Manganese cycle

Last updated
Manganese cycles through the lithosphere, the hydrosphere, and the atmosphere. Arrows show processes and direction of transport. Global manganese cycle jpeg.jpg
Manganese cycles through the lithosphere, the hydrosphere, and the atmosphere. Arrows show processes and direction of transport.

The manganese cycle is the biogeochemical cycle of manganese through the atmosphere, hydrosphere, biosphere and lithosphere. There are bacteria that oxidise manganese to insoluble oxides, and others that reduce it to Mn2+ in order to use it. [1]

Contents

Manganese is a heavy metal that comprises about 0.1% of the Earth's crust and a necessary element for biological processes. It is cycled through the Earth in similar ways to iron, but with distinct redox pathways. Human activities have impacted the fluxes of manganese among the different spheres of the Earth.

Global manganese cycle

Manganese is a necessary element for biological functions such as photosynthesis, and some manganese oxidizing bacteria utilize this element in anoxic environments. [2] [3] Movement of manganese (Mn) among the global "spheres" (described below) is mediated by both physical and biological processes. Manganese in the lithosphere enters the hydrosphere from erosion and dissolution of bedrock in rivers, in solution it then makes its way into the ocean. Once in the ocean, Mn can form minerals and sink to the ocean floor where the solid phase is buried. The global manganese cycle is being altered by anthropogenic influences, such as mining and mineral processing for industrial use, as well as through the burning of fossil fuels. [4]

Lithosphere

Manganese precipitates in soils in the form of manganese-iron oxide minerals, which promote nutrient and organic matter accumulation due to their high surface area. Soilprofile.PNG
Manganese precipitates in soils in the form of manganese-iron oxide minerals, which promote nutrient and organic matter accumulation due to their high surface area.

Manganese is the tenth most abundant metal in the Earth's crust, making up approximately 0.1% of the total composition, or about 0.019 mol kg−1, which is found mostly in the oceanic crust. [5] [6]

Crust

Manganese (Mn) commonly precipitates in igneous rocks in the form of early-stage crystalline minerals, which, once exposed to water and/or oxygen, are highly soluble and easily oxidized to form Mn oxides on the surfaces of rocks. [7] Dendritic crystals rich in Mn form when microbes reprecipitate the Mn from the rocks on which they develop onto the surface after utilizing the Mn for their metabolism. For certain cyanobacteria found on desert varnish samples, for example, it has been found that manganese is used as a catalytic antioxidant to facilitate survival in the harsh sunlight and water conditions they face on desert rock surfaces. [8]

Soil

Manganese is an important soil micronutrient for plant growth, playing an essential role as a catalyst in the oxygen-evolving complex of photosystem II, a photosynthetic pathway. [6] Soil fungi in particular have been found to oxidize the reduced, soluble form of manganese (Mn2+) under anaerobic conditions, and may reprecipitate it as manganese oxides (Mn+3 to Mn+7) under aerobic conditions, where the preferred metabolic pathway typically involves the utilization of oxygen. [9] [10] Although not all iron-reducing bacteria have the capability of reducing manganese, there is overlap in the taxa that can perform both metabolisms; these organisms are very common in a range of environmental conditions. Challenges however persist in isolating these microbes in cultures. [11] [12]

Depending on the pH, organic substrate availability, and oxygen concentration, Mn can either behave as an oxidation catalyst or an electron receptor. [13] Though much of the total Mn that is cycled in soil is biologically-mediated, some inorganic reactions also contribute to Mn oxidation or precipitation of Mn oxides. The reduction potential (pe) and pH are two known constraints on the solubility of Mn in soils. [13] As pH increases, Mn speciation becomes less sensitive to variations in pe. In acidic (pH = 5) soils with high reduction potentials (pe > 8), the forms of Mn are mostly reducible, with exchangeable and soluble Mn decreasing dramatically in concentration with increases in pe. [13] Mn is also found in inorganic chelation complexes, where Mn forms coordinate bonds with SO42-, HCO3−, and Cl− ions. These complexes are important for organic matter stabilization in soils, as they have high surface areas and interact with organic matter through adsorption. [14]

Hydrosphere

Manganese enters the ocean as dust or runoff in the form of dissolved Mn (II). It leaves the ocean via diffusion. This dissolved Mn is oxidized and reduced by organisms, and then sinks to the ocean floor. As it sinks it undergoes aggregation or scavenging. From the ocean floor, Mn is lost through burial, and is inputted into the ocean cycle by sediment diffusion and hydrothermal vents. Mn Cycle Diagram.png
Manganese enters the ocean as dust or runoff in the form of dissolved Mn (II). It leaves the ocean via diffusion. This dissolved Mn is oxidized and reduced by organisms, and then sinks to the ocean floor. As it sinks it undergoes aggregation or scavenging. From the ocean floor, Mn is lost through burial, and is inputted into the ocean cycle by sediment diffusion and hydrothermal vents.

Iron (Fe) and Manganese (Mn) similarities in their respective cycles and are often studied together. Both have similar sources in the hydrosphere, which are hydrothermal vent fluxes, [16] dust inputs, [17] and weathering of rocks. [18] [19] The major removal of Mn from the ocean involves similar processes to Fe as well, with the most abundant removal from the hydrosphere via biological uptake, [20] oxidative precipitation, [21] and scavenging. [22] Microorganisms oxidize the bioavailable Mn(II) to form Mn(IV), an insoluble manganese oxide that aggregates to form particulate matter that can then sink to the ocean floor. [23] Manganese is important in aquatic ecosystems for photosynthesis and other biological functions. [2]

