscillation

The first EOF (Fig. 2a) captures in-phase variability for all analyzed stations. This monopolar structure (positive values at all stations) emphasizes that mainly the large-scale atmospheric circulation influences the multidecadal variability of the summer temperature over Romania. Although the structure of the first EOF is monopolar, there is a clear difference between the northwestern and southeastern parts of the country. This difference is due to the influence of the Carpathian Mountains, which acts as a barrier between the northwestern and southeastern parts of the country. The associated time coefficient (PC1), which gives the temporal evolution of the dominant pattern of temperature over Romania shows important multidecadal variations for the 1899–2003 period (Fig. 2b). A cold interval (1899–1920) was followed by a prolonged warm period (1925–1965). The last 20 years of the analyzed interval are also characterized by a warm phase. The second EOF (not shown), which explains 6.81 % of the total variance, is characterized by a strong dipole between the high altitude stations and low altitude stations.
Fig. 2

a First EOF of summer (June/July/August—JJA) temperature (TT) and b the corresponding time series (PC1)

PC1 time series, smoothed with a 21-year running mean filter, resembles the evolution of the summer AMO index (Fig. 3a). AMO was identified as the first rotated EOF of the Atlantic SST and has a periodicity of around 60–80 years (Enfield et al. 2001). The correlation coefficient between PC1 and summer AMO index is 0.8 (99 % significance level). High (low) summer temperatures occur during the warm (cold) phase of the AMO index. This supports the analysis of Sutton and Hodson (2005) which showed that the occurrence of extreme temperatures over Europe is related to long-term changes in the AMO phase.
Fig. 3

a The time series of PC1 (blue line) and time series of summer AMO index (red line), after a 21 years running mean has been applied. b The continuous wavelet power spectrum of the time series of PC1. c The continuous wavelet power spectrum of the time series of summer AMO index. d Squared wavelet coherence between the time series of PC1 and summer AMO index. The thick black line contour is the 5 % significance level against red noise. Arrows indicate the phase of the coherence, where right is in phase and left is in out-of-phase. Colors show the power (or variance). More details of the method are found in Torrence and Compo (1998)

The wavelet power spectra of summer PC1 (Fig. 3b) and summer AMO index (Fig. 3c) reveals that the power of the two time series is broadly distributed, the most significant peak being in the 60-year band. The cross wavelet transform (XVT) between PC1 and summer AMO index is shown in Fig. 3d. The cross wavelet analysis between the two time series provides a measure of coherence at each frequency (Torrence and Compo 1998). Both time series show high coherency in the 60-year band, which is known to be a periodicity characteristic to AMO (Schlesinger and Ramankutty 1994).

3.2 Relationship with global SST

Several studies have established that large-scale SST anomalies are linked to decadal climate variability (Dai et al. 1997; Cayan et al. 1998; Latif et al. 2000). Rajagopalan et al. (1998) found evidence of significant coherence at decadal time scale between tropical South Atlantic SST and NAO, with warm SSTs associated with the positive phase of NAO.

To assess the links between the summer temperature over Romania and global SST, we have constructed the composite maps of summer SST for the years of High (>1 standard deviation) and Low (<−1 standard deviation) values of summer PC1. This threshold was chosen as a compromise between the strength of the climate anomalies associated to temperature variability and the number of maps that satisfy this criterion. Further analysis has shown that the results are not sensitive to the exact threshold values used for our composite analysis. Here, we will show just the map corresponding to the difference between High and Low years.

The composite map between summer PC1 and summer SST is shown in Fig. 4. The main characteristic of the composite map is the quasimonopolar structure in the North Atlantic with positive SST anomalies over the entire North Atlantic. The PC1 time series is strongly related with SST anomalies over the whole basin, consistent with the correlation between PC1 and AMO (Fig. 2a). As indicated by other studies (Latif et al. 2004; Knight et al. 2005) such a quasimonopolar structure is associated with the extreme phases of the AMO (Mesta-Nuñez and Enfield 1999). High (low) SST anomalies are associated with positive (negative) phase of AMO. Taking into account the structure of the composite map, we can say that during the warm phase of the AMO, Romania experiences relatively high summer temperatures, which is in agreement with the evolution of the summer PC1 time series, presented in Fig. 2a.
Fig. 4

