The stratospheric polar vortex as a cause for the temporal variability of solar activity and galactic cosmic ray effects on the lower atmosphere circulation S.Veretenenko, M.Ogurtsov Ioffe Physical-Technical Institute, Russian Academy of Sciences, St.Petersburg, Russia 23rd ECRS GCR effects on troposphere pressure in different epochs the large-scale atmospheric circulation Epoch of increasing meridional circulation (C type) Epoch of decreasing meridional circulation (C type) (1982-2000 гг.) (1953-1981 гг.) -0 .7 6 -0 . 0.4 -0.5 -0 .5 40 0.3 0.4 0 -20 0.3 0.4 0.6 0.4 -0 .4 -40 -0 .4 -0 . 4 -0 .4 -0.4 -0.2 -160-120 - 80 - 40 0 0.2 0.4 3 0. .5 -0 -0 .5 -60 -80 -0 .4 Arctic front, January Arctic front, July Polar front, January Polar front, July Equatorial trough axis, January Equatorial trough axis, July -0.5 -0 .4 .5 -0 0.3 0 40 80 120 160 0.6 0.2 4 -0 . -0.4 -20 -40 -80 0. 4 0.4 0.4 20 0 -0 .5 0.4 -60 -0.6 0.4 80 -0 .6 60 0.5 20 -0 .4 Correlation coefficients between GPH 700 hPa and NM (Climax). Period: 1953-1981 -0 .4 0.6 .5 -0 0.7 -0 .5 4 -0 . 40 -0 . 5 60 0. 6 80 -0 .5 Correlation coefficients between GPH 700 hPa and NM (Climax). Period: 1982-2000 -160-120 - 80 - 40 0.5 5 0. 0.6 0 40 80 120 160 Arctic front, January Arctic front, July -0.6 -0.4 -0.2 0 0.2 0.4 0.6 Polar front, January Polar front, July Equatorial trough axis, January Equatorial trough axis, July GCR increase in the minima of the 11-year cycle is accompanied • Intensification of near-ground Arctic anticyclones • Intensification of extratropical cyclogenesis at Polar fronts • Weakening of the equatorial trough (tropical cyclogenesis) • Weakening of near-ground Arctic anticyclones •Weakening of extratropical cyclogenesis •Intensification of the equatorial trough Veretenenko and Ogurtsov, Adv. Space Res., 2012 Time variation of SA/GCR effects on troposphere pressure and the evolution of the large-scale atmospheric circulation Veretenenko and Ogurtsov, Adv. Space Res., 2012 Time variations of the correlation between troposphere pressure at high/middle latitudes and sunspot numbers reveal a pronounced ~60-year periodicity. 160 (a) 120 160 80 W, days 100 E, days C, days 200 80 W E C 120 0.8 1900 1920 1940 1960 1980 2000 (b) 0.4 0 -0.4 Polar Vortex -0.8 1880 16 Spectral power density Correlation coefficient 1880 40 1900 1920 Meridional form C (c) Reversals of the correlation sign at high latitudes occurred in the 1890s, the early 1920s, 1950s and the early 1980s 63 yrs 12 8 25 yrs 4 0 1940 Years 1960 1980 2000 0 0.04 0.08 0.12 0.16 16 0.2 Frequency, yr-1 The reversals of the sign of SA/GCR effects coincide with the changes in the evolution of the large-scale meridional circulation (the form C according to Vangengeim-Girs classification). Spectral density 120 Polar region 64 12 85°N 80°N 75°N 8 36 23 4 0 0 0.04 0.08 0.12 Frequency, yr -1 0.16 0.2 The results obtained show: Regional character of SA/GCR effects on troposphere pressure which is determined by peculiarities of baric systems forming in the regions under study; SA/GCR effects may change the sign depending on the time period; The sign of SA/GCR effects seems to be determined by the evolution of the large-scale meridional circulation; There are long-term variations, with the period being ~60 years, of the amplitude and sign of SA/GCR effects on troposphere pressure of high and middle latitudes The aim of this work is to study what processes may influence the evolution of the circulation epochs and the sign of SA/GCR effects on troposphere pressure? Main elements of the large-scale circulation of the atmosphere at middle and high latitudes Troposphere 4 x 10 0 20 -160 160 0 20 -160 1.24 40 160 1.6 40 1.22 -120 60 120 1.4 -120 1.2 60 1.2 1.18 80 120 80 1 1.16 - 80 0.8 80 - 80 80 1.14 0.6 1.12 - 40 0.4 1.1 40 - 40 40 1.08 0 0.2 0 GPH 200 hPa. January 2005. Magnitude of temperature gradients (grad/100 km). Layer 1000-500 hPa. January 2005. Planetary frontal zone (areas of high temperature contrasts in the troposphere ) Polar vortex (area of low pressure In the upper troposphere) Stratosphere AIR TEMPERATURE. 20 hPa. January 2005. -160 0 20 TEMPERATURE GRADIENT. 20 hPa. January 2005. 