Temperature vertical profile

Figure 7-2 shows the vertical profiles of temperature, dew point, light scattering (a measure of aerosol concentration) and the concentrations of O3 and SO2. Here we see that up to about 1.5 km, the temperature, dew point, light scattering... 

Fig. 7-2 Vertical profiles of physical (temperature, dew point, and backscatter coefficient) and chemical (ozone, sulfur dioxide) variables near Scranton, PA during the afternoon of 20 July 1978. (Modified with permission from P. K. Mueller and G. M. Hidy (1982). "The Sulfate Regional Documentation of SURE Sampling Sites", EPRI report EA-1901, v. 3, Electric Power Research Institute.)...

Figure 2. Vertical profiles of temperature, nitrate, pigments, and activity ratios in the eastern...

Model results in seawater are in good agreement with observational data of PFOA. Most differences can be attpageributed to deficiencies of the emission scenario. Despite this fact, the difference between model results and observational data are due to the limited horizontal and process resolution and the fact that the physical parameters of the model (temperature, surface pressure, vorticity or divergence of the wind velocity field) were not relaxed to observational data. Regarding these limitations, in particular individual vertical profiles compare quite well with observations. This study underlines the importance of the ocean as a transport medium of PFOA. The contribution of volatile precursor substances to long-range transport needs to be assessed. 

The O2 content of the surface waters is lower at mid-latitudes because of higher temperatures, which lead to lower gas solubility. As shown in Figure 10.1a, the ther-mocline is characterized by a concentration minimum that increases in intensity from the Atlantic to the North Pacific. Note that the O2 minimum is less pronounced in the vertical profile from 45°S as compared to 9°N in the Atlantic Ocean because of close proximity to the site of AABW formation. Mid-water phosphate and nitrate maxima... 

Vertical profiles of O2 and particulate and dissolved trace metal concentrations at 32.5°E and 44.5°N in the Black Sea. (a) Temperature, salinity, fluorescence, and O2 (b) ammonium, silica, nitrate+nitrite, and phosphate (c) Fe (d) Mn (e) Co (f) Pb (g) Cu (h) Zn (I) Cd and Ni. In the trace metal profiles, the dissolved concentrations are represented as solid circles, the total particulate concentrations by open circles, the acid-leachable particulate concentrations by open squares, and the suspended particulate matter concentrations by the solid triangles. Source-. After Tankere, S. P. C., et al. (2001). Continental Shelf Research, 21, 1501-1532. 

Figure 23.7 Vertical profiles of water temperature (dotted line) and of measured (circles) and calculated (solid line) PCE concentration in Greifensee (Switzerland) for the period May to October 1985. Numbers give PCE inventory in moles (M = measured, C = calculated). From the model calculation it can be concluded that between May 6 and July 1, 1985, about 360 moles of PCE entered the lake, thus leading to a significant increase of the concentration in the lake during several months. After July 1, the input was virtually zero.

We measured H202 vertical profiles in Lake Erie (14, 18) and noted the similarity with oceanic profiles (23, 24). The major difference is the depth to which H202 is mixed in oceanic environments. To emphasize the effect of solar radiation and wind speed on the distribution of H202 in the epilimnion, we measured four vertical profiles of H202 concentration and temperature in Jacks Lake on 4 days, September 11-14, 1990, all at 4 00 p.m. 

The monthly mean ozone from the Dobson time series (1957-1986) of Vigna di Valle (50 km apart from Rome) and from TOMS (Total Ozone Mapping Spectrometer) satellite data (1979-1991) version 6 are assumed as climatological frames of reference for Rome and Ispra, respectively. Aerosol optical depths at 550 nm are estimated by means of sunphotometry. Data from the two meteorological stations of Rome and Milan airports are used to describe the atmospheric conditions. Standard vertical profiles of pressure, temperature, relative humidity and ozone density are selected. 

Figure 2. Schematic vertical profiles (a) h (dashed) and h (solid) and (b) q (dashed) and q (solid), (c) The temperature profile, corresponding to cpT = h — gZ — Lyq, illustrates die constant lapse rate within the boundary layer and the reduced lapse rate above the boundary layer. The boundary level (1 km) is indicated by die horizontal dashed line in each panel. These profiles illustrate typical climatic values that are determined by moist convective adjustment in the free atmosphere and dry adiabatic convection in the boundary layer. [Used by permission of Geological Society of America, from Forest et al. (1999), Geol. Soc. Am. Bull., Vol. Ill, Fig. 2, p. 500.]...