The composite map between JJA PC1 and SST (the contour lines indicate the SST-normalized anomalies significant at 95 % significance level on a standard t test)

3.3 Relationship with the frequency of daily circulation patterns from the North Atlantic

To study the connection with the atmospheric circulation, we used the frequency of the daily circulation patterns published by Philipp et al. (2007). These daily patterns were derived using a clustering scheme that combines the concepts of simulated annealing and diversified randomization (SANDRA), which is a more stable statistical scheme compared to the commonly used k-means method (Philipp et al. 2007). Application of the SANDRA algorithm to daily atmospheric circulation in the domain (20°N–75°N; 70°W–40°E) can be optimally represented by nine, 11, six, and eight patterns in winter (DJF), spring (MAM), summer (JJA), and autumn (SON), respectively (Philipp et al. 2007). In total, 34 patterns characterize the atmospheric circulation over the whole year. In our study, we have used the frequency of the six summer patterns covering the period 1850 to 2003. A detailed description of the patterns is given in Philipp et al. (2007).

To identify the daily atmospheric circulation patterns related to the summer temperature variability over Romania, we correlate the summer PC1 and the summer AMO index with the time series of the frequency of the summer daily circulation patterns. The correlation coefficients between JJA PC1, the summer AMO index, and the frequency of JJA patterns are given in Fig.  5a. The time series of summer PC1 and summer AMO index are significantly positively correlated (99 % significance level) with the frequency of clusters 3 and 6 and negatively correlated (99 % significance level) with the frequency of clusters 2 and 4, respectively. The time series of summer PC1 and the frequency of patterns 2, 3, 4, and 6 are shown in Fig.  5b. The temporal evolution of the time series is similar, being in agreement with the correlation coefficients. All time series present strong multidecadal variability.
Fig. 5

a Correlation coefficients between summer PC1 (black bar) and summer AMO index (red bar) and the summer patterns frequency and b time series of PC1 (black line) and time series of pattern 2 (red line), pattern 3 (blue line), pattern 4 (green line), and pattern 6 (magenta line)

Since the spatial structures of the summer patterns are already published (Philipp et al. 2007) and available online at the EMULATE web page (http://www.metoffice.gov.uk/hadobs/emslp/), we present here only the patterns that are strongly related to the summer PC1, that is, clusters 2, 3, 4, and 6, respectively. To have a clear image of the atmospheric circulation patterns associated with the frequency of the daily circulation patterns 2, 3, 4, and 6 at multidecadal time scales, we have constructed the composite maps of summer SLP for the years when the times series of each pattern was higher than 1 standard deviation (High) and lower than −1 standard deviation (Low), respectively. In Fig. 6, we show just the maps corresponding to the difference between High and Low years. Prior to the composite analysis, both the times series of the pattern frequency and SLP data were smoothed with a 21-year running mean filter. The resulting patterns (Fig. 6a, b, c, d) resemble the corresponding daily anomaly patterns presented in the original paper of Philipp et al. (2007).
Fig. 6

SLP pattern associated with the multidecadal variations in the frequency of a pattern 2, b pattern 3, c pattern 4, and d pattern 6. Units: hPa

The composite maps of patterns 2 and 4 (negatively correlated with summer PC1) and SLP are shown in Fig. 6a and Fig. 6c, respectively. According to these patterns, negative temperature (TT) anomalies are associated with positive SLP anomalies centered over the northern part of the Atlantic Ocean and Scandinavia and negative SLP anomalies centered over the northern part of Africa. This pattern favors the advection of cold air from the high latitudes throughout the southeastern part of Europe, including Romania. The composite maps of patterns 3 and 6 (positively correlated with PC1) and SLP are presented in Fig. 6c and d, respectively. The low-pressure system over the British Isle and the high-pressure system over the south-central part of Europe induce negative temperature anomalies over the western part of Europe and positive temperature anomalies over the eastern part of Europe, including Romania. According to Sutton and Hodson (2005), the positive phase of AMO is associated with a low SLP center situated west of the United Kingdom, a pattern that is similar to the ones identified for patterns 4 and 6, respectively.

These results are also in agreement with the recent results of Della-Marta et al. (2007) who showed that extreme high temperatures over Europe have a multidecadal oscillation. One possible mechanism for the patterns identified is that AMO modulates the frequency of these daily patterns during its extreme phases, and in this way, modulates the variability of summer temperature. These tendencies are clearly reflected in the correlations between summer PC1, the summer AMO index, and the patterns frequencies.

