1. Statistical Analysis of S-Pol Polarimetric Radar Data from NAME 2004 Timothy J. Lang, Robert Cifelli, Steven A. Rutledge, Angela Rowe, and Lee Nelson Colorado State University, Fort Collins, CO Contact Info: Timothy Lang, CSU Atmospheric Science, Ft Collins, CO 80523; (970) 491-6944, tlang@atmos.colostate.edu P8A.7 NAME radar network (only Cabo, Guasave, and S-Pol data were available for analysis) S-Pol 24-h Ops 7/8-8/21; Two Modes Climatology Used most frequently; 200-km range Full-volume 360s, complete in 15 min Rain-map angles (0.8,1.3,1.8°) & 0.0° Storm Microphysics ~90 hours total spread over ~35 cases Usually 150-km range 2-3 PPIs with 0-1 RHIs in 15 min 360s @ rain-map angles (0.8,1.3,1.8°) ● Threshold on  HV,  (  DP ) – noise, clutter ● Threshold on Z H, Z DR – insects ● Threshold on LDR,  DP – second trip ● 21-pt (3.15 km) finite impulse response (FIR) filter on  DP ● Adaptive linear fit to calculate K DP (i.e., higher Z H, fewer pts used) ● Z H, Z DR rain attenuation correction via  DP method (Carey et al. 2000) ● Z H corrected for gaseous attenuation (Battan 1973) ● Rainfall from CSU blended polarimetric algorithm (Cifelli et al. 2002) (Base Z-R: Z=133R 1.5 pol-tuned via Bringi et al. 2004) ● Blockage corrected via Cifelli et al. (2002) and Lang et al. (2007) ● Data gridded to 0.02° x 0.02° x 1 km 3-D grid, matched in horizontal to 2-D regional grids of Lang et al. (2007), using SPRINT ● 15-min temporal resolution (3818 volumes for entire project) ● Grids extend ~1.6° in each direction from S-Pol ● Grids include all polarimetric variables plus fuzzy-logic hydrometeor ID via Tessendorf et al. (2005) ● Break down gridpoints by terrain (over water, 0-500 m land, 500-1500 m, and 1500+ m MSL) to investigate possible topographic influences ● Using lowest gridpoint containing rainfall, examine reflectivity, Z DR and D 0, K DP, and rainfall rate, following Carey et al. (2001) ● D 0 via D 0 = 1.529*(Z DR ) 0.467 ● Use Cifelli et al. (2002) to examine ice and liquid water mass contents in vertical 2. Quality Control and Methodology Three radars in core Monsoon region (NAME Tier I; NW Mexico) Network covered Gulf of California, Sierra Madre Occidental, Coastal Plain, Baja Peninsula, Pacific Ocean S-Pol – S-Band, Polarimetric, Doppler SMN – Cabo and Guasave radars (C-Band, Doppler) (only used S-Pol in this study) 1. Overview In this poster we report on preliminary results from an investigation into the statistical characteristics of convection during NAME 2004, emphasizing rainfall and microphysical structure. We seek to understand the basic characteristics of precipitation in this region, and how they may be affected by the complex terrain. While reflectivity statistics are similar among the different terrain bands, clear differences in D 0 between land (coastal plain and SMO) and sea (Gulf of California) exist. Generally, larger D 0 s are more common over land, and for high reflectivities (i.e., convection) the sea D 0 is typically smaller than the land D 0. 3. Statistical Results Despite this, higher K DP values and rainfall rates are more common over the water. Though data are noisy and few samples are available, it appears that precipitating systems over the sea are producing high rain rates via DSDs with a smaller D 0. In general, DSD differences between different land elevation bands are smaller than those between land and sea. On average, precipitating systems over the water contain lower precipitation-sized ice mass values than those over land, while differences between the different land elevation bands are small. Ice - solid Liquid water - dash Land and ocean radar characteristics are nearly 12 h out of phase with one another. Convection peaks during the morning over water, during the afternoon over land. This is similar to the results of Lang et al. (2007) using the 2-D regional multi-radar dataset. 4. Diurnal Cycle Results Similar trends to the above can be found in K DP, rainfall, and liquid and ice mass values. Conditional mean rain rates are higher over water. This may be related to strong but less frequent systems there (Lang et al. 2007). There are minor morning peaks in the land data. The afternoon peaks mostly coincide, with minor differences that do not follow a trend (sometimes low elevations peak first, sometimes high elevations do). This may be related to increased noise due to relatively fewer data points in any one land elevation band. 5. Preliminary Conclusions The largest differences in precipitation and microphysical characteristics appear to be between land and sea, not between different land elevation bands. The heaviest precipitation over the water appears to be the result of DSDs with smaller D 0 values, consistent with a reduced influence of ice-based precipitation processes. Precipitation over the water is nearly 12 h out of phase with precipitation over the land. More detailed analyses of the entire NAME radar dataset, and of NAME convection in particular, are planned for the future.