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1. Introduction Upper-level westerly jet streams are ubiquitous and important features of the subtropical atmospheric flow. On relatively short time scales (up to a few days) these jets serve as waveguides for synoptic-scale Rossby waves, which in turn can trigger high impact weather events (e.g., Martius et al. 2008 ; Feldstein and Dayan 2008 ). With regard to the transport of chemical constituents, the subtropical jets can act as local barriers for meridional exchange (e.g., Shuckburgh et
1. Introduction Upper-level westerly jet streams are ubiquitous and important features of the subtropical atmospheric flow. On relatively short time scales (up to a few days) these jets serve as waveguides for synoptic-scale Rossby waves, which in turn can trigger high impact weather events (e.g., Martius et al. 2008 ; Feldstein and Dayan 2008 ). With regard to the transport of chemical constituents, the subtropical jets can act as local barriers for meridional exchange (e.g., Shuckburgh et
1. Cyclogenesis downstream of extratropical transition Recurving tropical cyclones, in particular those that undergo extratropical transition (ET; Jones et al. 2003 ), exert a profound impact on the midlatitude circulation. Several recent studies have investigated this impact in some detail and documented a distinct modification of the upper-level jet stream (e.g., Riemer et al. 2008 ; Riemer and Jones 2010 , 2014 ; Archambault et al. 2013 ; Grams et al. 2011 , 2013a ; Pantillon et al
1. Cyclogenesis downstream of extratropical transition Recurving tropical cyclones, in particular those that undergo extratropical transition (ET; Jones et al. 2003 ), exert a profound impact on the midlatitude circulation. Several recent studies have investigated this impact in some detail and documented a distinct modification of the upper-level jet stream (e.g., Riemer et al. 2008 ; Riemer and Jones 2010 , 2014 ; Archambault et al. 2013 ; Grams et al. 2011 , 2013a ; Pantillon et al
moves poleward and starts to interact with the midlatitude flow ( Fig. 1a ). This results in the formation of a jet streak ( Fig. 1b ) and a poleward deflection of the jet near the transitioning cyclone in conjunction with the development of a ridge–trough couplet ( Fig. 1b ). At the same time, a region of enhanced moisture flux—a so-called atmospheric river ( Zhu and Newell 1998 )—forms ahead of the downstream trough. The ridge–trough couplet continues to amplify, a new cyclone develops farther
moves poleward and starts to interact with the midlatitude flow ( Fig. 1a ). This results in the formation of a jet streak ( Fig. 1b ) and a poleward deflection of the jet near the transitioning cyclone in conjunction with the development of a ridge–trough couplet ( Fig. 1b ). At the same time, a region of enhanced moisture flux—a so-called atmospheric river ( Zhu and Newell 1998 )—forms ahead of the downstream trough. The ridge–trough couplet continues to amplify, a new cyclone develops farther
gradual than that of the carrier wave (dotted) or the RWP signal (blue). Fig . 1. Schematic of a Rossby wave packet (RWP) at a specific time. The blue line represents , the black dotted line is the underlying carrier wave , and the two red lines depict plus (upper line) and minus (lower line) the amplitude . A real world example is presented in Fig. 2 . Figure 2a shows the midlatitude jet with large meridional undulations over North America. Over the rest of hemisphere, the jet is more zonally
gradual than that of the carrier wave (dotted) or the RWP signal (blue). Fig . 1. Schematic of a Rossby wave packet (RWP) at a specific time. The blue line represents , the black dotted line is the underlying carrier wave , and the two red lines depict plus (upper line) and minus (lower line) the amplitude . A real world example is presented in Fig. 2 . Figure 2a shows the midlatitude jet with large meridional undulations over North America. Over the rest of hemisphere, the jet is more zonally
1. Introduction The large-scale midlatitude flow is dominated by the upper-level jet stream that serves as a waveguide for Rossby waves (e.g., Martius et al. 2010 ). Because their general evolution follows dry dynamics that can be represented at grid scale in numerical weather prediction (NWP) models, Rossby waves may be expected to feature a high degree of predictability ( Grazzini and Vitart 2015 ). However, major forecast uncertainty and error in the midlatitudes in current NWP models have
1. Introduction The large-scale midlatitude flow is dominated by the upper-level jet stream that serves as a waveguide for Rossby waves (e.g., Martius et al. 2010 ). Because their general evolution follows dry dynamics that can be represented at grid scale in numerical weather prediction (NWP) models, Rossby waves may be expected to feature a high degree of predictability ( Grazzini and Vitart 2015 ). However, major forecast uncertainty and error in the midlatitudes in current NWP models have