4 Discussion

In this study, we have investigated the decadal variability of summer temperature over Romania and its connection with global SST and large-scale atmospheric circulation. We have found evidences supporting the analysis of Sutton and Hodson (2005) and Della-Marta et al. (2007) which stated that the occurrence of warmer than average summer temperatures over Europe are related to long-term changes in the AMO.

The first principal component of summer temperature over Romania presents a strong multidecadal variation. A cold interval starting from 1899 up to 1920 was followed by a very warm period from 1925 until 1965. Since around 1990, the time series shows the indication of a new warm period. These extreme phases are significantly correlated with the phases of the summer AMO index. High values of PC1 of the summer temperature over Romania are significantly correlated with anomalously high SST over the entire North Atlantic basin. This monopolar structure of the SST anomalies is associated with AMO and confirms the findings presented before. There is also a strong evidence that the frequency of US droughts (McCabe et al. 2004) and the frequency of European heat waves (Della-Marta et al. 2007) are both sensitive to Atlantic SSTs.

The alternance of these warm and cold phases might be related to the frequency of different weather patterns. The correlation coefficients between summer PC1, summer AMO index, and the frequency of the summer circulation patterns (Philipp et al. 2007) shows that both PC1 and AMO index are significantly related with four summer patterns (pattern 2, 3, 4, and 6, respectively). According to Philipp et al. (2007), the frequency of pattern 2 has increased and the associated pattern, in the SLP field, was associated with the strong cooling around 1900, a cooling which is also present in our summer PC1 time series.

One of the main aspects of our study is that we proved that not only on global or continental scale, but also at regional scale, the influence of AMO has a strong impact, especially during summer. Taking into account that AMO index has increased since around 1990, we may experience a period similar to 1925–1965 and the summer temperatures may be greater than the average in the next decade. These results have implications for predicting the evolution of summer temperature on decadal time scales.

Notes

Acknowledgments

Part of this work was supported by a grant of the Romanian National Authority for Scientific Research, CNCS-UEFISCDI; project number PNII-ID-PCCE-2011-2-0073 CLIMHYDEX.