The surface distribution for mean annual h results from two properties of atmospheric flow conservation of h following the large-scale flow and the maintenance of the vertical profile of h by convective processes. These features of the climate system allow one to quantify the expected errors for assuming that mean annual h is invariant with longitude and altitude for the present-day distribution. Forest et al. (1999) examined the distribution and calculated the expected error from assuming zonal invariance to be 4.5 kJ/kg for the mean annual climate. This error translates to an altitude error of 460 m and is compared with an equivalent error of 540 m from the mean annual temperature approach. Moreover, the uncertainty of the terrestrial lapse rate, y(, increases the expected error in elevation as elevations increase, particularly when small lapse rates are assumed. 

Analysis of the data on temperature measured in boreholes made an important contribution ito ideas about SAT changes in the past. For instance, Bodri and Cermak (1999) noted that if the amplitude of long-term SAT variations during transitions from glaciations to interglacial periods had reached 10K-15K in the Holocene (the last 10,000-14,000 years), changes of several °K would have taken place on time scales from decades to centuries. In this connection, analysis has been made of the data on the vertical profiles of temperature measured at different depths in boreholes, and maps have been drawn of SAT changes over the Czech Republic, which took place between 1100 bc to 1300 bc (small climatic optimum), between 1400 and 1500, and between 1600 and 1700 (main phases of the Little Ice Age). 

Calculations of RF due to the growth in tropospheric ozone concentration gave a value of 0.4 0.15 Wm 2. A decrease in total content of ozone in the stratosphere could lead to RF equal to 0.2 0.1Wm"2. Though these changes in sign mutually cancel each other out to a great extent, this does not imply that they are insignificant, since variations of the ozone content in the troposphere and stratosphere aflect substantially—but diflerently—the formation of the temperature vertical profile. 

The AGDISP and FSCBG models accept the following meteorological data vertical wind speed and direction, temperature profile, relative wind speed, turbulence, depth of mixing layer, vertical profile of wind speed, vertical profile of wind direction, effect of canopy, and effect of complex terrain. 

Figure 4. North basin vertical profiles for temperature, D. O., and SO42 on September 19,1986.

Fig. 3 Vertical profiles of the water potential temperature (T , degrees Celsius), water salinity (S, practical salinity unit), and water specific potential density (or , kgm-3) a in upper layer of the Black Sea central area in August 1995 and b in deep layer (mean values based on high vertical resolution CTD measurements). 1 Upper mixed layer, 2 seasonal pycnocline (thermocline), 3 cool intermediate layer, 4 main pycnocline (halocline), 5 deep pycnocline, 6 bottom mixed layer...

Consideration of the thermohaline structure of the Black Sea provides new results on the statistical and physical analysis of the historical data of ship-borne observations of the vertical profiles of the temperature and salinity of the waters. The general features of the vertical thermohaline structure of the Black Sea waters, the seasonal and interannual variabilities of the horizontal structure of the temperature and salinity in all the main water layers are described. The relations of the large-scale features of the hydrology of the Black Sea waters to external forcing (heat and moisture fluxes across the water surface, river mouths and straits, fluxes of the momentum and relative vorticity of wind) are shown. The generalization of the results of the studies of the T,S-structure of the Black Sea waters and of its seasonal and interannual variability allows the following conclusions to be made. 

Fig. 2 Vertical profiles of temperature, salinity, density, dissolved oxygen and nitrate in the northern Arabian Sea during the northeast monsoon (SS161)...

Figure 1 Vertical structure of the atmosphere. The vertical profile of temperature can be used to define the different atmospheric layers...

Figure 14.4 Comparison of vertical profiles of (A) temperature, (B) salinity, (C) silicate, (D) nitrate and (E) phosphate in the upper 200 m at one site each in the Arabian Sea (19.17°N, 67.17°E US JGOFS Cruise TN043 sampling date 13/01/1995) and the Bay of Bengal (19.11 °N, 92.65° E WOCE Leg 109N sampling date 24/02/1995).

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