Search Results
variability of the zonal jets in the model. At any instant in time, the mean zonal flow comprises a dominant jet, together with two or three secondary jets primarily on its poleward side. The main jet wobbles quasiperiodically, in a manner that appears similar to the “annular mode” behavior of atmospheric jets. At the same time, the secondary jets, poleward of the main jet, migrate systematically equatorward such that, once every period of the main jet’s fluctuation, one secondary jet merges with the main
variability of the zonal jets in the model. At any instant in time, the mean zonal flow comprises a dominant jet, together with two or three secondary jets primarily on its poleward side. The main jet wobbles quasiperiodically, in a manner that appears similar to the “annular mode” behavior of atmospheric jets. At the same time, the secondary jets, poleward of the main jet, migrate systematically equatorward such that, once every period of the main jet’s fluctuation, one secondary jet merges with the main
in surface weather ( Thompson and Wallace 2001 ; Thompson et al. 2002 ). The dynamical coupling of the troposphere with the stratosphere 1 in the NH is captured by the northern annular mode (NAM; see Thompson and Wallace 1998 ; Baldwin and Dunkerton 1999 ; Thompson and Wallace 2000) . In the winter stratosphere the annular mode is linked to the temperature and strength of the polar vortex. In the lowermost troposphere, the NAM appears as the Arctic Oscillation and, in particular, over the
in surface weather ( Thompson and Wallace 2001 ; Thompson et al. 2002 ). The dynamical coupling of the troposphere with the stratosphere 1 in the NH is captured by the northern annular mode (NAM; see Thompson and Wallace 1998 ; Baldwin and Dunkerton 1999 ; Thompson and Wallace 2000) . In the winter stratosphere the annular mode is linked to the temperature and strength of the polar vortex. In the lowermost troposphere, the NAM appears as the Arctic Oscillation and, in particular, over the
1. Introduction What determines the zonal structure of the North Atlantic Oscillation (NAO) and the annular modes, the dominant patterns of variability in the extratropical atmosphere on intraseasonal time scales of 10–100 days? Various authors, including Limpasuvan and Hartmann (2000) , DeWeaver and Nigam (2000) , and Benedict et al. (2004) show or suggest that these large-scale patterns are driven and maintained by eddy–mean flow interactions and that their decorrelation time scale is on
1. Introduction What determines the zonal structure of the North Atlantic Oscillation (NAO) and the annular modes, the dominant patterns of variability in the extratropical atmosphere on intraseasonal time scales of 10–100 days? Various authors, including Limpasuvan and Hartmann (2000) , DeWeaver and Nigam (2000) , and Benedict et al. (2004) show or suggest that these large-scale patterns are driven and maintained by eddy–mean flow interactions and that their decorrelation time scale is on
1. Introduction The annular modes are the leading patterns of variability in the extratropics of each hemisphere ( Thompson and Wallace 1998 , 2000 ). The spatial structure is often described in terms of a dipole of pressure or geopotential, with a ring of anomalously high values in the midlatitudes, and a region of anomalously low values centered toward the pole. The patterns’ signature appears robustly in other meteorological fields, most notably zonal wind ( Lorenz and Hartmann 2001 , 2003
1. Introduction The annular modes are the leading patterns of variability in the extratropics of each hemisphere ( Thompson and Wallace 1998 , 2000 ). The spatial structure is often described in terms of a dipole of pressure or geopotential, with a ring of anomalously high values in the midlatitudes, and a region of anomalously low values centered toward the pole. The patterns’ signature appears robustly in other meteorological fields, most notably zonal wind ( Lorenz and Hartmann 2001 , 2003
symmetry. Therefore there has been a growing acceptance to refer to these modes as annular ( DeWeaver and Nigam 2000 ). It has even been suggested that the dominant modes in each hemisphere bear a resemblance and should be referred to as the northern annular mode (NAM) and the southern annular mode ( Limpasuvan and Hartmann 2000 ). The AO or NAM is strongly correlated with the well-known teleconnection pattern, the North Atlantic Oscillation (NAO). Whether the dominant mode of Northern Hemisphere (NH
symmetry. Therefore there has been a growing acceptance to refer to these modes as annular ( DeWeaver and Nigam 2000 ). It has even been suggested that the dominant modes in each hemisphere bear a resemblance and should be referred to as the northern annular mode (NAM) and the southern annular mode ( Limpasuvan and Hartmann 2000 ). The AO or NAM is strongly correlated with the well-known teleconnection pattern, the North Atlantic Oscillation (NAO). Whether the dominant mode of Northern Hemisphere (NH