References

  1. Ansell T, Jones PD, Allan R, Lister D, Parker D, Brunet M, Moberg A, Jacobeit J, Brohan P, Rayner NA, Aguilar E, Barriendos M, Brandsma T, Cox NJ, Della-Marta P, Drebs A, Founda D, Gerstengarbe F, Hickey K, Jonsson T, Luterbacher J, Nordli O, Oesterle H, Petrakis M, Philipp A, Rodwell MJ, Saladie O, Sigro J, Slonosky V, Srnec L, Garcia-Suarez A, Tuomenvirta H, Wang X, Wanner H, Werner P, Wheeler D, Xoplaki E (2006) Daily mean sea level pressure reconstructions for the European–North Atlantic region for the period 1850–2003. J Clim 19:2717–2742CrossRefGoogle Scholar
  2. Bárdossy A, Caspary H (1990) Detection of climate change in Europe by analyzing European atmospheric circulation patterns from 1881 to 1989. Theor Appl Climatol 42:155–167CrossRefGoogle Scholar
  3. Barnston AG, Livezey RE (1987) Classification, seasonality and persistence of low frequency atmospheric circulation patterns. Mon Weather Rev 115:1083–1126CrossRefGoogle Scholar
  4. Beck C, Jacobeit J, Jones PD (2007) Frequency and within-type variations of large scale circulation types and their effects on low-frequency climate variability in Central Europe since 1780. Int J Climatol 27:473–491CrossRefGoogle Scholar
  5. Bojariu R, Paliu D (2001) In: Brunet M, Lopez D (eds) North Atlantic oscillation projection on Romanian climate fluctuations in the cold season, detecting and modelling regional climate change and associated impacts. Springer, Berlin, pp 345–356CrossRefGoogle Scholar
  6. Busuioc A, Dumitrescu A, Soare E, Orzan A (2007) Summer anomalies in 2007 in the context of extremely hot and dry summers in Romania. Romanian J Meteor 9:1–16Google Scholar
  7. Cahynová M, Huth R (2009) Changes of atmospheric circulation in central Europe and their influence on climatic trends in the Czech Republic. Theor Appl Climatol 96:57–68CrossRefGoogle Scholar
  8. Cayan DR, Dettinger MD, Diaz HF, Graham NE (1998) Decadal variability of precipitation over western North America. J Clim 11:3148–3166CrossRefGoogle Scholar
  9. Christiansen B (2007) Atmospheric circulation regimes: can cluster analysis provide the number? J Clim 20:2229–2250CrossRefGoogle Scholar
  10. Compagnucci RH, Richman MB (2008) Can principal component analysis provide atmospheric circulation or teleconnection patterns? Int J Climatol 28:703–726CrossRefGoogle Scholar
  11. Croley TE II, Luukkonen CL (2003) Potential effects of climate change on ground water in Lansing, Michigan. J Am Water Resour Assoc 39(1):149–163CrossRefGoogle Scholar
  12. Dai AG, Fung IY, DelGenio AD (1997) Surface observed global land precipitation variations during 1900–1988. J Clim 10:2943–2962CrossRefGoogle Scholar
  13. Daubechies I (1990) The wavelet transform, time–frequency localization and signal analysis. IEEE Trans Inf Theory 36:965–1005CrossRefGoogle Scholar
  14. Della-Marta PM, Luterbacher J, von Weissenfluh H, Xoplaki E, Brunet M, Wanner H (2007) Summer heat waves over western Europe 1880–2003, their relationship to large scale forcings and predictability. Clim Dyn 29:251–275CrossRefGoogle Scholar
  15. Dorn W, Dethloff K, Rinke A, Roeckner E (2003) Competition of NAO regime changes and increasing greenhouse gases and aerosols with respect to Arctic climate projections. Clim Dyn 21:447–458CrossRefGoogle Scholar
  16. Dzerdzeevski BL (1968) Circulation of the atmosphere—circulation mechanisms of the atmosphere in the northern hemisphere in the 20th century (in Russian). Results of Meteorological Investigations, IGY Committee, Moscow. Inst. of Geography, Akad. Nauk., USSR, pp 240Google Scholar
  17. Enfield DB, Mestas-Nuñez AM, Trimble PJ (2001) The Atlantic multidecadal oscillation and its relation to rainfall and river flows in the continental US. Geophys Res Lett 28:277–280CrossRefGoogle Scholar
  18. Fereday DR, Knight JR, Scaife AA, Folland CK, Philipp A (2008) Cluster analysis of North Atlantic–European circulation types and links with tropical Pacific Sea surface temperatures. J Clim 21:3687–3703CrossRefGoogle Scholar
  19. Fischer EM, Schär C (2009) Future changes in daily summer temperature variability: driving processes and role for temperature extremes. Clim Dyn 33:917–935CrossRefGoogle Scholar
  20. Folland CK, Parker DE, Palmer TN (1986) Sahel rainfall and worldwide sea temperatures 1901–85. Nature 320:602–607CrossRefGoogle Scholar
