Biogeochemical cycle (original) (raw)

Chemical transfer pathway between Earth's biological and non-biological parts

A biogeochemical cycle, or more generally a cycle of matter,[1] is the movement and transformation of chemical elements and compounds between living organisms, the atmosphere, and the Earth's crust. Major biogeochemical cycles include the carbon cycle, the nitrogen cycle and the water cycle. In each cycle, the chemical element or molecule is transformed and cycled by living organisms and through various geological forms and reservoirs, including the atmosphere, the soil and the oceans. It can be thought of as the pathway by which a chemical substance cycles (is turned over or moves through) the biotic compartment and the abiotic compartments of Earth. The biotic compartment is the biosphere and the abiotic compartments are the atmosphere, lithosphere and hydrosphere.

For example, in the carbon cycle, atmospheric carbon dioxide is absorbed by plants through photosynthesis, which converts it into organic compounds that are used by organisms for energy and growth. Carbon is then released back into the atmosphere through respiration and decomposition. Additionally, carbon is stored in fossil fuels and is released into the atmosphere through human activities such as burning fossil fuels. In the nitrogen cycle, atmospheric nitrogen is converted by plants into usable forms such as ammonia and nitrates through the process of nitrogen fixation. These compounds can be used by other organisms, and nitrogen is returned to the atmosphere through denitrification and other processes. In the water cycle, the universal solvent water evaporates from land and oceans to form clouds in the atmosphere, and then precipitates back to different parts of the planet. Precipitation can seep into the ground and become part of groundwater systems used by plants and other organisms, or can runoff the surface to form lakes and rivers. Subterranean water can then seep into the ocean along with river discharges, rich with dissolved and particulate organic matter and other nutrients.

There are biogeochemical cycles for many other elements, such as for oxygen, hydrogen, phosphorus, calcium, iron, sulfur, mercury and selenium. There are also cycles for molecules, such as water and silica. In addition there are macroscopic cycles such as the rock cycle, and human-induced cycles for synthetic compounds such as for polychlorinated biphenyls (PCBs). In some cycles there are geological reservoirs where substances can remain or be sequestered for long periods of time.

Biogeochemical cycles involve the interaction of biological, geological, and chemical processes. Biological processes include the influence of microorganisms, which are critical drivers of biogeochemical cycling. Microorganisms have the ability to carry out wide ranges of metabolic processes essential for the cycling of nutrients and chemicals throughout global ecosystems. Without microorganisms many of these processes would not occur, with significant impact on the functioning of land and ocean ecosystems and the planet's biogeochemical cycles as a whole. Changes to cycles can impact human health. The cycles are interconnected and play important roles regulating climate, supporting the growth of plants, phytoplankton and other organisms, and maintaining the health of ecosystems generally. Human activities such as burning fossil fuels and using large amounts of fertilizer can disrupt cycles, contributing to climate change, pollution, and other environmental problems.

Generalized biogeochemical cycle[2]

Simplified version of the nitrogen cycle

Energy flows directionally through ecosystems, entering as sunlight (or inorganic molecules for chemoautotrophs) and leaving as heat during the many transfers between trophic levels. However, the matter that makes up living organisms is conserved and recycled. The six most common elements associated with organic molecules — carbon, nitrogen, hydrogen, oxygen, phosphorus, and sulfur — take a variety of chemical forms and may exist for long periods in the atmosphere, on land, in water, or beneath the Earth's surface. Geologic processes, such as weathering, erosion, water drainage, and the subduction of the continental plates, all play a role in this recycling of materials. Because geology and chemistry have major roles in the study of this process, the recycling of inorganic matter between living organisms and their environment is called a biogeochemical cycle.[3]

The six aforementioned elements are used by organisms in a variety of ways. Hydrogen and oxygen are found in water and organic molecules, both of which are essential to life. Carbon is found in all organic molecules, whereas nitrogen is an important component of nucleic acids and proteins. Phosphorus is used to make nucleic acids and the phospholipids that comprise biological membranes. Sulfur is critical to the three-dimensional shape of proteins. The cycling of these elements is interconnected. For example, the movement of water is critical for leaching sulfur and phosphorus into rivers which can then flow into oceans. Minerals cycle through the biosphere between the biotic and abiotic components and from one organism to another.[4]

Ecological systems (ecosystems) have many biogeochemical cycles operating as a part of the system, for example, the water cycle, the carbon cycle, the nitrogen cycle, etc. All chemical elements occurring in organisms are part of biogeochemical cycles. In addition to being a part of living organisms, these chemical elements also cycle through abiotic factors of ecosystems such as water (hydrosphere), land (lithosphere), and/or the air (atmosphere).[5]

