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John M. Peters, Erik R. Nielsen, Matthew D. Parker, Stacey M. Hitchcock, and Russ S. Schumacher

inflow layer (EIL; Thompson et al. 2007 ). We refer to storms within an environment where the lower bound of the EIL (as defined by the aforementioned CAPE and CIN thresholds) is above the earth’s surface as elevated. In this article, we use an observational analysis of an elevated MCS’s near environment to demonstrate how numerical weather prediction (NWP) models’ moisture errors within an MCS’s EIL influence the ability of these models to accurately predict the MCS. Horizontal and temporal

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Stacey M. Hitchcock and Russ S. Schumacher

several different methods of classification, but two distinct categories consistently emerge for events over the central Great Plains. In synoptic-type events, a strong midtropospheric trough and slow moving surface front lead to strong forcing for ascent in a region with southerly flow and associated moisture transport. During the warm season, isentropic ascent of warm, moist air transported by the nocturnal low-level jet (LLJ) can lift an air to saturation on the cool side of a stationary or warm

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Manda B. Chasteen, Steven E. Koch, and David B. Parsons

warm season. During the daytime, an east–west temperature gradient had developed over the southern plains, and a surface low and dryline were located over the Edwards Plateau region of west Texas at 0200 UTC ( Fig. 2 ). A quasi-stationary front, which was characterized primarily by a pronounced wind shift and low-level moisture gradient, extended northeastward from the low pressure center into central Oklahoma. Additionally, an extensive radar fine line had moved into northern Oklahoma, which was

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Samuel K. Degelia, Xuguang Wang, and David J. Stensrud

moist layer that is key to generating nocturnal CI. Peters et al. (2017) connect errors in mesoscale convective system (MCS) forecasts to moisture biases, and in the simulations with negative moisture biases the models produce errors in both CI timing and location due to the parcels requiring additional residence time within the lifting regions. Assimilating kinematic and thermodynamic observations can improve many of the above issues related to forecasting nocturnal CI. Recently, Degelia et al

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Stacey M. Hitchcock, Russ S. Schumacher, Gregory R. Herman, Michael C. Coniglio, Matthew D. Parker, and Conrad L. Ziegler

an elevated layer between 0200 and 0500 UTC ( Trier and Parsons 1993 ). Changes were associated with the southward progression of a shallow surface front, and an increase in moisture advection in conjunction with the onset of the southerly nocturnal LLJ. These observations led to a schematic (Fig. 20 in Trier and Parsons 1993 ) of isentropic ascent of high θ e air associated with the LLJ over a quasi-stationary frontal zone. This has become a relatively common conceptual model for nocturnal

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Joshua G. Gebauer, Alan Shapiro, Evgeni Fedorovich, and Petra Klein

enhances the southerly geostrophic wind. It is likely that the effects described by Holton (1967) , Shapiro and Fedorovich (2009) , and Parish (2016) all contribute to the LLJ intensity and frequency maximum over the Great Plains. The LLJ has long been considered to be a key contributor to the nocturnal precipitation maximum over the Great Plains, although not all mechanisms involved are well understood. A well-defined diurnal oscillation in moisture flux over the region is associated with the

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Stanley B. Trier, James W. Wilson, David A. Ahijevych, and Ryan A. Sobash

-tropospheric baroclinic zone, which is intensified by MCS outflow. In the current study we use PECAN radiosonde data and a 50-member model ensemble to examine effects of mesoscale vertical motions on nocturnal elevated CI. Model-based budget studies ( Trier et al. 2014a , b ) have illustrated the critical role of mesoscale vertical motions in reducing negative buoyancy in environments of both initiating and mature elevated MCSs. Both upward transports of moisture that raise the relative humidity of convecting air

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Tammy M. Weckwerth and Ulrike Romatschke

). The compositing process used in our analyses smoothed out the jet streak structure so the jet coupling is not as prominent as that shown in Squitieri and Gallus (2016) . Significant low-level moisture associated with the LLJ was observed in the region ( Fig. 16a ). The enhanced moisture at 300 mb ( Fig. 15a ) was likely caused by a combination of advection from the southwest and upward moisture transport by the sustained deep convection in the region. Break days also showed 850-mb southerly flow

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Aaron Johnson and Xuguang Wang

), upstream of the spurious convection in 10min.6cycle, has dewpoints around 58°–62°F at 2100 UTC in THOM while 10min.6cycle dewpoints are about 62°–66°F. The 10min.6cycle dewpoints are too moist, compared with the observed dewpoints of ~61°F in this area (not shown). It is in this region of excess moisture where the 10min.6cycle forecast develops spurious convection in advance of the observed MCS ( Figs. 5c,d ). The low-level air that had been advected into northwest Oklahoma and southwest Kansas by 1800

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Tammy M. Weckwerth, Kristy J. Weber, David D. Turner, and Scott M. Spuler

1. Introduction There is a long-standing and certain need for improved atmospheric moisture measurements within and just above the atmospheric boundary layer (BL; defined here to be the lowest 2–3 km above the earth’s surface). Several recent National Research Council (NRC) reports highlighted the requirement for improved moisture and wind measurements in the BL as a necessary step toward improving numerical weather prediction (NWP) and quantitative precipitation forecasting (QPF) skill ( NRC

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