Jump to content

Phytoplankton

From Wikipedia, the free encyclopedia

Part of a series on
Plankton
Phytoplankton
Trophic mode
By size
By taxonomy
By habitat
Other types
Blooms
Related topics

Phytoplankton (/ˌfaɪtoʊˈplæŋktən/) are the autotrophic (self-feeding) components of the plankton community and a key part of ocean and freshwater ecosystems. The name comes from the Greek words φυτόν (phyton), meaning 'plant', and πλαγκτός (planktos), meaning 'wanderer' or 'drifter'.[1][2][3]

Phytoplankton obtain their energy through photosynthesis, as trees and other plants do on land. This means phytoplankton must have light from the sun, so they live in the well-lit surface layers (euphotic zone) of oceans and lakes. In comparison with terrestrial plants, phytoplankton are distributed over a larger surface area, are exposed to less seasonal variation and have markedly faster turnover rates than trees (days versus decades). As a result, phytoplankton respond rapidly on a global scale to climate variations.

Phytoplankton form the base of marine and freshwater food webs and are key players in the global carbon cycle. They account for about half of global photosynthetic activity and at least half of the oxygen production, despite amounting to only about 1% of the global plant biomass.

Phytoplankton are very diverse, comprising photosynthesizing bacteria (cyanobacteria) and various unicellular protist groups (notably the diatoms).

Most phytoplankton are too small to be individually seen with the unaided eye. However, when present in high enough numbers, some varieties may be noticeable as colored patches on the water surface due to the presence of chlorophyll within their cells and accessory pigments (such as phycobiliproteins or xanthophylls) in some species.

Types

[edit]

Phytoplankton are photosynthesizing microscopic protists and bacteria that inhabit the upper sunlit layer of marine and fresh water bodies of water on Earth. Paralleling plants on land, phytoplankton undertake primary production in water,[2] creating organic compounds from carbon dioxide dissolved in the water. Phytoplankton form the base of — and sustain — the aquatic food web,[4] and are crucial players in the Earth's carbon cycle.[5]

Diatoms are one of the most common types
of phytoplankton
A cyanobacteria species (Cylindrospermum sp)

Phytoplankton are very diverse, comprising photosynthesizing bacteria (cyanobacteria) and various unicellular protist groups (notably the diatoms). Many other organism groups formally named as phytoplankton, including coccolithophores and dinoflagellates, are now no longer included as they are not only phototrophic but can also eat.[6] These organisms are now more correctly termed mixoplankton.[7] This recognition has important consequences for how we view the functioning of the planktonic food web.[8]

Ecology

[edit]
Global distribution of ocean phytoplankton – NASA
This visualization shows a model simulation of the dominant phytoplankton types averaged over the period 1994–1998. * Red = diatoms (big phytoplankton, which need silica) * Yellow = flagellates (other big phytoplankton) * Green = prochlorococcus (small phytoplankton that cannot use nitrate) * Cyan = synechococcus (other small phytoplankton) Opacity indicates concentration of the carbon biomass. In particular, the role of the swirls and filaments (mesoscale features) appear important in maintaining high biodiversity in the ocean.[5][9]

Phytoplankton obtain energy through the process of photosynthesis and must therefore live in the well-lit surface layer (termed the euphotic zone) of an ocean, sea, lake, or other body of water. Phytoplankton account for about half of all photosynthetic activity on Earth.[10][11][12] Their cumulative energy fixation in carbon compounds (primary production) is the basis for the vast majority of oceanic and also many freshwater food webs (chemosynthesis is a notable exception).

While almost all phytoplankton species are obligate photoautotrophs, there are some that are mixotrophic and other, non-pigmented species that are actually heterotrophic (the latter are often viewed as zooplankton).[2][13] Of these, the best known are dinoflagellate genera such as Noctiluca and Dinophysis, that obtain organic carbon by ingesting other organisms or detrital material.

Phytoplankton live in the photic zone of the ocean, where photosynthesis is possible. During photosynthesis, they assimilate carbon dioxide and release oxygen. If solar radiation is too high, phytoplankton may fall victim to photodegradation. Phytoplankton species feature a large variety of photosynthetic pigments which species-specifically enables them to absorb different wavelengths of the variable underwater light.[14] This implies different species can use the wavelength of light different efficiently and the light is not a single ecological resource but a multitude of resources depending on its spectral composition.[15] By that it was found that changes in the spectrum of light alone can alter natural phytoplankton communities even if the same intensity is available.[16] For growth, phytoplankton cells additionally depend on nutrients, which enter the ocean by rivers, continental weathering, and glacial ice meltwater on the poles. Phytoplankton release dissolved organic carbon (DOC) into the ocean. Since phytoplankton are the basis of marine food webs, they serve as prey for zooplankton, fish larvae and other heterotrophic organisms. They can also be degraded by bacteria or by viral lysis. Although some phytoplankton cells, such as dinoflagellates, are able to migrate vertically, they are still incapable of actively moving against currents, so they slowly sink and ultimately fertilize the seafloor with dead cells and detritus.[17]

Cycling of marine phytoplankton [17]