160 0 20 -160 160 40 -120 40 60 120 -120 60 80 120 80 1.3706 - 80 80 - 80 80 -79 - 40 40 - 40 40 0 -80 -75 -70 -65 -60 C 0 -55 -50 -45 -40 Polar vortex (cyclonic circulation in the middle/upper troposphere and stratosphere at high latitudes) Planetary frontal zone (regions of high temperature contrasts in the troposphere) Extratropical cyclones and anticyclones -35 0.7 0.8 0.9 1 1.1 C/100 km 1.2 1.3 In the stratosphere the polar vortex is seen as a region of low temperature with enhanced temperature gradients on its edges. GCR effects on troposphere pressure in the high-latitudinal area Epoch of increasing meridional circulation (1982-2000) Correlation coefficients betw een GPH 700 hPa and NM (Clim ax). Period: 1982-2000 0 20 0.6 Epoch of decreasing meridional circulation (1953-1981) Correlation coefficients betw een GPH 700 hPa and NM (Clim ax). Period: 1953-1981 0 20 0.6 40 -0.3 -0.5 -0.4 60 0.4 40 0.3 0.4 0.4 -0.6 0.4 60 -0.5 0.2 -0.4 80 0.6 0 0.4 0.6 0.7 0.3 -0.5 -0.2 -0.6 -0.4 0.4 -0.5 0.2 0.3 0 -0.3 -0.2 0.2 -0.4 -0.7 -0.6 -0.5 -0.4 0.4 80 0.3 0.4 0.5 -0.3 -0.4 -0.6 -0.6 1 2 3 4 5 6 Confidence levels for R(GPH700,NM) according to Monte-Carlo tests.1982-2000. 0 20 -160 1 2 3 0 20 -160 60 120 0.97 0.95 -120 60 120 0.97 0.95 0.98 0.9 80 0.9 0.95 0.97 0.98 80 0.97 0.98 160 40 0.95 - 80 6 0.95 0.9 80 0.97 5 Confidence levels for R(GPH700,NM)according to Monte-Carlo tests. 1953-1981. 160 40 0.9 0.95 0.97 -120 4 0.99 - 80 0.9 0.95 0.97 0.98 80 0.9 0.95 0.9 - 40 40 0 - 40 40 0 In the high-latitudinal area (independently of the time period) 0.95 0.9 0.9 0.95 0.9 Most. statistically significant correlation coefficients between troposphere pressure and GCR are observed: at Polar fronts (Polar frontal zones) at middle latitudes in the periods of increasing meridional circulation. Correlation coefficients betw een GPH 700 hPa and NM (Clim ax). Period: 1982-2000 0 20 0.6 Correlation coefficients betw een GPH 700 hPa and NM (Clim ax). Period: 1953-1981 0 20 0.6 40 -0.3 -0.5 -0.4 60 0.4 40 0.3 0.4 0.4 -0.6 -0.5 0.2 -0.4 80 0 0.4 0.6 0.7 0.3 -0.5 -0.2 -0.6 -0.4 0.3 0 -0.2 0.2 -0.4 -0.7 -0.6 -0.5 -0.4 0.2 -0.3 0.4 -0.5 0.4 80 0.3 0.4 0.5 0.6 0.4 60 -0.3 -0.4 -0.6 -0.6 1 2 3 4 5 1 6 AIR TEMPERATURE. 20 hPa. January 2005. -160 0 20 2 3 5 6 TEMPERATURE GRADIENT. 20 hPa. January 2005. 160 0 20 -160 160 40 -120 4 40 60 120 -120 60 80 120 80 1.3706 - 80 80 - 80 80 -79 - 40 40 - 40 40 0 -80 -75 -70 -65 -60 C 0 -55 -50 -45 -40 -35 0.7 0.8 0.9 1 1.1 1.2 The area of the polar vortex formation is an area of most significant correlations between troposphere pressure and GCR variations independently on the time period and the epoch of the largescale circulation 1.3 C/100 km This suggests a possible contribution of processes taking place in the polar vortex to GCR effects on the lower atmosphere circulation ~60-year cycle in the climate of the Arctic and the polar vortex state Gudkovich et al., Problems of Arctic and Antarctic, 2009 ~60-year cycle in the Arctic climate manifests itself as the rotation of cold and warm epochs which is closely related to the polar vortex states: Strong vortex warm epoch Weak vortex cold epoch The transitions between warm and cold epochs in the Arctic detected on the base of sea-level temperatures were found in the early 1920s, 1950s and 1980s Anomalies of mean yearly sea-level temperatures at latitudes 70-85N in the Arctic. The reversals of the sign of SA/GCR effects coincide well with the transitions between cold and warm epochs in the Arctic corresponding to the different states of the vortex. Time evolution of SA/GCR effects on troposphere pressure and the strength of the polar vortex according to NCEP/NCAR reanalysis data Correlation coefficient 0.8 a) 1950-1980 – the period of a weak vortex. 0.4 • Decrease of pressure gradients between middle and high latitudes • Increase of stratospheric temperature in the vortex area • Weakening of the C form of meridional circulation. • Cold epoch in the Arctic. 0 -0.4 R(SLP, Rz) R(GPH700, NM) -0.8 Frequency, days 120 110 b) 1980-2010 – the period of a strong vortex 100 • Increase of pressure gradients between middle and high latitudes • Decrease of stratospheric temperature in the vortex area • Intensification of the meridional circulation C. • Warm epoch in the Arctic. 