At that time, Without this natural greenhouse effect, Earthâs surface would be much colder than current conditions. In the latter half of the 20th century up until the 1990s, EESC values steadily increased (see Figure Q15-1), causing global ozone depletion. Children are to use the map below and locate the following countries listed at the bottom of the map. Halons are a group of industrial compounds that contain at least one bromine and one carbon atom; halons may or may not contain a chlorine atom. in the midlatitude stratosphere in 1997 (see Figure Q13-1). Other non-halogen gases that influence stratospheric ozone abundances have also increased in the stratosphere as a result of emissions from human activities (see Q20). ClO is a highly reactive gas that is involved in The first term represents the trapping by ozone of outgoing infrared radiation released by the surface and lower atmosphere: this is a cooling term because less ozone results in less trapping of heat. The magnitude of the dual benefit has steadily increased since 1987, as shown by the differences between the Computer model They are sequenced so children will need to complete them in the order below. two separate oxygen atoms. completely phased out. Note the large difference in the vertical scales: total chlorine entering the stratosphere It is a colorless, odorless, tasteless, non-toxic, inert, monatomic gas, the first in the noble gas group in the periodic table. Latitudes poleward of 60° account for only about 13% of Earthâs surface. The value shown in Figure Q15-1 is for the midlatitude, lower stratosphere (about 19 km altitude). Halocarbons and radiative forcing of climate. A 1964â1980 baseline is used because large amounts of ozone depletion had not occurred during these years (see Figure Q10-3). Ozone and climate and a suppressed immune system for humans and also damages terrestrial plant life, single-cell organisms, as well as aquatic For all regions, values of EESC increase smoothly with time starting in 1960, reach a peak near the end of the past century, and decrease gradually until the end of this century. depletions have occurred in the Antarctic since 1990. Ozone Emissions of HFC-23 are excluded. The initial step in the depletion of stratospheric ozone by human activities is the emission, at Earthâs surface, of gases that contain chlorine and bromine and have long atmospheric lifetimes. at Palmer equaled or exceeded those measured in I have also set up 'Class Dojo' for the children and work can be submitted through that as well. Achieving the maximum climate protection from the implementation of the Amendment requires that compounds replacing high-GWP HFCs have smaller or negligible GWPs. Other reactions. In addition to a large abundance of these reactive gases, the formation of the Antarctic ozone hole requires temperatures low enough to form polar stratospheric clouds (PSCs), isolation from air in other stratospheric regions, and sunlight (see Q8). Most of Earthâs ozone resides in the stratosphere, All children have been given their usernames and login detaIls for Times Table Rockstars today. Amendments and Adjustments. Antarctic ozone hole features. The importance for stratospheric ozone of very short-lived iodine containing source gases is an area of active research. Even the most severe Arctic ozone depletion does not lead to total ozone amounts as low as those seen in the Antarctic, because Arctic ozone abundances during early winter before the onset of ozone depletion are much larger than those in the Antarctic. The equal vertical scales in each panel allow direct comparisons of ozone and EESC changes between regions. Volcanic eruptions are an additional source of uncertainty that cannot be included in the ozone projections in Figures Q20-2 and Q20-3. CFC-11-equivalent emission unit means release of an ODS would result in the same amount of ozone depletion as release of the same mass of CFC-11; world-avoided scenario and the observed ODS abundance scenario (blue shaded region) in each panel. The Montreal Protocol does not control the production and consumption of very short-lived chlorine source gases, although the atmospheric abundances of some (notably dichloromethane, CH2Cl2) have increased substantially in recent years. Please keep in touch through year5@howebridge.wigan.sch.uk or class dojo where i have been awarding points for the work that children are sending through. These variations are caused by large-scale movements of stratospheric air and the chemical production and destruction of ozone. altitude of the ozone layer (16 km). A volcanic eruption of this nature has not occurred during the time period of the modern observational record. Figure Q7-1. The very low winter temperatures in the Antarctic stratosphere cause polar stratospheric clouds (PSCs) to form. After filling out the order form, you fill in the sign up details. If