Mid-Level Vorticity, Moisture, and Gross Moist Stability in the Tropical Atmosphere
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1 Mid-Level Vorticity, Moisture, and Gross Moist Stability in the Tropical Atmosphere David Raymond, Saška Gjorgjievska, Sharon Sessions, Carlos López, Željka Fuchs Physics Department and Geophysical Research Center New Mexico Tech Supported by the National Science Foundation and the Office of Naval Research
2 Special thanks to collaborators: Saška Gjorgjievska Sharon Sessions Carlos López Željka Fuchs
3 Showers and rains: Ramage (1971) divides tropical precipitation into two regimes: Showers: Fine weather with relatively dry conditions, high CAPE, low shear; Rains: Cloudy weather with moist conditions, low CAPE, higher shear; The rains regime produces more average rainfall; The showers regime produces higher peak rainfall. Williams et al. (1992) make similar distinction and correlate higher lightning rates with the showers regime. Is low CAPE and high moisture a cause or an effect of convection with higher average rainfall?
4 In situ measurements: TPARC/TCS08 (2008) project in western Pacific ELDORA radar (NRL P-3) Dropsondes from 10 km (Kessler C-130Js) PREDICT/GRIP/IFEX (2010) project in western Atlantic and Caribbean Dropsondes from km (NSF/NCAR G-V, NASA DC-8)
5 Two examples; Hagupit2 and Nuri2: km absolute vorticity (ks 1 ) and relative wind (20 m/s/deg) 10 m/s Hagupit2 Nuri lat (deg) lat (deg) lon (deg) lon (deg) 0.2
6 Thermodynamic Effect of Vortices West Pacific wave Reed and Recker (1971) warm PV anomaly Developing disturbance warm PV anomaly cool
7 Hagupit2 dynamics: Hagupit total planetary 10 8 ent satent 10 8 height (km) circulation (km 2 /s) entropy (J/K/kg) mass flux (10 9 kg/s)
8 Nuri2 profiles: Nuri total planetary 10 8 ent satent 10 8 height (km) circulation (km 2 /s) entropy (J/K/kg) mass flux (10 9 kg/s)
9 Thermodynamics: Instability index: s lo : average s over [1, 3] km s hi : average s over [5, 7] km I = s lo s hi Saturation fraction: / F = rdp r S dp / (s s d ) dp (s s d ) dp r: mixing ratio r S : saturation mixing ratio s d : dry entropy s: moist entropy s : saturated moist entropy
10 Instability index: height (km) Mean Soundings Nuri2 Hagupit2 I-H2 I = instability index I-N moist entropy (J/K/kg)
11 Mean Nuri2 - Hagupit2 temperatures: 10 8 Temperature difference: nuri2 hagupit2 z vs dtemp z vs dtvirt height (km) temp diff (K)
12 Differences quantified: Nuri2 Hagupit2 Instability index 11 J/ K/ kg 27 J/ K/ kg Saturation fraction Normalized GMS Mass flux bottom-heavy top-heavy Vorticity maximum middle levels surface (weak) Fate rapid devel delayed devel
13 TCS08/PREDICT: Instability index vs mid-level vorticity instability index (J/K/kg) H2 N mid-level absolute vorticity (ks 1 )
14 TCS08/PREDICT: Saturation fraction vs instability index 0.90 N saturation fraction H instability index (J/K/kg)
15 Normalized Gross Moist Stability (NGMS) NGMS = ( TR L ) ( [ h (ρv h s)] + ρv z s top [ h (ρv h r)] + ρv z r top [χ]: Horizontal average and vertical integral of χ. χ top : Horizontal average of χ at domain top. T R : Constant reference temperature; L: Latent heat constant; ρ: Density; s: Specific moist entropy; r: Water vapor mixing ratio; v h : System-relative horizontal wind; v z : Vertical wind. )
16 NGMS and the mass flux profile: high NGMS top-heavy low NGMS bottom-heavy div height conv div div conv θe mass flux
17 TCS08/PREDICT: NGMS vs mid-level vorticity NGMS H2 0.0 N mid-level absolute vorticity (ks 1 )
18 TCS08/PREDICT: NGMS vs instability index NGMS H2 0.0 N instability index (J/K/kg)
19 TCS08/PREDICT: NGMS vs saturation fraction NGMS H2 0.0 N saturation fraction
20 Rain and mass flux profiles from WTG cloud simulations: (Raymond, D. J. and S. L. Sessions, 2007) A B height (m) unperturbed δθ = ± 0.5 K δθ = ± 1.0 K δθ = ± 2.0 K unperturbed δr = 0.25 g/kg δr = 0.5 g/kg δr = 1.0 g/kg θ perturbation (K) moisture perturbation (g/kg)
21 Rain and Mass Flux Profiles (cont...) A unperturbed δθ = ± 0.5 K δθ = ± 1.0 K δθ = ± 2.0 K B unperturbed δr = 0.25 g/kg δr = 0.5 g/kg δr = 1.0 g/kg height (m) v y =7m/s mass flux (kg/m 2 s) v y =7m/s mass flux (kg/m 2 s)
22 Chain of causality Increased mid-level vorticity Decreased instability index Convective dynamics Horizontal and vertical shear Increased saturation fraction Decreased NGMS Increased rain and energy transfer to the large scale
23 References Raymond, D. J. and S. L. Sessions, 2007: Evolution of convection during tropical cyclogenesis. Geophys. Res. Letters, 34, L06811, doi: /2006gl Ramage, C. S., 1971: Monsoon Meteorology. Academic Press, New York, 296 pp. Williams, E. R., S. A. Rutledge, S. G. Geotis, N. Renno, E. Rasmussen, and T. Rickenbach, 1992: A radar and electrical study of tropical hot towers. J. Atmos. Sci., 49,
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