90 80 C 70 H, gp.m 30 20 500 hPa c) 10 0 -10 H(40-65N) -20 The sign reversals of SA/GCR effects in the 1950s and 1980s correspond to the transitions between the different vortex states. Polynomial fit -30 Temperature, K 2 50 hPa d) 1 0 -1 T (60-90N) -2 1880 Polynomial fit 1900 1920 1940 Years 1960 1980 2000 Thus, the ~60-year variation of the amplitude and sign of SA/GCR effects on troposphere pressure seems to be closely related to the changes of the vortex strength and the corresponding changes of the large-scale atmospheric circulation Strong vortex : GCR increase in the 11-year cycle intensification of mid-latitudinal cyclones and polar anticyclones Weak vortex : GCR increase in the 11-yr cycle weakening of mid-latitudinal cyclones and polar anticyclones A possible reason for the sign reversals of SA/GCR effects may be changes in the troposphere-stratosphere coupling caused by different conditions for propagation of planetary waves in the periods of a strong or weak vortex. The polar vortex state seems to play an important part in the mechanism of solar-atmospheric links Temperature. 20 hPa. January 2005. a) -160 11 0 20 -35 160 40 -40 7 3 -120 2 60 -45 120 1 -50 0.5 80 -55 -60 0.5 - 80 -79 1 80 -65 2 3 - 40 -70 15 7 11 -75 40 -80 0 C The polar vortex location and vertical geomagnetic cutoff rigidities (in GV) according to Shea and Smart (1983). The area of the vortex formation is characterized by low rigidities, so GCR particles with a broad energy range may precipitate here including the low energy component strongly modulated by solar activity. Ion production rate in the vortex area is higher compared with that at middle and low latitudes Height, km Pressure, hPa b) 10 30 Temperature Temperature gradient Ion-pair production rate 20 25 30 20 50 70 100 15 150 200 10 300 400 500 5 700 850 1000 •The highest values of ionization due to GCR are observed in the lower part of the vortex (10-15 km) where temperature gradients at the vortex edges start increasing. • The 11-yr modulation of GCR fluxes is the strongest at 20-25 km where the vortex is most pronounced. 0 -90 0.4 0 -80 0.8 -70 -60 -50 Temperature, °Ñ 1.2 1.6 2 2.4 -40 2.8 -30 3.2 Temperature gradient, °Ñ/100 km 10 20 30 Ion-pair production rate, cm-3s-1 3.6 -20 Bazilevskaya et al., Space Sci. Rev, 2008 4 40 Height dependences of the Arctic air mass characteristics in January 2005 and the ion-pair production rate in free air at polar latitudes (R = 0-0.6 GV) according to Bazilevskaya et al. (2008). Monthly averaged fluxes of ionizing particles over Murmansk region (R =0.6 GV) The vortex location is favorable for the mechanisms of solar activity influence on the atmosphere circulation involving variations of GCR intensity Possible mechanisms of solar activity influence on the lower atmosphere circulation may involve changes of the vortex state associated with different agents (e.g., GCR variations, UV fluxes) Intensification of the polar vortex in the period when it is strong seems to contribute to an increase of temperature contrasts in tropospheric frontal zones and an intensification of extratropical cyclogenesis Conclusions: The evolution of the stratospheric polar vortex plays an important part in the mechanism of solar-climatic links. The detected long-term oscillations of correlations between troposphere pressure at middle and high latitudes and SA/GCR characteristics seem to be closely related to the changes of the polar vortex strength. The vortex strength reveals a roughly 60-year periodicity influencing the large-scale atmospheric circulation and the sign of SA/GCR effects on troposphere pressure. When the vortex is strong, meridional processes intensify and an increase of GCR fluxes results in an enhancement of cyclonic activity at middle latitudes and anticyclone formation at polar latitudes. When the vortex is weak, meridional processes weaken and GCR effects on the development of baric systems at middle and high latitudes change the sign. A possible reason for the sign reversals may be different troposphere-stratosphere coupling during the periods of a strong and weak vortex.