Chlorine cycle

Chlorine plays a large role in atmospheric cycling and climate, including, but not limited to chlorofluorocarbons (CFCs).[7] The major flux of chlorine into the troposphere comes from sea salt aerosol spray. Both organic and inorganic chlorine is transferred into the troposphere from the oceans.[2] Biomass combustion is another source of both organic and inorganic forms of chlorine to the troposphere from the terrestrial reservoir.[2] Typically, organic chlorine forms are highly un-reactive and will be transferred to the stratosphere from the troposphere. The major flux of chlorine from the troposphere is via surface deposition into water systems.

Part of a series on
Biogeochemical cycles
Water cycle Water cycle deep water cycle
Carbon cycle Global atmospheric terrestrial oceanic Sequestration carbon sink deep carbon cycle soil carbon mycorrhizal fungi Boreal forests
Nutrient cycle Hydrogen cycle Nitrogen cycle human impact nitrification nitrogen and lichens fixation assimilation Oxygen cycle Phosphorus cycle assimilation Sulfur cycle assimilation
Rock cycle Calcium cycle Silica cycle Carbonate–silicate cycle
Marine cycle Marine biogeochemical cycles Biological pump microbial loop viral shunt Calcareous ooze Siliceous ooze
Methane cycle Atmospheric methane Methane clathrate clathrate gun hypothesis Arctic methane emissions
Other cycles aluminum arsenic boron bromine cadmium chlorine chromium copper fluorine gold iodine iron lead lithium manganese mercury ozone–oxygen selenium vanadium zinc
Related topics Biogeochemistry geochemical cycle chemical cycling environmental chemistry Biosequestration Deep biosphere Ocean acidification acid rain Biogeochemical planetary boundaries
Research groups DAAC GEOTRACES IMBER NOBM SOLAS
Category

Oceans are the largest source of chlorine in the Earth's hydrosphere.[2] In the hydrosphere, chlorine exists primarily as chloride due to the high solubility of the Cl⁻ ion.[3] The majority of chlorine fluxes are within the hydrosphere due to chloride ions' solubility and reactivity within water systems.[2] The cryosphere is able to retain some chlorine deposited by rainfall and snow, but the majority is eluted into oceans.

The largest reservoir of chlorine resides in the lithosphere, where 2.2×10²² kg of global chlorine is found in Earth's mantle.[2] Volcanic eruptions will sporadically release high levels of chlorine as HCl into the troposphere, but the majority of the terrestrial chlorine flux comes from seawater sources mixing with the mantle.[2]

Organically bound chlorine is as abundant as chloride ions in terrestrial soil systems, or the pedosphere.[1] Discovery of multiple Cl-mediating genes in microorganisms and plants indicate that numerous biotic processes use chloride and produce organic chlorinated compounds, as well as many abiotic processes.[1][3][4][5] These chlorinated compounds can then be volatilized or leached out of soils, which makes the overall soil environment a global sink of chlorine.[1] Multiple anaerobic prokaryotes have been found to contain genes and show activity for chlorinated organic volatilization[8]

Chlorine's ability to completely dissociate in water is also why it is an essential electrolyte in many biological processes.[6] Chlorine, along with phosphorus, is the sixth most common element in organic matter.[1] Cells utilize chloride to balance pH and maintain turgor pressure at equilibrium. The high electrical conductivity of Cl⁻ ions are essential for neuron signalling in the brain and regulate many other essential functions in biology[9]

The depleting effects of chlorofluorocarbons (CFCs) on ozone over Antarctica has been studied extensively since the 1980s.[7] The low reactivity of CFCs allow it to reach the upper stratosphere, where it interacts with UV-C radiation and forms highly reactive chloride ions that interact with methane.[7] These highly reactive chlorine ions will also interact with volatile organic compounds to form other ozone depleting acids.[10]

Chlorine-36 is the radioactive isotope produced in many nuclear facilities as byproduct waste.[3] Its half-life of 3.01×10⁵ years, mobility in the pedosphere, and ability to be taken up by organisms has made it an isotope of high concern among researchers.[3] The high solubility and low reactiveness of ³⁶Cl⁻ is also has also made it a useful application for research of biogeochemical cycling of chlorine, as most research uses it as an isotope tracer[1][3][4][5][7]