Freshwater and estuary

Advection from tidal flows re-suspends estuary beds and can unearth manganese. [24] The particulate manganese is dissolved via reduction that forms Mn (II), adding it to the internal cycle of manganese in organisms in the ecosystem. Estuary biogeochemistry is heavily influenced by tidal oscillations, temperature, and pH changes, and thus the manganese input into the internal cycling is variable. [24] Mn in rivers and streams typically has a lower residence time than estuaries, and a large majority of the Mn is soluble Mn (II). [25] In these freshwater ecosystems, the manganese cycling is depended on sediment fluxes that provide an influx of Mn into the system. Oxidation of Mn (II) from sediment drives the redox reactions that fuel the biogeochemical processes with Mn, as well as Mn reducing microbes. [26]

Marine

In the ocean, different patterns of manganese cycling are seen. In the photic zone, there is a decrease in Mn particulate formation during the daytime, as rates of microbially catalyzed oxidation decrease and photo-dissolution of Mn oxides increases. [26] The GEOTRACES program has led the production of the first global manganese model, in which predictions of global manganese distribution can be made. [27] This global model found strong removal rates of Mn as water moves from the Atlantic Ocean surface to the North Atlantic deep water resulting in Mn depletion in water moving southward along the thermohaline conveyor. [26] Overall, when looking at organism interactions with manganese, it is known that redox reactions play a key role, as well as that Mn has important biological functions, however far less is known about uptake and remineralization processes such as with iron. [26]

Early Earth

Terrestrial manganese has existed since the formation of Earth around 4.6 Ga. [28] The Sun and the Solar System formed during the collapse of a molecular cloud populated with many trace metals, including manganese. [29] The chemical composition of the molecular cloud determined the composition of the many celestial bodies that form within it. [29] Nearby supernova explosions populated the cloud with manganese; the most common manganese-forming supernovae are Type Ia supernovae. [29] [30]  

The early Earth contained very little free oxygen (O2) until the Great Oxygenation Event around 2.35 Ga. [31] [32] [33] [34] [35] Without O2, redox cycling of Mn was limited. Instead, soluble Mn(II) was only released into the oceans via silicate weathering on igneous rocks and supplied through hydrothermal vents. [36] The increase in Mn oxidation occurred during the Archean Eon (> 2.5 Ga), whereas the first evidence of manganese redox cycling appears ~ 2.4 Ga, before the Great Oxygenation Event and during the Paleoproterozoic Era. [36] [37]

Although the Great Oxygenation Event raised the abundance of oxygen on Earth, the oxygen levels were still relatively low compared to modern levels. [38] It is believed that many primary producers were anoxygenic phototrophs and took advantage of abundant hydrogen sulfide (H2S) to catalyze photosynthesis. [39] [40] [41] Anoxygenic phototrophy and oxygenic photosynthesis both require electron donors, with all known forms of anoxygenic phototrophy relying on reaction center electron acceptors with reduction potentials around 250-500 mV. Oxygenic photosynthesis requires reduction potentials around 1250 mV. [36] It has been hypothesized that this wide difference in reduction potential indicates an evolutionary missing link in the origin of oxygenic photosynthesis. [36] Mn(II) is the leading candidate for bridging this gap. [40] [42] The water-oxidizing complex, a key component of PSII, begins with the oxidation of Mn(II), which, along with additional evidence, strongly supports the hypothesis that manganese was a necessary step in the evolution of oxygenic photosynthesis. [36] [37] [40] [42] [43]

Anthropogenic influences

While manganese naturally occurs in the environment, the global Mn cycle is influenced through anthropogenic activities. Mn is utilized in many commercial products, such as fireworks, leather, paint, glass, fertilizer, animal feed, and dry cell batteries. [44] However, the effect of Mn pollution from these sources is minor compared to that of mining and mineral processing. [4] The burning of fossil fuels, such as coal and natural gas, further contribute to the anthropogenic cycling of Mn. [45]

Mining and mineral processing

Anthropogenic influences on the manganese cycle mainly stem from industrial mining and mineral processing, specifically, within the iron and steel industries. [4] Mn is used in iron and steel production to improve hardness, strength, and stiffness, [4] and is the primary component used in low-cost stainless steel and aluminum alloy production. [46] Anthropogenic mining and mineral processing has spread Mn through three methods: wastewater discharge, industrial emissions, and releases in soils. [47]

Wastewater discharge

Waste from mining and mineral processing facilities is typically separated into liquid and solid forms. [48] Due to insufficient management and poor mining processes, especially in developing countries, liquid waste containing Mn can be discharged into bodies of water through anthropogenic effluents. [49] Domestic wastewater and sewage sludge disposal are the main anthropogenic sources of Mn within aquatic ecosystems. [48] In marine systems, the disposal of mine tailings contributes to aquatic anthropogenic Mn concentrations [50] where high levels can be toxic to marine life. [51]

Industrial emissions

The main anthropogenic influence of Mn input to the atmosphere is through industrial emissions, [52] and roughly 80% of industrial emissions of Mn is due to steel and iron processing facilities. [53] In the Northern Hemisphere, some of the Mn pollutants released through industrial emissions are transferred to Arctic regions through atmospheric circulation, where particulates settle and accumulate in natural bodies of water. [54] [55]

Such atmospheric pollution of Mn can be hazardous for humans working or living near industrial facilities. Dust and smoke containing manganese dioxide and manganese tetroxide released into the air during mining is a primary cause of manganism in humans. [56]

Releases in soils

The solid waste disposal of substances containing Mn by industrial sources typically ends up in landfills. [4] Additional Mn deposition in soils can result from particulate settling of Mn released through industrial emissions. [4] An analysis of datasets on the soil chemistry of North America and Europe revealed greater than 50% of Mn in ridge soils near iron or steel processing facilities was attributed to anthropogenic industrial inputs, whether through solid waste disposal or previously airborne particulates depositing in soils. [57]