Phytoplankton are crucially dependent on a number of nutrients. These are primarily macronutrients such as nitrate, phosphate or silicic acid, which are required in relatively large quantities for growth. Their availability in the surface ocean is governed by the balance between the so-called biological pump and upwelling of deep, nutrient-rich waters. The stoichiometric nutrient composition of phytoplankton drives — and is driven by — the Redfield ratio of macronutrients generally available throughout the surface oceans. Phytoplankton also rely on trace metals such as iron (Fe), manganese (Mn), zinc (Zn), cobalt (Co), cadmium (Cd) and copper (Cu) as essential micronutrients, influencing their growth and community composition.[18] Limitations in these metals can lead to co-limitations and shifts in phytoplankton community structure.[19][20] Across large areas of the oceans such as the Southern Ocean, phytoplankton are often limited by the lack of the micronutrient iron. [21] This has led to some scientists advocating iron fertilization as a means to counteract the accumulation of human-produced carbon dioxide (CO2) in the atmosphere.[22] Large-scale experiments have added iron (usually as salts such as ferrous sulfate) to the oceans to promote phytoplankton growth and draw atmospheric CO2 into the ocean. Controversy about manipulating the ecosystem and the efficiency of iron fertilization has slowed such experiments.[23][24] The ocean science community still has a divided attitude toward the study of iron fertilization as a potential marine Carbon Dioxide Removal (mCDR) approach.[25][26]

Phytoplankton depend on B vitamins for survival. Areas in the ocean have been identified as having a major lack of some B Vitamins, and correspondingly, phytoplankton.[27]

The effects of anthropogenic warming on the global population of phytoplankton is an area of active research. Changes in the vertical stratification of the water column, the rate of temperature-dependent biological reactions, and the atmospheric supply of nutrients are expected to have important effects on future phytoplankton productivity.[28][29]

Bioluminescence in phytoplankton triggered by the agitation of waves crashing on a beach

The effects of anthropogenic ocean acidification on phytoplankton growth and community structure has also received considerable attention. The cells of coccolithophore phytoplankton are typically covered in a calcium carbonate shell called a coccosphere that is sensitive to ocean acidification. Because of their short generation times, evidence suggests some phytoplankton can adapt to changes in pH induced by increased carbon dioxide on rapid time-scales (months to years).[30][31]

Phytoplankton serve as the base of the aquatic food web, providing an essential ecological function for all aquatic life. Under future conditions of anthropogenic warming and ocean acidification, changes in phytoplankton mortality due to changes in rates of zooplankton grazing may be significant.[32] One of the many food chains in the ocean – remarkable due to the small number of links – is that of phytoplankton sustaining krill (a crustacean similar to a tiny shrimp), which in turn sustain baleen whales.

The El Niño-Southern Oscillation (ENSO) cycles in the Equatorial Pacific area can affect phytoplankton.[33] Biochemical and physical changes during ENSO cycles modify the phytoplankton community structure.[33] Also, changes in the structure of the phytoplankton, such as a significant reduction in biomass and phytoplankton density, particularly during El Nino phases can occur.[34] The sensitivity of phytoplankton to environmental changes is why they are often used as indicators of estuarine and coastal ecological condition and health.[35] To study these events satellite ocean color observations are used to observe these changes. Satellite images help to have a better view of their global distribution.[33]

Diversity

[edit]
When two currents collide (here the Oyashio and Kuroshio currents) they create eddies. Phytoplankton concentrates along the boundaries of the eddies, tracing the motion of the water.
Algal bloom off south west England
NASA satellite view of Southern Ocean phytoplankton bloom

The term phytoplankton encompasses all photoautotrophic microorganisms in aquatic food webs. However, unlike terrestrial communities, where most autotrophs are plants, phytoplankton are a diverse group, incorporating protistan eukaryotes and both eubacterial and archaebacterial prokaryotes. There are about 5,000 known species of marine phytoplankton.[36] How such diversity evolved despite scarce resources (restricting niche differentiation) is unclear.[37]

In terms of numbers, the most important groups of phytoplankton include the diatoms, cyanobacteria and dinoflagellates, although many other groups of algae are represented. One group, the coccolithophorids, is responsible (in part) for the release of significant amounts of dimethyl sulfide (DMS) into the atmosphere. DMS is oxidized to form sulfate which, in areas where ambient aerosol particle concentrations are low, can contribute to the population of cloud condensation nuclei, mostly leading to increased cloud cover and cloud albedo according to the so-called CLAW hypothesis.[38][39] Different types of phytoplankton support different trophic levels within varying ecosystems. In oligotrophic oceanic regions such as the Sargasso Sea or the South Pacific Gyre, phytoplankton is dominated by the small sized cells, called picoplankton and nanoplankton (also referred to as picoflagellates and nanoflagellates), mostly composed of cyanobacteria (Prochlorococcus, Synechococcus) and picoeucaryotes such as Micromonas. Within more productive ecosystems, dominated by upwelling or high terrestrial inputs, larger dinoflagellates are the more dominant phytoplankton and reflect a larger portion of the biomass.[40]

Growth strategies

[edit]

In the early twentieth century, Alfred C. Redfield found the similarity of the phytoplankton's elemental composition to the major dissolved nutrients in the deep ocean.[41] Redfield proposed that the ratio of carbon to nitrogen to phosphorus (106:16:1) in the ocean was controlled by the phytoplankton's requirements, as phytoplankton subsequently release nitrogen and phosphorus as they are remineralized. This so-called "Redfield ratio" in describing stoichiometry of phytoplankton and seawater has become a fundamental principle to understand marine ecology, biogeochemistry and phytoplankton evolution.[42] However, the Redfield ratio is not a universal value and it may diverge due to the changes in exogenous nutrient delivery[43] and microbial metabolisms in the ocean, such as nitrogen fixation, denitrification and anammox.

