Search Results
and around the tropopause in the extratropics (e.g., Stone et al. 1999 ). The exchange of air caused by these large-scale motions across the tropopause plays an essential role in the abundance of chemical constituents in both the troposphere and stratosphere ( Holton et al. 1995 ): for example, the stratosphere–troposphere exchange (STE) on the isentropic surface is mainly due to mixing by Rossby wave breaking and stirring effects by differential advection near the jet stream (e.g., Chen et al
and around the tropopause in the extratropics (e.g., Stone et al. 1999 ). The exchange of air caused by these large-scale motions across the tropopause plays an essential role in the abundance of chemical constituents in both the troposphere and stratosphere ( Holton et al. 1995 ): for example, the stratosphere–troposphere exchange (STE) on the isentropic surface is mainly due to mixing by Rossby wave breaking and stirring effects by differential advection near the jet stream (e.g., Chen et al
-dimensional, nondivergent flow on the surface of a sphere. The BVE contains the nonlinear interactions of atmospheric motions and has been used extensively in the study of large-scale atmospheric dynamics. Charney et al. (1950) performed the first successful numerical weather prediction based on the BVE. Atmospheric flows have a wide range of time and length scales, which can vary from seconds to decades and from micrometers to several thousand kilometers. Because of limited computational resources, resolving all of
-dimensional, nondivergent flow on the surface of a sphere. The BVE contains the nonlinear interactions of atmospheric motions and has been used extensively in the study of large-scale atmospheric dynamics. Charney et al. (1950) performed the first successful numerical weather prediction based on the BVE. Atmospheric flows have a wide range of time and length scales, which can vary from seconds to decades and from micrometers to several thousand kilometers. Because of limited computational resources, resolving all of
). This circulation can be superimposed on the normal convective motions representing an idealized large-scale circulation that provides a linkage between two regions. Most studies have used a reference-column approach, whereby the large-scale circulation is determined by temperature differences between the area modeled and an assumed environmental profile; more recently, Daleu et al. (2012 , 2015a ) extended this approach to two coupled regions, which enables a more explicit representation of the
). This circulation can be superimposed on the normal convective motions representing an idealized large-scale circulation that provides a linkage between two regions. Most studies have used a reference-column approach, whereby the large-scale circulation is determined by temperature differences between the area modeled and an assumed environmental profile; more recently, Daleu et al. (2012 , 2015a ) extended this approach to two coupled regions, which enables a more explicit representation of the
1. Introduction Large-scale organized motions, or coherent structures, are a characteristic of turbulent flows that have been observed across a wide range of scales and flow geometries, from laboratory flows to the atmospheric boundary layer (ABL). Their occurrence, characteristics, and formation mechanisms, as well as their relative importance in the transport of momentum and heat, have been the subject of extensive research and discussion for several decades ( Hussain 1983 ; Robinson
1. Introduction Large-scale organized motions, or coherent structures, are a characteristic of turbulent flows that have been observed across a wide range of scales and flow geometries, from laboratory flows to the atmospheric boundary layer (ABL). Their occurrence, characteristics, and formation mechanisms, as well as their relative importance in the transport of momentum and heat, have been the subject of extensive research and discussion for several decades ( Hussain 1983 ; Robinson
Scientists and Engineers . McGraw-Hill, 593 pp . Burger , A. , 1958 : Scale considerations of planetary motions of the atmosphere. Tellus , 10 , 195 – 205 . Charney , J. G. , 1948 : On the scale of atmospheric motions. Geofys. Publ. , 17 , 1 – 17 . Charney , J. G. , 1963 : A note on large-scale motions in the tropics. J. Atmos. Sci. , 20 , 607 – 609 . Frank , W. M. , and J. L. McBride , 1989 : The vertical distribution of heating in AMEX and GATE cloud clusters. J. Atmos
Scientists and Engineers . McGraw-Hill, 593 pp . Burger , A. , 1958 : Scale considerations of planetary motions of the atmosphere. Tellus , 10 , 195 – 205 . Charney , J. G. , 1948 : On the scale of atmospheric motions. Geofys. Publ. , 17 , 1 – 17 . Charney , J. G. , 1963 : A note on large-scale motions in the tropics. J. Atmos. Sci. , 20 , 607 – 609 . Frank , W. M. , and J. L. McBride , 1989 : The vertical distribution of heating in AMEX and GATE cloud clusters. J. Atmos
