What Is The Meaning Of Carbon Dioxide – For the thermonuclear reaction involving carbon that powers some stars, see CNO cycle. For the organic chemical ring structures, see Cyclic compound. For the geochemical cycle, see carbonate-silicate cycle.

The rapid carbon cycle, showing the movement of carbon between the land, atmosphere and oceans in billions of tonnes (gigatons) per year. Yellow numbers are natural flows, red are human contributions, and white are stored carbon. Effects of the slow (or deep) carbon cycle, such as volcanic and tectonic activity, are not included.

What Is The Meaning Of Carbon Dioxide

The carbon cycle is that part of the biogeochemical cycle in which carbon is exchanged between the biosphere, pedosphere, geosphere, hydrosphere and atmosphere of the Earth. Other major biogeochemical cycles include the nitrogen cycle and the water cycle. Carbon is the main component of biological compounds, as well as the main component of many minerals, such as limestone. The carbon cycle comprises the sequence of events that are essential for the Earth to be able to sustain life. It describes the movement of carbon as it is recycled and reused in the biosphere, and the long-term processes of carbon sequestration (storage) in and release from carbon sinks.

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To describe the dynamics of the carbon cycle, a distinction can be made between the fast and slow carbon cycles. The rapid carbon cycle is also called the biological carbon cycle. Rapid carbon cycles can be completed in a few years, with substances moving from the atmosphere to the biosphere and back to the atmosphere. Slow or geological cycles (also called the deep carbon cycle) can take millions of years to complete, with substances moving through the Earth’s crust between rocks, soil, the ocean, and the atmosphere.

For many centuries, human activities have disrupted the rapid carbon cycle by changing land use and, in addition, by actually extracting fossil carbon on an industrial scale (coal, oil and gas extraction and cement production) from the geosphere.

Carbon dioxide in the atmosphere has increased by nearly 52% from pre-industrial levels by 2020, resulting in greater warming of the atmosphere and Earth’s surface by the sun.

Increased carbon dioxide has also caused a decrease in ocean pH, fundamentally altering marine chemistry.

Svs: National Carbon Dioxide (co₂) Budgets Inferred From Atmospheric Observations

Most fossil carbon has only been extracted in the last half century, and rates continue to rise rapidly, contributing to human-induced climate change.

The global carbon cycle is now commonly divided into the following major carbon reservoirs (also called carbon pools), which are interconnected by exchange pathways:

Carbon exchanges between reservoirs occur as a result of various chemical, physical, geological and biological processes. The ocean contains the largest active pool of carbon near the Earth’s surface.

The natural fluxes of carbon between the atmosphere, ocean, terrestrial ecosystems and sediments are fairly balanced; thus carbon levels would be roughly stable without human influence.

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A computer model showing a year in the life of atmospheric carbon dioxide and how it travels around the world

Carbon in the Earth’s atmosphere exists in two main forms: carbon dioxide and methane. Both gases absorb and retain heat in the atmosphere and are partly responsible for the greenhouse effect.

Methane produces a larger greenhouse effect per volume compared to carbon dioxide, but exists in much lower concentrations and is shorter-lived than carbon dioxide. Thus, carbon dioxide contributes more to the global greenhouse effect than methane.

Carbon dioxide is removed from the atmosphere mainly through photosynthesis and destroys the terrestrial and oceanic biosphere. Carbon dioxide also dissolves directly from the atmosphere into bodies of water (oceans, lakes, etc.) as well as precipitation when raindrops fall through the atmosphere. When carbon dioxide is dissolved in water, it reacts with water molecules to form carbonic acid, which contributes to ocean acidity. It can be absorbed by rocks through weathering. It can also acidify other surfaces it touches or wash them off into the ocean.

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Human activities over the past two centuries have increased the amount of carbon in the atmosphere by almost 50% by 2020, mainly in the form of carbon dioxide, both by changing the ability of ecosystems to draw carbon dioxide from the atmosphere and by releasing it directly, such as through burning fossil fuels and concrete production.

In the distant future (2 to 3 billion years), the rate at which carbon dioxide is absorbed into the soil via the carbonate-silicate cycle is likely to increase due to expected changes in the Sun as it ages. The expected increased luminosity of the Sun is likely to accelerate the rate of surface weathering.

