Idealized Simulations of Atmospheric Coastal Flow along the Central Coast of California

Cui, Zhiqiang; Tjernström, Michael; Grisogono, Branko

doi:10.1175/1520-0450(1998)037<1332:isoacf>2.0.co;2

Cited by 40 publications

(23 citation statements)

References 45 publications

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“…The model is well documented and has been used in a variety of applications including orographic flows (Enger et al, 1993;Grisogono 1995;Enger and Grisogono, 1998) and coastal flows Grisogono and Tjernström, 1996;Sundararajan and Tjernström, 2000). It has been used in a number of studies based on the CW96 experiment (Tjernström, 1999;Tjernström and Grisogono, 2000;and Söderberg and Tjernström, 2001) as well as more general studies of US West Coast flow (Cui et al, 1998;Söderberg and Tjernström, 2002).…”

Section: Model Discussionsupporting

confidence: 64%

“…Supercritical flow was associated with every major cape and headland; at each the flow was observed to accelerate to form an expansion fan, accompanied by a significant drop in BL depth. Details of the spatial variability and extent of the jet have been examined by several modelling studies Holt, 1996;Cui et al, 1998;Edwards et al, 2001). The basic features of the flow around headlands can be reproduced by simple shallow water models (Winant et al, 1988;Samelson, 1992), but Dorman et al (1999) noted that such models cannot explain the considerable small-scale complexity found in the aircraft observations.…”

Section: Synoptic Situation and Mesoscale Dynamicsmentioning

confidence: 99%

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The Turbulence Structure of the Stable Atmospheric Boundary Layer Around a Coastal Headland: Aircraft Observations and Modelling Results

Brooks

Söderberg

Tjernström

2003

Boundary-Layer Meteorology

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The turbulence structure of a stable marine atmospheric boundary layer in the vicinity of a coastal headland is examined using aircraft observations and numerical simulation.Measurements are drawn from a flight by the NCAR C-130 around Cape Mendocino on the coast of Northern California on June 7 1996 during the Coastal Waves 96 field program.Local similarity scaling of the velocity variances is found to apply successfully within the continuously turbulent layer; the empirical scaling function is similar to that found by several previous studies. Excellent agreement is found between the modelled and observed scaling results. No significant change in scaling behaviour is observed for the region within the expansion fan that forms downstream of the cape, suggesting that the scaling can be applied to horizontally heterogeneous conditions; however, the precise form of the function relating scaled velocities and stability is observed to change close to the surface. This result, differences between the scaling functions found here and in other studies, and the departure of these functions from the constant value predicted by the original theory leads us to question the nature of the similarity functions observed. We hypothesize that the form of the functions is controlled by non-local contributions to the velocity variance budgets, and that differences in the non-local terms between studies explain the differences in the observed scaling functions.2

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Section: Model Discussionsupporting

confidence: 64%

Section: Synoptic Situation and Mesoscale Dynamicsmentioning

confidence: 99%

The Turbulence Structure of the Stable Atmospheric Boundary Layer Around a Coastal Headland: Aircraft Observations and Modelling Results

Brooks

Söderberg

Tjernström

2003

Boundary-Layer Meteorology

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“…Several studies have addressed the dynamics of CLLJ, mostly on the California jet (Winant et al, 1988;Burk and Thompson, 1996;Cui et al, 1998;Dorman et al, 1999;Tjernstro¨m and Grisogono, 2000;Edwards et al, 2001), showing that thermal wind processes, along with the landÁ sea temperature gradient define its structure. Due to the synoptic forcing, the large-scale flow in the MABL is equatorward and coast-parallel.…”

Section: Introductionmentioning

confidence: 99%

“…Most studies about CLLJ published in the literature are based on field campaigns during the summer (Beardsley et al, 1987;Zemba and Friehe, 1987;Winant et al, 1988, Sundararajan andTjernstro¨m, 1999), and on modelling and theoretical efforts (Cui et al, 1998;Rogerson, 1999). These studies have focused mainly on the California and ChileÁPeru coastal jets, with some exceptions on the SomaliÁOman jet (Findlater, 1969;Ardanui, 1979) and more recently on the Benguela jet (Nicholson, 2010).…”

Section: Introductionmentioning

confidence: 99%

Climatology of the Iberia coastal low-level wind jet: weather research forecasting model high-resolution results