The living factors of the planet can be referred to collectively as the biosphere. All the nutrients — such as carbon, nitrogen, oxygen, phosphorus, and sulfur — used in ecosystems by living organisms are a part of a closed system; therefore, these chemicals are recycled instead of being lost and replenished constantly such as in an open system.[5]

The major parts of the biosphere are connected by the flow of chemical elements and compounds in biogeochemical cycles. In many of these cycles, the biota plays an important role. Matter from the Earth's interior is released by volcanoes. The atmosphere exchanges some compounds and elements rapidly with the biota and oceans. Exchanges of materials between rocks, soils, and the oceans are generally slower by comparison.[2]

The flow of energy in an ecosystem is an open system; the Sun constantly gives the planet energy in the form of light while it is eventually used and lost in the form of heat throughout the trophic levels of a food web. Carbon is used to make carbohydrates, fats, and proteins, the major sources of food energy. These compounds are oxidized to release carbon dioxide, which can be captured by plants to make organic compounds. The chemical reaction is powered by the light energy of sunshine.

Sunlight is required to combine carbon with hydrogen and oxygen into an energy source, but ecosystems in the deep sea, where no sunlight can penetrate, obtain energy from sulfur. Hydrogen sulfide near hydrothermal vents can be utilized by organisms such as the giant tube worm. In the sulfur cycle, sulfur can be forever recycled as a source of energy. Energy can be released through the oxidation and reduction of sulfur compounds (e.g., oxidizing elemental sulfur to sulfite and then to sulfate).

Although the Earth constantly receives energy from the Sun, its chemical composition is essentially fixed, as the additional matter is only occasionally added by meteorites. Because this chemical composition is not replenished like energy, all processes that depend on these chemicals must be recycled. These cycles include both the living biosphere and the nonliving lithosphere, atmosphere, and hydrosphere.

Biogeochemical cycles can be contrasted with geochemical cycles. The latter deals only with crustal and subcrustal reservoirs even though some process from both overlap.

Beach scene simultaneously showing the atmosphere (air), hydrosphere (ocean) and lithosphere (ground)

Some roles of marine organisms in biogeochemical cycling in the Southern Ocean[7]

The global ocean covers more than 70% of the Earth's surface and is remarkably heterogeneous. Marine productive areas, and coastal ecosystems comprise a minor fraction of the ocean in terms of surface area, yet have an enormous impact on global biogeochemical cycles carried out by microbial communities, which represent 90% of the ocean's biomass.[8] Work in recent years has largely focused on cycling of carbon and macronutrients such as nitrogen, phosphorus, and silicate: other important elements such as sulfur or trace elements have been less studied, reflecting associated technical and logistical issues.[9] Increasingly, these marine areas, and the taxa that form their ecosystems, are subject to significant anthropogenic pressure, impacting marine life and recycling of energy and nutrients.[10][11][12] A key example is that of cultural eutrophication, where agricultural runoff leads to nitrogen and phosphorus enrichment of coastal ecosystems, greatly increasing productivity resulting in algal blooms, deoxygenation of the water column and seabed, and increased greenhouse gas emissions,[13] with direct local and global impacts on nitrogen and carbon cycles. However, the runoff of organic matter from the mainland to coastal ecosystems is just one of a series of pressing threats stressing microbial communities due to global change. Climate change has also resulted in changes in the cryosphere, as glaciers and permafrost melt, resulting in intensified marine stratification, while shifts of the redox-state in different biomes are rapidly reshaping microbial assemblages at an unprecedented rate.[14][15][16][17][9]

Global change is, therefore, affecting key processes including primary productivity, CO2 and N2 fixation, organic matter respiration/remineralization, and the sinking and burial deposition of fixed CO2.[17] In addition to this, oceans are experiencing an acidification process, with a change of ~0.1 pH units between the pre-industrial period and today, affecting carbonate/bicarbonate buffer chemistry. In turn, acidification has been reported to impact planktonic communities, principally through effects on calcifying taxa.[18] There is also evidence for shifts in the production of key intermediary volatile products, some of which have marked greenhouse effects (e.g., N2O and CH4, reviewed by Breitburg in 2018,[15] due to the increase in global temperature, ocean stratification and deoxygenation, driving as much as 25 to 50% of nitrogen loss from the ocean to the atmosphere in the so-called oxygen minimum zones[19] or anoxic marine zones,[20] driven by microbial processes. Other products, that are typically toxic for the marine nekton, including reduced sulfur species such as H2S, have a negative impact for marine resources like fisheries and coastal aquaculture. While global change has accelerated, there has been a parallel increase in awareness of the complexity of marine ecosystems, and especially the fundamental role of microbes as drivers of ecosystem functioning.[16][9]