you follow the link this will take you to the login page. Tropospheric conversion. These reactive products participate in the destruction of stratospheric ozone (see Q1). A cause of death and an exact age for Hale was not immediately available. With continued compliance, substantial recovery of The UV Index varies with A large ozone hole has occurred each year since the early 1990s as shown in Figure Q10-2. to begin with either ClO or Cl. I have also attached some further maths activities from the White Rose website and with accompanying worksheets. The effects on ozone These lessons are good as they have a teacher video to accompany them. Links between stratospheric ozone depletion and changes in surface climate were first found in research studies in the early 2000s, based on both observations and models. However, as long as atmospheric abundances of ODSs remain elevated, the possibility of This timeline highlights milestones related to the history of ozone in this figure. other atmospheric constituents such as carbon, oxygen, nitrogen, and hydrogen. (The unit âparts per trillionâ is defined in the caption of Figure Q6-1.). midday position in the local sky, which depends After spring, these low values disappear from total ozone maps as polar air mixes with lower-latitude air containing much higher amounts of ozone. the stratosphere. The reactive gases can be grouped into the reservoir gases, which do not directly destroy The first total ozone measurements made in Antarctica with Dobson spectrophotometers occurred in the 1950s following extensive measurements in the Northern Hemisphere and Arctic region. Rainwater and ice efficiently scavenge and remove HCl while the plume is still in the lower atmosphere (troposphere). stratospheric ozone coincident with the decline in EESC constitutes an initial sign of ozone recovery. The response of radiative forcing to ODS emission reductions is a slow decline attributable to the high abundances of the two principal contributing gases, CFC-11 and CFC-12, and their long atmospheric lifetimes (50â100 years). Volcanic aerosol is primarily composed of sulfur compounds (sulfate). At high latitudes during winter and spring, most stratospheric Values of EESC are derived from surface observations of ozone-depleting substances (ODSs) and represent the potential for ozone depletion from halogens at particular times and locations of the stratosphere (see Q15). They do not need to complete all of it: the idea is that children can be creative and be introduced to planning and organising money in a fun way that they can be in charge of. of the Antarctic ozone hole are We are really proud of the children and have really enjoyed seeing their work and hearing your comments about their achievements. The EESC scenarios in Figure Q18-1 (lower left panel) provide a measure of the year-to-year potential of the atmospheric abundances of ODSs to destroy stratospheric ozone. Teachers will continue to update the website and blog. You don't need to complete all of the worksheets, just complete what you can during the Maths lesson. In Note that while Ozone-depleting substances (ODSs) and their substitutes make up a large fraction of the halocarbons in todayâs atmosphere. the science of stratospheric ozone depletion, international scientific These models show how changes in ozone are expected to vary across geographic regions by evaluating the complex interactions of the processes that control ozone and climate involving radiation, chemistry, and transport. Values of EESC have peaked and are now in a slow decline. Therefore, only a fraction of their halogen content potentially contributes to ozone depletion in the stratosphere. Total ozone varies strongly with latitude over the globe, with the largest values occurring at middle and high latitudes during most of the year (see Figure Q3-1). variations of the stratospheric circulation. For example, in the ozone profile over South Pole, Antarctica on 9 October 2006 (see red line in left panel of Figure Q11-3), ozone abundances are essentially zero over the altitude region of 14 to 21 km. In the Antarctic at the South Pole (left panel), a normal ozone layer was observed to be present between 1962 and 1971. The largest source related to human activities is agriculture, especially the use of fertilizer. Oxygen molecules (O2), The contributions from very short-lived gases (see Figure Q6-1) are not included in this EESC time series. another O2. Natural sources make a much larger fractional contribution to bromine entering The principal steps in stratospheric ozone depletion caused by human activities are shown in Figure Q5-1. The Nobel Prize in Chemistry in 1995 was awarded for research The contributions from very short-lived gases (see Figure Q6-1), which have been minor to this point, are not However, it is only after midcentury that the abundance of ODSs is expected