Sorry! Cold advection at low levels normally results in an increase of sfc pressure, so is not at all a source for cyclogenesis.

Right! Baroclinic instability, associated to horizontal temperature gradients, is the main source for cyclogenesis at mid latitudes. Some upper level perturbations may destabilize and take energy from the vertical shear of the flow, providing that baroclinicity and stability stratification are adequate, (Charney, 1947 and Eady, 1949). Stability stratification is specially important at low levels. The lower the instability the shorter the wavelengths that can become unstable. An alternative way to model conceptually baroclinic instability, is in terms of potential vorticity anomalies, (Hoskins et al. 1985). We will come back to this point later in the module.

Right! The influence of orography on cyclogenesis is well documented in Smith (1979), Speranza et al. (1982), Pierrehumbert (1982), Dell’Osso (1984) and Buzzi et al. (2003). We will come back to this point later.

Right!, Johnson and Downey (1976), Kocin and Uccellini (1990), and Gyakum 1983, show how latent heat release in the presence of rain, contributes to the intensification of cyclones, in terms of surface pressure falls, increase of low level circulation, and vertical growth of the cyclone.

Right!, PBL vertical heat fluxes can produce changes in stability stratification at low levels and so in the speed of deepening of the cyclone. They can also create a low level initial "seed", ready for further development. These PBL heat fluxes seem to be more important in cyclogenesis that take place over the sea, than over land (Mailhot and Chouinard, 1988).

Right, certain velocity horizontal profiles may lead to destabilization. In this case the perturbation may grow by taking energy from the horizontal shear of the flow. Similarly, when a barotropic fluid passes over a mountain, conservation of potential vorticity may lead to the formation of a cyclone on the lee side (vortex tube stretching mechanism).

Sorry, this one is false, evaporation of rain produce a temperature drop, which will be a brake for further surface pressure falls.

Sorry, convergence at upper levels fills the column of air over the cyclone, and that will encourage surface pressure to raise.

Right, air-sea thermodynamic desequilibrium may lead by itself to surface pressure development via feedback mechanisms between surface heat fluxes and wind, in a similar way to that of tropical cyclones. See Emanuel, 2005.

Sorry! Cold advection at low levels normally results in an increase of sfc pressure, so is not at all a source for cyclogenesis.

Right! Baroclinic instability, associated to horizontal temperature gradients, is the main source for cyclogenesis at mid latitudes. Some upper level perturbations may destabilize and take energy from the vertical shear of the flow, providing that baroclinicity and stability stratification are adequate, (Charney, 1947 and Eady, 1949). Stability stratification is specially important at low levels. The lower the instability the shorter the wavelengths that can become unstable. An alternative way to model conceptually baroclinic instability, is in terms of potential vorticity anomalies, (Hoskins et al. 1985). We will come back to this point later in the module.

Right! The influence of orography on cyclogenesis is well documented in Smith (1979), Speranza et al. (1982), Pierrehumbert (1982), Dell’Osso (1984) and Buzzi et al. (2003). We will come back to this point later.

Right!, Johnson and Downey (1976), Kocin and Uccellini (1990), and Gyakum 1983, show how latent heat release in the presence of rain, contributes to the intensification of cyclones, in terms of surface pressure falls, increase of low level circulation, and vertical growth of the cyclone.

Right!, PBL vertical heat fluxes can produce changes in stability stratification at low levels and so in the speed of deepening of the cyclone. They can also create a low level initial "seed", ready for further development. These PBL heat fluxes seem to be more important in cyclogenesis that take place over the sea, than over land (Mailhot and Chouinard, 1988).

Right, certain velocity horizontal profiles may lead to destabilization. In this case the perturbation may grow by taking energy from the horizontal shear of the flow. Similarly, when a barotropic fluid passes over a mountain, conservation of potential vorticity may lead to the formation of a cyclone on the lee side (vortex tube stretching mechanism).

Sorry, this one is false, evaporation of rain produce a temperature drop, which will be a brake for further surface pressure falls.

Sorry, convergence at upper levels fills the column of air over the cyclone, and that will encourage surface pressure to raise.

Right, air-sea thermodynamic desequilibrium may lead by itself to surface pressure development via feedback mechanisms between surface heat fluxes and wind, in a similar way to that of tropical cyclones. See Emanuel, 2005.