1. Introduction During a stratospheric sudden warming (SSW) event, the polar stratospheric temperature increases accompanied by a weakening of the polar night jet. Major SSW events (MSSW) are defined as SSW events with a reversal of the zonal mean zonal wind from westerlies to easterlies at 60°N and a 10-hPa layer. Those events represent the greatest part of intraseasonal variability in the winter middle atmosphere and are associated with low predictive skill at lead times more than 10 days
1. Introduction During a stratospheric sudden warming (SSW) event, the polar stratospheric temperature increases accompanied by a weakening of the polar night jet. Major SSW events (MSSW) are defined as SSW events with a reversal of the zonal mean zonal wind from westerlies to easterlies at 60°N and a 10-hPa layer. Those events represent the greatest part of intraseasonal variability in the winter middle atmosphere and are associated with low predictive skill at lead times more than 10 days
diabatic processes and upper-level divergent flow that impinges on the midlatitude waveguide (e.g., Riemer et al. 2008 ; Hodyss and Hendricks 2010 ; Torn 2010 ; Archambault et al. 2015 ; Torn et al. 2015 ). Negative PV advection by the divergent flow deflects PV contours poleward and strengthens the meridional PV gradient, which results in a downstream ridge amplification and a jet streak intensification, respectively. The ridge amplification and jet streak intensification may result in the
diabatic processes and upper-level divergent flow that impinges on the midlatitude waveguide (e.g., Riemer et al. 2008 ; Hodyss and Hendricks 2010 ; Torn 2010 ; Archambault et al. 2015 ; Torn et al. 2015 ). Negative PV advection by the divergent flow deflects PV contours poleward and strengthens the meridional PV gradient, which results in a downstream ridge amplification and a jet streak intensification, respectively. The ridge amplification and jet streak intensification may result in the
” constitutes a clear example for a two-phase development. The precursor rapidly crossed the North Atlantic as a DRW before it intensified to one of the most harmful storms in central Europe in the last few decades. Wernli et al. (2002) identified an intensive straight zonal jet during the DRW propagation phase of Lothar far to the north of the low-level vortex and excluded a significant upper-level forcing of the surface low due to the absence of waves on the intense jet. They demonstrated that later in
” constitutes a clear example for a two-phase development. The precursor rapidly crossed the North Atlantic as a DRW before it intensified to one of the most harmful storms in central Europe in the last few decades. Wernli et al. (2002) identified an intensive straight zonal jet during the DRW propagation phase of Lothar far to the north of the low-level vortex and excluded a significant upper-level forcing of the surface low due to the absence of waves on the intense jet. They demonstrated that later in
its long persistence extending to mid-August is not ( Matsueda 2011 ). Thus, the question arises: what are the causes of this long-lasting heat wave or rather the blocking high? Blocking, in general, denotes the effect of a synoptic system acting as a barrier to the westerly flow splitting the jet stream ( Elliott and Smith 1949 ). The formation of a block over Europe can be ascribed to the convergence (or absorption) of wave activity density flux associated with an incoming anomalous quasi
its long persistence extending to mid-August is not ( Matsueda 2011 ). Thus, the question arises: what are the causes of this long-lasting heat wave or rather the blocking high? Blocking, in general, denotes the effect of a synoptic system acting as a barrier to the westerly flow splitting the jet stream ( Elliott and Smith 1949 ). The formation of a block over Europe can be ascribed to the convergence (or absorption) of wave activity density flux associated with an incoming anomalous quasi
Europe results in significant errors in the forecasting of heavy precipitation in southern Switzerland. The focus of this study is on the model representation of one particular aspect of synoptic-scale Rossby waves, namely their waveguides. In the extratropics and subtropics, narrow and zonally extended areas of enhanced potential vorticity (PV) gradients, which are coaligned with the jet streams, act as waveguides for synoptic-scale Rossby waves (e.g., Schwierz et al. 2004 ; Martius et al. 2010
Europe results in significant errors in the forecasting of heavy precipitation in southern Switzerland. The focus of this study is on the model representation of one particular aspect of synoptic-scale Rossby waves, namely their waveguides. In the extratropics and subtropics, narrow and zonally extended areas of enhanced potential vorticity (PV) gradients, which are coaligned with the jet streams, act as waveguides for synoptic-scale Rossby waves (e.g., Schwierz et al. 2004 ; Martius et al. 2010
