Sunday, September 10, 2006

Green House Gases, Global Warming & Climate Change

Climate change

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Variations in CO2, temperature and dust from the Vostok ice core over the last 400 000 years
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Variations in CO2, temperature and dust from the Vostok ice core over the last 400 000 years

Climate change refers to the variation in the Earth's global climate or in regional climates over time. It describes changes in the variability or average state of the atmosphere—or average weather—over time scales ranging from decades to millions of years. These changes may come from processes internal to the Earth, be driven by external forces (e.g. variations in sunlight intensity) or, most recently, be caused by human activities.

In recent usage, especially in the context of environmental policy, the term "climate change" often refers only to the ongoing changes in modern climate, including the rise in average surface temperature known as global warming. In some cases, the term is also used with a presumption of human causation, as in the United Nations Framework Convention on Climate Change (UNFCCC). The UNFCCC uses "climate variability" for non-human caused variations.[1]

For information on temperature measurements over various periods, and the data sources available, see temperature record. For attribution of climate change over the past century, see attribution of recent climate change.

Climate change factors

Climate changes reflect variations within the Earth's environment, natural processes going on around it, and the impact of human activity. The external factors which can shape climate are often called climate forcings and include such processes as variations in solar radiation, the Earth's orbit, and greenhouse gas concentrations.

Variations within the Earth's climate

Weather, in and of itself, is a chaotic non-linear dynamical system, but in many cases, it is observed that the climate (i.e., the average state of weather) is fairly stable and predictable. This includes the average temperature, amount of precipitation, days of sunlight, and many other variables that might be measured at any given site. However, there are also changes within the Earth's environment that can affect the climate.

Glaciation

Percentage of advancing glaciers in the Alps in the last 80 years
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Percentage of advancing glaciers in the Alps in the last 80 years

Glaciers are recognized as one of the most sensitive indicators of climate change, advancing substantially during climate cooling (e.g., the Little Ice Age of the last century) and retreating during climate warming on moderate time scales. Glaciers grow and collapse, both contributing to natural variability and greatly amplifying external forces. For the last century, however, glaciers have been unable to regenerate enough ice during the winters to make up for the ice lost during the summer months (see glacier retreat for more).

The most important climate processes of the last several million years are the glacial and interglacial cycles of the present ice age. Though shaped by orbital variations, the internal responses involving continental ice sheets and 130 m sea-level change certainly played a key role in deciding what climate response would be observed in most regions. Other changes, including Heinrich events, Dansgaard–Oeschger events and the Younger Dryas show the potential for glacial variations to influence climate even in the absence of specific orbital changes.

Ocean variability

A schematic of modern thermohaline circulation
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A schematic of modern thermohaline circulation

On the scale of mere decades, climate changes can also result from changes within the ocean/atmosphere systems. Many climate states, most obviously El Niño Southern oscillation, but also including the Pacific decadal oscillation, the North Atlantic oscillation, and the Arctic oscillation, have been recognized as modes within the climate system, owing their existence at least in part to different ways that heat can be stored in the oceans and move between different reservoirs. On longer time scales, ocean processes such as thermohaline circulation play a key role in redistributing heat, and could, if changed, dramatically impact climate.

The memory of climate

More generally, most forms of internal variability in the climate system can be recognized as a form of hysteresis, meaning that the current state of climate reflects not only the inputs, but also the history of how it got there. For example, a decade of dry conditions may cause lakes to shrink, plains to dry up and deserts to expand. In turn, these conditions may lead to less rainfall in the following years. In short, climate change can be a self-perpetuating process because different aspects of the environment respond at different rates and in different ways to the fluctuations that inevitably occur.

Non-climate factors driving climate change

Greenhouse gases

Carbon dioxide variations during the last 500 million years
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Carbon dioxide variations during the last 500 million years

Current studies indicate that radiative forcing by greenhouse gases is the primary cause of global warming. Greenhouse gases are also important in understanding Earth's climate history. According to these studies, the greenhouse effect, which is the warming produced as greenhouse gases trap heat, plays a key role in regulating Earth's temperature.

Over the last 600 million years, carbon dioxide concentrations have varied from perhaps >5000 ppm to less than 200 ppm, due primarily to the impact of geological processes and biological innovations. Curiously, it has been argued (Veizer et al. 1999) that variations in greenhouse gas concentrations over tens of millions of years have not been well correlated to climate change, with plate tectonics perhaps playing a more dominant role. However there are several examples of rapid changes in the concentrations of greenhouse gases in the Earth's atmosphere that do appear to correlate to strong warming, including the Paleocene–Eocene thermal maximum, the Permian–Triassic extinction event, and the end of the Varangian snowball earth event.

During the modern era, rising carbon dioxide levels are implicated as the primary cause to global warming since 1950.

Plate tectonics

On the longest time scales, plate tectonics will reposition continents, shape oceans, build and tear down mountains and generally serve to define the stage upon which climate exists. More recently, plate motions have been implicated in the intensification of the present ice age when, approximately 3 million years ago, the North and South American plates collided to form the Isthmus of Panama and shut off direct mixing between the Atlantic and Pacific Oceans.