Microorganisms drive much of the biogeochemical cycling in the earth system.[21][22]

The chemicals are sometimes held for long periods of time in one place. This place is called a reservoir, which, for example, includes such things as coal deposits that are storing carbon for a long period of time.[23] When chemicals are held for only short periods of time, they are being held in exchange pools. Examples of exchange pools include plants and animals.[23]

Plants and animals utilize carbon to produce carbohydrates, fats, and proteins, which can then be used to build their internal structures or to obtain energy. Plants and animals temporarily use carbon in their systems and then release it back into the air or surrounding medium. Generally, reservoirs are abiotic factors whereas exchange pools are biotic factors. Carbon is held for a relatively short time in plants and animals in comparison to coal deposits. The amount of time that a chemical is held in one place is called its residence time or turnover time (also called the renewal time or exit age).[23]

Basic one-box model

Box models are widely used to model biogeochemical systems.[24][25] Box models are simplified versions of complex systems, reducing them to boxes (or storage reservoirs) for chemical materials, linked by material fluxes (flows). Simple box models have a small number of boxes with properties, such as volume, that do not change with time. The boxes are assumed to behave as if they were mixed homogeneously.[25] These models are often used to derive analytical formulas describing the dynamics and steady-state abundance of the chemical species involved.

The diagram at the right shows a basic one-box model. The reservoir contains the amount of material M under consideration, as defined by chemical, physical or biological properties. The source Q is the flux of material into the reservoir, and the sink S is the flux of material out of the reservoir. The budget is the check and balance of the sources and sinks affecting material turnover in a reservoir. The reservoir is in a steady state if Q = S, that is, if the sources balance the sinks and there is no change over time.[25]

The residence or turnover time is the average time material spends resident in the reservoir. If the reservoir is in a steady state, this is the same as the time it takes to fill or drain the reservoir. Thus, if τ is the turnover time, then τ = M/S.[25] The equation describing the rate of change of content in a reservoir is

d M d t = Q − S = Q − M τ . {\displaystyle {\frac {dM}{dt}}=Q-S=Q-{\frac {M}{\tau }}.} {\displaystyle {\frac {dM}{dt}}=Q-S=Q-{\frac {M}{\tau }}.}

When two or more reservoirs are connected, the material can be regarded as cycling between the reservoirs, and there can be predictable patterns to the cyclic flow.[25] More complex multibox models are usually solved using numerical techniques.

Simple three box model. Simplified budget of ocean carbon flows[26]

Measurement units

Global biogeochemical box models usually measure:

The diagram on the left shows a simplified budget of ocean carbon flows. It is composed of three simple interconnected box models, one for the euphotic zone, one for the ocean interior or dark ocean, and one for ocean sediments. In the euphotic zone, net phytoplankton production is about 50 Pg C each year. About 10 Pg is exported to the ocean interior while the other 40 Pg is respired. Organic carbon degradation occurs as particles (marine snow) settle through the ocean interior. Only 2 Pg eventually arrives at the seafloor, while the other 8 Pg is respired in the dark ocean. In sediments, the time scale available for degradation increases by orders of magnitude with the result that 90% of the organic carbon delivered is degraded and only 0.2 Pg C yr−1 is eventually buried and transferred from the biosphere to the geosphere.[26]

More complex model with many interacting boxes. Export and burial rates of terrestrial organic carbon in the ocean[27]

The diagram on the right shows a more complex model with many interacting boxes. Reservoir masses here represents carbon stocks, measured in Pg C. Carbon exchange fluxes, measured in Pg C yr−1, occur between the atmosphere and its two major sinks, the land and the ocean. The black numbers and arrows indicate the reservoir mass and exchange fluxes estimated for the year 1750, just before the Industrial Revolution. The red arrows (and associated numbers) indicate the annual flux changes due to anthropogenic activities, averaged over the 2000–2009 time period. They represent how the carbon cycle has changed since 1750. Red numbers in the reservoirs represent the cumulative changes in anthropogenic carbon since the start of the Industrial Period, 1750–2011.[28][29][27]

