Atmospheric data altitude, 718

Beyer (B8) has recently reported experimental data obtained in small test motors under atmospheric and altitude conditions. At atmospheric pressure, his results showed the observed ignition delay to be a function of the delivery rate, as shown in Fig. 10. Additional data obtained in small test motors by Fullman and Nielsen (F6) are shown for comparison. These latter investigators conducted studies on the effects of various injectors, with delivery from both the head end and the aft end. Their results indicate that the hollow-cone injector is the most efficient. This subject has been treated in more detail by Miller (M7). 

Figure Bl.4.3. (a) A schematic illustration of the THz emission spectrum of a dense molecular cloud core at 30 K and the atmospheric transmission from ground and airborne altitudes (adapted, with pennission, from [17]). (b) The results of 345 GHz molecular line surveys of tlu-ee cores in the W3 molecular cloud the graphics at left depict tire evolutionary state of the dense cores inferred from the molecular line data [21],...

A-6 Altitude and Atmospheric Pressures, 578 A-7 Vapor Pressure Curves, 579 A-8 Pressure Conversion Chart, 580 A-9 Vacuum Conversion, 581 A-10 Decimal and Millimeter Equivalents of Fractions, 582 A-11 Particle Size Measurement, 582 . A-12 Viscosity Conversions, 583 A-13 Viscosity Conversion, 584 A-14 Commercial Wrought Steel Pipe Data, 585 A-15 ... 

Troposphere is used here to represent the lowest layer of the atmosphere, ranging from the ground to the base of the stratosphere at 10—15 km altitude. Essentially, all data on particulate organic matter is from near ground level in the lower troposphere. 

The transition zones between the various regions of the atmosphere are known as the tropopause, stratopause, and mesopause, respectively. Their locations, of course, are not fixed, but vary with latitude, season, and year. Thus Fig. 1.1 represents an average profile for mid-latitudes. Specific temperatures, pressures, densities, winds, and the concentrations of some atmospheric constituents as a function of altitude, geographic position, and time are incorporated into a NASA model, the Global. Reference Atmosphere Model (GRAM) information on obtaining this model and data is included in Appendix IV. 

Gierczak et al. (1998) have also measured the temperature dependence for the absorption cross sections in addition to the quantum yields as a function of pressure and temperature. They have used these data, combined with the kinetics of the OH-acetone reaction, which is the other major removal process, to calculate the contributions of the OH reactions and of photolysis to the loss of acetone in the atmosphere as a function of altitude. Figure 4.31 shows that photolysis is a significant, but not the major, contributor at the... 

Indeed, Wallace and Hunten118 show that such a production mechanism would fit their intensity-altitude data for the atmospheric band in the dayglow. 

Measurements either from the ground or from satellites have been a major contribution to this effort, and satellite instruments such as LIMS (Limb Infrared Monitor of the Stratosphere) on the Nimbus 7 satellite (I) in 1979 and ATMOS (Atmospheric Trace Molecular Spectroscopy instrument), a Fourier transform infrared spectrometer aboard Spacelab 3 (2) in 1987, have produced valuable data sets that still challenge our models. But these remote techniques are not always adequate for resolving photochemistry on the small scale, particularly in the lower stratosphere. In some cases, the altitude resolution provided by remote techniques has been insufficient to provide unambiguous concentrations of trace gas species at specific altitudes. Insufficient altitude resolution is a handicap particularly for those trace species with large gradients in either altitude or latitude. Often only the most abundant species can be measured. Many of the reactive trace gases, the key species in most chemical transformations, have small abundances that are difficult to detect accurately from remote platforms. 

A large number of observations, both remote and in situ, confirm this qualitative picture of the loss of ozone over Antarctica. The in situ data have come from instruments carried on small balloons and the NASA ER-2 high-altitude aircraft. Small-balloon measurements are of particle distributions and sizes, ozone, and water vapor (23, 33). ER-2 measurements, listed in Table I, are of particle size and composition atmospheric parameters such as temperature, pressure, lapse rate, and winds and trace gas abundances of 03, N20, NOy or NO, CIO and BrO, and stable gases, including CH4, chlorofluorocarbons, halons, and others (34-45). 