Burning of fossil fuels

Anthropogenically sourced Mn from the burning of fossil fuels has been found in the atmosphere, hydrosphere, and lithosphere. [45] Mn is a trace element in fly ash, a residue from the use of coal for power production, which often ends up in the atmosphere, soils, and bodies of water. [58] Methylcyclopentadienyl Mn tricarbonyl (MMT), a gasoline additive containing Mn, also contributes to Mn anthropogenic cycling. [59] Due to the use of MMT as a fuel additive, motor vehicles are a significant source of Mn in the atmosphere, especially in regions of high traffic activity. [60] In some regions, roughly 40% of Mn in the atmosphere was due to exhaust from traffic. [60] Particulate manganese phosphate, manganese sulfate, and manganese oxide are the primary emissions from MMT combustion through its usage in gasoline. [61] [62] A portion of these particulates eventually leave the atmosphere to settle in soils and bodies of water. [45]

Related Research Articles

<span class="mw-page-title-main">Manganese</span> Chemical element, symbol Mn and atomic number 25

Manganese is a chemical element; it has symbol Mn and atomic number 25. It is a hard, brittle, silvery metal, often found in minerals in combination with iron. Manganese was first isolated in the 1770s. Manganese is a transition metal with a multifaceted array of industrial alloy uses, particularly in stainless steels. It improves strength, workability, and resistance to wear. Manganese oxide is used as an oxidising agent; as a rubber additive; and in glass making, fertilisers, and ceramics. Manganese sulfate can be used as a fungicide.

<span class="mw-page-title-main">Carbon cycle</span> Natural processes of carbon exchange

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

<span class="mw-page-title-main">Primary production</span> Synthesis of organic compounds from carbon dioxide by biological organisms

In ecology, primary production is the synthesis of organic compounds from atmospheric or aqueous carbon dioxide. It principally occurs through the process of photosynthesis, which uses light as its source of energy, but it also occurs through chemosynthesis, which uses the oxidation or reduction of inorganic chemical compounds as its source of energy. Almost all life on Earth relies directly or indirectly on primary production. The organisms responsible for primary production are known as primary producers or autotrophs, and form the base of the food chain. In terrestrial ecoregions, these are mainly plants, while in aquatic ecoregions algae predominate in this role. Ecologists distinguish primary production as either net or gross, the former accounting for losses to processes such as cellular respiration, the latter not.

<span class="mw-page-title-main">Manganese nodule</span> Mineral concretion on the sea bottom made of concentric layers of iron/manganese hydroxides

Polymetallic nodules, also called manganese nodules, are mineral concretions on the sea bottom formed of concentric layers of iron and manganese hydroxides around a core. As nodules can be found in vast quantities, and contain valuable metals, deposits have been identified as a potential economic interest. Depending on their composition and autorial choice, they may also be called ferromanganese or polymetallic nodules. Ferromanganese nodules are mineral concretions composed of silicates and insoluble iron and manganese oxides that form on the ocean seafloor and terrestrial soils. The formation mechanism involves a series of redox oscillations driven by both abiotic and biotic processes. As a byproduct of pedogenesis, the specific composition of a ferromanganese nodule depends on the composition of the surrounding soil. The formation mechanisms and composition of the nodules allow for couplings with biogeochemical cycles beyond iron and manganese. The high relative abundance of nickel, copper, manganese, and other rare metals in nodules has increased interest in their use as a mining resource.

<span class="mw-page-title-main">Oxygen cycle</span> Biogeochemical cycle of oxygen

Oxygen cycle refers to the movement of oxygen through the atmosphere (air), biosphere (plants and animals) and the lithosphere (the Earth’s crust). The oxygen cycle demonstrates how free oxygen is made available in each of these regions, as well as how it is used. The oxygen cycle is the biogeochemical cycle of oxygen atoms between different oxidation states in ions, oxides, and molecules through redox reactions within and between the spheres/reservoirs of the planet Earth. The word oxygen in the literature typically refers to the most common oxygen allotrope, elemental/diatomic oxygen (O2), as it is a common product or reactant of many biogeochemical redox reactions within the cycle. Processes within the oxygen cycle are considered to be biological or geological and are evaluated as either a source (O2 production) or sink (O2 consumption).

<span class="mw-page-title-main">Photosystem II</span> First protein complex in light-dependent reactions of oxygenic photosynthesis

Photosystem II is the first protein complex in the light-dependent reactions of oxygenic photosynthesis. It is located in the thylakoid membrane of plants, algae, and cyanobacteria. Within the photosystem, enzymes capture photons of light to energize electrons that are then transferred through a variety of coenzymes and cofactors to reduce plastoquinone to plastoquinol. The energized electrons are replaced by oxidizing water to form hydrogen ions and molecular oxygen.

<span class="mw-page-title-main">Iron cycle</span>

The iron cycle (Fe) is the biogeochemical cycle of iron through the atmosphere, hydrosphere, biosphere and lithosphere. While Fe is highly abundant in the Earth's crust, it is less common in oxygenated surface waters. Iron is a key micronutrient in primary productivity, and a limiting nutrient in the Southern ocean, eastern equatorial Pacific, and the subarctic Pacific referred to as High-Nutrient, Low-Chlorophyll (HNLC) regions of the ocean.

<span class="mw-page-title-main">Geobiology</span> Study of interactions between Earth and the biosphere

Geobiology is a field of scientific research that explores the interactions between the physical Earth and the biosphere. It is a relatively young field, and its borders are fluid. There is considerable overlap with the fields of ecology, evolutionary biology, microbiology, paleontology, and particularly soil science and biogeochemistry. Geobiology applies the principles and methods of biology, geology, and soil science to the study of the ancient history of the co-evolution of life and Earth as well as the role of life in the modern world. Geobiologic studies tend to be focused on microorganisms, and on the role that life plays in altering the chemical and physical environment of the pedosphere, which exists at the intersection of the lithosphere, atmosphere, hydrosphere and/or cryosphere. It differs from biogeochemistry in that the focus is on processes and organisms over space and time rather than on global chemical cycles.

