Fine-Scale Observations of a Pre-Convective Convergence Line in the Central Great Plains on 19 June 2002 The Problem Questions: 1. How do mesoscale atmospheric processes and surface fluxes alter the convective boundary layer (CBL) to generate a dryline boundary? 2. How is dryline convergence maintained, at very small scales (Ziegler and Rasmussen 1998)? 3. How does deep convection initiate along a dryline at those scales? Vertical Structure and Evolution Density Current Dynamics Sustained Convergence Early soundings through the CBL demonstrate the presence of a strong capping inversion at 850 mb and increasing values of CAPE. First series of stepped traverses shows θ e and ‘r’ differences 3 K and 1.5 g kg -1, resp. across the dryline, later to increase to 10 K and 6 g kg -1 indicating dryline strengthening. By 21 UTC cross dryline confluence increases with values of 10 ms -1 over distances of hundreds of meters. Murphey et al. (2005) find that horizontal shearing along the dryline due to confluence yields high vertical vorticity along a contorted dryline on this day. A first stepped traverse shows that the dry air is cooler (θ v lower), consistent with the westward tilt of the dryline & the negative solenoidal circulation. Dual-Doppler analysis confirms the dryline tilt to the W and the negative solenoidal circulation. The first stepped traverse observes θ v 0.5K cooler on the dry side than moist side, anda peak of 0.5K at the dryline. A remarkable transformation occurs between the 2 nd and 3 rd dryline stepped traverses: the dryline shifts from a westward to an eastward tilt with a consistent θ v gradient reversal. Denser air flips from the W side to the E side of the dryline, possibly because of larger surface sensible heat flux to the W. The vertical velocity dipole consistently shifts, the solenoidal circulation becomes positive, and the eastward propagating fine-line becomes stationary. All this is consistent with density current theory. DOW3 along with mobile mesonet data clearly show strong confluence near the dryline and along the UWKA flight track. During the 3 rd stepped traverse the dryline becomes quasi-stationary and better-defined, according to DOW3 data. LearJet dropsondes and UWKA stepped traverses observe a deep core of positive buoyancy near the dryline. By the last series of transects the CBL depth above the dryline exceeds 3200 m AGL. Advection of high θ e air into the CBL ‘dome’ results in the erosion of CIN. Discussion There is a weak θ v (virtual pot. temp.) gradient across the dryline. This gradient is consistent with the vertical tilt of the echo plume, and the vertical velocity couplet, indicating a thermally direct solenoidal circulation. The circulation and tilt reverse when the θ v (virtual pot. temp.) gradient reverses. At the fine-line convergence zone (the dryline), anomalously high θ v occurred, deepening in time till CI. Conclusions Updrafts greater than 5 m/s are observed, collocated with anomalously high values of θ v This leads to local deepening of the CBL along the fine-line, leading to CI. Dual-Doppler wind field demonstrates the existence of solenoidal circulations consistent with horizontal density differences, and changes in dryline propagation speed. Benjamin Daniel Sipprell, and Bart Geerts, University of Wyoming, Laramie, USA JP3J.1 DOW3 data, local mesonets and mobile mesonets show an increasingly intense southerly jet and thus increasing confluent flow into a evolving stationary dryline. REFERENCES: Murphey, Hanne V. and Wakimoto, Roger M., 2005: Dryline on 19 June 2002 during IHOP. Part I: Airborne Doppler and LEANDRE II Analysis of the Thin Line Structure and Convection Initiation. Mon. Wea. Rev.: in press. Ziegler, Conrad L. and Rasmussen, Erik N., 1998: The Initiation of Moist Convection at the Dryline: Forecasting Issues from a Case Study Perspective. Wea. and Forecasting: Vol. 13, No. 4, pp. 1106–1131. Objectives: 1. To describe the kinematic and thermodynamic properties of a pre- convective dryline at very high resolutions and in vertical cross sections. 2. To demonstrate via a case study that fine-scale convergence is driven by the buoyancy gradient, sustained by density current dynamics. Early (unusual eastward tilt) Late (classic westward tilt)