1 / 25

Flash-Flood-Producing Convective Systems Associated with Mesoscale Convective Vortices

Purpose. To understand the processes responsible for initiating, organizing, and maintaining convective systems that produce excessive rainfall and lead to flash floodingTo investigate convective systems that initiate near midlevel circulations (such as mesoscale convective vortices) and remain nea

ginger
Download Presentation

Flash-Flood-Producing Convective Systems Associated with Mesoscale Convective Vortices

An Image/Link below is provided (as is) to download presentation Download Policy: Content on the Website is provided to you AS IS for your information and personal use and may not be sold / licensed / shared on other websites without getting consent from its author. Content is provided to you AS IS for your information and personal use only. Download presentation by click this link. While downloading, if for some reason you are not able to download a presentation, the publisher may have deleted the file from their server. During download, if you can't get a presentation, the file might be deleted by the publisher.

E N D

Presentation Transcript

    1. Flash-Flood-Producing Convective Systems Associated with Mesoscale Convective Vortices Russ S. Schumacher Department of Atmospheric Science, Colorado State University and National Center for Atmospheric Research

    2. Purpose To understand the processes responsible for initiating, organizing, and maintaining convective systems that produce excessive rainfall and lead to flash flooding To investigate convective systems that initiate near midlevel circulations (such as mesoscale convective vortices) and remain nearly stationary for 6-12 hours

    3. Background: MCVs Latent heating in mesoscale convective systems (MCSs) redistributes potential vorticity (PV), sometimes resulting in a positive PV anomaly (and cyclonic circulation) at midlevels, referred to as a mesoscale convective vortex (MCV) Raymond and Jiang (1990) showed how MCVs in shear can initiate and/or maintain convection via isentropic upglide on the downshear side of the vortex Trier et al. (2000) showed that this lifting also leads to destabilization and moist absolutely-unstable layers When a low-level jet approaches the MCV, the downshear side is upwind: convection that develops moves slowly (e.g., Fritsch et al. 1994)

    4. Background: MCVs and heavy rainfall Bosart and Sanders (1981), Fritsch et al. (1994), and Trier and Davis (2002) studied significant flash flood events near MCVs Fritsch et al. showed that when a strong low-level jet approaches the MCV, convection is favored near the center of the vortex This leads to slow system motion and heavy rainfall

    6. Case selection We identified six warm-season extreme rain events associated with MCVs or other midlevel circulations The selection of cases was somewhat subjective, but all had the following in common: Gauge-observed rainfall in excess of 200 mm (7.9 in) in less than 12 hours Heavy rainfall produced by a convective system that had “back-building/quasi-stationary” organization at some point The presence of a preexisting midlevel circulation near where the convection developed Flash flooding resulting from the rainfall

    7. 6-7 May 2000 Max rainfall: 309 mm (12.1 in); 2 fatalities and $100M in damage Analyzed in Schumacher and Johnson (2008, MWR, Oct. issue)

    8. 6-7 May 2000 MCS Surface observations and WRF simulations reveal a convectively-generated mesolow and pressure trough, no cold pool More details: see Schumacher and Johnson (2008), MWR, October issue

    9. 20 August 2007 Formed from remnants of TS Erin after surface low weakened Max rainfall: 266 mm (10.5 in); most damage was to rural roads

    10. 25 June 2008 Occurred after we performed the analysis, but fits the bill… Max rainfall: 219 mm (8.6 in)

    11. Soundings

    12. Composite analysis: Midlevel vorticity Composites computed from RUC 0-h analyses, centered at location of maximum rainfall Results projected onto a map centered at Springfield, MO (black box denotes heavy rainfall location) Average vorticity in the 700-500-hPa layer, 600-hPa heights and winds

    13. Composite: Midlevel vorticity & LLJ

    14. Composite CAPE & CIN Little CAPE in heavy rain area in the afternoon LLJ brings high-?e air into area, and vortex-related destabilization also takes place By the time the MCS develops, over 1000 J/kg of CAPE and no CIN

    15. Composite sounding Calculated at RUC grid point and time nearest heavy rainfall Stable near surface, but elevated parcels have 1149 J/kg of CAPE and no CIN Nearly saturated at low levels; PW=49 mm (1.93”) ~15 m/s LLJ and weak midlevel winds produces “hairpin” hodograph – shear vector turns sharply with height

    16. Summary: Extreme rainfall near MCVs

    17. Conclusions Analyzed 6 events where extreme local rainfall (>200 mm) occurred near a midlevel cyclonic circulation Lifting associated with the interaction between a strong low-level jet and the midlevel vortex helped to initiate and maintain deep convection Strong LLJ, weak midlevel winds ? “hairpin” hodograph Thermodynamic environment: very high RH, moderate CAPE, little CIN; destabilized by vortex-related lifting

    20. Background: MCVs in shear Raymond and Jiang (1990) described how MCVs (or other midlevel PV anomalies) in shear can help to initiate and/or maintain additional convection via isentropic upglide on the downshear side of the vortex Trier et al. (2000) showed that this region is destabilized and that moist absolutely unstable layers (MAULs; Bryan and Fritsch 2000) can form by the lifting of conditionally unstable air to saturation

    21. Operational Model QPF

    22. Operational Model QPF

    23. Rainfall totals

    24. Summary: 6-7 May 2000 MCS

    25. Parcel trajectories along gravity wave

    26. Observational evidence These MCSs are small, so they don’t often pass over a surface station The 20 August 2007 case does provide some evidence for these waves

More Related