Fast and slow cycles

[edit]

The fast cycle operates through the biosphere, including exchanges between land, atmosphere, and oceans. The yellow numbers are natural fluxes of carbon in billions of tons (gigatons) per year. Red are human contributions and white are stored carbon.[30]

The slow cycle operates through rocks, including volcanic and tectonic activity

There are fast and slow biogeochemical cycles. Fast cycle operate in the biosphere and slow cycles operate in rocks. Fast or biological cycles can complete within years, moving substances from atmosphere to biosphere, then back to the atmosphere. Slow or geological cycles can take millions of years to complete, moving substances through the Earth's crust between rocks, soil, ocean and atmosphere.[31]

As an example, the fast carbon cycle is illustrated in the diagram below on the left. This cycle involves relatively short-term biogeochemical processes between the environment and living organisms in the biosphere. It includes movements of carbon between the atmosphere and terrestrial and marine ecosystems, as well as soils and seafloor sediments. The fast cycle includes annual cycles involving photosynthesis and decadal cycles involving vegetative growth and decomposition. The reactions of the fast carbon cycle to human activities will determine many of the more immediate impacts of climate change.[32][33][34][35]

The slow cycle is illustrated in the diagram above on the right. It involves medium to long-term geochemical processes belonging to the rock cycle. The exchange between the ocean and atmosphere can take centuries, and the weathering of rocks can take millions of years. Carbon in the ocean precipitates to the ocean floor where it can form sedimentary rock and be subducted into the Earth's mantle. Mountain building processes result in the return of this geologic carbon to the Earth's surface. There the rocks are weathered and carbon is returned to the atmosphere by degassing and to the ocean by rivers. Other geologic carbon returns to the ocean through the hydrothermal emission of calcium ions. In a given year between 10 and 100 million tonnes of carbon moves around this slow cycle. This includes volcanoes returning geologic carbon directly to the atmosphere in the form of carbon dioxide. However, this is less than one percent of the carbon dioxide put into the atmosphere by burning fossil fuels.[31][32]

The terrestrial subsurface is the largest reservoir of carbon on earth, containing 14–135 Pg of carbon[36] and 2–19% of all biomass.[37] Microorganisms drive organic and inorganic compound transformations in this environment and thereby control biogeochemical cycles. Current knowledge of the microbial ecology of the subsurface is primarily based on 16S ribosomal RNA (rRNA) gene sequences. Recent estimates show that <8% of 16S rRNA sequences in public databases derive from subsurface organisms[38] and only a small fraction of those are represented by genomes or isolates. Thus, there is remarkably little reliable information about microbial metabolism in the subsurface. Further, little is known about how organisms in subsurface ecosystems are metabolically interconnected. Some cultivation-based studies of syntrophic consortia[39][40][41] and small-scale metagenomic analyses of natural communities[42][43][44] suggest that organisms are linked via metabolic handoffs: the transfer of redox reaction products of one organism to another. However, no complex environments have been dissected completely enough to resolve the metabolic interaction networks that underpin them. This restricts the ability of biogeochemical models to capture key aspects of the carbon and other nutrient cycles.[45] New approaches such as genome-resolved metagenomics, an approach that can yield a comprehensive set of draft and even complete genomes for organisms without the requirement for laboratory isolation[42][46][47] have the potential to provide this critical level of understanding of biogeochemical processes.[48]

Some of the more well-known biogeochemical cycles are shown below:

Many biogeochemical cycles are currently being studied for the first time. Climate change and human impacts are drastically changing the speed, intensity, and balance of these relatively unknown cycles, which include:

Biogeochemical cycles always involve active equilibrium states: a balance in the cycling of the element between compartments. However, overall balance may involve compartments distributed on a global scale.

As biogeochemical cycles describe the movements of substances on the entire globe, the study of these is inherently multidisciplinary. The carbon cycle may be related to research in ecology and atmospheric sciences.[53] Biochemical dynamics would also be related to the fields of geology and pedology.[54]

