How has Antarctica's climate changed in the past? Is Antarctica being affected by 'global warming' and how might we expect its climate to change in the future? What evidence is needed to address these questions?
The problem of human-caused climate change (commonly referred to as global warming) is now well known: the concentrations of 'greenhouse gases' in the atmosphere (notably carbon dioxide and methane) are now well above their pre-industrial levels, primarily due to our use of fossil fuels (coal, oil, and natural gas) but also due to deforestation and agricultural practices. As greenhouse gases accumulate in the atmosphere, more heat energy from the Earth's surface is intercepted before escaping to space, thereby causing the atmosphere to warm.
Of course greenhouse gases are not the only factor influencing the Earth's climate, and much of the complexity surrounding the global warming issue (such as the amount, rate and pattern of warming) involves trying to understand the knock-on effects that the rise in greenhouse gases will have on other parts of the climate system. There are also natural variations in climate that occur on a range of different timescales, and there are variations, both natural and human-caused, in the way the greenhouse gases themselves cycle between atmosphere, land, and oceans. In short, understanding and predicting climate change is far more complex than it may at first seem.
Studies of Antarctica, particularly analyses of Antarctic ice cores, have played a crucial role in this endeavour. As described further below, the ice cores have enabled scientists to reconstruct past climate changes spanning hundreds of thousands of years. Past variations in climate due to natural causes are now far better understood than they used to be, and this has provided vital context against which to assess more recent changes caused by people. The polar regions are also often described as the 'canary in the coal mine' for detection of global warming, and some of the research stations discussed in Section 2.2 provide important weather data for assessing the polar response to the rise in greenhouse gases. And, as Antarctica holds about 90% of all the ice on the planet, what happens in Antarctica will have major effects on the rest of the world.
Before looking further at what we have learned about climate change from Antarctica, it's worth reviewing some key concepts about evidence and timescales.
Antarctica hasn't always had the climate that it has now. In the geological past Antarctica has been much warmer, and fossils indicate that at various times trees have covered much of the continent. These warm times for Antarctica were the result of different tectonic configurations and patterns of ocean circulation many millions of years ago (see Section 1.2). For at least the last 6 million years, ice has covered most of the continent.
In contrast with the much older geological evidence, the ice core record extends from the present day back to about 800 000 years ago. Over this time span the distribution of land and sea across the world has been essentially the same as today; and therefore, the changes recorded in Antarctic ice are more informative about how the climate varies under the present tectonic configuration and how it may change in the near future.
Ice cores are obtained by drilling into an ice sheet or glacier and extracting cylindrical sections of ice.
These sections of ice represent many thousands of years of snow accumulation: the addition of snow each year buries underlying layers of snow, and over time these layers become compressed into glacier ice. Each layer of an ice core is derived from snow that fell at a certain time in the past, and each layer is like a time capsule, containing information about what the atmosphere was like at the time the snow fell.
The beauty of ice cores is that they contain a variety of forms of evidence that can tell us so many different things about the past climate and environment. The evidence is also continuous through time and can be dated with a high degree of precision. Some important types of evidence and information are:
The basic idea behind the interpretation of stable isotopes in ice cores is that as air cools and condensation occurs, the heavier isotopes of hydrogen and oxygen will condense out more readily than the lighter isotopes. This means that the colder the air is, the more depleted the water vapour will be in heavy isotopes; so when precipitation forms, the H2O added to the ice sheet is 'light' (e.g. the ratios of 18O to 16O and 2H to 1H will be less). Conversely, as the atmosphere over the ice sheet warms, there will be an increase in the ratio of heavy to light isotopes.
These ratios are expressed as per mille (rather than per cent), and they are measured in relation to 'standard mean ocean water' (SMOW). Because H2O with the lighter isotopes is evaporated more easily from the ocean, the isotope ratios of water vapour in the atmosphere (and hence precipitation reaching an ice sheet) are always negative in relation to SMOW. For example, oxygen isotope ratios from the Byrd ice core, West Antarctica, range between -33o/oo and -43o/oo. Because there is a shift of about a 0.7o/oo for every 1°C change in mean annual air temperature, the Byrd ice core shows temperature fluctuations on the order of 15°C over the past 100 000 years.