<span class="mw-page-title-main">Iron-oxidizing bacteria</span> Bacteria deriving energy from dissolved iron

Iron-oxidizing bacteria are chemotrophic bacteria that derive energy by oxidizing dissolved iron. They are known to grow and proliferate in waters containing iron concentrations as low as 0.1 mg/L. However, at least 0.3 ppm of dissolved oxygen is needed to carry out the oxidation.

<span class="mw-page-title-main">Birnessite</span> Manganese hydroxide mineral

Birnessite (nominally MnO2·nH2O), also known as δ-MnO2, is a hydrous manganese dioxide mineral with a chemical formula of Na0.7Ca0.3Mn7O14·2.8H2O. It is the main manganese mineral species at the Earth's surface, and commonly occurs as fine-grained, poorly crystallized aggregates in soils, sediments, grain and rock coatings (e.g., desert varnish), and marine ferromanganese nodules and crusts. It was discovered at Birness, Aberdeenshire, Scotland.

<span class="mw-page-title-main">Great Oxidation Event</span> Paleoproterozoic surge in atmospheric oxygen

The Great Oxidation Event (GOE) or Great Oxygenation Event, also called the Oxygen Catastrophe, Oxygen Revolution, Oxygen Crisis or the Holocaust, was a time interval during the Early Earth's Paleoproterozoic Era when the Earth's atmosphere and the shallow ocean first experienced a rise in the concentration of oxygen. This began approximately 2.460–2.426 Ga (billion years) ago, during the Siderian period, and ended approximately 2.060 Ga, during the Rhyacian. Geological, isotopic, and chemical evidence suggests that biologically-produced molecular oxygen (dioxygen or O2) started to accumulate in Earth's atmosphere and changed it from a weakly reducing atmosphere practically devoid of oxygen into an oxidizing one containing abundant free oxygen, with oxygen levels being as high as 10% of their present atmospheric level by the end of the GOE.

<span class="mw-page-title-main">Phosphorus cycle</span> Biogeochemical movement

The phosphorus cycle is the biogeochemical cycle that describes the movement of phosphorus through the lithosphere, hydrosphere, and biosphere. Unlike many other biogeochemical cycles, the atmosphere does not play a significant role in the movement of phosphorus, because phosphorus and phosphorus-based compounds are usually solids at the typical ranges of temperature and pressure found on Earth. The production of phosphine gas occurs in only specialized, local conditions. Therefore, the phosphorus cycle should be viewed from whole Earth system and then specifically focused on the cycle in terrestrial and aquatic systems.

The Boring Billion, otherwise known as the Mid Proterozoic and Earth's Middle Ages, is the time period between 1.8 and 0.8 billion years ago (Ga) spanning the middle Proterozoic eon, characterized by more or less tectonic stability, climatic stasis, and slow biological evolution. It is bordered by two different oxygenation and glacial events, but the Boring Billion itself had very low oxygen levels and no evidence of glaciation.

<span class="mw-page-title-main">Oceanic carbon cycle</span> Ocean/atmosphere carbon exchange process

The oceanic carbon cycle is composed of processes that exchange carbon between various pools within the ocean as well as between the atmosphere, Earth interior, and the seafloor. The carbon cycle is a result of many interacting forces across multiple time and space scales that circulates carbon around the planet, ensuring that carbon is available globally. The Oceanic carbon cycle is a central process to the global carbon cycle and contains both inorganic carbon and organic carbon. Part of the marine carbon cycle transforms carbon between non-living and living matter.

A lithium ion manganese oxide battery (LMO) is a lithium-ion cell that uses manganese dioxide, MnO
2, as the cathode material. They function through the same intercalation/de-intercalation mechanism as other commercialized secondary battery technologies, such as LiCoO
2. Cathodes based on manganese-oxide components are earth-abundant, inexpensive, non-toxic, and provide better thermal stability.

<span class="mw-page-title-main">Photogeochemistry</span>

Photogeochemistry merges photochemistry and geochemistry into the study of light-induced chemical reactions that occur or may occur among natural components of Earth's surface. The first comprehensive review on the subject was published in 2017 by the chemist and soil scientist Timothy A Doane, but the term photogeochemistry appeared a few years earlier as a keyword in studies that described the role of light-induced mineral transformations in shaping the biogeochemistry of Earth; this indeed describes the core of photogeochemical study, although other facets may be admitted into the definition.

<span class="mw-page-title-main">Aluminum cycle</span>

Aluminum is the third most abundant element in the lithosphere at 82,000 ppm. It occurs in low levels, 0.9 ppm, in humans. Aluminum is known to be an ecotoxicant and expected to be a health risk to people. Global primary production (GPP) of aluminum was about 52 million tons in 2013 and remains one of the world's most important metals. It is used for infrastructure, vehicles, aviation, energy and more due to its lightweight, ductility, and cheap cost. Aluminum is harvested from gibbsite, boehmite, and diaspore which make up bauxite. The aluminum cycle is the biogeochemical cycle by which aluminum is moved through the environment by natural and anthropogenic processes. The biogeochemical cycle of aluminum is integral with silicon and phosphorus. For example, phosphates store aluminum that has been sedimented and aluminum is found in diatoms. Aluminum has been found to prevent growth in organisms by making phosphates less available. The humans/lithosphere ratio (B/L) is very low at 0.000011. This level shows that aluminum is more essential in the lithospheric cycle than in the biotic cycle.

<span class="mw-page-title-main">Arsenic cycle</span>

The arsenic (As) cycle is the biogeochemical cycle of natural and anthropogenic exchanges of arsenic terms through the atmosphere, lithosphere, pedosphere, hydrosphere, and biosphere. Although arsenic is naturally abundant in the Earth's crust, long-term exposure and high concentrations of arsenic can be detrimental to human health.

<span class="mw-page-title-main">Chromium cycle</span> Biogeochemical cycle

The chromium cycle is the biogeochemical cycle of chromium through the atmosphere, hydrosphere, biosphere and lithosphere.

