Deep convection

There is a zonal atmospheric circulation system associated with this normal ocean condition called the Walker Cell (Eig. 10-7). Evaporation rates are high over the warm pool and warm moist air ascends to great heights (deep convection) producing extensive cloud systems and rain. The Walker Cell is closed by westerly winds aloft and subsidence in the high-pressure zone of the eastern Pacific. 

Pickering, K. E., A. M. Thompson, J. R. Scala, W.-K. Tao, R. R. Dickerson, and J. Simpson, Free Tropospheric Ozone Production Following Entrainment of Urban Plumes into Deep Convection, J. Geophys. Res., 97, 17985-18000 (1992). 

Wang, C P. J. Crutzen, V. Ramanathan, and S. F. Williams, The Role of a Deep Convective Storm over the Tropical Pacific Ocean in the Redistribution of Atmospheric Chemical Species, J. Geophys. Res., 100, 11509-11516 (1995). 

Waliser, D. E., N. E. Graham, and C. J. Gautier, Comparison of the Highly Reflective Cloud and Outgoing Longwave Radiation Datasets for Use in Estimating Tropical Deep Convection, J. Clim., 6, 331-353 (1993). 

Wallace, J. M., Effect of Deep Convection on the Regulation of Tropical Sea Surface Temperature, Nature, 357, 230-231 (1992). 

Opposite to the downward transport of 03s, upward transport of 03t from the troposphere into the stratosphere takes place. This maximizes in summer when deep convective mixing is strongest, concurrent with the maximum photochemical activity. After transport, 03t is chemically destroyed in the stratosphere. We note that reversible cross-tropopause transports of 03s and 03t are not included in the budgets, so Figure 3a and Table 2 represent net mass fluxes. 

Itis ofinterestthatLi is easily destroyed by (p, alpha) reactions atT = 2.5 MK or greater, so that when newly born stars arrive on the Main Sequence, they have already destroyed Li throughout most of their interiors by these nuclear interactions in the deep convection of the pre-Main-Sequence evolution. The observed Li has survived only in the outermost few percent by mass of the interior of the stars. 

A. Stickler, et ah. Influence of summertime deep convection on formaldehyde in the middle and upper troposphere over Europe, /. Geophys. Res.-Atmos. Ill (D14) (2006) D14308. 

The physics package consists of a comprehensive set of physical parametrization schemes (Benoit et al. 1989). Specifically, the atmospheric boundary layer (ABE) is based on a prognostic equation for TKE. The surface temperature over land surface is calculated using the force-restore method combined with a stratified surface layer. Deep convective processes are handled by a Kuo-type convective parametrization (Kuo 1974) for the resolutions that we have adopted for this study. 

Lurmann EW, Lloyd AC, Atkinson R (1986) A chemical mechanism for use in long-range transport/acid deposition computer modelling. J Geophys Res 91 10905-10936 Marcal V, Rivire ED, Held G, Cautenet S, Freitas S (2006) Modelling study of the impact of deep convection on the UTLS air composition - Part I analysis of ozone precursors. Atmos Chem Phys 6 1567-1584... 

Because we are focussed on air pollution problems, high-impact weather is rarely of concern so, its simplified approach to deep convection, absence of a stratosphere (maximum altitude is 8 km), and its explicit but simplified rain processes, are not significant... 

Figure 17.5 also shows the track of flight 10 during PEACE-B on 14 May 2002. A mid-latitude cyclone was located over central China on 13 May. Warm and moist southerly winds in the lower troposphere intensified ahead of this surface cyclone over southern China, converging into a fi ont extending between 20°N, 100°E and 30°N, 115°E. Deep convective clouds, with tops above 10 km around 30°N, 105-120°E, are found in an infrared (IR) image obtained by the Geostationary... 

Diurnal deep convection resulting from surface warming, which is most prevalent in central Amazonia. 

Deep convection in northern Amazonia related to the ITCZ-like convection and moisture transported from the Atlantic. This depends on the meridional SST gradient of the tropical North Atlantic. 

Marengo, J. 1995b. "Interannual variability of deep convection in the tropical South American sector as deduced from ISCCP C2 data." International Journal of Climatology 15 995-1010. 

Lightning formation of NO is most important in areas of deep convective activities such as occurring in tropical continental regions. 

Anthropogenic contamination reaches the ocean bottom in the northern part of the North Atlantic because of the deep convection of the North Atlantic Deep Water. Further south in the basin the contamination reaches to depths of 2000 m. The depth at which the profiles reach half their surface maximum is between 600 and 1000 m. Note that this depth is not greatly different from the value of 800 m estimated in Fig. 11.6 for the depth of ocean equilibrium required to accommodate about half of the fossil fuel released to the atmosphere. It has been shown with global circulation models that a present-day flux of 2.2 Pg y into the ocean is required to accommodate the inventory of GO2 indicated in Fig. 11.7 (Table 11.3). 

Figure 19,4 shows a simulated time series of vertical temperature profiles in comparison with measurements. The k-profile scheme generates a realistic seasonal thermocline cycle with winter water encapsulation below the thermocline. The important role of deep convection for the formation of winter water is obvious. Nevertheless, the thermocline... 

A summary of H2S observations over the period from 2002 to 2007 is given in Table 5. It can be seen that the H2S concentration is highly variable at the interannual scale, spanning from zero or nearly zero to at least 80 mg 1. Equally variable is the depth of the sulfide layer, which was as deep as 35 m in October, 2006, but as shallow as 15 m in September, 2005. In 2004, following deep convection during the winter 2003-2(X)4 [2], there were no H2S present at all. 

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