- Abstract
- 1. Introduction: Hints of mesoscale convection
- 2. World War II and the amazing work of Hamilton and Archbold
- 3. The emergence of mesometeorology and radar in the 1950s
- 4. The rise of radar meteorology
- 5. The 1960s–early 80s: The beginning of the satellite era
- 6. The 1970s: The far-reaching impact of GATE
- 7. Precipitation in MCSs: The universality of the convective–stratiform paradigm
- 8. Scales of air motions and thermodynamical processes within an MCS
- 9. Wind shear in the environment in relation to the structure of MCSs
- 10. Boundary layer and cold pools below MCSs
- 11. Elevated MCSs
- 12. Canonical life cycle of an MCS, modes of heating, and potential vorticity generation
- 13. Microphysics and the connection between convective and stratiform precipitation of MCSs
- 14. Modeling of individual MCSs
- 15. Dynamical interpretations
- 16. Relationship of MCSs to synoptic-scale and larger circulations
- 17. Global distribution of mesoscale convection: Variability and impacts on the global circulation
- 18. Representing MCS dynamics in global climate models
- 19. Current and future research on MCSs
- a. Initiation and upscale growth of convection to form MCSs
- b. Forms of MCSs over the globe
- c. MCSs and tropical cyclone genesis
- d. Extreme precipitation and flooding and societal impacts
- e. Scale interaction and parameterization in global models
- f. Aerosol, global warming, and MCSs in a changing climate
- 20. Conclusions: The characteristics and importance of MCSs
- Acknowledgments
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Fig . 17-1.(a) Surface wind and squall line, and (b) cloud outline and circulation in a vertical plane in a West African “disturbance line.” From Hamilton and Archbold (1945); © Royal Meteorological Society.
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Fig . 17-2.Time cross section through squall line and cold front, Wilmington, OH, 0730–1135 eastern standard time (EST) 29 May 1947. Heavy lines show boundaries of squall-front and polar-front layers; heavy dotted lines show boundaries of subsidence inversion. Light solid lines show isotherms (0°C); light dashed lines show isolines of mixing ratio (g kg−1). Below the cross section is the time of radiosonde observation before or after squall-line passage; distance scale is in miles. From Newton (1950).
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Fig . 17-3.Schematic section through a squall line. Adapted from Fujita (1955). © 1955 Tetsuya Fujita. Published by Taylor and Francis Group LLC. CC BY 4.0.
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Fig . 17-4.Schematic structure of surface precipitation features seen in early meteorological radar data. Adapted from Ligda (1956). Reprinted with permission of OSTIV.
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Fig . 17-5.Examples of radar data from the rain areas of midlatitude MCSs. Low elevation reflectivity patterns from the National Severe Storms Laboratory radar located at Norman (NOR), OK, are indicated by shading levels corresponding to 20–24 dBZ (light gray), 25–34 dBZ (dark gray), 35–44 dBZ (black), 45–54 dBZ (white), 55–64 dBZ (light gray), and >65 dBZ (dark gray). Range rings are at 20, 200, and 240 km. Registration marks on outermost ring are at 90-azimuth intervals (north toward top of figure). From Houze et al. (1990).
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Fig . 17-6.Infrared image showing temperature ranges corresponding to the various gray shades. From Maddox (1980).
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Fig . 17-7.Schematic cross section through a squall-line system observed over the eastern tropical Atlantic Ocean. Streamlines show flow relative to squall line. Thin dashed streamlines show convective updraft circulation. Thin solid streamlines show convective-scale downdraft circulation associated with mature squall-line element, and wide arrows show mesoscale downdraft below the base of the anvil cloud. Wide, dashed arrows show mesoscale ascent in the anvil. Dark shading shows strong radar echo in the melting band and in the heavy precipitation zone of the mature squall-line element. Light shading shows weaker radar echoes. Scalloped line indicates visible cloud boundaries. Adapted from Houze (1977) by Houze and Betts (1981).
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Fig . 17-8.Total rain integrated over the convective (circled points) and stratiform regions of a squall-line MCS located over the eastern tropical Atlantic Ocean. The data were obtained by three shipborne radars. The three types of symbols indicate different methods used for combining the information from the three radars. From Houze (1977).
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Fig . 17-9.Stratiform rain fraction obtained from TRMM precipitation radar data. From Schumacher and Houze (2003).
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Fig . 17-10.Conceptual model of a tropical oceanic squall line with trailing-stratiform precipitation. All flow is relative to the squall line, which was moving from right to left. Numbers in ellipses are typical values of equivalent potential temperature (K). Adapted from Zipser (1977).
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Fig . 17-11.Airflow pattern inferred by multiple-Doppler radar synthesis in the convective region of a tropical squall-line system observed by dual-Doppler radar in Ivory Coast, West Africa, on 23 Jun 1981. System is moving from right to left. Vertical arrow indicates scale of airflow vectors. Horizontal arrow C shows velocity of individual convective cells. Airflow vectors are computed relative to the cells. Contours show radar reflectivity (dBZ). From Roux (1988).
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Fig . 17-12.Conceptual model of the kinematic, microphysical, and radar echo structure of a convective line with trailing-stratiform precipitation viewed in a vertical cross section oriented perpendicular to the convective line (and generally parallel to its motion). Medium and dark shading indicate intermediate and strong radar reflectivities. Adapted from Houze et al. (1989).