<span class="mw-page-title-main">Particulate inorganic carbon</span>

Particulate inorganic carbon (PIC) can be contrasted with dissolved inorganic carbon (DIC), the other form of inorganic carbon found in the ocean. These distinctions are important in chemical oceanography. Particulate inorganic carbon is sometimes called suspended inorganic carbon. In operational terms, it is defined as the inorganic carbon in particulate form that is too large to pass through the filter used to separate dissolved inorganic carbon.

References

  1. ↑ Ehrlich, Henry Lutz; Newman, Dianne K. (22 December 2008). Geomicrobiology. CRC Press. pp. 347–426. ISBN   978-0-8493-7907-9.
  2. 1 2 Raven, John A. (1990-09-01). "Predictions of Mn and Fe use efficiencies of phototrophic growth as a function of light availability for growth and of C assimilation pathway". New Phytologist. 116 (1): 1–18. doi:10.1111/j.1469-8137.1990.tb00505.x. ISSN   0028-646X.
  3. ↑ Wang, Xuan; Xie, Guo-Jun; Tian, Ning; Dang, Cheng-Cheng; Cai, Chen; Ding, Jie; Liu, Bing-Feng; Xing, De-Feng; Ren, Nan-Qi; Wang, Qilin (2022-05-20). "Anaerobic microbial manganese oxidation and reduction: A critical review". Science of the Total Environment. 822: 153513. doi:10.1016/j.scitotenv.2022.153513. ISSN   0048-9697. PMID   35101498. S2CID   246434330.
  4. 1 2 3 4 5 6 Howe, Paul; Malcolm, Heath; WHO; Dobson, Stuart; Organization, World Health (2004-12-17). Manganese and Its Compounds: Environmental Aspects. World Health Organization. ISBN   978-92-4-153063-7.
  5. ↑ Post, Jeffrey E. (1999-03-30). "Manganese oxide minerals: Crystal structures and economic and environmental significance". Proceedings of the National Academy of Sciences. 96 (7): 3447–3454. doi: 10.1073/pnas.96.7.3447 . ISSN   0027-8424. PMC   34287 . PMID   10097056.
  6. 1 2 Schmidt, Sidsel Birkelund; Jensen, Poul Erik; Husted, Søren (2016-07-01). "Manganese Deficiency in Plants: The Impact on Photosystem II". Trends in Plant Science. 21 (7): 622–632. doi:10.1016/j.tplants.2016.03.001. ISSN   1360-1385. PMID   27150384.
  7. ↑ Post, Jeffrey E. (1999-03-30). "Manganese oxide minerals: Crystal structures and economic and environmental significance". Proceedings of the National Academy of Sciences. 96 (7): 3447–3454. doi: 10.1073/pnas.96.7.3447 . ISSN   0027-8424. PMC   34287 . PMID   10097056.
  8. ↑ Lingappa, Usha F.; Yeager, Chris M.; Sharma, Ajay; Lanza, Nina L.; Morales, Demosthenes P.; Xie, Gary; Atencio, Ashley D.; Chadwick, Grayson L.; Monteverde, Danielle R.; Magyar, John S.; Webb, Samuel M.; Valentine, Joan Selverstone; Hoffman, Brian M.; Fischer, Woodward W. (2021-06-22). "An ecophysiological explanation for manganese enrichment in rock varnish". Proceedings of the National Academy of Sciences. 118 (25): e2025188118. doi: 10.1073/pnas.2025188118 . ISSN   0027-8424. PMC   8237629 . PMID   34161271.
  9. ↑ Mann, P. J. G.; Quastel, J. H. (August 1946). "Manganese Metabolism in Soils". Nature. 158 (4005): 154–156. doi:10.1038/158154a0. ISSN   1476-4687. S2CID   43335147.
  10. ↑ Thompson, Ian A.; Huber, Don M.; Guest, Chris A.; Schulze, Darrell G. (2005-06-25). "Fungal manganese oxidation in a reduced soil". Environmental Microbiology. 7 (9): 1480–1487. doi:10.1111/j.1462-2920.2005.00842.x. ISSN   1462-2912. PMID   16104870.
  11. ↑ Ghiorse, W. C. (1984-10-01). "Biology of Iron-And Manganese-Depositing Bacteria". Annual Review of Microbiology. 38 (1): 515–550. doi:10.1146/annurev.mi.38.100184.002503. ISSN   0066-4227. PMID   6388499.
  12. ↑ Ghiorse, William C. (1988), Graham, Robin D.; Hannam, Robert J.; Uren, Nicholas C. (eds.), "The Biology of Manganese Transforming Microorganisms in Soil", Manganese in Soils and Plants: Proceedings of the International Symposium on ‘Manganese in Soils and Plants’ held at the Waite Agricultural Research Institute, The University of Adelaide, Glen Osmond, South Australia, August 22–26, 1988 as an Australian Bicentennial Event, Dordrecht: Springer Netherlands, pp. 75–85, doi:10.1007/978-94-009-2817-6_6, ISBN   978-94-009-2817-6 , retrieved 2022-10-17
  13. 1 2 3 Norvell, W. A. (1988), Graham, Robin D.; Hannam, Robert J.; Uren, Nicholas C. (eds.), "Inorganic Reactions of Manganese in Soils", Manganese in Soils and Plants: Proceedings of the International Symposium on ‘Manganese in Soils and Plants’ held at the Waite Agricultural Research Institute, The University of Adelaide, Glen Osmond, South Australia, August 22–26, 1988 as an Australian Bicentennial Event, Dordrecht: Springer Netherlands, pp. 37–58, doi:10.1007/978-94-009-2817-6_4, ISBN   978-94-009-2817-6 , retrieved 2022-10-17