The dynamic stoichiometry shown in unicellular algae reflects their capability to store nutrients in an internal pool, shift between enzymes with various nutrient requirements and alter osmolyte composition.[44][45] Different cellular components have their own unique stoichiometry characteristics,[42] for instance, resource (light or nutrients) acquisition machinery such as proteins and chlorophyll contain a high concentration of nitrogen but low in phosphorus. Meanwhile, growth machinery such as ribosomal RNA contains high nitrogen and phosphorus concentrations.

Based on allocation of resources, phytoplankton is classified into three different growth strategies, namely survivalist, bloomer[46] and generalist. Survivalist phytoplankton has a high ratio of N:P (>30) and contains an abundance of resource-acquisition machinery to sustain growth under scarce resources. Bloomer phytoplankton has a low N:P ratio (<10), contains a high proportion of growth machinery, and is adapted to exponential growth. Generalist phytoplankton has similar N:P to the Redfield ratio and contain relatively equal resource-acquisition and growth machinery.

Factors affecting abundance

[edit]

The NAAMES study was a five-year scientific research program conducted between 2015 and 2019 by scientists from Oregon State University and NASA to investigated aspects of phytoplankton dynamics in ocean ecosystems, and how such dynamics influence atmospheric aerosols, clouds, and climate (NAAMES stands for the North Atlantic Aerosols and Marine Ecosystems Study). The study focused on the sub-arctic region of the North Atlantic Ocean, which is the site of one of Earth's largest recurring phytoplankton blooms. The long history of research in this location, as well as relative ease of accessibility, made the North Atlantic an ideal location to test prevailing scientific hypotheses[47] in an effort to better understand the role of phytoplankton aerosol emissions on Earth's energy budget.[48]

NAAMES was designed to target specific phases of the annual phytoplankton cycle: minimum, climax and the intermediary decreasing and increasing biomass, in order to resolve debates on the timing of bloom formations and the patterns driving annual bloom re-creation.[48] The NAAMES project also investigated the quantity, size, and composition of aerosols generated by primary production in order to understand how phytoplankton bloom cycles affect cloud formations and climate.[49]

Competing hypothesis of plankton variability[47]
Figure adapted from Behrenfeld & Boss 2014.[50]
Courtesy of NAAMES, Langley Research Center, NASA[51]
World concentrations of surface ocean chlorophyll as viewed by satellite during the northern spring, averaged from 1998 to 2004. Chlorophyll is a marker for the distribution and abundance of phytoplankton.
Global patterns of monthly phytoplankton species richness and species turnover
(A) Annual mean of monthly species richness and (B) month-to-month species turnover projected by SDMs. Latitudinal gradients of (C) richness and (D) turnover. Colored lines (regressions with local polynomial fitting) indicate the means per degree latitude from three different SDM algorithms used (red shading denotes ±1 SD from 1000 Monte Carlo runs that used varying predictors for GAM). Poleward of the thin horizontal lines shown in (C) and (D), the model results cover only <12 or <9 months, respectively.[52]

Factors affecting productivity

[edit]
Environmental factors that affect phytoplankton productivity [53][54]

Phytoplankton are the key mediators of the biological pump. Understanding the response of phytoplankton to changing environmental conditions is a prerequisite to predict future atmospheric concentrations of CO2. Temperature, irradiance and nutrient concentrations, along with CO2 are the chief environmental factors that influence the physiology and stoichiometry of phytoplankton.[55] The stoichiometry or elemental composition of phytoplankton is of utmost importance to secondary producers such as copepods, fish and shrimp, because it determines the nutritional quality and influences energy flow through the marine food chains.[56] Climate change may greatly restructure phytoplankton communities leading to cascading consequences for marine food webs, thereby altering the amount of carbon transported to the ocean interior.[57][53]

The figure gives an overview of the various environmental factors that together affect phytoplankton productivity. All of these factors are expected to undergo significant changes in the future ocean due to global change.[58] Global warming simulations predict oceanic temperature increase; dramatic changes in oceanic stratification, circulation and changes in cloud cover and sea ice, resulting in an increased light supply to the ocean surface. Also, reduced nutrient supply is predicted to co-occur with ocean acidification and warming, due to increased stratification of the water column and reduced mixing of nutrients from the deep water to the surface.[59][53]

Role of phytoplankton

[edit]
Role of phytoplankton on various compartments of the marine environment [60]

The compartments influenced by phytoplankton include the atmospheric gas composition, inorganic nutrients, and trace element fluxes as well as the transfer and cycling of organic matter via biological processes (see figure). The photosynthetically fixed carbon is rapidly recycled and reused in the surface ocean, while a certain fraction of this biomass is exported as sinking particles to the deep ocean, where it is subject to ongoing transformation processes, e.g., remineralization.[60]

Phytoplankton contribute to not only a basic pelagic marine food web but also to the microbial loop. Phytoplankton are the base of the marine food web and because they do not rely on other organisms for food, they make up the first trophic level. Organisms such as zooplankton feed on these phytoplankton which are in turn fed on by other organisms and so forth until the fourth trophic level is reached with apex predators. Approximately 90% of total carbon is lost between trophic levels due to respiration, detritus, and dissolved organic matter. This makes the remineralization process and nutrient cycling performed by phytoplankton and bacteria important in maintaining efficiency.[61]

Phytoplankton blooms in which a species increases rapidly under conditions favorable to growth can produce harmful algal blooms (HABs).