  1. ^ "CK12-Foundation". flexbooks.ck12.org. Retrieved 2022-03-21.
  2. ^ a b Moses, M. (2012) Biogeochemical cycles Archived 2021-11-22 at the Wayback Machine. Encyclopedia of Earth.
  3. ^ Biogeochemical Cycles Archived 2021-09-27 at the Wayback Machine, OpenStax, 9 May 2019. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  4. ^ Fisher M. R. (Ed.) (2019) Environmental Biology, 3.2 Biogeochemical Cycles Archived 2021-09-27 at the Wayback Machine, OpenStax. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  5. ^ a b "Biogeochemical Cycles". The Environmental Literacy Council. Archived from the original on 30 April 2015. Retrieved 20 November 2017.
  6. ^ Avelar, S., van der Voort, T.S. and Eglinton, T.I. (2017) "Relevance of carbon stocks of marine sediments for national greenhouse gas inventories of maritime nations". Carbon balance and management, 12(1): 10.doi:10.1186/s13021-017-0077-x. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License. Archived 2017-10-16 at the Wayback Machine.
  7. ^ Henley, Sian F.; Cavan, Emma L.; Fawcett, Sarah E.; Kerr, Rodrigo; Monteiro, Thiago; Sherrell, Robert M.; Bowie, Andrew R.; Boyd, Philip W.; Barnes, David K. A.; Schloss, Irene R.; Marshall, Tanya; Flynn, Raquel; Smith, Shantelle (2020). "Changing Biogeochemistry of the Southern Ocean and Its Ecosystem Implications". Frontiers in Marine Science. 7. doi:10.3389/fmars.2020.00581. hdl:11336/128446. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  8. ^ Alexander, Vera; Miloslavich, Patricia; Yarincik, Kristen (2011). "The Census of Marine Life—evolution of worldwide marine biodiversity research". Marine Biodiversity. 41 (4): 545–554. Bibcode:2011MarBd..41..545A. doi:10.1007/s12526-011-0084-1. S2CID 25888475.
  9. ^ a b c Murillo, Alejandro A.; Molina, Verónica; Salcedo-Castro, Julio; Harrod, Chris (2019). "Editorial: Marine Microbiome and Biogeochemical Cycles in Marine Productive Areas". Frontiers in Marine Science. 6. doi:10.3389/fmars.2019.00657. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  10. ^ Galton, D. (1884) 10th Meeting: report of the royal commission on metropolitan sewage Archived 2021-09-24 at the Wayback Machine. J. Soc. Arts, 33: 290.
  11. ^ Hasler, Arthur D. (1969). "Cultural Eutrophication is Reversible". BioScience. 19 (5): 425–431. doi:10.2307/1294478. JSTOR 1294478.
  12. ^ Jickells, T. D.; Buitenhuis, E.; Altieri, K.; Baker, A. R.; Capone, D.; Duce, R. A.; Dentener, F.; Fennel, K.; Kanakidou, M.; Laroche, J.; Lee, K.; Liss, P.; Middelburg, J. J.; Moore, J. K.; Okin, G.; Oschlies, A.; Sarin, M.; Seitzinger, S.; Sharples, J.; Singh, A.; Suntharalingam, P.; Uematsu, M.; Zamora, L. M. (2017). "A reevaluation of the magnitude and impacts of anthropogenic atmospheric nitrogen inputs on the ocean". Global Biogeochemical Cycles. 31 (2): 289. Bibcode:2017GBioC..31..289J. doi:10.1002/2016GB005586. hdl:1874/348077. S2CID 5158406.
  13. ^ Bouwman, A. F.; Van Drecht, G.; Knoop, J. M.; Beusen, A. H. W.; Meinardi, C. R. (2005). "Exploring changes in river nitrogen export to the world's oceans". Global Biogeochemical Cycles. 19 (1). Bibcode:2005GBioC..19.1002B. doi:10.1029/2004GB002314. S2CID 131163837.
  14. ^ Altieri, Andrew H.; Gedan, Keryn B. (2015). "Climate change and dead zones". Global Change Biology. 21 (4): 1395–1406. Bibcode:2015GCBio..21.1395A. doi:10.1111/gcb.12754. PMID 25385668. S2CID 24002134.