  14. ↑ Grygo-Szymanko, Emilia; Tobiasz, Anna; Walas, Stanisław (2016-06-01). "Speciation analysis and fractionation of manganese: A review". TrAC Trends in Analytical Chemistry. 80: 112–124. doi:10.1016/j.trac.2015.09.010. ISSN   0165-9936.
  15. ↑ van Hulten, Marco; Dutay, Jean-Claude; Middag, Rob; de Baar, Hein; Roy-Barman, Matthieu; Gehlen, Marion; Tagliabue, Alessandro; Sterl, Andreas (2016-07-11). "Manganese in the world ocean: a first global model" (PDF). doi: 10.5194/bg-2016-282 .{{cite journal}}: Cite journal requires |journal= (help)
  16. ↑ German, C. R.; Casciotti, K. A.; Dutay, J.-C.; Heimbürger, L. E.; Jenkins, W. J.; Measures, C. I.; Mills, R. A.; Obata, H.; Schlitzer, R.; Tagliabue, A.; Turner, D. R.; Whitby, H. (2016-11-28). "Hydrothermal impacts on trace element and isotope ocean biogeochemistry". Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences. 374 (2081): 20160035. doi:10.1098/rsta.2016.0035. PMC   5069535 . PMID   29035265.
  17. ↑ Arimoto, R.; Duce, R. A.; Ray, B. J.; Unni, C. K. (1985). "Atmospheric trace elements at Enewetak Atoll: 2. Transport to the ocean by wet and dry deposition". Journal of Geophysical Research. 90 (D1): 2391. doi:10.1029/JD090iD01p02391. ISSN   0148-0227.
  18. ↑ Froelich, P. N.; Klinkhammer, G. P.; Bender, M. L.; Luedtke, N. A.; Heath, G. R.; Cullen, Doug; Dauphin, Paul; Hammond, Doug; Hartman, Blayne; Maynard, Val (1979-07-01). "Early oxidation of organic matter in pelagic sediments of the eastern equatorial Atlantic: suboxic diagenesis". Geochimica et Cosmochimica Acta. 43 (7): 1075–1090. doi:10.1016/0016-7037(79)90095-4. ISSN   0016-7037.
  19. ↑ Jensen, Laramie T.; Morton, Peter; Twining, Benjamin S.; Heller, Maija I.; Hatta, Mariko; Measures, Christopher I.; John, Seth; Zhang, Ruifeng; Pinedo-Gonzalez, Paulina; Sherrell, Robert M.; Fitzsimmons, Jessica N. (2020-11-01). "A comparison of marine Fe and Mn cycling: U.S. GEOTRACES GN01 Western Arctic case study". Geochimica et Cosmochimica Acta. 288: 138–160. doi: 10.1016/j.gca.2020.08.006 . ISSN   0016-7037. S2CID   224924072.
  20. ↑ Sunda, William (2012). "Feedback Interactions between Trace Metal Nutrients and Phytoplankton in the Ocean". Frontiers in Microbiology. 3: 204. doi: 10.3389/fmicb.2012.00204 . ISSN   1664-302X. PMC   3369199 . PMID   22701115.
  21. ↑ Bruland, K.W.; Lohan, M.C. (2003), "Controls of Trace Metals in Seawater", Treatise on Geochemistry, Elsevier, pp. 23–47, doi:10.1016/b0-08-043751-6/06105-3, ISBN   9780080437514 , retrieved 2022-10-28
  22. ↑ Balistrieri, L.; Brewer, P.G.; Murray, J.W. (1981-02-01) [1981-02]. "Scavenging residence times of trace metals and surface chemistry of sinking particles in the deep ocean". Deep Sea Research Part A. Oceanographic Research Papers. 28 (2): 101–121. doi:10.1016/0198-0149(81)90085-6. ISSN   0198-0149.
  23. ↑ van Hulten, Marco; Dutay, Jean-Claude; Middag, Rob; de Baar, Hein; Roy-Barman, Matthieu; Gehlen, Marion; Tagliabue, Alessandro; Sterl, Andreas (2016-07-11). "Manganese in the world ocean: a first global model" (PDF). doi: 10.5194/bg-2016-282 .{{cite journal}}: Cite journal requires |journal= (help)
  24. 1 2 Morris, A. W.; Bale, A. J.; Howland, R. J. M. (1982-02-01). "The dynamics of estuarine manganese cycling". Estuarine, Coastal and Shelf Science. 14 (2): 175–192. doi:10.1016/S0302-3524(82)80044-3. ISSN   0272-7714.
  25. ↑ Laxen, Duncan P. H.; Davison, William; Woof, Colin (1984-10-01). "Manganese chemistry in rivers and streams". Geochimica et Cosmochimica Acta. 48 (10): 2107–2111. doi:10.1016/0016-7037(84)90390-9. ISSN   0016-7037.
  26. 1 2 3 4 Buffle, Jacques; Leeuwen, Herman P. van (2018-10-24). Revival: Environmental Particles (1993): Volume 2. CRC Press. ISBN   978-1-351-27079-3.
  27. ↑ van Hulten, Marco; Dutay, Jean-Claude; Middag, Rob; de Baar, Hein; Roy-Barman, Matthieu; Gehlen, Marion; Tagliabue, Alessandro; Sterl, Andreas (2016-07-11). "Manganese in the world ocean: a first global model" (PDF). doi: 10.5194/bg-2016-282 .{{cite journal}}: Cite journal requires |journal= (help)
  28. ↑ Bouvier, Audrey; Wadhwa, Meenakshi (2010-08-22). "The age of the Solar System redefined by the oldest Pb–Pb age of a meteoritic inclusion". Nature Geoscience. 3 (9): 637–641. doi:10.1038/ngeo941. ISSN   1752-0908.
  29. 1 2 3 Carroll, Bradley W.; Ostlie, Dale A. (2017-10-29). An Introduction to Modern Astrophysics (2 ed.). Cambridge University Press. doi:10.1017/9781108380980. ISBN   978-1-108-42216-1.