Aquaculture

[edit]
See also: Algaculture and Culture of microalgae in hatcheries

Phytoplankton are a key food item in both aquaculture and mariculture. Both utilize phytoplankton as food for the animals being farmed. In mariculture, the phytoplankton is naturally occurring and is introduced into enclosures with the normal circulation of seawater. In aquaculture, phytoplankton must be obtained and introduced directly. The plankton can either be collected from a body of water or cultured, though the former method is seldom used. Phytoplankton is used as a foodstock for the production of rotifers,[62] which are in turn used to feed other organisms. Phytoplankton is also used to feed many varieties of aquacultured molluscs, including pearl oysters and giant clams. A 2018 study estimated the nutritional value of natural phytoplankton in terms of carbohydrate, protein and lipid across the world ocean using ocean-colour data from satellites,[63] and found the calorific value of phytoplankton to vary considerably across different oceanic regions and between different time of the year.[63][64]

The production of phytoplankton under artificial conditions is itself a form of aquaculture. Phytoplankton is cultured for a variety of purposes, including foodstock for other aquacultured organisms,[62] a nutritional supplement for captive invertebrates in aquaria. Culture sizes range from small-scale laboratory cultures of less than 1L to several tens of thousands of litres for commercial aquaculture.[62] Regardless of the size of the culture, certain conditions must be provided for efficient growth of plankton. The majority of cultured plankton is marine, and seawater of a specific gravity of 1.010 to 1.026 may be used as a culture medium. This water must be sterilized, usually by either high temperatures in an autoclave or by exposure to ultraviolet radiation, to prevent biological contamination of the culture. Various fertilizers are added to the culture medium to facilitate the growth of plankton. A culture must be aerated or agitated in some way to keep plankton suspended, as well as to provide dissolved carbon dioxide for photosynthesis. In addition to constant aeration, most cultures are manually mixed or stirred on a regular basis. Light must be provided for the growth of phytoplankton. The colour temperature of illumination should be approximately 6,500 K, but values from 4,000 K to upwards of 20,000 K have been used successfully. The duration of light exposure should be approximately 16 hours daily; this is the most efficient artificial day length.[62]

Anthropogenic changes

[edit]
Plot demonstrating increases in phytoplankton species richness with increased temperature
See also: Human impact on marine life

Marine phytoplankton perform half of the global photosynthetic CO2 fixation (net global primary production of ~50 Pg C per year) and half of the oxygen production despite amounting to only ~1% of global plant biomass.[65] In comparison with terrestrial plants, marine phytoplankton are distributed over a larger surface area, are exposed to less seasonal variation and have markedly faster turnover rates than trees (days versus decades).[65] Therefore, phytoplankton respond rapidly on a global scale to climate variations. These characteristics are important when one is evaluating the contributions of phytoplankton to carbon fixation and forecasting how this production may change in response to perturbations. Predicting the effects of climate change on primary productivity is complicated by phytoplankton bloom cycles that are affected by both bottom-up control (for example, availability of essential nutrients and vertical mixing) and top-down control (for example, grazing and viruses).[66][65][67][68][69][70] Increases in solar radiation, temperature and freshwater inputs to surface waters strengthen ocean stratification and consequently reduce transport of nutrients from deep water to surface waters, which reduces primary productivity.[65][70][71] Conversely, rising CO2 levels can increase phytoplankton primary production, but only when nutrients are not limiting.[72][73][74][32]

Some studies indicate that overall global oceanic phytoplankton density has decreased in the past century,[75] but these conclusions have been questioned because of the limited availability of long-term phytoplankton data, methodological differences in data generation and the large annual and decadal variability in phytoplankton production.[76][77][78][79] Moreover, other studies suggest a global increase in oceanic phytoplankton production[80] and changes in specific regions or specific phytoplankton groups.[81][82] The global Sea Ice Index is declining,[83] leading to higher light penetration and potentially more primary production;[84] however, there are conflicting predictions for the effects of variable mixing patterns and changes in nutrient supply and for productivity trends in polar zones.[70][32]

The effect of human-caused climate change on phytoplankton biodiversity is not well understood. Should greenhouse gas emissions continue rising to high levels by 2100, some phytoplankton models predict an increase in species richness, or the number of different species within a given area. This increase in plankton diversity is traced to warming ocean temperatures. In addition to species richness changes, the locations where phytoplankton are distributed are expected to shift towards the Earth's poles. Such movement may disrupt ecosystems, because phytoplankton are consumed by zooplankton, which in turn sustain fisheries. This shift in phytoplankton location may also diminish the ability of phytoplankton to store carbon that was emitted by human activities. Human (anthropogenic) changes to phytoplankton impact both natural and economic processes.[85]

See also

[edit]
Wikimedia Commons has media related to Phytoplankton.
Wikimedia Commons has media related to Algal blooms.