to fall to values that were present before the Antarctic ozone hole was first observed in the early 1980s, due to the long atmospheric lifetime of these gases. Nevertheless, it is vital to human well-being human pollution. Because PSCs often contain a significant fraction of available HNO3, their descent removes HNO3 from regions of the ozone layer. atmospheric ozone is contained in the stratospheric âozone layerâ, which shields Earthâs surface from An 'alertDismissed' token is used to prevent Model studies indicate that even though long-lived greenhouse gases that of polar regions, leading to an increase in global Model inputs include historical and projected concentrations of ODSs, CO2, CH4, N2O, air pollutant gases, as well as solar output. Also shown are the contributions to total chlorine and bromine in 2016, highlighting the reductions of 10% and 11%, respectively, achieved under the controls of the Montreal Protocol. After this, make payment for your order using the most convenient payment system for yourself. HFCs have ODPs of zero and are also strong greenhouse gases, as quantified by a metric termed the Global Warming Potential (GWP) (see Q17). A comparison of the I have left Friday free in case children need to finish off or have ran out of time. in global total ozone over the past half century is the abundance of stratospheric halogens. Satellite instruments have been routinely These gases, referred to as halogen source gases, and also as ozone-depleting substances (ODSs), chemically release their chlorine and bromine atoms after they reach the stratosphere. For example, an increase in cloud cover usually results in a reduction of UV radiation below the clouds and could at the same time increase UV radiation at a location in the mountains above the clouds. As a result, ClO remains chemically active for a longer period, thereby increasing chemical ozone destruction. in the Arctic. https://classroom.thenational.academy/schedule-by-year/year-5. Values are higher throughout These compounds are expected to cover the application demand from sectors in which the use of high-GWP HFCs is phased down. and the answers provided here were prepared and reviewed and HCFCs are ozone-depleting substances (ODSs) since they contain either chlorine or bromine (see Q6). The baseline scenario of ODS emissions can be contrasted with a scenario of ODS emissions that the world has avoided by successfully implementing the Montreal Protocol (see Figure Q18-1). and project future values of ozone. variations in meteorological conditions, volcanic eruptions, changes First, ozone-depleted air over both polar regions is dispersed away from the poles during and after each winter/spring period, thereby reducing average ozone at midlatitudes. winter cover an extensive area that at times exceeds that of the Antarctic continent and can last for several months, leading to Halogen source gases do not react directly with ozone. use chemical reactions that are unique to ozone. Cycle 1 is most important in the stratosphere at altitudes above about 30 km (18.6 miles), where solar UV-C radiation (100 to 280 nanometer (nm) wavelengths) is most intense (see Figure Q2-1). of stratospheric sulfate particles, and substitutes, do not destroy ozone (ODPs equal zero) since they are mixtures of only hydrogen, fluorine, and carbon atoms. Montreal Protocol controls are based on several factors that are considered separately for each ODS. The baseline scenario is labeled âFrom observed ODS abundancesâ in Figure Q18-1 since, for 1960â2016, the emissions are based upon analysis of observed abundances of the principal ODS gases at Earthâs surface (see Figure Q15-1). In the Arctic, the other 50% is attributable to natural variations Sunlight is needed to break apart (ClO)2 and BrCl, resulting in abundances of ClO and BrO large enough to drive rapid ozone loss by Cycles 2 and 3. Carbon dioxide is considered a long-lived gas, since a significant fraction remains in the atmosphere 100â 1000 years after emission. The avoided emissions are a measure of the ozone layer protection afforded by the Protocol. the greenhouse gas emissions assumed in future climate projections. Small amounts of these gases dissolve in ocean waters. Without Montreal Protocol controls, the climate forcing due to ODSs could now be nearly two and a half times the present value. decreases in methyl bromide are expected to be modest, since industrial production is now much smaller than occurred in the Increasing CO2 results in 2011 (blue colors) are unusual in the Arctic record, although not unexpected. From very short-lived source gases described in Figure Q19-1 N2O produces reactive nitrogen gases that lead to low. Need them from all HFCs chemical ozone destruction can reach furthest into the stratosphere over Antarctica reacts continually sunlight! 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