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procedures for generating and analyzing gravity wave products were tested as part of a larger coordinated DEEPWAVE “dry run” from 5 to 18 August 2013. Immediately after download and postprocessing, AIRS gravity wave products were plotted and then uploaded as image files to an online field catalog, where the science team could access this imagery through a web tool, along with many other products, such as forecasts from a small subset of operational NWP systems. The DEEPWAVE science team convened daily
procedures for generating and analyzing gravity wave products were tested as part of a larger coordinated DEEPWAVE “dry run” from 5 to 18 August 2013. Immediately after download and postprocessing, AIRS gravity wave products were plotted and then uploaded as image files to an online field catalog, where the science team could access this imagery through a web tool, along with many other products, such as forecasts from a small subset of operational NWP systems. The DEEPWAVE science team convened daily
shown in Fig. 1 (bottom). Figure 2 shows the extent of all DEEPWAVE measurements in altitude and latitude. F ig . 2. North–south cross section showing the types of airborne and ground-based instruments contributing to DEEPWAVE measurements and their coverage in latitude and altitude. DEEPWAVE began with a test flight-planning exercise from 1 to 10 August 2013 to gain experience with forecasting and flight planning and to assess the reliability of such forecasts in preparation for the real field
shown in Fig. 1 (bottom). Figure 2 shows the extent of all DEEPWAVE measurements in altitude and latitude. F ig . 2. North–south cross section showing the types of airborne and ground-based instruments contributing to DEEPWAVE measurements and their coverage in latitude and altitude. DEEPWAVE began with a test flight-planning exercise from 1 to 10 August 2013 to gain experience with forecasting and flight planning and to assess the reliability of such forecasts in preparation for the real field
Airborne Wind Lidar Measurements of Vertical and Horizontal Winds for the Investigation of Orographically Induced Gravity Waves( Baumgarten 2010 ; Hildebrand et al. 2012 ). For instance, Kaifler et al. (2015) used temperature perturbations derived from Rayleigh lidar measurements (28–76 km altitude) to characterize GWs over New Zealand and showed that enhanced GW potential energy densities in the mesosphere are surprisingly associated with mountain waves excited by only low to moderate tropospheric wind speeds between 2 and 12 m s −1 . Although the aforementioned lidar technique represents a valuable tool to characterize GWs
( Baumgarten 2010 ; Hildebrand et al. 2012 ). For instance, Kaifler et al. (2015) used temperature perturbations derived from Rayleigh lidar measurements (28–76 km altitude) to characterize GWs over New Zealand and showed that enhanced GW potential energy densities in the mesosphere are surprisingly associated with mountain waves excited by only low to moderate tropospheric wind speeds between 2 and 12 m s −1 . Although the aforementioned lidar technique represents a valuable tool to characterize GWs
. Data sources Operational analyses of the Integrated Forecast System (IFS) of the European Centre for Medium-Range Weather Forecasts (ECMWF) are used to provide meteorological data to characterize the atmospheric situation. The 6-hourly operational analysis and hourly forecast fields of the IFS cycle 40r1 have a horizontal resolution on the reduced linear Gaussian grid of about 16 km (T L 1279) and 137 vertical model levels (L137) from the ground to ~80 km (0.01 hPa) with layer thicknesses gradually
. Data sources Operational analyses of the Integrated Forecast System (IFS) of the European Centre for Medium-Range Weather Forecasts (ECMWF) are used to provide meteorological data to characterize the atmospheric situation. The 6-hourly operational analysis and hourly forecast fields of the IFS cycle 40r1 have a horizontal resolution on the reduced linear Gaussian grid of about 16 km (T L 1279) and 137 vertical model levels (L137) from the ground to ~80 km (0.01 hPa) with layer thicknesses gradually
higher altitudes (e.g., Siskind 2014 ). Thereby, the wind field and the thermal structure of the middle atmosphere are modified (e.g., Lindzen 1981 ; Holton and Alexander 2000 ). Internal gravity waves have been measured and analyzed with a large variety of active and passive remote sensing techniques as well as with in situ observations. These observational tools include airborne and ground-based lidars (e.g., Alexander et al. 2011 ; Dörnbrack et al 2002 ; Rauthe et al. 2008 ; Williams et al
