Studies on radioactivity in aerosols as a function of meteorological variables in Salamanca (Spain)

Po-210 and Pb-210 as atmospheric tracers and global atmospheric Pb-210 fallout: a Review

“…Based on 30-year (1967e1996) long series of daily 210 Pb measurements in Finland, Paatero et al (1998) observed that daily variations are due to synoptic-scale weather situations while the seasonal variations are attributed to the efficiency of vertical mixing of the lower atmosphere. However, there are sites where higher 210 Pb in the summer months have also been reported (e.g., in Spain, Garcia-Talavera et al, 2001;Azahra et al, 2004a;Dueñas et al, 2005Dueñas et al, , 2009). …”

Characteristics of the atmospheric electric field and correlation with CO2 at a rural site in southern Balkans

“…From an atmospheric pollution perspective, the boundary layer height (BLH) is the main driver of the aerosol concentrations close to the ground. This occurs because at Mediterranean sites at the same latitude as our site, the BLH during summertime can be at times even 10 times greater than that during winter owing to the decreased convection during winter (e.g., Georgoulias et al 2009). The large amounts of Aitkin nuclei very effectively reduce the concentration of small ions that dominate the electrical conductivity of air, which leads to reduced local conductivity and subsequently to PG maximization.…”

Analysis of temperature influences on the amplitude–frequency characteristics of Rn gas concentration

“…where F 1 is the function of Rn emanation from the soil (including the influence of external temperature) (Gaso et al, 1994;Hoyos et al, 1998;Iakovleva and Ryzhakova, 2003;Li et al, 1992;Przylibski, 1999;Stranden et al, 1984;Zmazek et al, 2005); F 2 is the daily variation of Rn due to vertical warm convection arising shortly after sunrise (Mishel, 1987); F 3 is the variation of Rn due to rain and Rn dissolved in underground water (Mishel, 1987;Provost et al, 2004;Richon et al, 2005); F 4 is the variation of Rn due to fluctuations in atmospheric pressure (Clements and Wilkening, 1974;Dowell et al, 1991;Hoyos et al, 1998;Garavaglia et al, 1999;Iakovleva and Ryzhakova, 2003;Washington and Rose, 1990;Zimmer and Erzinger, 2003); F 5 is the variation of Rn due to air movement (direction and speed of wind or ventilation) (Dueñas et al, 1999;Garcia-Talavera et al, 2001;Lee and Yu, 2000;Scott, 1992); F 6 is the variation of Rn related to deep geodynamics, especially that arising near earthquake epicenters (Atkinson, 1981;Bolt, 1993;Maeda and Yoshida, 1990); F 7 is the variation of Rn due to strong geomagnetic storms in periods of solar chromo spherical bursts (Semi-Zade, 1978, 1992; F 8 is the variation of Rn, caused by the settling of aerosols following dust storms, which can transfer a number of radioactive elements (Ganor et al, 1991;Mamane et al, 1980) and may lead to a sharp increase of radon.…”

“…In spite of many attempts to understand Rn anomalies, connected with geodynamic processes and earthquakes (Garavaglia et al, 1999;Garcia-Talavera et al, 2001;Hartmann and Levy, 2005;Hauksson and Goddard, 1981;Perrier et al, 2004;Planinic et al, 2001Planinic et al, , 2004Khan, 1993;Mogro-Campero and Fleischer, 1977;Segovia et al, 1995;Singh et al, 1999;Tsvetkova et al, 2001;Virk and Sing, 1993;Wakita, 1996;Zmazek et al, 2003Zmazek et al, , 2005, few have succeeded. This is due to the unclear nature of the anomalous Rn gas, and the weakly developed methodology of identification of Rn anomalies, induced by geodynamic and other unrelated factors.…”