References

[edit]
  1. ^ Thurman, H. V. (2007). Introductory Oceanography. Academic Internet Publishers. ISBN 978-1-4288-3314-2.[page needed]
  2. ^ a b c Pierella Karlusich, Juan José; Ibarbalz, Federico M.; Bowler, Chris (3 January 2020). "Phytoplankton in the Tara Ocean". Annual Review of Marine Science. 12 (1): 233–265. Bibcode:2020ARMS...12..233P. doi:10.1146/annurev-marine-010419-010706. ISSN 1941-1405. PMID 31899671. S2CID 209748051.
  3. ^ Pierella Karlusich, Juan José; Ibarbalz, Federico M; Bowler, Chris (2020). "Exploration of marine phytoplankton: from their historical appreciation to the omics era". Journal of Plankton Research. 42: 595–612. doi:10.1093/plankt/fbaa049. hdl:11336/143676.
  4. ^ Ghosal; Rogers; Wray, S.; M.; A. "The Effects of Turbulence on Phytoplankton". Aerospace Technology Enterprise. NTRS. Retrieved 16 June 2011.{{cite web}}: CS1 maint: multiple names: authors list (link)
  5. ^ a b Modeled Phytoplankton Communities in the Global Ocean NASA Hyperwall, 30 September 2015. Public Domain This article incorporates text from this source, which is in the public domain.
  6. ^ Mitra, Aditee; Caron, David A.; Faure, Emile; Flynn, Kevin J.; Leles, Suzana Gonçalves; Hansen, Per J.; McManus, George B.; Not, Fabrice; do Rosario Gomes, Helga; Santoferrara, Luciana F.; Stoecker, Diane K.; Tillmann, Urban (27 February 2023). "The Mixoplankton Database (MDB): Diversity of photo-phago-trophic plankton in form, function, and distribution across the global ocean". Journal of Eukaryotic Microbiology. 70 (4): e12972. doi:10.1111/jeu.12972. ISSN 1066-5234. PMID 36847544.
  7. ^ Flynn, Kevin J; Mitra, Aditee; Anestis, Konstantinos; Anschütz, Anna A; Calbet, Albert; Ferreira, Guilherme Duarte; Gypens, Nathalie; Hansen, Per J; John, Uwe; Martin, Jon Lapeyra; Mansour, Joost S; Maselli, Maira; Medić, Nikola; Norlin, Andreas; Not, Fabrice (26 July 2019). "Mixotrophic protists and a new paradigm for marine ecology: where does plankton research go now?". Journal of Plankton Research. 41 (4): 375–391. doi:10.1093/plankt/fbz026. hdl:10261/192145. ISSN 0142-7873.
  8. ^ Glibert, Patricia M.; Mitra, Aditee (21 January 2022). "From webs, loops, shunts, and pumps to microbial multitasking: Evolving concepts of marine microbial ecology, the mixoplankton paradigm, and implications for a future ocean". Limnology and Oceanography. 67 (3): 585–597. Bibcode:2022LimOc..67..585G. doi:10.1002/lno.12018. ISSN 0024-3590.
  9. ^ "MIT Darwin Project". Massachusetts Institute of Technology.
  10. ^ Michael J. Behrenfeld; et al. (30 March 2001). "Biospheric primary production during an ENSO transition" (PDF). Science. 291 (5513): 2594–7. Bibcode:2001Sci...291.2594B. doi:10.1126/science.1055071. PMID 11283369. S2CID 38043167.
  11. ^ "NASA Satellite Detects Red Glow to Map Global Ocean Plant Health" Archived 10 April 2021 at the Wayback Machine NASA, 28 May 2009.
  12. ^ "Satellite Sees Ocean Plants Increase, Coasts Greening". NASA. 2 March 2005. Archived from the original on 29 October 2011. Retrieved 9 June 2014.
  13. ^ Mitra, Aditee; Flynn, Kevin J.; Tillmann, Urban; Raven, John A.; Caron, David; Stoecker, Diane K.; Not, Fabrice; Hansen, Per J.; Hallegraeff, Gustaaf; Sanders, Robert; Wilken, Susanne; McManus, George; Johnson, Mathew; Pitta, Paraskevi; Våge, Selina; Berge, Terje; Calbet, Albert; Thingstad, Frede; Jeong, Hae Jin; Burkholder, Joann; Glibert, Patricia M.; Granéli, Edna; Lundgren, Veronica (1 April 2016). "Defining Planktonic Protist Functional Groups on Mechanisms for Energy and Nutrient Acquisition: Incorporation of Diverse Mixotrophic". Protist. 167 (2): 106–120. doi:10.1016/j.protis.2016.01.003. hdl:10261/131722. ISSN 1434-4610. PMID 26927496.
  14. ^ Kirk, John T. O. (1994). Light and Photosynthesis in Aquatic Ecosystems (2 ed.). Cambridge: Cambridge University Press. doi:10.1017/cbo9780511623370. ISBN 9780511623370.
  15. ^ Stomp, Maayke; Huisman, Jef; de Jongh, Floris; Veraart, Annelies J.; Gerla, Daan; Rijkeboer, Machteld; Ibelings, Bas W.; Wollenzien, Ute I. A.; Stal, Lucas J. (November 2004). "Adaptive divergence in pigment composition promotes phytoplankton biodiversity". Nature. 432 (7013): 104–107. Bibcode:2004Natur.432..104S. doi:10.1038/nature03044. ISSN 1476-4687. PMID 15475947. S2CID 4409758.
  16. ^ Hintz, Nils Hendrik; Zeising, Moritz; Striebel, Maren (2021). "Changes in spectral quality of underwater light alter phytoplankton community composition". Limnology and Oceanography. 66 (9): 3327–3337. Bibcode:2021LimOc..66.3327H. doi:10.1002/lno.11882. ISSN 1939-5590. S2CID 237849374.