  15. ^ a b Breitburg, Denise; Levin, Lisa A.; Oschlies, Andreas; Grégoire, Marilaure; Chavez, Francisco P.; Conley, Daniel J.; Garçon, Véronique; Gilbert, Denis; Gutiérrez, Dimitri; Isensee, Kirsten; Jacinto, Gil S.; Limburg, Karin E.; Montes, Ivonne; Naqvi, S. W. A.; Pitcher, Grant C.; Rabalais, Nancy N.; Roman, Michael R.; Rose, Kenneth A.; Seibel, Brad A.; Telszewski, Maciej; Yasuhara, Moriaki; Zhang, Jing (2018). "Declining oxygen in the global ocean and coastal waters". Science. 359 (6371): eaam7240. Bibcode:2018Sci...359M7240B. doi:10.1126/science.aam7240. PMID 29301986. S2CID 206657115.
  16. ^ a b Cavicchioli, Ricardo; et al. (2019). "Scientists' warning to humanity: Microorganisms and climate change". Nature Reviews Microbiology. 17 (9): 569–586. doi:10.1038/s41579-019-0222-5. PMC 7136171. PMID 31213707.
  17. ^ a b Hutchins, David A.; Jansson, Janet K.; Remais, Justin V.; Rich, Virginia I.; Singh, Brajesh K.; Trivedi, Pankaj (2019). "Climate change microbiology — problems and perspectives". Nature Reviews Microbiology. 17 (6): 391–396. doi:10.1038/s41579-019-0178-5. PMID 31092905. S2CID 155102440.
  18. ^ Stillman, Jonathon H.; Paganini, Adam W. (2015). "Biochemical adaptation to ocean acidification". Journal of Experimental Biology. 218 (12): 1946–1955. doi:10.1242/jeb.115584. PMID 26085671. S2CID 13071345.
  19. ^ Bertagnolli, Anthony D.; Stewart, Frank J. (2018). "Microbial niches in marine oxygen minimum zones". Nature Reviews Microbiology. 16 (12): 723–729. doi:10.1038/s41579-018-0087-z. PMID 30250271. S2CID 52811177.
  20. ^ Ulloa, O.; Canfield, D. E.; Delong, E. F.; Letelier, R. M.; Stewart, F. J. (2012). "Microbial oceanography of anoxic oxygen minimum zones". Proceedings of the National Academy of Sciences. 109 (40): 15996–16003. Bibcode:2012PNAS..10915996U. doi:10.1073/pnas.1205009109. PMC 3479542. PMID 22967509. S2CID 6630698.
  21. ^ Falkowski, P. G.; Fenchel, T.; Delong, E. F. (2008). "The Microbial Engines That Drive Earth's Biogeochemical Cycles". Science. 320 (5879): 1034–1039. Bibcode:2008Sci...320.1034F. doi:10.1126/science.1153213. PMID 18497287. S2CID 2844984.
  22. ^ Zakem, Emily J.; Polz, Martin F.; Follows, Michael J. (2020). "Redox-informed models of global biogeochemical cycles". Nature Communications. 11 (1): 5680. Bibcode:2020NatCo..11.5680Z. doi:10.1038/s41467-020-19454-w. PMC 7656242. PMID 33173062. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  23. ^ a b c Baedke, Steve J.; Fichter, Lynn S. "Biogeochemical Cycles: Carbon Cycle". Supplemental Lecture Notes for Geol 398. James Madison University. Archived from the original on 1 December 2017. Retrieved 20 November 2017.
  24. ^ Sarmiento, J.L.; Toggweiler, J.R. (1984). "A new model for the role of the oceans in determining atmospheric P CO 2". Nature. 308 (5960): 621–24. Bibcode:1984Natur.308..621S. doi:10.1038/308621a0. S2CID 4312683.
  25. ^ a b c d e Bianchi, Thomas (2007) Biogeochemistry of Estuaries Archived 2021-09-25 at the Wayback Machine page 9, Oxford University Press. ISBN 9780195160826.
  26. ^ a b Middelburg, J.J.(2019) Marine carbon biogeochemistry: a primer for earth system scientists, page 5, Springer Nature. ISBN 9783030108229. doi:10.1007/978-3-030-10822-9. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  27. ^ a b Kandasamy, Selvaraj; Nagender Nath, Bejugam (2016). "Perspectives on the Terrestrial Organic Matter Transport and Burial along the Land-Deep Sea Continuum: Caveats in Our Understanding of Biogeochemical Processes and Future Needs". Frontiers in Marine Science. 3. doi:10.3389/fmars.2016.00259. S2CID 30408500. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  28. ^ Sarmiento, Jorge L.; Gruber, Nicolas (2002). "Sinks for Anthropogenic Carbon". Physics Today. 55 (8): 30–36. Bibcode:2002PhT....55h..30S. doi:10.1063/1.1510279. S2CID 128553441.
  29. ^ Chhabra, Abha (2013). "Carbon and Other Biogeochemical Cycles". Intergovernmental Panel on Climate Change. doi:10.13140/2.1.1081.8883.