Sorry! Cold advection at low levels normally results in an increase of sfc pressure, so is not at all a source for cyclogenesis.

Right! Baroclinic instability, associated to horizontal temperature gradients, is the main source for cyclogenesis at mid latitudes. Some upper level perturbations may destabilize and take energy from the vertical shear of the flow, providing that baroclinicity and stability stratification are adequate, (Charney, 1947 and Eady, 1949). Stability stratification is specially important at low levels. The lower the instability the shorter the wavelengths that can become unstable. An alternative way to model conceptually baroclinic instability, is in terms of potential vorticity anomalies, (Hoskins et al. 1985). We will come back to this point later in the module.

Right! The influence of orography on cyclogenesis is well documented in Smith (1979), Speranza et al. (1982), Pierrehumbert (1982), Dell’Osso (1984) and Buzzi et al. (2003). We will come back to this point later.

Right!, Johnson and Downey (1976), Kocin and Uccellini (1990), and Gyakum 1983, show how latent heat release in the presence of rain, contributes to the intensification of cyclones, in terms of surface pressure falls, increase of low level circulation, and vertical growth of the cyclone.

Right!, PBL vertical heat fluxes can produce changes in stability stratification at low levels and so in the speed of deepening of the cyclone. They can also create a low level initial "seed", ready for further development. These PBL heat fluxes seem to be more important in cyclogenesis that take place over the sea, than over land (Mailhot and Chouinard, 1988).

Right, certain velocity horizontal profiles may lead to destabilization. In this case the perturbation may grow by taking energy from the horizontal shear of the flow. Similarly, when a barotropic fluid passes over a mountain, conservation of potential vorticity may lead to the formation of a cyclone on the lee side (vortex tube stretching mechanism).

Sorry, this one is false, evaporation of rain produce a temperature drop, which will be a brake for further surface pressure falls.

Sorry, convergence at upper levels fills the column of air over the cyclone, and that will encourage surface pressure to raise.

Right, air-sea thermodynamic desequilibrium may lead by itself to surface pressure development via feedback mechanisms between surface heat fluxes and wind, in a similar way to that of tropical cyclones. See Emanuel, 2005.

Sorry! Cold advection at low levels normally results in an increase of sfc pressure, so is not at all a source for cyclogenesis.

Right! Baroclinic instability, associated to horizontal temperature gradients, is the main source for cyclogenesis at mid latitudes. Some upper level perturbations may destabilize and take energy from the vertical shear of the flow, providing that baroclinicity and stability stratification are adequate, (Charney, 1947 and Eady, 1949). Stability stratification is specially important at low levels. The lower the instability the shorter the wavelengths that can become unstable. An alternative way to model conceptually baroclinic instability, is in terms of potential vorticity anomalies, (Hoskins et al. 1985). We will come back to this point later in the module.

Right! The influence of orography on cyclogenesis is well documented in Smith (1979), Speranza et al. (1982), Pierrehumbert (1982), Dell’Osso (1984) and Buzzi et al. (2003). We will come back to this point later.

Right!, Johnson and Downey (1976), Kocin and Uccellini (1990), and Gyakum 1983, show how latent heat release in the presence of rain, contributes to the intensification of cyclones, in terms of surface pressure falls, increase of low level circulation, and vertical growth of the cyclone.

Right!, PBL vertical heat fluxes can produce changes in stability stratification at low levels and so in the speed of deepening of the cyclone. They can also create a low level initial "seed", ready for further development. These PBL heat fluxes seem to be more important in cyclogenesis that take place over the sea, than over land (Mailhot and Chouinard, 1988).

Right, certain velocity horizontal profiles may lead to destabilization. In this case the perturbation may grow by taking energy from the horizontal shear of the flow. Similarly, when a barotropic fluid passes over a mountain, conservation of potential vorticity may lead to the formation of a cyclone on the lee side (vortex tube stretching mechanism).

Sorry, this one is false, evaporation of rain produce a temperature drop, which will be a brake for further surface pressure falls.

Sorry, convergence at upper levels fills the column of air over the cyclone, and that will encourage surface pressure to raise.

Right, air-sea thermodynamic desequilibrium may lead by itself to surface pressure development via feedback mechanisms between surface heat fluxes and wind, in a similar way to that of tropical cyclones. See Emanuel, 2005.