Solar variation

Variations in solar activity during the last several centuries based on observations of sunspots and beryllium isotopes.
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Variations in solar activity during the last several centuries based on observations of sunspots and beryllium isotopes.

The sun, as the ultimate source of nearly all energy in the climate system, is an integral part of shaping Earth's climate. On the longest time scales, the sun itself is getting brighter as it continues its main sequence evolution. Early in Earth's history, it is thought to have been too cold to support liquid water at the Earth's surface, leading to what is known as the Faint young sun paradox.

On more modern time scales, there are also a variety of forms of solar variation, including the 11–year solar cycle and longer-term modulations. However, the 11–year sunspot cycle does not manifest itself clearly in the climatological data. These variations are considered to be influential in triggering the Little Ice Age and for some of the warming observed from 1900 to 1950.

Orbital variations

In their impact on climate, orbital variations are in some sense an extension of solar variability, because slight variations in the Earth's orbit lead to changes in the distribution and abundance of sunlight reaching the Earth's surface. Such orbital variations, known as Milankovitch cycles, are a highly predictable consequence of basic physics due to the mutual interactions of the Earth, its moon, and the other planets. These variations are considered the driving factors underlying the glacial and interglacial cycles of the present ice age. Subtler variations are also present, such as the repeated advance and retreat of the Sahara desert in response to orbital precession.

Volcanism

A single eruption of the kind that occurs several times per century can impact climate, causing cooling for a period of a few years. For example, the eruption of Mount Pinatubo in 1991 is barely visible on the global temperature profile. Huge eruptions, known as large igneous provinces, occur only a few times every hundred million years, but can reshape climate for millions of years and cause mass extinctions.

Human influences

Anthropogenic factors are acts by humans that change the environment and influence climate. The biggest factor of present concern is the increase in CO2 levels due to emissions from fossil fuel combustion, followed by aerosols (particulate matter in the atmosphere) which exerts a cooling effect. Other factors, including land use, ozone depletion, and deforestation also impact climate.

Fossil fuels

Carbon dioxide variations over the last 400,000 years, showing a rise since the industrial revolution.
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Carbon dioxide variations over the last 400,000 years, showing a rise since the industrial revolution.

Beginning with the industrial revolution in the 1850s and accelerating ever since, the human consumption of fossil fuels has elevated CO2 levels from a concentration of ~280 ppm to more than 370 ppm today. These increases are projected to reach more than 560 ppm before the end of the 21st century. Along with rising methane levels, these changes are anticipated to cause an increase of 1.4–5.6 °C between 1990 and 2100. (reference needed)

Aerosols

Anthropogenic aerosols, particularly sulphate aerosols from fossil fuel combustion, are believed to exert a cooling influence; see graph.[2] This, together with natural variability, is believed to account for the relative "plateau" in the graph of 20th century temperatures in the middle of the century.

Land use

Prior to widespread fossil fuel use, humanity's largest impact on local climate is likely to have resulted from land use. Irrigation, deforestation, and agriculture fundamentally change the environment. For example, they change the amount of water going into and out of a given locale. They also may change the local albedo by influencing the ground cover and altering the amount of sunlight which is absorbed. For example, there is evidence to suggest that the climate of Greece and other Mediterranean countries was permanently changed by widespread deforestation between 700 BC and 0 BC (the wood being used for ship-building, construction and fuel purposes), with the result that the modern climate in the region is significantly hotter and drier and the species of trees which were used for ship-building in the ancient world can no longer be found in the area.

A controversial hypothesis by William Ruddiman suggests that the rise of agriculture and the accompanying deforestation led to the increases in carbon dioxide and methane during the period 5000–8000 years ago. These increases, which reversed previous declines, may have been responsible for delaying the onset of the next glacial period, according to Ruddimann's hypothesis.

Interplay of factors

If a certain forcing (for example, solar variation) acts to change the climate, then there may be mechanisms which act to amplify or reduce the effects. These are called positive and negative feedbacks. As far as is known, the climate system is generally stable with respect to these feedbacks: positive feedbacks do not "run away". Part of the reason for this is the existence of a powerful negative feedback between temperature and emitted radiation: radiation increases as the fourth power of absolute temperature.

However, a number of important positive feedbacks do exist. The glacial and interglacial cycles of the present ice age provide an important example. It is believed that orbital variations provide the timing for the growth and retreat of ice sheets. However, the ice sheets themselves reflect sunlight back into space and hence promote cooling and their own growth, known as the ice–albedo feedback. Further, falling sea levels and expanding ice decrease plant growth and indirectly lead to declines in carbon dioxide and methane. This leads to further cooling.

Similarly, rising temperatures caused, for example, by anthropogenic emissions of greenhouse gases could lead to retreating snow lines, revealing darker ground underneath, and consequently result in more absorption of sunlight.