  30. ^ Riebeek, Holli (16 June 2011). "The Carbon Cycle". Earth Observatory. NASA. Archived from the original on 5 March 2016. Retrieved 5 April 2018.
  31. ^ a b Libes, Susan M. (2015). Blue planet: The role of the oceans in nutrient cycling, maintain the atmosphere system, and modulating climate change Archived 2021-01-20 at the Wayback Machine In: Routledge Handbook of Ocean Resources and Management, Routledge, pages 89–107. ISBN 9781136294822.
  32. ^ a b Bush, Martin J. (2020). Climate Change and Renewable Energy. pp. 109–141. doi:10.1007/978-3-030-15424-0_3. ISBN 978-3-030-15423-3. S2CID 210305910. Archived from the original on 2021-09-27. Retrieved 2021-09-27.
  33. ^ Rothman, D. H. (2002). "Atmospheric carbon dioxide levels for the last 500 million years". Proceedings of the National Academy of Sciences. 99 (7): 4167–4171. Bibcode:2002PNAS...99.4167R. doi:10.1073/pnas.022055499. PMC 123620. PMID 11904360.
  34. ^ Carpinteri, Alberto; Niccolini, Gianni (2019). "Correlation between the Fluctuations in Worldwide Seismicity and Atmospheric Carbon Pollution". Sci. 1: 17. doi:10.3390/sci1010017. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  35. ^ Rothman, Daniel (January 2015). "Earth's carbon cycle: A mathematical perspective". Bulletin of the American Mathematical Society. 52 (1): 47–64. doi:10.1090/S0273-0979-2014-01471-5. hdl:1721.1/97900. ISSN 0273-0979. Archived from the original on 2021-11-22. Retrieved 2021-09-27.
  36. ^ McMahon, Sean; Parnell, John (2014). "Weighing the deep continental biosphere". FEMS Microbiology Ecology. 87 (1): 113–120. Bibcode:2014FEMME..87..113M. doi:10.1111/1574-6941.12196. PMID 23991863. S2CID 9491320.
  37. ^ Kallmeyer, J.; Pockalny, R.; Adhikari, R. R.; Smith, D. C.; d'Hondt, S. (2012). "Global distribution of microbial abundance and biomass in subseafloor sediment". Proceedings of the National Academy of Sciences. 109 (40): 16213–16216. doi:10.1073/pnas.1203849109. PMC 3479597. PMID 22927371.
  38. ^ Schloss, Patrick D.; Girard, Rene A.; Martin, Thomas; Edwards, Joshua; Thrash, J. Cameron (2016). "Status of the Archaeal and Bacterial Census: An Update". mBio. 7 (3). doi:10.1128/mBio.00201-16. PMC 4895100. PMID 27190214.
  39. ^ Abreu, Nicole A.; Taga, Michiko E. (2016). "Decoding molecular interactions in microbial communities". FEMS Microbiology Reviews. 40 (5): 648–663. doi:10.1093/femsre/fuw019. PMC 5007284. PMID 27417261.
  40. ^ Bosse, Magnus; Heuwieser, Alexander; Heinzel, Andreas; Nancucheo, Ivan; Melo Barbosa Dall'Agnol, Hivana; Lukas, Arno; Tzotzos, George; Mayer, Bernd (2015). "Interaction networks for identifying coupled molecular processes in microbial communities". BioData Mining. 8: 21. doi:10.1186/s13040-015-0054-4. PMC 4502522. PMID 26180552.
  41. ^ Braker, Gesche; Dörsch, Peter; Bakken, Lars R. (2012). "Genetic characterization of denitrifier communities with contrasting intrinsic functional traits". FEMS Microbiology Ecology. 79 (2): 542–554. Bibcode:2012FEMME..79..542B. doi:10.1111/j.1574-6941.2011.01237.x. PMID 22092293.
  42. ^ a b Hug, Laura A.; Thomas, Brian C.; Sharon, Itai; Brown, Christopher T.; Sharma, Ritin; Hettich, Robert L.; Wilkins, Michael J.; Williams, Kenneth H.; Singh, Andrea; Banfield, Jillian F. (2016). "Critical biogeochemical functions in the subsurface are associated with bacteria from new phyla and little studied lineages". Environmental Microbiology. 18 (1): 159–173. Bibcode:2016EnvMi..18..159H. doi:10.1111/1462-2920.12930. PMID 26033198. S2CID 43160538. Archived from the original on 2021-09-27. Retrieved 2021-09-27.