  17. ^ a b Käse L, Geuer JK. (2018) "Phytoplankton responses to marine climate change–an introduction". In Jungblut S., Liebich V., Bode M. (Eds) YOUMARES 8–Oceans Across Boundaries: Learning from each other, pages 55–72, Springer. doi:10.1007/978-3-319-93284-2_5. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License.
  18. ^ Sunda, William (7 June 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.
  19. ^ Browning, Thomas J.; Moore, C. Mark (17 August 2023). "Global analysis of ocean phytoplankton nutrient limitation reveals high prevalence of co-limitation". Nature Communications. 14 (1): 5014. Bibcode:2023NatCo..14.5014B. doi:10.1038/s41467-023-40774-0. ISSN 2041-1723. PMC 10435517. PMID 37591895.
  20. ^ Moore, C. M.; Mills, M. M.; Arrigo, K. R.; Berman-Frank, I.; Bopp, L.; Boyd, P. W.; Galbraith, E. D.; Geider, R. J.; Guieu, C.; Jaccard, S. L.; Jickells, T. D.; La Roche, J.; Lenton, T. M.; Mahowald, N. M.; Marañón, E. (September 2013). "Processes and patterns of oceanic nutrient limitation". Nature Geoscience. 6 (9): 701–710. Bibcode:2013NatGe...6..701M. doi:10.1038/ngeo1765. ISSN 1752-0908.
  21. ^ Tagliabue, Alessandro; Bowie, Andrew R.; Boyd, Philip W.; Buck, Kristen N.; Johnson, Kenneth S.; Saito, Mak A. (March 2017). "The integral role of iron in ocean biogeochemistry". Nature. 543 (7643): 51–59. Bibcode:2017Natur.543...51T. doi:10.1038/nature21058. ISSN 1476-4687. PMID 28252066.
  22. ^ Richtel, M. (1 May 2007). "Recruiting Plankton to Fight Global Warming". The New York Times.
  23. ^ Monastersky, Richard (1995). "Iron versus the Greenhouse: Oceanographers Cautiously Explore a Global Warming Therapy". Science News. 148 (14): 220–1. doi:10.2307/4018225. JSTOR 4018225.
  24. ^ Buesseler, Ken O.; Bianchi, Daniele; Chai, Fei; Cullen, Jay T.; Estapa, Margaret; Hawco, Nicholas; John, Seth; McGillicuddy, Dennis J.; Morris, Paul J.; Nawaz, Sara; Nishioka, Jun; Pham, Anh; Ramakrishna, Kilaparti; Siegel, David A.; Smith, Sarah R. (9 September 2024). "Next steps for assessing ocean iron fertilization for marine carbon dioxide removal". Frontiers in Climate. 6. doi:10.3389/fclim.2024.1430957. ISSN 2624-9553.
  25. ^ Luhn, Alec. "Scientists Will Engineer the Ocean to Absorb More Carbon Dioxide". Scientific American. Retrieved 21 October 2024.
  26. ^ Cullen, John J.; Boyd, Philip W. (29 July 2008). "Predicting and verifying the intended and unintended consequences of large-scale ocean iron fertilization". Marine Ecology Progress Series. 364: 295–301. Bibcode:2008MEPS..364..295C. doi:10.3354/meps07551. ISSN 0171-8630.
  27. ^ Sañudo-Wilhelmy, Sergio (23 June 2012). "Existence of vitamin 'deserts' in the ocean confirmed". ScienceDaily.
  28. ^ Henson, S. A.; Sarmiento, J. L.; Dunne, J. P.; Bopp, L.; Lima, I.; Doney, S. C.; John, J.; Beaulieu, C. (2010). "Detection of anthropogenic climate change in satellite records of ocean chlorophyll and productivity". Biogeosciences. 7 (2): 621–40. Bibcode:2010BGeo....7..621H. doi:10.5194/bg-7-621-2010. hdl:1912/3208.
  29. ^ Steinacher, M.; Joos, F.; Frölicher, T. L.; Bopp, L.; Cadule, P.; Cocco, V.; Doney, S. C.; Gehlen, M.; Lindsay, K.; Moore, J. K.; Schneider, B.; Segschneider, J. (2010). "Projected 21st century decrease in marine productivity: a multi-model analysis". Biogeosciences. 7 (3): 979–1005. Bibcode:2010BGeo....7..979S. doi:10.5194/bg-7-979-2010. hdl:11858/00-001M-0000-0011-F69E-5.
  30. ^ Collins, Sinéad; Rost, Björn; Rynearson, Tatiana A. (25 November 2013). "Evolutionary potential of marine phytoplankton under ocean acidification". Evolutionary Applications. 7 (1): 140–155. doi:10.1111/eva.12120. ISSN 1752-4571. PMC 3894903. PMID 24454553.
  31. ^ Lohbeck, Kai T.; Riebesell, Ulf; Reusch, Thorsten B. H. (8 April 2012). "Adaptive evolution of a key phytoplankton species to ocean acidification". Nature Geoscience. 5 (5): 346–351. Bibcode:2012NatGe...5..346L. doi:10.1038/ngeo1441. ISSN 1752-0894.
  32. ^ a b c Cavicchioli, Ricardo; Ripple, William J.; Timmis, Kenneth N.; Azam, Farooq; Bakken, Lars R.; Baylis, Matthew; Behrenfeld, Michael J.; Boetius, Antje; Boyd, Philip W.; Classen, Aimée T.; Crowther, Thomas W.; Danovaro, Roberto; Foreman, Christine M.; Huisman, Jef; Hutchins, David A.; Jansson, Janet K.; Karl, David M.; Koskella, Britt; Mark Welch, David B.; Martiny, Jennifer B. H.; Moran, Mary Ann; Orphan, Victoria J.; Reay, David S.; Remais, Justin V.; Rich, Virginia I.; Singh, Brajesh K.; Stein, Lisa Y.; Stewart, Frank J.; Sullivan, Matthew B.; 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. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License.
