In this research paper we have evaluated the relation between surface Ozone (O 3), Sun Spot Number (SSN) and Carbon Monoxide (CO) over an American station “Tutuila” for the long period of 35 years (1980-2015). It was analyzed that CO and O 3 show an increasing trend over the maximum months of the year, whereas SSN shows decreasing trend throughout the year. We have concluded that, for O 3 the increasing trend is found to be maximum in the month of December, whereas surprisingly just a month before it i.e., in November, the value was negative. We also analyze here the CO data for the same period. It is observed that the CO increases from January to June. Its increment is found to be minimum in January month and maximum in the month of April. After it, the CO shows the decay trend from July to September, and then again increases from October to December months. NO 2 data of 11 years is also studied here and concluded that, the variation observed in March month is very small and is positive. In the same way, a positive trend is observed for NO 2 data in June month, but in rest all the months the value is negative.
The Earth’s atmosphere is split into 5 layers: troposphere, stratosphere, mesosphere, thermosphere, and exosphere (Perevedentsev et al., 2019). Many of the human activities are badly affecting the atmosphere (Lu et al., 2018), and the stratosphere layer is a matter of great concern which is harmful to human itself (Anwar et al., 2016). It has been observed from past studies that concentrations of ozone in the upper stratosphere have increased in the last 15 years (Rozema et al., 2005). Depletion of the ozone layer by chlorine and bromine species has been a major environmental issue (Sivasakthivel & Reddy, 2011). The ozone layer, which absorbs and scatters the solar UV radiations, lies in this region (Brenna et al., 2019). The ozone layer is a naturally occurring gas in the region of the stratosphere, where ozone particles are accumulated (Wargan, 2018). But the thickness of the ozone layer varies with altitude and seasonal change (Davis et al., 2017). Life is protected from UV rays by the stratospheric ozone layer, which acts as a shield or sunscreen (Park et al., 2020). Surface ozone is a highly efficient greenhouse gas; its global warming potential is about 1200-2000 times that of CO2. Ozone is produced in the troposphere by photochemical oxidation of CO (Minschwaner et al., 2010), CH4, and Non-Methane Volatile Organic Carbons (NMVOCs) in the presence of NOx (Minschwaner & Manney, 2015). Loss of ozone in troposphere takes place through chemical reactions and dry deposition. As an important greenhouse gas, O3 is making significant contributions to climate change. The concentration of photochemical oxidants can be decreased by controlling their precursors such as: nitrogen oxides NOx (NO and NO2) and Volatile Organic Compounds (VOCs) etc. (Ravishankara et al., 2009). Sunspots are areas that appear dark on the surface of the sun because of some temperature variation (Solanki, 2003). They are electrically charged gases that generate areas of powerful magnetic fields. These are regions of reduced surface temperature caused by concentrations of magnetic flux. Sunspots usually appear in pairs. The amount of solar activities changes with the stages in the solar cycle (Willett, 1962). Observational evidence for a relation between atmospheric total ozone amount and sunspot number (SSN) has been presented and debated for more than two decades (Angell, 1989).
Generally, ozone production depends on several factors such as temperature, solar activity, wind, speed, and direction (Fleming et al., 2020). This work represents the influence of solar activity. However, previous studies have shown that ozone formation totally depends on the activities taking place on sun such as sunspots, solar winds, etc., which can alter the concentration of ozone (Arsenovic et al., 2018). They affect human health and have an impact on climatic change. One of the various problems caused by air pollution in urban areas is photochemical oxidants. The formation of ground-level ozone depends on several factors like, the intensity of solar radiation, the concentrations of NOx and VOCs, and also on the ratio of NOx to VOCs (Qin et al., 2004). Variability of ground air temperature, wind speed and direction, relative humidity, and precipitation associated with climate change have the potential to affect the distribution and deposition of O3. Nitrogenous compounds emitted by humans in a small amount like NO, N2O and NO2 are considered to be most responsible for the depletion of the ozone layer (Zoran et al., 2020). Nitrous oxide is also a greenhouse gas, so reducing its emission from man-made sources would be good for both the ozone layer and climate. A study on Arctic and Antarctic ozone depletion has helped us in understanding ozone depletion more clearly (Solomon et al., 2014; Tilmes et al., 2005; Dameris et al., 2021; Bernhard et al., 2020). The main causes of ozone depletion are chlorofluorocarbons (CFCs), HCFCs and halons, apart from it CO and NOx also affect the stratospheric and tropospheric ozone, so here in the present study our main focus is only on the CO and NOx. Since the stratospheric ozone is formed by molecular ozone in the presence of solar UV radiation and hence solar activity i.e., the sunspot number, which represents how the sun is active, plays a major role. So, we have discussed the relation between ozone, sunspot number, NO2 and CO data. This paper explores the interactions between these gases and stratospheric ozone.
For the present study, we required sufficient long-term data for a station, so we choose an American station “Tutuila” (
we used surface ozone, which were collected at American station “Tutila” and this data is retrieved from https://www.esrl.noaa.gov/. The ESRL Global Monitoring Division has been measuring surface ozone at several global locations since 1973. Tutuila is the main and the largest island of American Samoa. It is the third-largest island in the Samoan Islands chain of the Central Pacific. It is located roughly 4000 kilometers northeast of Brisbane, Australia, and lies something over 1200 kilometers to the northeast of Fiji. The American Samoa Observatory (SMO) is located in the middle of the South Pacific, about midway between Hawaii and New Zealand and its coordinates are 14.295˚S, 170.70˚W. The observatory is situated on the northeastern tip of Tutuila Island, American Samoa, at Cape Matatula. The observatory was established in 1974 on a 26.7-acre site.