  21. Folland CK, Colman AW, Rowell DP, Davey MK (2001) Predictability of northeast Brazil rainfall and real-time forecast skill, 1987–98. J Clim 14:1937–1958CrossRefGoogle Scholar
  22. Goldenberg SB, Landsea CW, Mestas-Nuñez AM, Gray WM (2001) The recent increase in the Atlantic hurricane activity: causes and implications. Science 293:474–479CrossRefGoogle Scholar
  23. Goubanova K, Li L (2007) Extremes in temperature and precipitation around the Mediterranean basin in an ensemble of future climate scenario simulations. Glob Planet Chang 57:27–42CrossRefGoogle Scholar
  24. Hess P, Brezowsky H (1969) Katalog der Grosswetterlagen Europas, 2. neu bearbeitete und ergänzte Aufl. Berichte des Deutschen Wetterdienstes 113. Offenbach am MainGoogle Scholar
  25. Hunt BG, Gordon HB (1988) The problem of naturally occurring drought. Clim Dyn 3:19–33CrossRefGoogle Scholar
  26. Hurrell JW (1995) Decadal trends in the North Atlantic oscillation: regional temperatures and precipitation. Science 269:676–679CrossRefGoogle Scholar
  27. Huth R, Beck C, Philipp A, Demuzere M, Ustrnul Z, Cahynová M, Kyselý J, Tveito OE (2008) Classifications of atmospheric circulation patterns. Ann N Y Acad Sci 1146:105–152CrossRefGoogle Scholar
  28. IPCC (2007) In: Solomon S, Qin D, Manning M, Chen Z, Marquis M, Averyt KB, Tignor M, Miller HL (eds) The physical science basis. Contribution of working group I to the fourth assessment report of the IPCC. Cambridge University Press, Cambridge, UK, p 996Google Scholar
  29. Klein Tank AMG, Können GP (2003) Trends in indices of daily temperature and precipitation extremes in Europe. J Clim 16:3665–3680CrossRefGoogle Scholar
  30. Klein Tank AMG, Können GP, Selten FM (2005) Signals of anthropogenic influence on European warming as seen in the trend patterns of daily temperature variance. Int J Climatol 25:1–16CrossRefGoogle Scholar
  31. Knight JR, Allan RJ, Folland CK, Vellinga M, Mann ME (2005) A signature of persistent natural thermohaline circulation cycles in observed climate. Geophys Res Lett 32:L20708. doi: 10.1029/2005GL024233 CrossRefGoogle Scholar
  32. Knight JR, Folland CK, Scaife AA (2006) Climate impacts of the Atlantic multidecadal oscillation. Geophys Res Lett 33:L17706. doi: 10.1029/2006GL026242 CrossRefGoogle Scholar
  33. Kyselý J, Huth R (2006) Changes in atmospheric circulation over Europe detected by objective and subjective methods. Theor Appl Climatol 85:19–36CrossRefGoogle Scholar
  34. Latif M, Arpe K, Roeckner E (2000) Oceanic control of decadal North Atlantic sea level pressure variability in winter. Geophys Res Lett 27:727–730CrossRefGoogle Scholar
  35. Latif M, Botset ERM, Esch M, Haak H, Hagemann S, Jungclaus J, Legutke S, Marsland S, Mikolajewicz U (2004) Reconstructing, monitoring and predicting multidecadal-scale changes in the North Atlantic thermohaline circulation with sea surface temperature. J Clim 17:1605–1614CrossRefGoogle Scholar
  36. Luterbacher J, Dietrich D, Xoplaki E, Grosjean M, Wanner H (2004) European seasonal and annual temperature variability, trends and extremes since 1500. Science 303:1499–1503CrossRefGoogle Scholar
  37. Mann ME, Park J (1994) Global scale modes of surface temperature variability on interannual to century time scales. J Geophys Res 99:25819–25833CrossRefGoogle Scholar
  38. McCabe GJ, Palecki MA, Betancourt JL (2004) Pacific and Atlantic Ocean influences on multidecadal drought frequency in the United States. Proc Natl Acad Sci 101:4136–4141CrossRefGoogle Scholar
  39. Mesta-Nuñez AM, Enfield DB (1999) Rotated global modes of non-ENSO sea surface temperature variability. J Clim 12:2734–2746CrossRefGoogle Scholar
  40. Osborn TJ, Briffa KR, Tett SFB, Jones PD, Trigo RM (1999) Evaluation of the North Atlantic oscillation as simulated by a coupled climate model. Clim Dyn 15:685–702CrossRefGoogle Scholar
  41. Philipp A (2009) Comparison of principal component and cluster analysis for classifying circulation pattern sequences for the European domain. Theor Appl Climatol 96:31–41. doi: 10.1007/s00704-008-0037-1 CrossRefGoogle Scholar
  42. Philipp A, Della-Marta PM, Jacobeit J, Fereday DR, Jones PD, Moberg A, Wanner H (2007) Long term variability of daily North Atlantic–European pressure patterns since 1850 classified by simulated annealing clustering. J Clim 20(16):4065–4095CrossRefGoogle Scholar