higher altitudes (e.g., Siskind 2014 ). Thereby, the wind field and the thermal structure of the middle atmosphere are modified (e.g., Lindzen 1981 ; Holton and Alexander 2000 ). Internal gravity waves have been measured and analyzed with a large variety of active and passive remote sensing techniques as well as with in situ observations. These observational tools include airborne and ground-based lidars (e.g., Alexander et al. 2011 ; Dörnbrack et al 2002 ; Rauthe et al. 2008 ; Williams et al
analyses valid at 0000, 0600, 1200, and 1800 UTC and 1-hourly high-resolution forecasts at intermediate lead times (+1, +2, +3, +4, +5, +7, +8, +9, +10, and +11 h) of the 0000 and 1200 UTC forecast runs of the Integrated Forecast System (IFS) of the European Centre for Medium-Range Weather Forecasts (ECMWF) are further used to visualize the temporal evolution of the upstream conditions at 44.20°S, 167.50°E ( Fig. 1 ). The IFS cycle 40r1 has a horizontal resolution of about 16 km, 137 vertical model
analyses valid at 0000, 0600, 1200, and 1800 UTC and 1-hourly high-resolution forecasts at intermediate lead times (+1, +2, +3, +4, +5, +7, +8, +9, +10, and +11 h) of the 0000 and 1200 UTC forecast runs of the Integrated Forecast System (IFS) of the European Centre for Medium-Range Weather Forecasts (ECMWF) are further used to visualize the temporal evolution of the upstream conditions at 44.20°S, 167.50°E ( Fig. 1 ). The IFS cycle 40r1 has a horizontal resolution of about 16 km, 137 vertical model
; Doyle et al. 2011 ) were applied to the DEEPWAVE study area to provide real-time forecast guidance during the field campaign period ( Fritts et al. 2016 ). COAMPS is a fully compressible, nonhydrostatic terrain-following mesoscale model. The finite-difference schemes are of second-order accuracy in time and space in this application. The boundary layer and free-atmospheric turbulent mixing and diffusion are represented using a prognostic equation for the turbulence kinetic energy budget following
; Doyle et al. 2011 ) were applied to the DEEPWAVE study area to provide real-time forecast guidance during the field campaign period ( Fritts et al. 2016 ). COAMPS is a fully compressible, nonhydrostatic terrain-following mesoscale model. The finite-difference schemes are of second-order accuracy in time and space in this application. The boundary layer and free-atmospheric turbulent mixing and diffusion are represented using a prognostic equation for the turbulence kinetic energy budget following
, 2006a : Fourier-ray modeling of short-wavelength trapped lee waves observed in infrared satellite imagery near Jan Mayen . Mon. Wea. Rev. , 134 , 2830 – 2848 , https://doi.org/10.1175/MWR3218.1 . 10.1175/MWR3218.1 Eckermann , S. D. , A. Dörnbrack , H. Flentje , S. B. Vosper , M. J. Mahoney , T. P. Bui , and K. S. Carslaw , 2006b : Mountain wave–induced polar stratospheric cloud forecasts for aircraft science flights during SOLVE/THESEO 2000 . Wea. Forecasting , 21 , 42
, 2006a : Fourier-ray modeling of short-wavelength trapped lee waves observed in infrared satellite imagery near Jan Mayen . Mon. Wea. Rev. , 134 , 2830 – 2848 , https://doi.org/10.1175/MWR3218.1 . 10.1175/MWR3218.1 Eckermann , S. D. , A. Dörnbrack , H. Flentje , S. B. Vosper , M. J. Mahoney , T. P. Bui , and K. S. Carslaw , 2006b : Mountain wave–induced polar stratospheric cloud forecasts for aircraft science flights during SOLVE/THESEO 2000 . Wea. Forecasting , 21 , 42
and satellite navigation systems, and air velocity and angle-of-attack data from static and dynamic pressure and temperature sensors at the aircraft fuselage and nose ( Cooper et al. 2014 ; Mallaun et al. 2015 ; Giez et al. 2017 ). These techniques allow to derive spectra of vertical energy and momentum fluxes in mountain gravity waves ( Smith et al. 2016 ). Occasionally, w spectra were observed for selected flight legs showing peaks at wavelengths of order 4–12 km, which are partially
and satellite navigation systems, and air velocity and angle-of-attack data from static and dynamic pressure and temperature sensors at the aircraft fuselage and nose ( Cooper et al. 2014 ; Mallaun et al. 2015 ; Giez et al. 2017 ). These techniques allow to derive spectra of vertical energy and momentum fluxes in mountain gravity waves ( Smith et al. 2016 ). Occasionally, w spectra were observed for selected flight legs showing peaks at wavelengths of order 4–12 km, which are partially