The CO data for the current study is downloaded from https://giovanni.gsfc.nasa.gov/. Giovanni is a tool that displays earth science data from NASA satellite directly on the internet. We have selected time series, area-averaged data of American station Tutuila, the same station for which ozone data was collected. For a comparative study of O3, SSN and CO we have downloaded CO surface concentration data for the same period of 35 years from 1980 to 2015. The source used for this data is MERRA-2 model and of spatial resolution 0.5 × 0.625 degree in the unit of ppbv. NO2 data for the period of 11 years from 2005-2015 is downloaded from the same site and for the same station i.e., Tutuila. The source used for this data is OMI and spatial resolution of 0.25 degree in the unit of 1/cm2.
For analyzing the data, we have selected one American station “Tutuila” and downloaded ozone data of the years 1980 to 2015 from the above-mentioned site. This data includes everyday hourly ground base ozone data. For better comparative study, SSN, CO, and NO2 data are also downloaded for the same period of the same station from their respective sites.
All the raw data downloaded was in grid form, which we have converted into the appropriate form. Further, we have calculated the monthly mean for every year data and got 12 data values i.e., one for each month. After it, we have plotted the monthly mean values of all the three substituent (O3, CO, SSN) against the years, so that the variation in all the three substituent can be easily concluded. The results obtained from each graph i.e., the slope and correlation coefficient for each month are collected and mentioned them in tabulated form. Similar graphs for NO2 data are also drawn. The result and conclusion obtained based on this study are given in the next section.
The monthly mean variation in CO, O3, SSN with years are shown in
It is observed from these figures and
| Months | O3 | SSN | CO |
|---|---|---|---|
| January February March April May June July August September October November December | 0.00484 0.03412 0.07799 0.02079 0.01248 0.03106 0.03965 0.03981 0.06877 0.05886 −0.003 0.09357 | −1.95396 −1.73911 −1.81283 −1.73051 −2.26584 −1.92658 −1.82296 −1.94987 −1.61318 −1.8381 −1.42378 −1.84634 | 0.11313 0.14663 0.11735 0.20437 0.11514 0.1385 −0.01759 −0.04938 −0.08106 0.01371 0.00678 0.0429 |
increases and shows a linear increment. The maximum growth in ozone value is observed in December, and it is found to be 0.09357 and the minimum growth is observed in January, which is 0.00484. The decaying trend i.e., the negative trend is shown by ozone in November which is −0.003. Similarly, from graphs, we conclude that CO value shows a decreasing trend in the monsoon period of July, August, and September, whereas for the rest of the year its value shows an increasing trend with maximum growth in April with a value 0.20437 and minimum growth in the month of November with value 0.00678. We also observe that SSN value shows decreasing trends throughout the whole year with a maximum value of −1.42378 in the month of November and a minimum value of −2.26584 in May. Hence, we conclude that Ozone and CO show an increasing trend, while SSN shows a decreasing trend over 12 months.
From
The monthly mean variation for NO2 is shown in
| Months | Correlation between O3 and SSN | Correlation between O3 and CO |
|---|---|---|
| January February March April May June July August September October November December | 0.080472 0.235077 −0.04275 0.036025 0.026713 −0.2912 −0.1316 −0.17093 0.193345 0.035231 0.272573 −0.1415 | −0.26511 −0.06346 −0.119 −0.24857 −0.16902 0.026791 0.13152 0.100537 −0.12676 −0.22733 −0.12313 0.118135 |
these two gases. In some months we got a positive correlation and in other months we got a negative correlation. In February and July months we got physically accepted negative correlation, which are about −0.66 and −0.43 respectively, and in August month a positive correlation of about 0.41, whereas in rest of the months the value of Pearson correlation coefficient is found to be very less, which is not physically accepted.
On the basis of present study, in which we analyzed a data of about 35 years raging from 1980 to 2015 of Tutuila (American station) we can conclude that CO and O3 show an increasing trend over the maximum months of the year, whereas SSN shows decreasing trend throughout the year.
Ozone shows the maximum increasing trend in December month, whereas in the previous month of it i.e., in November month it shows a negative trend.
If we see the CO data for the same period then it is observed that the value of it increases from January to June and its value is found to be minimum in January month and maximum in the April. The decaying trend of CO is observed from July to September, and after it i.e., from October to December months it again increases, but its growth rate is very small.
The analyzed 11 years data of NO2 concluded that, the variation observed in March month is very small and is positive. In the same way, a positive trend is observed for NO2 data in June month, but in rest all the months the value is negative. The correlation between O3 and NO2 shows that both are negatively correlated in some months and positively correlated in some other months. The negative correlation value between these two gases is found to be physically accepted only in the month of February and July, and positively physically accepted value in the month of August only.
The authors declare no conflicts of interest regarding the publication of this paper.
Jaitawat, N., Saraswat, V., & Rathore, N. (2021). Study of Surface Ozone over an American Station for a Period of 3.5 Decade. American Journal of Climate Change, 10, 422-432. https://doi.org/10.4236/ajcc.2021.104022