similar to the present climate. We discuss why this is so. In section 3 we describe the variability observed in the coupled system. Because of the absence of meridional boundaries, there are no persistent east–west temperature gradients and the “ENSO” phenomenon is absent. The leading modes of variability are midlatitude “annular modes” in which the atmospheric westerlies fluctuate in both strength and position ( Thompson and Wallace 1998 ). This leads to changes in the zonal wind stress that also
similar to the present climate. We discuss why this is so. In section 3 we describe the variability observed in the coupled system. Because of the absence of meridional boundaries, there are no persistent east–west temperature gradients and the “ENSO” phenomenon is absent. The leading modes of variability are midlatitude “annular modes” in which the atmospheric westerlies fluctuate in both strength and position ( Thompson and Wallace 1998 ). This leads to changes in the zonal wind stress that also
-mean zonal wind will be referred to as the zonal index mode. The leading EOF of Northern Hemisphere (NH) extratropical sea level pressure (SLP) was defined by Thompson and Wallace (1998) as the Arctic Oscillation, or Northern Annular Mode [respectively the Antarctic Oscillation or Southern Annular Mode for the Southern Hemisphere (SH) SLP]. The EOF spatial structures are equivalent barotropic and dipole-like, and are approximately zonally symmetric with oppositely signed anomalies in the mid- and high
-mean zonal wind will be referred to as the zonal index mode. The leading EOF of Northern Hemisphere (NH) extratropical sea level pressure (SLP) was defined by Thompson and Wallace (1998) as the Arctic Oscillation, or Northern Annular Mode [respectively the Antarctic Oscillation or Southern Annular Mode for the Southern Hemisphere (SH) SLP]. The EOF spatial structures are equivalent barotropic and dipole-like, and are approximately zonally symmetric with oppositely signed anomalies in the mid- and high
1. Introduction The annular modes are the leading mode of variability in the extratropical atmosphere of each hemisphere ( Thompson and Wallace 2000 ). They take the form of dipole structures, centered on the time-mean jets and representing north–south fluctuations of the maximum jet speed. With a decorrelation time of 10–30 days, the annular modes are a key source of predictability for midlatitude weather, and their persistence has been linked to the extratropical atmosphere’s response to
1. Introduction The annular modes are the leading mode of variability in the extratropical atmosphere of each hemisphere ( Thompson and Wallace 2000 ). They take the form of dipole structures, centered on the time-mean jets and representing north–south fluctuations of the maximum jet speed. With a decorrelation time of 10–30 days, the annular modes are a key source of predictability for midlatitude weather, and their persistence has been linked to the extratropical atmosphere’s response to
1. Introduction In this study, we pursue the ongoing question of the zonal structure of the annular modes. The annular modes (AMs) are usually defined as the first EOF of the hemisphere-wide streamflow in the Northern Hemisphere (NH) or Southern Hemisphere (SH) extratropics ( Thompson and Wallace 1998 , 2000 ). The hemisphere-wide EOF analysis produces hemispheric-scale streamflow patterns with a dipolar meridional structure and relatively little zonal structure. On the other hand
1. Introduction In this study, we pursue the ongoing question of the zonal structure of the annular modes. The annular modes (AMs) are usually defined as the first EOF of the hemisphere-wide streamflow in the Northern Hemisphere (NH) or Southern Hemisphere (SH) extratropics ( Thompson and Wallace 1998 , 2000 ). The hemisphere-wide EOF analysis produces hemispheric-scale streamflow patterns with a dipolar meridional structure and relatively little zonal structure. On the other hand
1. Introduction In the extratropical circulation of both hemispheres, a long-recognized dominant pattern of variability at the intraseasonal to interannual time scales is the “annular mode,” which is often derived from empirical orthogonal function (EOF) analysis of meteorological fields such as zonal-mean zonal wind or geopotential heights and has been known for decades ( Kidson 1988 ; Thompson and Wallace 1998 ; Feldstein 2000 ). The leading EOF (EOF1) of features an equivalent
1. Introduction In the extratropical circulation of both hemispheres, a long-recognized dominant pattern of variability at the intraseasonal to interannual time scales is the “annular mode,” which is often derived from empirical orthogonal function (EOF) analysis of meteorological fields such as zonal-mean zonal wind or geopotential heights and has been known for decades ( Kidson 1988 ; Thompson and Wallace 1998 ; Feldstein 2000 ). The leading EOF (EOF1) of features an equivalent