Water vapor, methane, and carbon dioxide can also act as significant positive feedbacks, their levels rising in response to a warming trend, thereby accelerating that trend. Water vapor acts strictly as a feedback (excepting small amounts in the stratosphere), unlike the other major greenhouse gases, which can also act as forcings.

More complex feedbacks involve the possibility of changing circulation patterns in the ocean or atmosphere. For example, a significant concern in the modern case is that melting glacial ice from Greenland will interfere with sinking waters in the North Atlantic and inhibit thermohaline circulation. This could affect the Gulf Stream and the distribution of heat to Europe and the east coast of the United States.

Other potential feedbacks are not well understood and may either inhibit or promote warming. For example, it is unclear whether rising temperatures promote or inhibit vegetative growth, which could in turn draw down either more or less carbon dioxide. Similarly, increasing temperatures may lead to either more or less cloud cover.[3] Since on balance cloud cover has a strong cooling effect, any change to the abundance of clouds also impacts climate.[4]

Monitoring the current status of climate

Scientists use "Indicator time series" that represent the many aspects of climate and ecosystem status. The time history provides an historical context. Current status of the climate is also monitored with climate indices.[5][6][7]

Evidence for Climatic Change

Evidence for climatic change is taken from a variety of sources which can be used to reconstruct past climates. Most of the evidence is indirect—climatic changes are inferred from changes in indicators that reflect climate, such as vegetation, Dendrochronology, Ice cores, sea level change, glacial retreat.

Pollen Analysis

Species have particular climatic requirements which influence their geographical distributions. Each plant species has a distinctively shaped pollen grain and if these fall into oxygen-free environments, such as peat bogs, they resist decay. Changes in the pollen found in different levels of the bog indicate, by implication, changes in climate.

One limitation of this method is the fact that pollen can be transported considerable distances by wind or sometimes by wildlife.

Coleoptera

Remains of Coleoptera beetles are common in freshwater and land sediments. Different species of this beetle tend to be found under different climatic conditions. Knowledge of the present climatic range of the different species, and the age of the sediments in which remains are found, allows past climatic conditions to be worked out.

Glacial Geology

Advancing glaciers leave behind moraines and other features which often have datable material in them, recording the time when a glacier advance and deposited a feature. Similarly the lack of glacier cover can be identified by the presence of datable soil or volcanic tephra horizons. Glaciers are considered one of the most sensitive climate indicators by the IPCC, and their recent observed variations provide a global signal of climate change, see Retreat of glaciers since 1850.

Historical Records

Historical records include cave paintings, depth of grave digging in Greenland, diaries, documentary evidence of events (such as 'frost fairs' on the Thames) and evidence of areas of vine cultivation. Since 1873 daily weather reports have been documented, and the Royal Society has encouraged the collection of data since the seventeenth century. Parish records are often a good source of climate data.

Examples of climate change

Climate change has continued throughout the entire history of Earth. The field of paleoclimatology has provided information of climate change in the ancient past, supplementing modern observations of climate. Obviously, most of these prehistoric changes are solely the result of natural factors.

  1. Climate of the deep past
  2. Climate of the last 500 million years
  3. Climate of recent glaciations
  4. Recent climate

See also

References

  1. ^ http://www.grida.no/climate/ipcc_tar/wg1/518.htm
  2. ^ IPCC TAR SPM figure 3
  3. ^ http://www.grida.no/climate/ipcc_tar/wg1/271.htm
  4. ^ For additional discussion of feedbacks relevant to ongoing climate change, see http://www.grida.no/climate/ipcc_tar/wg1/260.htm
  5. ^ Arctic Change Indicators
  6. ^ Bering Sea Climate and Ecosystem Indicators
  7. ^ How scientists study climate change: Some important research concepts used by scientists to study climate variations
  • Increasing destructiveness of tropical cyclones over the past 30 years. K.A. Emanuel, Nature, 436 (2005), pp. 686-688. ftp://texmex.mit.edu/pub/emanuel/PAPERS/NATURE03906.pdf
  • What effects are we seeing now and what is still to come? Calvin Jones "Climate Change: Facts and Impacts"
  • Changing the Atmosphere: Expert Knowledge and Environmental Governance (Politics, Science & the Environment (Paperback)), edited by Clark Miller and Paul N. Edwards, MIT Press 2001
  • The anthropogenic greenhouse era began thousands of years ago, Ruddiman WF; Climatic Change, 61 (3): 261-293 Dec 2003
  • William F. Ruddiman (2005), Plows, Plagues, and Petroleum: How Humans Took Control of Climate, Princeton University Press
  • A test of the overdue-glaciation hypothesis, William F. Ruddiman, Stephen J. Vavrus, John E. Kutzbach, Quaternary Science Reviews 24 (2005) 1­1
  • A note on the relationship between ice core methane concentrations and insolation, Schmidt, GA, Shindel, DT and Harder, S; GRL v31 L23206, 16 December 2004.

External links

BBC articles

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