Search Results
and Roberts 2006 ; Koch et al. 2008a , b ; Tanamachi et al. 2008 ; Martin and Johnson 2008 ; Hartung et al. 2010 ; Marsham et al. 2011 ; Blake et al. 2017 ). These results are expected as Haghi et al. (2017) revealed that the interaction between the convectively generated cold pools and the SBL over this region typically resides in a partially blocked flow regime where bores will be generated ( Rottman and Simpson 1989 ). These bores will be long lived as the wave energy is typically
and Roberts 2006 ; Koch et al. 2008a , b ; Tanamachi et al. 2008 ; Martin and Johnson 2008 ; Hartung et al. 2010 ; Marsham et al. 2011 ; Blake et al. 2017 ). These results are expected as Haghi et al. (2017) revealed that the interaction between the convectively generated cold pools and the SBL over this region typically resides in a partially blocked flow regime where bores will be generated ( Rottman and Simpson 1989 ). These bores will be long lived as the wave energy is typically
( Johnson and Wang 2019 ). Physical parameterization schemes, especially microphysics (MP) and planetary boundary layer (PBL) schemes, are utilized in models to represent subgrid-scale interactions. In regards to an atmospheric bore, the wave speed, wavelengths, and amplitude will be compromised by the inability of a scheme to properly resolve the subgrid-scale interactions. For example, most of the PBL schemes are designed to reproduce ambient stratification with no regard to the turbulence occurring
( Johnson and Wang 2019 ). Physical parameterization schemes, especially microphysics (MP) and planetary boundary layer (PBL) schemes, are utilized in models to represent subgrid-scale interactions. In regards to an atmospheric bore, the wave speed, wavelengths, and amplitude will be compromised by the inability of a scheme to properly resolve the subgrid-scale interactions. For example, most of the PBL schemes are designed to reproduce ambient stratification with no regard to the turbulence occurring
finding was supported by observational analysis utilizing surface meteorological observations and radar “fine lines” that revealed that most convective outflows generated bores. Our investigation utilizes data also taken from IHOP_2002 to explore the vertical structure of bores and their potential to initiate and maintain deep convection. A key finding of this study that was not expected from hydraulic and linear wave theory of bores was that additional wave disturbances extend over the lower
finding was supported by observational analysis utilizing surface meteorological observations and radar “fine lines” that revealed that most convective outflows generated bores. Our investigation utilizes data also taken from IHOP_2002 to explore the vertical structure of bores and their potential to initiate and maintain deep convection. A key finding of this study that was not expected from hydraulic and linear wave theory of bores was that additional wave disturbances extend over the lower
well-mixed, deep planetary boundary layer (PBL)—to elevated nocturnal convection, which typically organizes at larger scales as the nocturnal stable boundary layer (SBL) deepens, and a low-level jet (LLJ) develops above the SBL ( Corfidi et al. 2008 ; Carbone and Tuttle 2008 ; Reif and Bluestein 2017 ). Convective cells develop when a parcel of air is lofted to its level of free convection (LFC), becoming buoyant with respect to its surrounding environment. Convective cells often initiate in the
well-mixed, deep planetary boundary layer (PBL)—to elevated nocturnal convection, which typically organizes at larger scales as the nocturnal stable boundary layer (SBL) deepens, and a low-level jet (LLJ) develops above the SBL ( Corfidi et al. 2008 ; Carbone and Tuttle 2008 ; Reif and Bluestein 2017 ). Convective cells develop when a parcel of air is lofted to its level of free convection (LFC), becoming buoyant with respect to its surrounding environment. Convective cells often initiate in the
conducive for gravity wave ducting ( Crook 1986 ; Koch and Clark 1999 ). The second main ingredient needed for successful NWP forecasts of bores is an accurate forecast of the parent convection that generates the density current, which in turn triggers the bore. This ingredient is satisfied in this study by initializing the simulations from analyses that include the parent convection. This is done using data assimilation that incorporates radar, surface, and upper-air observations. However, it will
conducive for gravity wave ducting ( Crook 1986 ; Koch and Clark 1999 ). The second main ingredient needed for successful NWP forecasts of bores is an accurate forecast of the parent convection that generates the density current, which in turn triggers the bore. This ingredient is satisfied in this study by initializing the simulations from analyses that include the parent convection. This is done using data assimilation that incorporates radar, surface, and upper-air observations. However, it will