  33. ^ a b c Masotti, I.; Moulin, C.; Alvain, S.; Bopp, L.; Tagliabue, A.; Antoine, D. (4 March 2011). "Large-scale shifts in phytoplankton groups in the Equatorial Pacific during ENSO cycles". Biogeosciences. 8 (3): 539–550. Bibcode:2011BGeo....8..539M. doi:10.5194/bg-8-539-2011. hdl:20.500.11937/40912.
  34. ^ Sathicqab, María Belén; Bauerac, Delia Elena; Gómez, Nora (15 September 2015). "Influence of El Niño Southern Oscillation phenomenon on coastal phytoplankton in a mixohaline ecosystem on the southeastern of South America: Río de la Plata estuary". Marine Pollution Bulletin. 98 (1–2): 26–33. Bibcode:2015MarPB..98...26S. doi:10.1016/j.marpolbul.2015.07.017. hdl:11336/112961. PMID 26183307.
  35. ^ Sathicq, María Belén; Bauer, Delia Elena; Gómez, Nora (15 September 2015). "Influence of El Niño Southern Oscillation phenomenon on coastal phytoplankton in a mixohaline ecosystem on the southeastern of South America: Río de la Plata estuary". Marine Pollution Bulletin. 98 (1–2): 26–33. Bibcode:2015MarPB..98...26S. doi:10.1016/j.marpolbul.2015.07.017. hdl:11336/112961. PMID 26183307.
  36. ^ Hallegraeff, G.M. (2003). "Harmful algal blooms: a global overview" (PDF). In Hallegraeff, Gustaaf M.; Anderson, Donald Mark; Cembella, Allan D.; Enevoldsen, Henrik O. (eds.). Manual on Harmful Marine Microalgae. Unesco. pp. 25–49. ISBN 978-92-3-103871-6.
  37. ^ Hutchinson, G. E. (1961). "The Paradox of the Plankton". The American Naturalist. 95 (882): 137–45. doi:10.1086/282171. S2CID 86353285.
  38. ^ Charlson, Robert J.; Lovelock, James E.; Andreae, Meinrat O.; Warren, Stephen G. (1987). "Oceanic phytoplankton, atmospheric sulphur, cloud albedo and climate". Nature. 326 (6114): 655–61. Bibcode:1987Natur.326..655C. doi:10.1038/326655a0. S2CID 4321239.
  39. ^ Quinn, P. K.; Bates, T. S. (2011). "The case against climate regulation via oceanic phytoplankton sulphur emissions". Nature. 480 (7375): 51–6. Bibcode:2011Natur.480...51Q. doi:10.1038/nature10580. PMID 22129724. S2CID 4417436.
  40. ^ Calbet, A. (2008). "The trophic roles of microzooplankton in marine systems". ICES Journal of Marine Science. 65 (3): 325–31. doi:10.1093/icesjms/fsn013.
  41. ^ Redfield, Alfred C. (1934). "On the Proportions of Organic Derivatives in Sea Water and their Relation to the Composition of Plankton". In Johnstone, James; Daniel, Richard Jellicoe (eds.). James Johnstone Memorial Volume. Liverpool: University Press of Liverpool. pp. 176–92. OCLC 13993674.
  42. ^ a b Arrigo, Kevin R. (2005). "Marine microorganisms and global nutrient cycles". Nature. 437 (7057): 349–55. Bibcode:2005Natur.437..349A. doi:10.1038/nature04159. PMID 16163345. S2CID 62781480.
  43. ^ Fanning, Kent A. (1989). "Influence of atmospheric pollution on nutrient limitation in the ocean". Nature. 339 (6224): 460–63. Bibcode:1989Natur.339..460F. doi:10.1038/339460a0. S2CID 4247689.
  44. ^ Sterner, Robert Warner; Elser, James J. (2002). Ecological Stoichiometry: The Biology of Elements from Molecules to the Biosphere. Princeton University Press. ISBN 978-0-691-07491-7.[page needed]
  45. ^ Klausmeier, Christopher A.; Litchman, Elena; Levin, Simon A. (2004). "Phytoplankton growth and stoichiometry under multiple nutrient limitation". Limnology and Oceanography. 49 (4 Part 2): 1463–70. Bibcode:2004LimOc..49.1463K. doi:10.4319/lo.2004.49.4_part_2.1463. S2CID 16438669.
  46. ^ Klausmeier, Christopher A.; Litchman, Elena; Daufresne, Tanguy; Levin, Simon A. (2004). "Optimal nitrogen-to-phosphorus stoichiometry of phytoplankton". Nature. 429 (6988): 171–4. Bibcode:2004Natur.429..171K. doi:10.1038/nature02454. PMID 15141209. S2CID 4308845.
  47. ^ a b Behrenfeld, M.J. and Boss, E.S. (2018) "Student's tutorial on bloom hypotheses in the context of phytoplankton annual cycles". Global change biology, 24(1): 55–77. doi:10.1111/gcb.13858.
  48. ^ a b Behrenfeld, Michael J.; Moore, Richard H.; Hostetler, Chris A.; Graff, Jason; Gaube, Peter; Russell, Lynn M.; Chen, Gao; Doney, Scott C.; Giovannoni, Stephen; Liu, Hongyu; Proctor, Christopher (22 March 2019). "The North Atlantic Aerosol and Marine Ecosystem Study (NAAMES): Science Motive and Mission Overview". Frontiers in Marine Science. 6: 122. doi:10.3389/fmars.2019.00122. ISSN 2296-7745.
