Dual Comb Optimization of the Acid Catalyst Concentration for Synthesis of Anti‐Cancer Agent Gamavuton‐0 by Using Mathematical and Statistical Software
1. Introduction
Aerosols are liquid and solid particles that are suspended in the atmosphere. They are produced from natural and man‐made activities Seinfeld Pandis, . Their scattering properties depend on their size, chemical and optical characteristics. Aerosol growth takes place under conditions of increasing relative humidity R and changes the scattering properties considerably. The parameter used to quantify aerosol scattering properties with R is the scattering enhancement factor, f RH . t is defined as Corresponding author Tel.: + ‐ ‐ 8; fax: + ‐ ‐ 8 . E ‐mail address: nofelobservatory.ph 12 the ratio of the scattering coefficient at a particular R, RH , to the dry scattering coefficient: dry RH RH RH f 1 where RH dry denotes the scattering coefficients at a dry R. Different aerosols have different responses to increasing R. Previous studies have shown that the changes of f RH with R for sea salt is high compared to dust Zieger et al., , Pan et al., . n Chiba, seasonal changes of R exist and aerosols are composed of different types Fukagawa et al, . The objective of this work is to measure and produce a monthly model of f RH of aerosols in Chiba. Such a study of hygroscopic growth of particles in the real atmosphere is important from the viewpoints of the influence of aerosol on the radiation budget and understanding the onset of cloud formation in which aerosols work as the cloud condensation nuclei Seinfeld and Pandis, .2. Aerosols and RH characteristics in Chiba
The composition of aerosols in Chiba varies according to seasons Fukagawa et al, . Ammonium sulfate and elementary carbon, for example, are seen to have high concentrations during summer and winter, respectively. Sea salt also exhibits high concentrations during summer. Ground measurements of R in Chiba show that summer and winter months have the highest ~8 and lowest ~ mean R values, respectively. owever, the month of February can have R values that can reach up to in the early hours of the morning. These variations of R and aerosols provide a complex nature of the collective scattering properties of aerosols. Nevertheless, measurement of f RH from ground data collected over a year can offer the seasonal changes of the scattering properties of aerosols. Conventionally measurements of f RH have been achieved using two integrating nephelometers that measure scattering coefficients of ambient and then dry air Fierz‐ Schmidhauser et al., , Zieger et al., . n this work, we propose the determination of f RH through the monitoring of the ambient atmosphere by employing visibility, nephelometer and aethalometer data.3. Methodology
The Japan Meteorological Agency JMA measures the hourly visibility values at Chiba city’s District Office using a present weather detector” Vaisala PWD . The data are obtained from JMA’s website http:www.data.jma.go.jp . The visibility meter is located around . km south of Chiba University Figure a . Figure b and c show the image of the aerosol measurement unit aethalometer, nephelometer, particle counter located at CEReS, Chiba University, and that of the visibility meter, respectively. The visibility meter can measure a maximum visibility value of km. n the present analysis, visibility values less than km are used to generate the extinction coefficient at 8 nm. Values of ambient R are also obtained from JMA’s website. The extinction coefficient is extracted from the visibility data using where ext and V are the extinction coefficient and the measured visibility. The factor . is the logarithmic attenuation of of the original intensity, i.e., ln . . The absorption coefficients at seven wavelengths from to nm are measured using an aethalometer Magee AE . The absorption coefficient at 8 nm is interpolated from the linear fit of the logarithm of the absorption coefficient and the logarithm of the , 996 . 2 V ext 2 13 wavelength. The difference of the extinction and absorption coefficient gives the scattering coefficient. n a month, the scattering coefficient values at the same R are grouped and averaged. The dry scattering coefficient used in calculating for f RH is the average of the scattering coefficient for RH . The f RH values are fitted using a power law relationship of Figure 1. a Location of the visibility meter with respect to Chiba University; b Aerosol measurement unit, and c Vaisala Present Weather DetectorPWD22 http:www.vaisala.comenmaritimeproductsvisibilityPagesPWDPresentweather.aspx4. Results and discussion
Figure a and b show the measured and modeled dependence of f RH with R for the months of April and June . These are representative months when f RH shows different responses with R at high R. n April, f RH values do not change that much with increasing R compared to the behavior of f RH in June. This can be attributed to the type of aerosols present in the atmosphere during these months. Previous studies have shown that f RH increases sharply with R for sea salt but not that much with dust Zieger et al., . Also, increasing weight percentage of organics in ammonium sulfates tend to decrease f RH values Garland et al., . n April, aerosols in Chiba have lower sea salt component, high concentration of dust and organics. Asian dust is transported from China and passes over Japan. Local dust may also contribute to the low f RH due to relatively dry conditions. n the month of June, the aerosols in Chiba have a higher concentration of sea salt, with less concentration of dust and organics. This may explain the steeper f RH values at high R. Figure shows the trend of modeled f RH with R for the year . The month of February has higher f RH values with increasing R and this can be attributed to high R during early morning although the mean R of this month is low. This also the reason why f RH values start to increase significantly at around 8 R. The summer months also show higher f RH values at high R. This can be attributed to relatively high R during daytime and nighttime compared to the other months. owever, f RH values start to increase signifi‐cantly at R. This may be attributed to the fact that, on the average, the aerosols in the atmosphere have significantly increa‐sed in size at a particular R compared to the size of the aerosols at the same R for different months. Thus, any increase in size contributes to a small increase in the scattering coefficient of these larger aerosols. b . 100 1 RH x ax RH f b 3 14 Figure 3. Modeled fRH values for the year 2014. Acknowledgement This work was supported by the CEReS Overseas Joint Research for FY . References Fierz‐Schmidhauser, P. et al. . Measurement of Relative umidity Dependent Light Scattering of Aerosols. Atmos. Meas. Tech., , ‐ . Copernicus Publications, Germany Fukagawa, S. et al. . Characterization of Seasonal Variation of Tropospheric Aerosols in Chiba, Japan. Atmos. Env., , ‐ 8. Elsevier Publications, The Netherlands. Garland, R.M. et al. . Parameterization for the Relative umidity Dependence of Light Extinction: Organic‐ammonium sulfate aerosol. J. Geophys. Res., , D . American Geophysical Union Publications, USA. Pan, X.L.. et al. . Observational Study of nfluence of Aerosol ygroscopic Growth on Scattering Coefficient over Rural area near Beijing Mega‐City. Atmos. Chem. Phys. , ‐ . C Copernicus Publications, Germany. Seinfeld, J.. Pandis, S.N. . Atmospheric Chemistry and Physics: From Air Pollution to Climate Change nd ed. , John Wiley Sons, USA. Zeiger, P. et al. . Effects of Relative umidity on Aerosol Light Scattering: Results from different European sites. Atmos. Chem. Phys., , ‐ . Copernicus Publications, Germany. Figure 2. a Measured and modeled fRH for the month of April 2014. The modeled fRH increases with RH according to Eq. 2 with a=4.455 and b=14.38. b Measured and modeled fRH for the month of June 2014. The modeled fRH sharply increases with RH according to Eq. 2 with a=16.88 and b=26.60.Parts
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