You can find out more about ice coring, about the interpretation of stable isotopes in ice cores, as well as about how other forms of evidence are analysed and interpreted, by viewing these websites:
Ice cores have been extracted from many glaciers and ice sheets around the world. Much of the pioneering work was done on Greenland ice; and, due to the higher snow accumulation rates on Greenland compared with Antarctica, the Greenland ice cores provide a more finely resolved record of change (with annual layer counting extending back to roughly 40 000 years ago). However, Greenland ice cores do not extend back much beyond 100 000 years, and the presence in the ice of wind blown carbonates from Canada contaminates past CO2 measurements. Hence the major ways in which Antarctic ice adds to the knowledge gained from Greenland are:
There are three main areas of Antarctica that have supplied long ice cores. The longest ice core record (extending back approximately 800 000 years) was taken from the Dome C area of East Antarctica by the EPICA team (European Project for Ice Coring in Antarctica). The coring was completed in 2004 to a depth of 3270m in the ice. Another important core, analysed in the 1990s, was taken from the Vostok station, also in East Antarctica. The Vostok ice core provides climate information extending back to about 400 000 years ago. West Antarctica is represented by the Byrd ice core record that was drilled to a depth of 2037m.
Antarctic ice cores have contributed a great deal to our understanding of climate change, particularly in the following ways:
The diagram below summarise these major insights:
The long term Antarctic temperature changes derived from the analysis of stable isotopes relate to the natural climate variations associated with the cycles of glacial expansion and retreat during the Quaternary Ice Age (glacial/interglacial cycles). On average, the cold, glacial phases last considerably longer than the interglacial phases during which warm conditions are sustained for around 10 000 years (our current interglacial has so far lasted for 11 700 years). Also notice from the EPICA diagram that the amplitude of warm/cold oscillations increased about 400 000 years ago. In addition to the temperature changes, these cycles were accompanied by large changes in sea-level (during the last glacial maximum sea-level was about 120m lower than now); and these sea-level changes were the result of changes in the total amount of ice on land (both in the Northern Hemisphere and in Antarctica).
You can learn more about the Ice Age and about glacial/interglacial cycles by visiting these websites:
Importantly, the concentrations of carbon dioxide, and other greenhouse gases, track the temperature changes very closely. While the pacing of these natural climate variations is due to cyclic changes in the Earth's orbit (Milankovitch cycles), the fluctuations in greenhouse gases play an important role in amplifying the initial temperature changes. In other words, the levels of greenhouse gases in the atmosphere were not only responding to the orbitally-induced temperature changes: they were also making the fluctuations in temperature larger than they would otherwise have been. This is good evidence for the suggestion that changing the concentration of greenhouse gases in the atmosphere (as we are doing today) will affect the Earth's climate.
The range of glacial/interglacial carbon dioxide and methane concentrations shown in the Antarctic ice cores is between 180 and 300ppm (parts per million) and 320 and 790ppb (parts per billion) respectively. Hence the current levels of about 390ppm and 1820ppb are well beyond natural variation in recent geological time.
From the previous discussion on the relationship between levels of greenhouse gases and Antarctic temperature revealed in ice cores, one would expect Antarctica to show signs of warming in response to the rapid rise in greenhouse gases that has occurred over the past century. However, it needs to be remembered that the climate system is highly complex; and due to the influence of other climate factors, different regions respond differently to the climate 'forcing' of greenhouse gases. There are also time lags to be aware of: it takes time for changes in the composition of the atmosphere to begin to influence the weather; moreover, it requires many years of data before meaningful climate trends can be separated from random, year-to-year weather variations.
In Antarctica, there are relatively few places with long enough instrumental records (i.e. weather stations using standard techniques of weather recording for more than 30 years) to investigate recent climate change. However, it is possible to draw some conclusions from the data that are available. The climate of the Antarctic Peninsula has been well monitored compared with other parts of the continent, and data show that this is the fastest warming part of the Southern Hemisphere: the mean annual temperature has risen by about 3°C over the past 50 years. This is shown in the long instrumental record (extending back to 1945) from Vernadsky station (see Student Activities below). As described in Section 1.5, this is causing the disintegration of Peninsula ice shelves. For comparison, the surface air temperature averaged across the planet has risen by 0.74°C over the past century.
In contrast with the Peninsula, climate records from the interior of the continent do not yet show a clear warming trend. According to the Fourth Assessment of the Intergovernmental Panel on Climate Change (IPCC) (published in 2007), Antarctica is the only continent that does not show significant human-caused warming (averaged for the continent as a whole) over the past 50 years. However, using satellite data some scientists have argued more recently that West Antarctica is warming.