This will eventually cause most of the carbon dioxide in the atmosphere to be released into the Earth’s crust as carbonate.

When the concentration of carbon dioxide in the atmosphere drops below about 50 parts per million (tolerances vary among species), C3 photosynthesis will no longer be possible.

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Plate tectonics will very likely stop for lack of water to lubricate them. The lack of volcanoes pumping out carbon dioxide will cause the carbon cycle to cycle between 1 billion and 2 billion years into the future.

The terrestrial biosphere includes organic carbon in all organisms that live on land, both living and dead, as well as carbon stored in soil. About 500 gigatons of carbon are stored above ground in plants and other living organisms,

Organic carbon is the main component of all organisms that live on earth. Autotrophs obtain it from the air in the form of carbon dioxide and convert it into organic carbon, while heterotrophs receive carbon by consuming other organisms.

Since carbon input to the terrestrial biosphere depends on biotic factors, it follows a diurnal and seasonal cycle. In CO

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Measurement, this function is separated in the Keeling curve. It is strongest in the Northern Hemisphere because that hemisphere has more land mass than the Southern Hemisphere and thus more room for ecosystems to absorb and emit carbon.

Carbon leaves the terrestrial biosphere in several ways and over different time periods. Organic carbon is rapidly released into the atmosphere during combustion or respiration. It can also be exported to the ocean through rivers or remain trapped in the soil as inert carbon.

Carbon stored in soil can remain there for up to thousands of years before being washed away by erosion into rivers or released into the atmosphere by soil respiration. Between 1989 and 2008, soil respiration increased by about 0.1% per year.

, about 3 times more carbon than humans put into the atmosphere each year by burning fossil fuels (this does not inhibit the net transfer of carbon from the soil to the atmosphere, as respiration is largely offset by soil carbon inputs).

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There are a few plausible explanations for this hard, but the most likely explanation is that higher temperatures increased the rates of decomposition of soil organic matter, which increased CO flux

. The length of carbon sequestration in soil depends on local climatic conditions and thus changes with climate change.

The ocean can be conceptually divided into a surface layer within which the water is in frequent (daily to annual) contact with the atmosphere, and a deep layer below a typical mixed layer depth of a few hundred meters or less, within which the time between successive contacts can be centuries. Dissolved inorganic carbon (DIC) in the surface layer is rapidly exchanged with the atmosphere and maintains the balance. Partly because its DIC concentration is about 15% higher

But mainly due to its larger volume, the deep ocean contains much more carbon – it is the largest pool of actively circulating carbon in the world, containing 50 times more than the atmosphere

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— but the time frame for reaching equilibrium with the atmosphere is hundreds of years: the exchange of carbon between the two layers, driven by thermohaline circulation, is slow.

Carbon accumulates in the ocean mainly through the dissolution of atmospheric carbon dioxide, a small part of which is converted into carbonate. It can also flow into the ocean through rivers as dissolved organic carbon. Organisms convert it to organic carbon through photosynthesis, and it can be exchanged throughout the food chain or precipitated in the deeper, carbon-rich layers of the oceans as dead soft tissue or in shellfish as calcium carbonate. It circulates in this layer for a long time before being deposited as sediment or eventually returned to surface waters by thermohaline circulation.

Shifts the pH of the ocean toward neutral in a process called ocean acidification. Ocean absorption of CO

Is one of the most important forms of carbon fixation. The predicted rate of pH decrease could slow the biological precipitation of calcium carbonates, thereby reducing the ocean’s ability to absorb CO

Svs: Oco 2 Gridded Global Carbon Dioxide (co₂)

A diagram showing the relative sizes (in gigatons) of Earth’s major carbon stores. Cumulative changes (up to 2014) due to land use and fossil carbon emissions are included for comparison.

The geological component of the carbon cycle operates slowly compared to other parts of the global carbon cycle. It is one of the most important factors that determine the amount of carbon in the atmosphere and thus global temperatures.

Approximately 80% of the carbon stored in the geosphere is represented by limestone and its derivatives, which are formed by the sedimentation of calcium carbonate stored in the shells of marine organisms. The remaining 20% ​​is stored as kerogi

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