1. Introduction Atmospheric bores are commonly observed in the nocturnal convective environment in the Great Plains ( Haghi et al. 2017 ). This is because the stable boundary layer and low-level jet often provide a suitable wave duct, while convectively generated cold pools frequently provide an obstacle to this stable and ducted low-level flow ( Rottman and Simpson 1989 ; Johnson et al. 2018 ). Several studies have demonstrated the importance of bores in both the initiation and maintenance of
1. Introduction Atmospheric bores are commonly observed in the nocturnal convective environment in the Great Plains ( Haghi et al. 2017 ). This is because the stable boundary layer and low-level jet often provide a suitable wave duct, while convectively generated cold pools frequently provide an obstacle to this stable and ducted low-level flow ( Rottman and Simpson 1989 ; Johnson et al. 2018 ). Several studies have demonstrated the importance of bores in both the initiation and maintenance of
deep-tropospheric gravity waves (e.g., Uccelini 1975 ; Koch et al. 1988 ; Fovell et al. 2006 ; Marsham and Parker 2006 ); cold fronts, density currents, and drylines (e.g., Charba 1974 ; Wilson and Schreiber 1986 ; Mahoney 1988 ; Weckwerth and Wakimoto 1992 ; Hane et al. 1993 ; Ziegler and Rasmussen 1998 ; Weiss and Bluestein 2002 ; Geerts et al. 2006 ; Weckwerth et al. 2008 ); inland or “vegetation” breezes (e.g., Sun and Ogura 1979 ; Mahfouf et al. 1987 ; Segal and Arritt 1992
deep-tropospheric gravity waves (e.g., Uccelini 1975 ; Koch et al. 1988 ; Fovell et al. 2006 ; Marsham and Parker 2006 ); cold fronts, density currents, and drylines (e.g., Charba 1974 ; Wilson and Schreiber 1986 ; Mahoney 1988 ; Weckwerth and Wakimoto 1992 ; Hane et al. 1993 ; Ziegler and Rasmussen 1998 ; Weiss and Bluestein 2002 ; Geerts et al. 2006 ; Weckwerth et al. 2008 ); inland or “vegetation” breezes (e.g., Sun and Ogura 1979 ; Mahfouf et al. 1987 ; Segal and Arritt 1992
array of PECAN Integrated Sounding Arrays (PISAs) to sample the vertical profiles of lower-tropospheric winds, temperature, and water vapor. These PISAs and the scanning radars and lidars of PECAN were used to sample the specific features (e.g., LLJ, bores, and gravity waves) and atmospheric regions (e.g., SBL and lower troposphere) relevant to better understanding of NCI. This manuscript brings together past NCI work and PECAN data to document frequencies of different NCI types, as categorized by
array of PECAN Integrated Sounding Arrays (PISAs) to sample the vertical profiles of lower-tropospheric winds, temperature, and water vapor. These PISAs and the scanning radars and lidars of PECAN were used to sample the specific features (e.g., LLJ, bores, and gravity waves) and atmospheric regions (e.g., SBL and lower troposphere) relevant to better understanding of NCI. This manuscript brings together past NCI work and PECAN data to document frequencies of different NCI types, as categorized by
lee of the Rocky Mountains ( Carbone et al. 2002 ; Li and Smith 2010 ), convective feedbacks such as gravity waves and bores ( Carbone et al. 2002 ; Marsham et al. 2011 ), and the Great Plains low-level jet (LLJ; Pitchford and London 1962 ; Trier and Parsons 1993 ; Higgins et al. 1997 ). The LLJ is a particularly important phenomenon that provides a source of buoyancy ( Trier and Parsons 1993 ; Helfand and Schubert 1995 ; Higgins et al. 1997 ) and forcing ( Pitchford and London 1962
lee of the Rocky Mountains ( Carbone et al. 2002 ; Li and Smith 2010 ), convective feedbacks such as gravity waves and bores ( Carbone et al. 2002 ; Marsham et al. 2011 ), and the Great Plains low-level jet (LLJ; Pitchford and London 1962 ; Trier and Parsons 1993 ; Higgins et al. 1997 ). The LLJ is a particularly important phenomenon that provides a source of buoyancy ( Trier and Parsons 1993 ; Helfand and Schubert 1995 ; Higgins et al. 1997 ) and forcing ( Pitchford and London 1962
in analyses valid at 1300 UTC, which are used to initialize a deterministic forecast from the ensemble mean analysis. The quality of the analyses is evaluated by verification of the forecasts, which all use the same physics configuration and differ only in their initial conditions. The forecast physics configuration is Thompson’s microphysics scheme, the Mellor–Yamada–Nakanishi–Niino (MYNN; Nakanishi and Niino 2009 ) planetary boundary layer (PBL) scheme, the Goddard shortwave ( Tao et al. 2003
in analyses valid at 1300 UTC, which are used to initialize a deterministic forecast from the ensemble mean analysis. The quality of the analyses is evaluated by verification of the forecasts, which all use the same physics configuration and differ only in their initial conditions. The forecast physics configuration is Thompson’s microphysics scheme, the Mellor–Yamada–Nakanishi–Niino (MYNN; Nakanishi and Niino 2009 ) planetary boundary layer (PBL) scheme, the Goddard shortwave ( Tao et al. 2003