Browse monthly and mean annual temperature data sets from various Antarctic stations at the British Antarctic Survey website.
One explanation for the difference seen between the Peninsula and the interior is the influence of the ocean. As sea surface temperatures gradually warm due to the influence of increased greenhouse gases, maritime air masses also pick up this added warmth – and being surrounded by sea, the Peninsula is affected by this transfer of heat from the ocean far more than places inland. The near sea surface temperature of the Antarctic Circumpolar Current to the west of the Peninsula has increased by about 1°C over the past 50 years.
You can find out more about the IPCC and its projections of future climate warming at the following websites:
Considering what the ice core records show, as greenhouse gases continue to accumulate in the atmosphere, it is likely that even the interior of the continent will eventually show signs of warming. Yet, it will be along the Peninsula and around Antarctica's coastline where the strongest evidence of climate change will be seen.
Impacts of climate warming on glaciers, ice shelves, and sea ice are discussed in Section 1, and impacts on ecoystems and wildlife are discussed in Section 3. Of global relevance, however, is how climate change in Antarctica will affect sea-level. As described in Section 1.4, this requires estimates to be made about the mass balance of Antarctic glaciers – if negative, then more mass is being discharged into the ocean (through iceberg calving for instance) than is accumulating on the glacier through snowfall, causing a net rise in sea-level. In 2007 the Intergovernmental Panel on Climate Change concluded that over the period from 1993-2003 melt from Antarctica contributed about 0.2mm per year to sea-level rise.
Most glaciers on the Antarctic Peninsula now have a negative mass balance, and glacial melt from the northern Peninsula is currently contributing to sea-level rise of 0.16mm per year (similar to the contribution from melting glaciers in Alaska). Analyses of the West Antarctic Ice Sheet also show areas of negative mass balance, and there is concern for the long-term future of the WAIS because of its lower surface altitude and the fact that much of it is grounded below sea-level. A particularly vulnerable part of the WAIS is the Amundsen Sea Embayment section which would raise sea-level by 1.5 metres if it disappeared. If the whole WAIS were to melt, it would raise average sea-level by up to 6 metres, although it would take hundreds of years for this to happen. Interestingly, and worryingly, the disappearance of the huge mass of the WAIS would reduce the region's gravitational pull on the sea, and therefore sea-levels would rise highest in areas more distant from West Antarctica, particularly along the North American coastline.
With its larger size, higher elevation, and higher grounding level, the East Antarctic Ice Sheet is less vulnerable to climate change, and it is possible that higher temperatures might even lead to a more positive mass balance and a thickening of the EAIS because of increased snowfall in the interior. The total contribution that Antarctica will make to global sea-level rise over the next century is still unclear and the subject of much research.
You can learn more about climatic change in the Antarctic and its consequences in these sections of the BAS website:
If you have Google Earth, you can follow this link to open up a file on Antarctic climate impacts (pictures and facts) that you can view in Google Earth:
1. Using the text above and any of the suggested weblinks, write a briefing paper to describe the evidence contained in Antarctic ice cores and to explain their significance for understanding the Earth's climate system.
2. Study the diagram above that compares long-term temperature changes and carbon dioxide levels revealed in the EPICA ice core and answer the following questions:
3a. The attached Excel spreadsheet contains mean annual temperature data from Vernadsky station (Faraday/Vernadsky) (located 65°15'S,64°16'W on Galindez Island, Antarctic Peninsula) along with mean annual carbon dioxide concentrations extending back to 1959. Copy the data attached here [insert spreadsheet link] into your own spreadsheet and do the following:
3b. Give your opinion about how strongly this graph supports the view that humans are causing climate change through greenhouse gas emissions. In what ways should one be careful in interpreting a correlation graph based on a single site? What additional evidence would help in coming to a conclusion about the effects of global warming on Antarctica?
3c. On correlation plots, by convention the independent variable is plotted on the X-axis and the dependent variable on the Y-axis (assuming that the X-axis variable affects the Y-axis variable but not vice versa). Why is this a safe assumption for your correlation graph using local temperature data? What problems might there be with this assumption if a similar plot were drawn using mean annual air temperature averaged across the Earth? (Hint: think about aspects of the global carbon cycle.)