  30. ↑ Leung, Shing-Chi; Nomoto, Ken’ichi (2018-07-13). "Explosive Nucleosynthesis in Near-Chandrasekhar-mass White Dwarf Models for Type Ia Supernovae: Dependence on Model Parameters". The Astrophysical Journal. 861 (2): 143. arXiv: 1710.04254 . doi: 10.3847/1538-4357/aac2df . ISSN   1538-4357. S2CID   250859408.
  31. ↑ Fischer, Woodward W; Hemp, James; Valentine, Joan Selverstone (2016-04-01). "How did life survive Earth's great oxygenation?". Current Opinion in Chemical Biology. Biocatalysis and biotransformation * Bioinorganic chemistry. 31: 166–178. doi:10.1016/j.cbpa.2016.03.013. ISSN   1367-5931. PMID   27043270.
  32. ↑ Johnson, Jena E.; Gerpheide, Aya; Lamb, Michael P.; Fischer, Woodward W. (2014-05-01). "O 2 constraints from Paleoproterozoic detrital pyrite and uraninite". Geological Society of America Bulletin. 126 (5–6): 813–830. doi:10.1130/B30949.1. ISSN   0016-7606.
  33. ↑ Farquhar, James; Bao, Huiming; Thiemens, Mark (2000-08-04). "Atmospheric Influence of Earth's Earliest Sulfur Cycle". Science. 289 (5480): 756–758. doi:10.1126/science.289.5480.756. ISSN   0036-8075. PMID   10926533.
  34. ↑ Paris, G.; Adkins, J. F.; Sessions, A. L.; Webb, S. M.; Fischer, W. W. (2014-11-07). "Neoarchean carbonate–associated sulfate records positive Δ 33 S anomalies". Science. 346 (6210): 739–741. doi:10.1126/science.1258211. ISSN   0036-8075. PMID   25378622. S2CID   20532947.
  35. ↑ Torres, Mark A.; Paris, Guillaume; Adkins, Jess F.; Fischer, Woodward W. (2018-09-23). "Riverine evidence for isotopic mass balance in the Earth's early sulfur cycle". Nature Geoscience. 11 (9): 661–664. doi:10.1038/s41561-018-0184-7. hdl: 1911/103259 . ISSN   1752-0894. S2CID   133714335.
  36. 1 2 3 4 5 Lingappa, Usha F.; Monteverde, Danielle R.; Magyar, John S.; Valentine, Joan Selverstone; Fischer, Woodward W. (2019-08-20). "How manganese empowered life with dioxygen (and vice versa)". Free Radical Biology and Medicine. Early Life on Earth and Oxidative Stress. 140: 113–125. doi:10.1016/j.freeradbiomed.2019.01.036. ISSN   0891-5849. PMID   30738765. S2CID   73436722.
  37. 1 2 Johnson, Jena E.; Webb, Samuel M.; Thomas, Katherine; Ono, Shuhei; Kirschvink, Joseph L.; Fischer, Woodward W. (2013-07-09). "Manganese-oxidizing photosynthesis before the rise of cyanobacteria". Proceedings of the National Academy of Sciences. 110 (28): 11238–11243. doi: 10.1073/pnas.1305530110 . ISSN   0027-8424. PMC   3710856 . PMID   23798417.
  38. ↑ Lyons, Timothy W.; Reinhard, Christopher T.; Planavsky, Noah J. (2014-02-19). "The rise of oxygen in Earth's early ocean and atmosphere". Nature. 506 (7488): 307–315. doi:10.1038/nature13068. ISSN   1476-4687. PMID   24553238. S2CID   4443958.
  39. ↑ Olson, Kenneth R.; Straub, Karl D. (2016-01-01). "The Role of Hydrogen Sulfide in Evolution and the Evolution of Hydrogen Sulfide in Metabolism and Signaling". Physiology. 31 (1): 60–72. doi: 10.1152/physiol.00024.2015 . ISSN   1548-9213. PMID   26674552.
  40. 1 2 3 Fischer, Woodward W.; Hemp, James; Johnson, Jena E. (2016-06-29). "Evolution of Oxygenic Photosynthesis". Annual Review of Earth and Planetary Sciences. 44 (1): 647–683. doi: 10.1146/annurev-earth-060313-054810 . ISSN   0084-6597.
  41. ↑ Tice, Michael M.; Lowe, Donald R. (2004-09-30). "Photosynthetic microbial mats in the 3,416-Myr-old ocean". Nature. 431 (7008): 549–552. doi:10.1038/nature02888. ISSN   0028-0836. PMID   15457255. S2CID   4412591.
  42. 1 2 Fischer, Woodward W.; Hemp, James; Johnson, Jena E. (2015-05-29). "Manganese and the Evolution of Photosynthesis". Origins of Life and Evolution of Biospheres. 45 (3): 351–357. doi:10.1007/s11084-015-9442-5. ISSN   0169-6149. PMID   26017176. S2CID   254894651.
  43. ↑ Hemp, James; Lücker, Sebastian; Schott, Joachim; Pace, Laura A; Johnson, Jena E; Schink, Bernhard; Daims, Holger; Fischer, Woodward W (2016-04-19). "Genomics of a phototrophic nitrite oxidizer: insights into the evolution of photosynthesis and nitrification". The ISME Journal. 10 (11): 2669–2678. doi:10.1038/ismej.2016.56. ISSN   1751-7362. PMC   5113846 . PMID   27093047.
  44. ↑ Chakraborty, Sudipta; Martinez-Finley, Ebany; Caito, Sam; Chen, Pan; Aschner, Michael (2014-07-09), "CHAPTER 9:Manganese", Binding, Transport and Storage of Metal Ions in Biological Cells, Metallobiology, pp. 260–281, doi:10.1039/9781849739979-00260, ISBN   978-1-84973-599-5 , retrieved 2022-11-09
  45. 1 2 3 Williams, Malcolm; Todd, G Daniel; Roney, Nickolette; Crawford, Jewell; Coles, Charleton; McClure, Peter R; Garey, Joan D; Zaccaria, Kimberly; Citra, Mario (2012). "Toxicological Profile for Manganes". Agency for Toxic Substances and Disease Registry (ATSDR) Toxicological Profiles. Agency for Toxic Substances and Disease Registry (US). PMID   24049862.{{cite journal}}: Cite journal requires |journal= (help)
