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Michael C. Coniglio, Stephen F. Corfidi, and John S. Kain

lower-tropospheric warm advection, convergence, and conditional instability, all of which are enhanced by a nocturnal low-level jet (LLJ) ( Blackadar 1957 ; Bonner 1968 ; McNider and Pielke 1981 ; Cotton et al. 1989 ; Laing and Fritsch 2000 ; Tuttle and Davis 2006 ). The development of a large, intense MCS resulted from a complex series of processes and mergers of several convective lines and clusters over a relatively short time period, which is also common for warm season MCSs ( McAnelly et

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Brian A. Colle, Kenneth A. Loescher, George S. Young, and Nathaniel S. Winstead

1. Introduction This paper is a continuation of Loescher et al. (2006 , hereafter Part I ) in which a temporal and spatial climatology of barrier jets along the Alaskan coast was constructed using synthetic aperture radar (SAR) satellite data from 1998 to 2003. The authors found that Alaskan barrier jets were more frequent from September through March and were closely linked to those coastal areas with steep terrain; however, the jet frequency was more closely associated with the high terrain

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WARREN SMITH and RUSSELL J. YOUNKIN

..UDC 561.6md:51.677.37An Operationally Useful Relationship Between thePolar Jet Stream and Heavy PrecipitationWARREN SMITH and RUSSELL J. YOUNKIN-National Meteorological Center,National Weather Service, NOAA, Suitland, Md.1 ABSTRACT-The jet stream is recognized as an impor- meteorological relationships involved, we developed com-1 tant atmospheric mechanism for vertical exchange pro- posite models from seven representative cases and studied cesses. It follows that certain jet stream

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Osamu Isoguchi, Masanobu Shimada, and Hiroshi Kawamura

some cases has shed light on previously unknown phenomena, especially about coastal wind fields. There are numerous works of research dealing with the orographically forced coastal wind fields such as katabatic winds, bora winds, gap winds, and barrier jets (e.g., Alpers et al. 1998 , 2009 ; Pan and Smith 1999 ; Sandvik and Furevik 2002 ; Loescher et al. 2006 ; Colle et al. 2006 ; Winstead et al. 2006 ). Alpers et al. (1998 , 2009) investigated katabatic wind fields over Mediterranean

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V. J. OLIVER, R. K. ANDERSON, and E. W. FERGUSON

October 1964 V. J. Oliver, R. K. Anderson, and E. W. Ferguson 441SOME EXAMPLES OF THE DETECTION OF JET STREAMS FROM TIROS PHOTOGRAPHS V. J. OLIVER, R. K. ANDERSON, and E. W. FERGUSON National Weather Satellite Center, U.S. Weather Bureau, Washington, D.C.ABSTRACTTIROS phot.ographs of cloud patterns in the vicinity of the jet stream are examined and compared with surface,upprr air, and pilot-rrport data. It is found that with certain conditions of lighting and

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A. T. Singleton and C. J. C. Reason

the jet streak that leads to their formation ( Price and Vaughan 1992 ) and are termed “polar,” “subtropical,” and “polar vortex.” Polar-type cutoff lows are formed as a result of equatorward extensions of a polar jet and tend to become situated poleward of the jet. Subtropical cutoff lows tend to be formed by equatorward extensions of a subtropical jet, or where a split in a zonal polar jet causes a weak equatorward branch. The polar vortex–type cutoff low forms from an extension of the polar

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WALTER H. HOECKER JR.

MONTHLY WEATHER REVIEW573THREE SOUTHERLY LOW-LEVEL JET SYSTEMS DELINEATED BY THEWEATHER BUREAU SPECIAL PIBAL NETWORK OF 1961WALTER H. HOECKER, JR. U.S. Weather Bureau, Washington, D.C.[Manuscript received January 24, 1963; revised April 30, 19631ABSTRACTFor the first time in meteorological hist,ory the broad aspects of the southerly low-level jet over the WesternPlains have been studied in fine detail both in time and space. This was accomplished in the spring of 1961 bymeans of a line of

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Matthew E. Pyle, Daniel Keyser, and Lance F. Bosart

1. Introduction Jet streaks, defined as localized wind speed maxima within jet streams (e.g., Palmén and Newton 1969 , p. 199; Bluestein 1993 , section 2.7.4), are a classic topic in midlatitude synoptic–dynamic meteorology. Studies relating upper-level jet streaks to cyclogenesis (e.g., Bjerknes 1951 ; Uccellini et al. 1984 , 1987 ; Uccellini and Kocin 1987 ; Wash et al. 1988 ; Velden and Mills 1990 ), severe weather (e.g., Beebe and Bates 1955 ; Uccellini and Johnson 1979

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RenéD. Garreaud and Ricardo C. Muñoz

, satellite scatterometer data and marine reports reveal an area of maximum surface wind speed extending a few hundred kilometers off the coast of central Chile (25°–35°S) where average values exceed 8 m s −1 during austral spring and summer (e.g., Halpern et al. 2002 ; Josey et al. 2002 ). Furthermore, vertical wind profiles obtained at the coast at 30°S during periods of strong southerly winds reveal a low-level jet (LLJ) structure with strong vertical shear above and below the wind maxima located

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James D. Doyle and Thomas T. Warner

2414 MONTHLY WEATHER REVIEW VOLUME II9A Carolina Coastal Low-Level Jet during GALE lOP 2 JAMES D. DOYLE AND THOMAS T. WARNERDepartment of Meteorology. The Pennsylvania State University, University Park. Pennsylvania(Manuscript received 11 November 1990, in final form 8 April 1991) During the Intensive Observation Period 2 of the Genesis of Atlantic Lows Experiment a persistent

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