) and the fifth-generation Pennsylvania State University–National Center for Atmospheric Research Mesoscale Model (MM5) (among many others). The KW approach was originally developed in the context of mesoscale cloud modeling—specifically, for horizontal grid spacings on the order of 1 km or so and with typical time steps on the order of 10 s or less. However, in recent years the method has increasingly been used for the simulation of large-scale flows as well. Global and planetary atmosphere
) and the fifth-generation Pennsylvania State University–National Center for Atmospheric Research Mesoscale Model (MM5) (among many others). The KW approach was originally developed in the context of mesoscale cloud modeling—specifically, for horizontal grid spacings on the order of 1 km or so and with typical time steps on the order of 10 s or less. However, in recent years the method has increasingly been used for the simulation of large-scale flows as well. Global and planetary atmosphere
showed beyond doubt the existence of an intense “mesoscale” eddy field involving baroclinic motions related to the baroclinic radii of about 35 km and smaller, as well as barotropic motions on a much larger scale. In oceanography, the expression mesoscale describes the spatial scale that is intermediate between the large-scale ocean circulation and the internal wave field and is thus very different from its meteorological usage (which is closer to the ocean “submesoscale”). A better descriptor is
showed beyond doubt the existence of an intense “mesoscale” eddy field involving baroclinic motions related to the baroclinic radii of about 35 km and smaller, as well as barotropic motions on a much larger scale. In oceanography, the expression mesoscale describes the spatial scale that is intermediate between the large-scale ocean circulation and the internal wave field and is thus very different from its meteorological usage (which is closer to the ocean “submesoscale”). A better descriptor is
1. Introduction Large-scale patterns of extratropical climate variability are typically identified through 1) correlation analyses between geographically separated points in the zonally varying circulation (i.e., so-called teleconnectivity) and/or 2) empirical orthogonal function (EOF) analysis. In both cases, the statistical analyses generally focus on the geopotential height, temperature, and/or zonal-wind fields. The purpose of this study is to investigate large-scale patterns of climate
1. Introduction Large-scale patterns of extratropical climate variability are typically identified through 1) correlation analyses between geographically separated points in the zonally varying circulation (i.e., so-called teleconnectivity) and/or 2) empirical orthogonal function (EOF) analysis. In both cases, the statistical analyses generally focus on the geopotential height, temperature, and/or zonal-wind fields. The purpose of this study is to investigate large-scale patterns of climate
1. Introduction Cloud-system-resolving model (CSRM) simulations subject to horizontally or zonally homogeneous boundary and forcing conditions can spontaneously develop large-scale circulations in the homogeneous direction. One example is the convectively coupled waves, which can develop without feedbacks from radiation or surface fluxes (e.g., Grabowski and Moncrieff 2001 ; Tulich et al. 2007 ; Kuang 2008a ; Nasuno et al. 2008 ; Blanco et al. 2016 ), and appear comparable in structure and
1. Introduction Cloud-system-resolving model (CSRM) simulations subject to horizontally or zonally homogeneous boundary and forcing conditions can spontaneously develop large-scale circulations in the homogeneous direction. One example is the convectively coupled waves, which can develop without feedbacks from radiation or surface fluxes (e.g., Grabowski and Moncrieff 2001 ; Tulich et al. 2007 ; Kuang 2008a ; Nasuno et al. 2008 ; Blanco et al. 2016 ), and appear comparable in structure and
-level synoptic flow; in particular, jet streaks and related secondary circulations. Although diurnal boundary layer influences are important for jet formation, the larger-scale, slowly varying circulation (e.g., monthly flow) on which diurnal influences superpose can be important for jet variability. Byerle and Paegle (2003) show North American orography to be influential in focusing global-scale flow features into regional responses, especially GPLLJ modulations. Stationary wave modeling also shows
-level synoptic flow; in particular, jet streaks and related secondary circulations. Although diurnal boundary layer influences are important for jet formation, the larger-scale, slowly varying circulation (e.g., monthly flow) on which diurnal influences superpose can be important for jet variability. Byerle and Paegle (2003) show North American orography to be influential in focusing global-scale flow features into regional responses, especially GPLLJ modulations. Stationary wave modeling also shows
