logging in or signing up Rowe Tucson poster Perrin Download Post to : URL : Related Presentations : Let's Connect Share Add to Flag Embed Email Send to Blogs and Networks Add to Channel Copy embed code: Embed: Flash iPad Dynamic Copy Does not support media & animations Automatically changes to Flash or non-Flash embed WordPress Embed Customize Embed URL: Copy Thumbnail: Copy The presentation is successfully added In Your Favorites. Views: 89 Category: Entertainment License: All Rights Reserved Like it (0) Dislike it (0) Added: February 25, 2008 This Presentation is Public Favorites: 0 Presentation Description No description available. Comments Posting comment... Premium member Presentation Transcript Slide1: MOTIVATION The local topography of the core North American Monsoon (NAM) region in northwestern Mexico is dominated by the Sierra Madre Occidental (SMO) and has been found to have important impacts on the diurnal cycle of precipitation (e.g., Gochis et al. 2004; Lang et al. 2007). This diurnal trend is characterized by initiation of convection over the peaks and western foothills of the SMO during late afternoon (Gochis et al. 2004), followed by a westward propagation and upscale growth into mesoscale convective systems (MCSs) during the late evening/early morning hours (e.g., Lang et al. 2007). Data from the NAME Event Rain gauge Network (NERN) revealed that precipitation over the lower elevations occurred less frequently and with greater intensity than over the SMO (Gochis et al. 2004). Due to the sparse coverage and obvious lack of vertical information from the NERN data, radar data are needed to further examine the structure, kinematics, and morphology of convection, including the diurnal cycle of precipitating clouds within the core monsoon region (Lang et al. 2007). RAINFALL INTENSITY AND FREQUENCY ANALYSIS OF WARM-CLOUD DEPTHS OBJECTIVES AND METHODOLOGY This study uses data provided by the NAME radar network to address the following objectives: To provide more detailed and comprehensive statistics of intensity and frequency of NAM precipitation, focusing on the effect of topography on the diurnal cycle To determine elevation-dependent trends in vertical characteristics of convection in the core monsoon region NAME radar network S-Pol (NCAR): S-band, polarimetric, Doppler Cabo and Guasave (SMN): C-band, Doppler 3-D data S-Pol only including all major polarimetric variables Same temporal and horizontal resolution as 2-D composites for comparison 1-km vertical resolution (1-20 km) Each grid point subjected to a convective-stratiform partitioning algorithm based on Yuter and Houze (1997) 2-D composites 0.02° lat/lon resolution Available every 15 min from 8 July 0000 UTC through 21 August 2345 UTC in 2004 Created for Tb, reflectivity, and rain rate S-Pol rain rates computed from CSU blended rainfall algorithm (Cifelli et al. 2002); SMN rain rates computed from Z=133 R1.5 Topographic data 0.02 grid spacing Data separated into four elevation groups: over water, 0-1000 m, 1000-2000 m, > 2000 m Cumulative distribution functions of rain rates reveal a transition to heavier precipitating events with decreasing elevation. The greatest 15-min and daily rain totals are confined to the lowest elevations compared to over the SMO (> 2000 m), implying the possibility for intense precipitation to occur over the SMO, but the duration of these events is not as long as for precipitation over the lower terrain. Consistent with NERN results, the diurnal cycle is characterized by frequent, low-intensity precipitation initiating over the SMO around 1600 LDT, and less frequent, but higher intensity precipitation over the lower terrain during the morning around 0800 LDT. VERTICAL CHARACTERISTICS The most intense convection occurs over the lower terrain during the evening and early morning. Convection over the SMO is less intense and limited to the afternoon (left). There is a greater contribution to convective rainfall from the deeper convection over the lower