Sorry! Cold advection at low levels normally results in an increase of sfc pressure, so is not at all a source for cyclogenesis.

Right! Baroclinic instability, associated to horizontal temperature gradients, is the main source for cyclogenesis at mid latitudes. Some upper level perturbations may destabilize and take energy from the vertical shear of the flow, providing that baroclinicity and stability stratification are adequate, (Charney, 1947 and Eady, 1949). Stability stratification is specially important at low levels. The lower the instability the shorter the wavelengths that can become unstable. An alternative way to model conceptually baroclinic instability, is in terms of potential vorticity anomalies, (Hoskins et al. 1985). We will come back to this point later in the module.

Right! The influence of orography on cyclogenesis is well documented in Smith (1979), Speranza et al. (1982), Pierrehumbert (1982), Dell’Osso (1984) and Buzzi et al. (2003). We will come back to this point later.

Right!, Johnson and Downey (1976), Kocin and Uccellini (1990), and Gyakum 1983, show how latent heat release in the presence of rain, contributes to the intensification of cyclones, in terms of surface pressure falls, increase of low level circulation, and vertical growth of the cyclone.

Right!, PBL vertical heat fluxes can produce changes in stability stratification at low levels and so in the speed of deepening of the cyclone. They can also create a low level initial "seed", ready for further development. These PBL heat fluxes seem to be more important in cyclogenesis that take place over the sea, than over land (Mailhot and Chouinard, 1988).

Right, certain velocity horizontal profiles may lead to destabilization. In this case the perturbation may grow by taking energy from the horizontal shear of the flow. Similarly, when a barotropic fluid passes over a mountain, conservation of potential vorticity may lead to the formation of a cyclone on the lee side (vortex tube stretching mechanism).

Sorry, this one is false, evaporation of rain produce a temperature drop, which will be a brake for further surface pressure falls.

Sorry, convergence at upper levels fills the column of air over the cyclone, and that will encourage surface pressure to raise.

Right, air-sea thermodynamic desequilibrium may lead by itself to surface pressure development via feedback mechanisms between surface heat fluxes and wind, in a similar way to that of tropical cyclones. See Emanuel, 2005.

Sorry! Cold advection at low levels normally results in an increase of sfc pressure, so is not at all a source for cyclogenesis.

Right! Baroclinic instability, associated to horizontal temperature gradients, is the main source for cyclogenesis at mid latitudes. Some upper level perturbations may destabilize and take energy from the vertical shear of the flow, providing that baroclinicity and stability stratification are adequate, (Charney, 1947 and Eady, 1949). Stability stratification is specially important at low levels. The lower the instability the shorter the wavelengths that can become unstable. An alternative way to model conceptually baroclinic instability, is in terms of potential vorticity anomalies, (Hoskins et al. 1985). We will come back to this point later in the module.

Right! The influence of orography on cyclogenesis is well documented in Smith (1979), Speranza et al. (1982), Pierrehumbert (1982), Dell’Osso (1984) and Buzzi et al. (2003). We will come back to this point later.

Right!, Johnson and Downey (1976), Kocin and Uccellini (1990), and Gyakum 1983, show how latent heat release in the presence of rain, contributes to the intensification of cyclones, in terms of surface pressure falls, increase of low level circulation, and vertical growth of the cyclone.

Right!, PBL vertical heat fluxes can produce changes in stability stratification at low levels and so in the speed of deepening of the cyclone. They can also create a low level initial "seed", ready for further development. These PBL heat fluxes seem to be more important in cyclogenesis that take place over the sea, than over land (Mailhot and Chouinard, 1988).

Right, certain velocity horizontal profiles may lead to destabilization. In this case the perturbation may grow by taking energy from the horizontal shear of the flow. Similarly, when a barotropic fluid passes over a mountain, conservation of potential vorticity may lead to the formation of a cyclone on the lee side (vortex tube stretching mechanism).

Sorry, this one is false, evaporation of rain produce a temperature drop, which will be a brake for further surface pressure falls.

Sorry, convergence at upper levels fills the column of air over the cyclone, and that will encourage surface pressure to raise.

Right, air-sea thermodynamic desequilibrium may lead by itself to surface pressure development via feedback mechanisms between surface heat fluxes and wind, in a similar way to that of tropical cyclones. See Emanuel, 2005.