Uptake of carbon monoxide by C3H mice following X irradiation of lung only or total-body irradiation with 60Co

D. S. Rappaport, Dennis E Niewoehner, T. H. Kim, C. W. Song, S. H. Levitt

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Abstract

Carbon monoxide uptake (V̇Co) and ventilation rate (VR) of C3H mice were determined at 14 weeks following either X irradiation of lungs only or total-body irradiation with 60Co at different dose rates. Following localized X irradiation of lung 97 cGy/min there was a reduction in V̇Co, which was inversely related to radiation dose, with a small reduction below control levels being detected at 7 Gy, the lowest dose tested. An increase in VT could be detected only at doses of 11 Gy, or more. Another group of animals received 11.5 Gy total-body irradiation at either 26.2 or 4.85 cGy/min followed by transplantation with syngeneic bone marrow. Following total-body irradiation, V̇Co was significantly reduced by about 37% at the highest dose rate and 23% at the lowest dose rate. In contrast, a trend toward elevated VR was detected only at the higher dose rate. The results indicate that V̇Co is a sensitive indicator of radiation-induced lung injury and that under the experimental conditions used V̇Co is a more sensitive indicator of radiation-induced lung injury in C3H mice than VR.

Original languageEnglish (US)
Pages (from-to)254-261
Number of pages8
JournalRadiation research
Volume93
Issue number2
DOIs
StatePublished - 1983

Bibliographical note

Funding Information:
A series of MCSs occurred daily over the Qinghai-Xizang Plateau during 25-28 July 1995. In this study, their physical characteristics and evolutions based on infrared satellite imagery, their largescale meteorological conditions, and CAPEs are analyzed. The main conclusions are summarized as follows. (1) These MCSs took place as a phenomenon of clustering MCSs under stable large-scale environmental conditions with the 200 hPa anticyclonic High and a 500 hPa warm and moist area over the plateau. There was a similar diurnal cycle in all these MCSs, whose initial convective activities became active at noon LST by solar heating, and then built up rapidly into a MCS, which formed and reached its peak in the early evening hours around 1800 LST and then abated gradually. That is, the upper-level anticyclonic high, the lower-level thermal forcing, and a diurnal cycle were something in common in all these MCSs. (2) Among them, the strongest were the MCSs on 26 and 28 July. However, they had different features and development mechanism. In the developing stage, on the Tb maps, the MCS on 26 July had quite a few meso-fl scale convective systems in its southwestern upstream, but the MCS on 28 July had just a few, but massive meso-~ scale convective systems in its central part; moreover, in the evolution there was a sharp growth and a gradual decrease for the MCS on 26 July, but a relatively slow further growth and a relatively rapid decrease for the MCS on 28 July. The MCS on 26 July was formed within the warm area with the strongest lower-level thermal forcing over the central plateau, but the MCS on 28 July was formed in the zone with dense isotherms. The MCS on 26 July was mainly associated with the relatively pure thermal effects peculiar to the Qinghai-Xizang Plateau, such as the great upper-level anticyclonic high and the strong lower-level thermal forcing, and was affected little by the westerlies. On the other hand, the MCS over the plateau on 28 July was influenced much by the westerlies, such as the westerly trough and its baroclinic zone. And, being correlative with all these aspects, CAPE, which is dependent on the vertical gradient of temperature and humidity, was the very important energy supply for the development of the MCS on 26 July, but not for the MCS on 28 July. Because the MCS on 28 July developed in the zone with dense isotherms associated with the westerly trough, its important energy supply was the available potential energy (APE) which is dependent on the horizontM gradient of temperature and is released through a quasi-geostrophic process. Acknowledgments. This work was supported by the Chinese National Climbing Project "The Tibetan Plateau Meteorological Experiment" and in part by the National Natural Science Foundation of China under Grant No. 49675296.

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