  46. ↑ Tangstad, Merete (2013-01-01), Gasik, Michael (ed.), "Chapter 7 - Manganese Ferroalloys Technology", Handbook of Ferroalloys, Oxford: Butterworth-Heinemann, pp. 221–266, ISBN   978-0-08-097753-9 , retrieved 2022-11-16
  47. ↑ Nkele, K.; Mpenyana-Monyatsi, L.; Masindi, V. (2022-12-01). "Challenges, advances and sustainabilities on the removal and recovery of manganese from wastewater: A review". Journal of Cleaner Production. 377: 134152. doi:10.1016/j.jclepro.2022.134152. ISSN   0959-6526. S2CID   252482228.
  48. 1 2 Nriagu, Jerome O.; Pacyna, Jozef M. (1988). "Quantitative assessment of worldwide contamination of air, water and soils by trace metals". Nature. 333 (6169): 134–139. doi:10.1038/333134a0. ISSN   1476-4687. PMID   3285219. S2CID   4262601.
  49. ↑ Nkele, K.; Mpenyana-Monyatsi, L.; Masindi, V. (2022-12-01). "Challenges, advances and sustainabilities on the removal and recovery of manganese from wastewater: A review". Journal of Cleaner Production. 377: 134152. doi:10.1016/j.jclepro.2022.134152. ISSN   0959-6526. S2CID   252482228.
  50. ↑ Florence, T. M.; Stauber, J. L.; Ahsanullah, M. (1994-06-06). "Toxicity of nickel ores to marine organisms". Science of the Total Environment. Nickel Biochemistry, Toxicology, and Ecologic Issues. 148 (2): 139–155. doi:10.1016/0048-9697(94)90391-3. ISSN   0048-9697. PMID   8029690.
  51. ↑ Marks, Becky; Peters, Adam; McGough, Doreen (2017-01-01). "Aquatic environmental risk assessment of manganese processing industries". NeuroToxicology. 58: 187–193. doi:10.1016/j.neuro.2016.04.011. ISSN   0161-813X. PMID   27090824. S2CID   24866936.
  52. ↑ Lioy, P. J. (1983). "Air pollution emission profiles of toxic and trace elements from energy related sources: status and needs". Neurotoxicology. 4 (3): 103–112. ISSN   0161-813X. PMID   6686299.
  53. ↑ "Manganese: Potential for Exposure" (PDF).
  54. ↑ Varotsos, Costas A.; Krapivin, Vladimir F. (2018-10-25). "Pollution of Arctic Waters Has Reached a Critical Point: an Innovative Approach to This Problem". Water, Air, & Soil Pollution. 229 (11): 343. doi:10.1007/s11270-018-4004-x. ISSN   1573-2932. S2CID   105926567.
  55. ↑ Danilov, Aleksandr Sergeevich; Smirnov, Yuri Dmitrievich; Pashkevich, Maria Anatolievna (2015-11-03). "Use of Biological Adhesive for Effective Dust Suppression in Mining Operations". Journal of Ecological Engineering. 16 (5): 9–14. doi: 10.12911/22998993/60448 . ISSN   2299-8993.
  56. ↑ Schiele, R (1991). Metals and their compounds in the environment - occurrence, analysis, and biological relevance. Weinheim VCH. pp. 1035–1044.
  57. ↑ Herndon, Elizabeth M.; Jin, Lixin; Brantley, Susan L. (2011-01-01). "Soils Reveal Widespread Manganese Enrichment from Industrial Inputs". Environmental Science & Technology. 45 (1): 241–247. doi:10.1021/es102001w. ISSN   0013-936X. PMID   21133425.
  58. ↑ Ibrahim, lubna Abdel Aziz (2015-10-01). "Chemical characterization and mobility of metal species in fly ash–water system". Water Science. 29 (2): 109–122. doi: 10.1016/j.wsj.2015.10.001 . ISSN   1110-4929. S2CID   101064919.
  59. ↑ Chen, Pan; Culbreth, Megan; Aschner, Michael (2016-07-01). "Exposure, epidemiology, and mechanism of the environmental toxicant manganese". Environmental Science and Pollution Research. 23 (14): 13802–13810. doi:10.1007/s11356-016-6687-0. ISSN   1614-7499. PMID   27102617. S2CID   34209604.
  60. 1 2 Davis, D. W.; Hsiao, K.; Ingels, R.; Shikiya, J. (1988). "Origins of manganese in air particulates in California". JAPCA. 38 (9): 1152–1157. doi:10.1080/08940630.1988.10466464. ISSN   0894-0630. PMID   3230404.
  61. ↑ Ter Haar, G. L.; Grifffing, M. E.; Brandt, M.; Oberding, D. G.; Kapron, M. (1975-08-01). "Methylcyclopentadienyl Manganese Tricarbonyl as an Antiknock: Composition and Fate of Manganese Exhaust Products". Journal of the Air Pollution Control Association. 25 (8): 858–859. doi:10.1080/00022470.1975.10470152. ISSN   0002-2470.
  62. ↑ Lynam, D R; Roos, J W; Pfeifer, G D; Fort, B F; Pullin, T G (1999-04-01). "Environmental effects and exposures to manganese from use of methylcyclopentadienyl manganese tricarbonyl (MMT) in gasoline". Neurotoxicology. 20 (2–3): 145–150. ISSN   1872-9711. PMID   10385878.
This page is based on this Wikipedia article
Text is available under the CC BY-SA 4.0 license; additional terms may apply.
Images, videos and audio are available under their respective licenses.