Favorable Conditions for Cyclogenesis Near the Atlantic Coast*

Austin, James M.

doi:10.1175/1520-0477-22.6.270

Cited by 12 publications

(6 citation statements)

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“…However, the High ahead of Storm B ridged back to the northwest to join a High moving down over central Canada. This was the beginning of blocking conditions, similar to those in the second case described by Austin [3], which made the major difference in later development of these two storms.…”

Section: As Storms a And B Moved Eastward The Hudson Baysupporting

confidence: 57%

A Comparison of Two Redeveloping Texas Lows, January 1958

Martin¹,

Bucci²

1958

Mon. Wea. Rev.

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Section: As Storms a And B Moved Eastward The Hudson Baysupporting

confidence: 57%

A Comparison of Two Redeveloping Texas Lows, January 1958

Martin¹,

Bucci²

1958

Mon. Wea. Rev.

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“…In structure, they resemble shallow quasi-stationary or warm fronts with temperature contrasts that can reach more than 10°C over short distances on the order of 100 km or less (Bosart 1975). Coastal fronts are of major importance in the coastal zone and adjacent inland areas since they are often associated with enhanced cloudiness and precipitation, can mark the transition zone between frozen and liquid precipitation, and provide a source of surface convergence and vorticity that often focuses cyclogenesis (Austin 1941;Carson 1950;Marks and Austin 1979;Bosart 1981). When these fronts move ashore, they have sometimes been associated with the development of severe weather (Businger et al 1991;Vescio et al 1993).…”

Section: Introductionmentioning

confidence: 99%

An Objective Climatology of Carolina Coastal Fronts

Appel

Riordan

Holley³

2005

Weather and Forecasting

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This study describes a simple objective method to identify cases of coastal frontogenesis offshore of the Carolinas and to characterize the sensible weather associated with frontal passage at measurement sites near the coast. The identification method, based on surface hourly data from offshore and adjacent land stations, was applied to an 11-yr dataset (1984–94). A total of 379 coastal fronts was found, 70 of which eventually made landfall along the North Carolina coast; 112 that remained offshore, and 197 were termed diurnal since they remained offshore but disappeared during daylight hours. Results show that most coastal and offshore sites experience a wind shift of about 40°–70° and a warming of about 2°–3°C during the hour of frontal passage. Exceptions include sites near colder waters where the rates are markedly reduced and frontal passage is often less discernible. Excluding diurnal fronts, just over half the cases were associated with cold-air damming (CAD) during the cold season of 16 October–15 April. Most of these winter cases linked with CAD were onshore fronts. During the warm season, most fronts were diurnal, but the association with CAD was still significant. To explore the synoptic-scale environment, composite maps for the cold season were generated for all three frontal subtypes from NCEP–NCAR reanalysis data. Results show a strong surface anticyclone centered north of the region of frontogenesis for all three composites. However, several features in the synoptic-scale regimes appear to differentiate the three frontal types. For example, cyclogenesis in the Gulf of Mexico and onshore southeasterly low-level flow along the southeast Atlantic coast accompanied by warm advection distinguish onshore fronts from the other two types. The offshore fronts are accompanied by more nearly zonal flow aloft and a surface anticyclone that stalls near the New England coastline. Finally, the diurnal type is associated with much weaker pressure and height fields and an east–west elongated surface anticyclone centered much farther south than in the other cases.

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“…Instead, most snowfall research has investigated the meteorological dynamics responsible for particular types of snowstorms (i.e. Bosart and Lin, 1984;Uccellini et al, 1985;MacDonald and Reiter, 1988) or on a statistical analysis of the proper conditions to produce heavy snowfall (Austin, 1941; Goree and Younkin, 1966;Browne and Younkin, 1970;Brandes and Spar, 1971; Sanders and Gyakum, 1980). anomalies (Namias, 1978;Walsh et al, 1982;Heim and Dewey, 1984), with daily temperature forecast errors (Dewey, 1977) and even with cyclone frequencies and severe weather outbreaks across the USA .…”

Section: Introductionmentioning

confidence: 99%

Temporal characteristics of USA snowfall 1945–1946 through to 1984–1985

Leathers

Mote

Kuivinen

et al. 1993

Intl Journal of Climatology

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The temporal variability of USA snowfall is investigated for the period 1945-1946 through to 1984-1985 using linear trend and principal components analyses. The results of the linear trend analysis indicate that two regions of the USA evidence significant changes in monthly snowfall over the period. These areas include the Great Lakes/upper mid-west and high plains regions of the USA. In the Great Lakes/upper mid-west sector, positive linear trends are found in monthly snowfall totals for the mid-winter months (December, January, February). For the high plains region, positive linear trends are found for the month of December. Principal components analysis (PCA) is used with seasonal snowfall data in order to better understand the spatial and temporal nature of seasonal snowfall variations across the USA. The PCA isolates six spatially coherent regions in which seasonal snowfall varied similarly over the 40-year period. Only one of these regions, centred on the Great Lakes and upper mid-west, displays any long-term change in seasonal snowfall, a positive trend during the period 1945-1946 through to 1984-1985. These results are discussed in the context of maninduced and natural environmental changes.

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Favorable Conditions for Cyclogenesis Near the Atlantic Coast*

Cited by 12 publications

References 0 publications

A Comparison of Two Redeveloping Texas Lows, January 1958

A Comparison of Two Redeveloping Texas Lows, January 1958

An Objective Climatology of Carolina Coastal Fronts

Temporal characteristics of USA snowfall 1945–1946 through to 1984–1985

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