  43. ^ McCarren, J.; Becker, J. W.; Repeta, D. J.; Shi, Y.; Young, C. R.; Malmstrom, R. R.; Chisholm, S. W.; Delong, E. F. (2010). "Microbial community transcriptomes reveal microbes and metabolic pathways associated with dissolved organic matter turnover in the sea". Proceedings of the National Academy of Sciences. 107 (38): 16420–16427. doi:10.1073/pnas.1010732107. PMC 2944720. PMID 20807744.
  44. ^ Embree, Mallory; Liu, Joanne K.; Al-Bassam, Mahmoud M.; Zengler, Karsten (2015). "Networks of energetic and metabolic interactions define dynamics in microbial communities". Proceedings of the National Academy of Sciences. 112 (50): 15450–15455. Bibcode:2015PNAS..11215450E. doi:10.1073/pnas.1506034112. PMC 4687543. PMID 26621749.
  45. ^ Long, Philip E.; Williams, Kenneth H.; Hubbard, Susan S.; Banfield, Jillian F. (2016). "Microbial Metagenomics Reveals Climate-Relevant Subsurface Biogeochemical Processes". Trends in Microbiology. 24 (8): 600–610. doi:10.1016/j.tim.2016.04.006. PMID 27156744. S2CID 3983278.
  46. ^ Eren, A. Murat; Esen, Özcan C.; Quince, Christopher; Vineis, Joseph H.; Morrison, Hilary G.; Sogin, Mitchell L.; Delmont, Tom O. (2015). "Anvi'o: An advanced analysis and visualization platform for 'omics data". PeerJ. 3: e1319. doi:10.7717/peerj.1319. PMC 4614810. PMID 26500826.
  47. ^ Alneberg, Johannes; Bjarnason, Brynjar Smári; De Bruijn, Ino; Schirmer, Melanie; Quick, Joshua; Ijaz, Umer Z.; Lahti, Leo; Loman, Nicholas J.; Andersson, Anders F.; Quince, Christopher (2014). "Binning metagenomic contigs by coverage and composition". Nature Methods. 11 (11): 1144–1146. doi:10.1038/nmeth.3103. PMID 25218180. S2CID 24696869.
  48. ^ Anantharaman, Karthik; Brown, Christopher T.; Hug, Laura A.; Sharon, Itai; Castelle, Cindy J.; Probst, Alexander J.; Thomas, Brian C.; Singh, Andrea; Wilkins, Michael J.; Karaoz, Ulas; Brodie, Eoin L.; Williams, Kenneth H.; Hubbard, Susan S.; Banfield, Jillian F. (2016). "Thousands of microbial genomes shed light on interconnected biogeochemical processes in an aquifer system". Nature Communications. 7: 13219. Bibcode:2016NatCo...713219A. doi:10.1038/ncomms13219. PMC 5079060. PMID 27774985. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License Archived 2017-10-16 at the Wayback Machine.
  49. ^ "Mercury Cycling in the Environment". Wisconsin Water Science Center. United States Geological Survey. 10 January 2013. Archived from the original on 11 April 2021. Retrieved 20 November 2017.
  50. ^ Organic contaminants that leave traces : sources, transport and fate. Ifremer. 2006. pp. 22–23. ISBN 9782759200139.
  51. ^ Galy, Valier; Peucker-Ehrenbrink, Bernhard; Eglinton, Timothy (2015). "Global carbon export from the terrestrial biosphere controlled by erosion". Nature. 521 (7551): 204–207. Bibcode:2015Natur.521..204G. doi:10.1038/nature14400. PMID 25971513. S2CID 205243485.
  52. ^ Hedges, J.I; Oades, J.M (1997). "Comparative organic geochemistries of soils and marine sediments". Organic Geochemistry. 27 (7–8): 319–361. Bibcode:1997OrGeo..27..319H. doi:10.1016/S0146-6380(97)00056-9.
  53. ^ McGuire, 1A. D.; Lukina, N. V. (2007). "Biogeochemical cycles" (PDF). In Groisman, P.; Bartalev, S. A.; NEESPI Science Plan Development Team (eds.). Northern Eurasia earth science partnership initiative (NEESPI), Science plan overview. Global Planetary Change. Vol. 56. pp. 215–234. Archived (PDF) from the original on 5 March 2016. Retrieved 20 November 2017.{{[cite book](/wiki/Template:Cite%5Fbook "Template:Cite book")}}: CS1 maint: numeric names: authors list (link)
  54. ^ "Distributed Active Archive Center for Biogeochemical Dynamics". daac.ornl.gov. Oak Ridge National Laboratory. Archived from the original on 11 February 2011. Retrieved 20 November 2017.