We thank J. M. Rodriguez and Atmospheric and Environmental Research, Inc., for providing the altitude distributions of trace gases and ozone reaction rates and K. R. Chan, D. W. Fahey, M. H. Proffitt, and L. E. Heidt for providing data prior to publication. We are also thankful for helpful discussions and encouragement from C. R. Webster and for help with publication from P. S. Stevens and D. W. Toohey. 

The model year 2015 was chosen to illustrate the impact of future aircraft activity, in particular the supersonic aircraft. As in the case discussed in Section 2.1, the background atmosphere is based on the scenario of IPCC-IS92a. For aircraft emission, data of NO, and water vapor are taken from Baughcum and Henderson (1998). For the projected fleet of 500 supersonic aircraft, different emission indices for NO, and cruising altitudes were assumed (see Table 4). 

Since 1992 the two Italian stations of Rome, urban site (latitude 41.9° N, longitude 12.5° E, altitude 60 m), and Ispra, semi-rural site (latitude 45.8° N, longitude 8.6° E, altitude 240 m), collect regular continuous measurements of spectral UV (290-325 nm) irradiance by means of Brewer Spectrophotometry. The measured data are compared with the output of the STAR model (System for Transfer of Atmospheric Radiation) [1], STAR is a multiple scattering radiative transfer model which considers all atmospheric factors modulating UV radiation at ground (ozone, aerosol, clouds, pollutants, albedo, pressure, temperature, humidity) [2], The model involves combination of a radiative transfer code, an initialisation procedure and an integration scheme. 

Fossil floras provide one of the most useful sources for obtaining data that can be used to estimate paleoelevation. The distribution of modern forests is clearly delineated largely in accordance with climate, which varies with both altitude and latitude. The correlation of modern vegetation with mean temperature parameters provides the basis for comparing Cenozoic fossil floras with the thermal distribution of these modern forest types to infer paleotemperatures. Such information is a valuable source for inferring climate fluctuations through time, and in combination with thermodynamic properties of the atmosphere, it also can be used to estimate paleoelevation. 

Our data obtained from both the ship cruise (Table II) and the flight measurements (Figure 3) suggest that photooxidation of DMS in the Southern Ocean atmosphere leads to a higher yield of MSA and a lower yield of SO2 compared to other world ocean areas. We conclude that these yields are possibly a function of latitude and altitude and, basically, of temperature as suggested by the recent laboratory studies of Hynes et al. (21). 

Fig. 1. The neutral composition of the Earth s atmosphere as a function of altitude. The sources of the altitudinal profile data are H, He, O, N2, 02, Ar, Ref.6) O3, Ref.7) H20, Refs. ) and10) NO, Refs.9) and 10) O 1 Ag), Ref.11) O below 90 km, Ref.12) CF2C12 and CFCI3, Ref.13) N20, Ref.14) H202, NO3 and N205, from model calculations given in Ref.ls) C02 is assumed to have a constant mixing ratio of 300 p.p.m. Clearly many other minority species are present in the lower atmosphere (e.g. OH, H02 see Ref.15)) but these have been omitted for clarity.

The accumulated mutual neutralization data from the FA experiments together with that available for the ternary recombination process, indicates that binary mutual neutralization is the dominant ionic recombination process above about 30 km in the atmosphere whereas below this altitude the ternary process becomes dominant210. It should be stressed that this generalization is based on dubious ternary recombination data and indeed on mutual neutralization data for moderate-sized clusters only. 

In an experiment done at the high altitudes of the Andes, the data obtained was 3.15 liters of a mystery gas at a temperature of 18°C and a pressure of 0.75 atmosphere. What is its volume at sea level with a pressure of 1.0 atmosphere and a temperature of 22°C ... 

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