Soares

Cardoso²,

Semedo

et al. 2014

Tellus A: Dynamic Meteorology and Oceanography

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A B S T R A C T Coastal low-level jets (CLLJ) are a low-tropospheric wind feature driven by the pressure gradient produced by a sharp contrast between high temperatures over land and lower temperatures over the sea. This contrast between the cold ocean and the warm land in the summer is intensified by the impact of the coastal parallel winds on the ocean generating upwelling currents, sharpening the temperature gradient close to the coast and giving rise to strong baroclinic structures at the coast. During summertime, the Iberian Peninsula is often under the effect of the Azores High and of a thermal low pressure system inland, leading to a seasonal wind, in the west coast, called the Nortada (northerly wind). This study presents a regional climatology of the CLLJ off the west coast of the Iberian Peninsula, based on a 9 km resolution downscaling dataset, produced using the Weather Research and Forecasting (WRF) mesoscale model, forced by 19 years of ERA-Interim reanalysis (1989Á2007). The simulation results show that the jet hourly frequency of occurrence in the summer is above 30% and decreases to about 10% during spring and autumn. The monthly frequencies of occurrence can reach higher values, around 40% in summer months, and reveal large inter-annual variability in all three seasons. In the summer, at a daily base, the CLLJ is present in almost 70% of the days. The CLLJ wind direction is mostly from north-northeasterly and occurs more persistently in three areas where the interaction of the jet flow with local capes and headlands is more pronounced. The coastal jets in this area occur at heights between 300 and 400 m, and its speed has a mean around 15 m/s, reaching maximum speeds of 25 m/s.

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“…The offshore dimensions of the smaller SB systems (e.g., over the island) were highly limited by the topography and the interaction with the other systems. The blocking effect of mountains can occur if the Burger number (B = h m N /f L ⊥ ) is higher than 1 (Cui et al, 1998;Kottmeier, 2000;Prtenjak et al, 2006) depending only on h m , the mountain's halfwidth (L ⊥ ), N and the Coriolis parameter (f ). For h m and L ⊥ , we substituted 1500 m and 50 km as the average vertical and horizontal spreading of the coastal mountainous belt, respectively.…”

Section: Discussion Of the Daytime Wind Characteristicsmentioning

confidence: 99%

Characteristics of shallow thermally driven flow in the complex topography of the south-eastern Adriatic

Prtenjak

Tomažić²,

Kavčič

et al. 2010

Ann. Geophys.

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Abstract. Characteristics of thermally induced flow, namely the sea breeze, are investigated along the south-eastern Adriatic. The chosen period 24-25 April 2006 favoured sea breeze development and simultaneously allowed a comparison of the large-scale wind influence (north-westerly wind versus south-easterly wind) and the complex terrain on the local circulations. Particular attention is paid to the smallscale formation of the wind field, convergence zones (CZs), channelling flows and small scale eddies, especially in the vicinity of two airports in the central part of south-eastern Adriatic. The results are based on wind measurements (from meteorological surface stations, radiosoundings, satellite data and sodar data) and further supplemented by model data at fine grid spacing.This study shows the formation of numerous irregular daytime and nighttime CZs, which occurred along the coastline in the lee of mountains and over the larger, elongated islands. The results show that the above mentioned airports are surrounded by daytime CZ formations within the lowermost 1000 m and associated updrafts of 1 m s −1 , especially if CZs are maintained by the north-westerly largescale winds. Whereas the daytime CZ was generated due to merged sea breezes, the weaker and shallower nighttime CZs were formed by wind convergence of the seaward breezes, and significantly modified by the large-scale flow of the topography (e.g., accelerated flow in the sea channels and substantial swirled flows around the islands).The passes between the coastal mountain peaks changed the inflow penetration, provoking the increase in wind speed of the channelled flow. The strongest sea breeze channellingCorrespondence to: M. T. Prtenjak (telisman@gfz.hr) was observed above the valley of the Neretva River, where the onshore flow reached 40 km inland with a strength of 8 m s −1 , and the highly asymmetric offshore part was confined within the sea channel.

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Idealized Simulations of Atmospheric Coastal Flow along the Central Coast of California

Cited by 40 publications

References 45 publications

The Turbulence Structure of the Stable Atmospheric Boundary Layer Around a Coastal Headland: Aircraft Observations and Modelling Results

The Turbulence Structure of the Stable Atmospheric Boundary Layer Around a Coastal Headland: Aircraft Observations and Modelling Results

Climatology of the Iberia coastal low-level wind jet: weather research forecasting model high-resolution results

Characteristics of shallow thermally driven flow in the complex topography of the south-eastern Adriatic

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