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Stratospheric ozone (O3) plays a critical role in the atmosphere due to its capacity to absorb biologically harmful solar UV radiation before it reaches the Earth¡¯s surface. Nitrogen dioxide (NO2) is a key trace gas in the ozone photochemical. The remote sensing of NO2 and other atmospheric minority gases is essential in order to understand the stratospheric O3 destruction and formation processes. A study carried out on the seasonal variation of the O3 and NO2 vertical column densities (VCDs) using a zenith©\sky DOAS (Differential Optical Absorption Spectroscopy) is presented. This system is composed of a spectral analyzer (portable mini©\spectrometer HR4000, Ocean Optics), two optical fibers (400 ¦Ì of core, 25 cm and 6 m of longitude) and an automatic mechanical shutter. NO23) plays a critical role in the atmosphere due to its capacity to absorb biologically harmful solar UV radiation before it reaches the Earth¡¯s surface. Nitrogen dioxide (NO2) is a key trace gas in the ozone photochemical. The remote sensing of NO2 and other atmospheric minority gases is essential in order to understand the stratospheric O3 destruction and formation processes. A study carried out on the seasonal variation of the O3 and NO2 vertical column densities (VCDs) using a zenith©\sky DOAS (Differential Optical Absorption Spectroscopy) is presented. This system is composed of a spectral analyzer (portable mini©\spectrometer HR4000, Ocean Optics), two optical fibers (400 ¦Ì of core, 25 cm and 6 m of longitude) and an automatic mechanical shutter. NO22) is a key trace gas in the ozone photochemical. The remote sensing of NO2 and other atmospheric minority gases is essential in order to understand the stratospheric O3 destruction and formation processes. A study carried out on the seasonal variation of the O3 and NO2 vertical column densities (VCDs) using a zenith©\sky DOAS (Differential Optical Absorption Spectroscopy) is presented. This system is composed of a spectral analyzer (portable mini©\spectrometer HR4000, Ocean Optics), two optical fibers (400 ¦Ì of core, 25 cm and 6 m of longitude) and an automatic mechanical shutter. NO22 and other atmospheric minority gases is essential in order to understand the stratospheric O3 destruction and formation processes. A study carried out on the seasonal variation of the O3 and NO2 vertical column densities (VCDs) using a zenith©\sky DOAS (Differential Optical Absorption Spectroscopy) is presented. This system is composed of a spectral analyzer (portable mini©\spectrometer HR4000, Ocean Optics), two optical fibers (400 ¦Ì of core, 25 cm and 6 m of longitude) and an automatic mechanical shutter. NO23 destruction and formation processes. A study carried out on the seasonal variation of the O3 and NO2 vertical column densities (VCDs) using a zenith©\sky DOAS (Differential Optical Absorption Spectroscopy) is presented. This system is composed of a spectral analyzer (portable mini©\spectrometer HR4000, Ocean Optics), two optical fibers (400 ¦Ì of core, 25 cm and 6 m of longitude) and an automatic mechanical shutter. NO23 and NO2 vertical column densities (VCDs) using a zenith©\sky DOAS (Differential Optical Absorption Spectroscopy) is presented. This system is composed of a spectral analyzer (portable mini©\spectrometer HR4000, Ocean Optics), two optical fibers (400 ¦Ì of core, 25 cm and 6 m of longitude) and an automatic mechanical shutter. NO2Differential Optical Absorption Spectroscopy) is presented. This system is composed of a spectral analyzer (portable mini©\spectrometer HR4000, Ocean Optics), two optical fibers (400 ¦Ì of core, 25 cm and 6 m of longitude) and an automatic mechanical shutter. NO22 and O3 VCDs are derived from zenithal solar spectra acquired during twilights (zenithal angles between 87¡ãand 91¡ã. The data retrieved by our instrument are compared with those coming from the SAOZ spectrometer (Systeme d'Analyse par Observation Zenithale, Laboratoire Atmosph¨¨es, Milieux, Observations Spatiales (LATMOS), France). Both systems are located in Rio Gallegos, Santa Cruz province, Argentine (51¡ã6¡¯S; 69¡ã9¡¯W, 15 m asl), in the CEILAP©\RG remote sensing station. We observed that NO2 VCD ranging from 6¡Á015 molec/cm2 in summer to 1.6¡Á015 molec/cm2 in winter and early spring. An anticorrelation (shifting approximately 40 days) between NO2 and O3 VCDs was calculated. A good agreement (average relative difference about 13%) among O3 VCD measurements of both instruments was observed. In the case of NO2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.3 VCDs are derived from zenithal solar spectra acquired during twilights (zenithal angles between 87¡ãand 91¡ã. The data retrieved by our instrument are compared with those coming from the SAOZ spectrometer (Systeme d'Analyse par Observation Zenithale, Laboratoire Atmosph¨¨es, Milieux, Observations Spatiales (LATMOS), France). Both systems are located in Rio Gallegos, Santa Cruz province, Argentine (51¡ã6¡¯S; 69¡ã9¡¯W, 15 m asl), in the CEILAP©\RG remote sensing station. We observed that NO2 VCD ranging from 6¡Á015 molec/cm2 in summer to 1.6¡Á015 molec/cm2 in winter and early spring. An anticorrelation (shifting approximately 40 days) between NO2 and O3 VCDs was calculated. A good agreement (average relative difference about 13%) among O3 VCD measurements of both instruments was observed. In the case of NO2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.Systeme d'Analyse par Observation Zenithale, Laboratoire Atmosph¨¨es, Milieux, Observations Spatiales (LATMOS), France). Both systems are located in Rio Gallegos, Santa Cruz province, Argentine (51¡ã6¡¯S; 69¡ã9¡¯W, 15 m asl), in the CEILAP©\RG remote sensing station. We observed that NO2 VCD ranging from 6¡Á015 molec/cm2 in summer to 1.6¡Á015 molec/cm2 in winter and early spring. An anticorrelation (shifting approximately 40 days) between NO2 and O3 VCDs was calculated. A good agreement (average relative difference about 13%) among O3 VCD measurements of both instruments was observed. In the case of NO2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.S; 69¡ã9¡¯W, 15 m asl), in the CEILAP©\RG remote sensing station. We observed that NO2 VCD ranging from 6¡Á015 molec/cm2 in summer to 1.6¡Á015 molec/cm2 in winter and early spring. An anticorrelation (shifting approximately 40 days) between NO2 and O3 VCDs was calculated. A good agreement (average relative difference about 13%) among O3 VCD measurements of both instruments was observed. In the case of NO2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.2 VCD ranging from 6¡Á015 molec/cm2 in summer to 1.6¡Á015 molec/cm2 in winter and early spring. An anticorrelation (shifting approximately 40 days) between NO2 and O3 VCDs was calculated. A good agreement (average relative difference about 13%) among O3 VCD measurements of both instruments was observed. In the case of NO2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.2 and O3 VCDs was calculated. A good agreement (average relative difference about 13%) among O3 VCD measurements of both instruments was observed. In the case of NO2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.3 VCD measurements of both instruments was observed. In the case of NO2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.2, a better agreement among results at sunrise than at sunset between SAOZ and ERO©\DOAS data was determined.