terrain (below). Echo-top height distributions reveal a trimodal structure similar to that observed in Johnson et al. (1999), with peaks at 5 km, 9 km, and 12 km (likely due to layers of enhanced stability).There is also a tendency for convection over the higher terrain to be shallower than over the coast (above). The CSU-NAME upper-air and surface gridded analyses (Johnson et al. 2007) were used to obtain average LCLs and melting levels to compare warm-cloud depths as a function of topography. There is a decreasing trend in warm-cloud depth with increasing elevation, reflecting the shallower convection over the SMO compared to the lower terrain. Clouds intercepting SMO peaks (Photo courtesy of David Gochis) A simplified model of stochastic droplet growth from the CSU RAMS microphysics algorithm (Saleeby and Cotton 2006) was used to simulate convective precipitation intensity for various warm-cloud depths. Maximum simulated rain rates are 36 mm hr-1 (1500 m depth), 38 mm hr-1 (2500 m), 41 mm hr-1 (3500 m), 51 mm hr-1 (4500 m). This simulated trend of decreasing convective precipitation intensity with increasing elevation (decreasing depth) corresponds qualitatively to the observed trend, suggesting that the differences in warm-cloud depth between elevation groups could explain the differences in rainfall rates with respect to topography. ACKNOWLEDGEMENTS Initial quality control and distribution of radar data was led by Bob Rilling of NCAR EOL, and further quality control of the data was aided by Chad Christianson, Lee Nelson, and Gustavo Periera of CSU. We would like to thank Paul Ciesielski (CSU) for the CSU-NAME upper-air and surface gridded analysis, and Stephen Saleeby (CSU) for the RAMS simulations. Radar observations and analyses were funded by the National Oceanic and Atmospheric Administration (NOAA; SMN radars) Grant NA17RJ1228 and the National Science Foundation (NSF; S-Pol) Grant ATM-0340544. REFERENCES Cifelli, R., W. A. Petersen, L. D. Carey, S. A. Rutledge, and M. A. F. Silva Dias, 2002: Radar observations of the kinematic, microphysical, and precipitation characteristics of two MCSs in TRMM LBA. J. Geophys. Res., 107, 8077. Gochis, D. J., A. Jimenez, C. J. Watts, J. Garatuza-Payan, and W. J. Shuttleworth, 2004: Analysis of 2002 and 2003 warm-season precipitation from the North American Monsoon Experiment event rain gauge network. Mon. Wea. Rev., 132, 2938–2953. Johnson, R. H., T. M. Rickenbach, S. A. Rutledge, P. E. Ciesielski, and W. H. Schubert, 1999: Trimodal characteristics of tropical convection. J. Climate, 12, 2397–2418. _______, P. E. Ciesielski, B. D. McNoldy, P. J. Rogers, and R. K. Taft, 2007: Multiscale variability of the flow during the North American Monsoon Experiment. J. Climate, 20, 1628-1648. Lang, T. J., D. A. Ahijevych, S. W. Nesbitt, R. E. Carbone, S. A. Rutledge, and R. Cifelli, 2007: Radar-observed characteristics of precipitating systems during NAME 2004. J. Climate, 20, 1713–1733. Saleeby, S. M., and W. R. Cotton, 2004: A large droplet mode and prognostic number concentration of cloud droplets in the Colorado State University Regional Atmospheric Modeling System (RAMS). Part I: Module descriptions and supercell test simulations. J. Appl. Meteor., 43, 182–195. Yuter, S. E., and R. A. Houze Jr., 1997: Measurements of raindrop size distributions over the Pacific warm pool and implications for Z–R relations. J. Appl. Meteor., 36, 847–867. Contact Info: Angela Rowe, CSU Atmospheric Science, Fort Collins, CO 80523 firstname.lastname@example.org Rain rate 2-D composite from 0000 UTC on 6 August 2004 Elevation groups in m (MSL) Conditional average reflectivity (dBZ) Cumulative frequency of stability (dT/dz) greater than -5° (solid), -4°(dashed), and -3° C km-1 (dotted) Average values plotted for a cross section along 24ºN. Warm-cloud depths computed as the difference in height between the melting level and the LCL. Elevation values less than 0 m indicate water. 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