  43. Rajagopalan B, Kushnir Y, Tourre YM (1998) Observed decadal midlatitude and tropical Atlantic climate variability. Geophys Res Lett 25:3967–3970CrossRefGoogle Scholar
  44. Rauthe M, Paeth H (2004) Relative importance of Northern hemisphere circulation modes in predicting regional climate change. J Clim 17:4180–4189CrossRefGoogle Scholar
  45. Rimbu N, Le Treut H, Janicot S, Boroneant C, Laurent C (2001) Decadal precipitation variability over Europe and its relation with surface atmospheric circulation and sea surface temperature. Q J R Meteorol Soc 127(572B):315–329CrossRefGoogle Scholar
  46. Rodwell MJ, Rowell DP, Folland CK (1999) Oceanic forcing of the wintertime North Atlantic oscillation and European climate. Nature 398:320–323CrossRefGoogle Scholar
  47. Rowell DP (2005) A scenario of European climate change for the late twenty-first century: seasonal means and interannual variability. Clim Dyn 25:837–849CrossRefGoogle Scholar
  48. Rowell DP, Folland CK, Maskell K, Ward MN (1995) Variability of summer rainfall over tropical north Africa (1906–92): observations and modelling. Q J R Meteorol Soc 121:669–704Google Scholar
  49. Schlesinger ME, Ramankutty N (1994) An oscillation in the global climate system of period 65–70 years. Nature 367:723–726CrossRefGoogle Scholar
  50. Slonosky VC, Yiou P (2001) The North Atlantic oscillation and its relationship with near surface temperature. Geophys Res Lett 28(5):807–810. doi: 10.1029/2000GL012063 CrossRefGoogle Scholar
  51. Smith TM, Reynolds RW, Peterson TC, Lawrimore J (2008) Improvements to NOAA's historical merged land–ocean surface temperature analysis (1880–2006). J Clim 21:2283–2296CrossRefGoogle Scholar
  52. Stephenson D, Pavan V, Collins M, Junge M, Quadrelli R, Participating CMIP2 modelling groups (2006) North Atlantic oscillation response to transient greenhouse gas forcing and the impact on European winter climate: a CMIP2 multi-model assessment. Clim Dyn 27:401–420CrossRefGoogle Scholar
  53. Sutton RT, Hodson DLR (2005) Atlantic Ocean forcing of North American and European summer climate. Science 290:2133–2137Google Scholar
  54. Thompson DWJ, Wallace JM (1998) The Arctic oscillation signature in the wintertime geopotential height and temperature fields. Geophys Res Lett 25:1297–1300CrossRefGoogle Scholar
  55. Tomozeiu R, Busuioc A, Stefan S (2002) Changes in seasonal mean of maximum air temperature in Romania and their connection with large-scale circulation. Int J Climatol 22:1181–1196CrossRefGoogle Scholar
  56. Torrence C, Compo GP (1998) A practical guide to wavelet analysis. Bull Am Meteorol Soc 79:61–78CrossRefGoogle Scholar
  57. Trigo RM, DaCamara CC (2000) Circulation weather types and their impact on the precipitation regime in Portugal. Int J Climatol 20:1559–1581CrossRefGoogle Scholar
  58. von Storch H, Zwiers FW (1999) Statistical analysis in climate research. Cambridge University Press, pp 510Google Scholar
  59. Watson RT and the Core Writing Team. Climate Change (2001) Synthesis report. Summary for policymakers. A report of the Intergovernmental Panel on Climate Change. IPCC Secretariat, c/o World Meteorological Organization, Geneva, SwitzerlandGoogle Scholar
  60. Xoplaki E, González-Rouco J, Luterbacher J, Wanner H (2003) Mediterranean summer air temperature variability and its connection to the large-scale atmospheric circulation and SSTs. Clim Dyn 20:723–739Google Scholar
  61. Yarnal B (1993) Synoptic climatology in environmental analysis. Belhaven, LondonGoogle Scholar
  62. Zorita E, Kharin V, von Storch H (1992) The atmospheric circulation and sea surface temperature in the North Atlantic area in winter: their interaction and relevance for Iberian precipitation. J Clim 5:1097–1108CrossRefGoogle Scholar

Copyright information

© Springer-Verlag Wien 2012

Authors and Affiliations

  • Monica Ionita
    • 1
    Email author
  • Norel Rimbu
    • 1
    • 2
    • 3
  • Silvia Chelcea
    • 4
  • Simona Patrut
    • 3
    • 5
  1. 1.Alfred Wegener Institute for Polar and Marine ResearchBremerhavenGermany
  2. 2.Climed NoradBucharestRomania
  3. 3.University of Bucharest, Faculty of PhysicsBucharest-MagureleRomania
  4. 4.National Institute of Hydrology and Water ManagementBucharestRomania
  5. 5.Ministry of Environment and ForestsBucharestRomania

Personalised recommendations