  49. ^ Engel, Anja; Bange, Hermann W.; Cunliffe, Michael; Burrows, Susannah M.; Friedrichs, Gernot; Galgani, Luisa; Herrmann, Hartmut; Hertkorn, Norbert; Johnson, Martin; Liss, Peter S.; Quinn, Patricia K. (30 May 2017). "The Ocean's Vital Skin: Toward an Integrated Understanding of the Sea Surface Microlayer". Frontiers in Marine Science. 4. doi:10.3389/fmars.2017.00165. hdl:10026.1/16046. ISSN 2296-7745.
  50. ^ Behrenfeld, Michael J.; Boss, Emmanuel S. (3 January 2014). "Resurrecting the Ecological Underpinnings of Ocean Plankton Blooms". Annual Review of Marine Science. 6 (1): 167–194. Bibcode:2014ARMS....6..167B. doi:10.1146/annurev-marine-052913-021325. ISSN 1941-1405. PMID 24079309. S2CID 12903662.
  51. ^ NAAMES: Science - Objectives Langley Research Center, NASA, Updated: 6 June 2020. Retrieved: 15 June 2020.
  52. ^ Righetti, D., Vogt, M., Gruber, N., Psomas, A. and Zimmermann, N.E. (2019) "Global pattern of phytoplankton diversity driven by temperature and environmental variability". Science advances, 5(5): eaau6253. doi:10.1126/sciadv.aau6253. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License.
  53. ^ a b c Beardall, John; Stojkovic, Slobodanka; Larsen, Stuart (2009). "Living in a high CO2world: Impacts of global climate change on marine phytoplankton". Plant Ecology & Diversity. 2 (2): 191–205. Bibcode:2009PlEcD...2..191B. doi:10.1080/17550870903271363. S2CID 83586220.
  54. ^ Basu, Samarpita; MacKey, Katherine (2018). "Phytoplankton as Key Mediators of the Biological Carbon Pump: Their Responses to a Changing Climate". Sustainability. 10 (3): 869. doi:10.3390/su10030869. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License.
  55. ^ Moreno, Allison R.; Hagstrom, George I.; Primeau, Francois W.; Levin, Simon A.; Martiny, Adam C. (2018). "Marine phytoplankton stoichiometry mediates nonlinear interactions between nutrient supply, temperature, and atmospheric CO2". Biogeosciences. 15 (9): 2761–2779. Bibcode:2018BGeo...15.2761M. doi:10.5194/bg-15-2761-2018.
  56. ^ Li, Wei; Gao, Kunshan; Beardall, John (2012). "Interactive Effects of Ocean Acidification and Nitrogen-Limitation on the Diatom Phaeodactylum tricornutum". PLOS ONE. 7 (12): e51590. Bibcode:2012PLoSO...751590L. doi:10.1371/journal.pone.0051590. PMC 3517544. PMID 23236517.
  57. ^ Irwin, Andrew J.; Finkel, Zoe V.; Müller-Karger, Frank E.; Troccoli Ghinaglia, Luis (2015). "Phytoplankton adapt to changing ocean environments". Proceedings of the National Academy of Sciences. 112 (18): 5762–5766. Bibcode:2015PNAS..112.5762I. doi:10.1073/pnas.1414752112. PMC 4426419. PMID 25902497.
  58. ^ Häder, Donat-P.; Villafañe, Virginia E.; Helbling, E. Walter (2014). "Productivity of aquatic primary producers under global climate change". Photochem. Photobiol. Sci. 13 (10): 1370–1392. Bibcode:2014PhPhS..13.1370H. doi:10.1039/C3PP50418B. hdl:11336/24725. PMID 25191675.
  59. ^ Sarmiento, J. L.; Slater, R.; Barber, R.; Bopp, L.; Doney, S. C.; Hirst, A. C.; Kleypas, J.; Matear, R.; Mikolajewicz, U.; Monfray, P.; Soldatov, V.; Spall, S. A.; Stouffer, R. (2004). "Response of ocean ecosystems to climate warming". Global Biogeochemical Cycles. 18 (3): n/a. Bibcode:2004GBioC..18.3003S. doi:10.1029/2003GB002134. hdl:1912/3392.
  60. ^ a b Heinrichs, Mara E.; Mori, Corinna; Dlugosch, Leon (2020). "Complex Interactions Between Aquatic Organisms and Their Chemical Environment Elucidated from Different Perspectives". YOUMARES 9 - the Oceans: Our Research, Our Future. pp. 279–297. doi:10.1007/978-3-030-20389-4_15. ISBN 978-3-030-20388-7. S2CID 210308256. Material was copied from this source, which is available under a Creative Commons Attribution 4.0 International License.
  61. ^ Lalli, Carol M. (16 May 1997). Biological oceanography an introduction. Elsevier Science. ISBN 978-0-7506-3384-0. OCLC 837077589.
  62. ^ a b c d McVey, James P., Nai-Hsien Chao, and Cheng-Sheng Lee. CRC Handbook of Mariculture Vol. 1 : Crustacean Aquaculture. New York: CRC Press LLC, 1993.[page needed]
  63. ^ a b Roy, Shovonlal (12 February 2018). "Distributions of phytoplankton carbohydrate, protein and lipid in the world oceans from satellite ocean colour". The ISME Journal. 12 (6): 1457–1472. Bibcode:2018ISMEJ..12.1457R. doi:10.1038/s41396-018-0054-8. ISSN 1751-7370. PMC 5955997. PMID 29434313.
  64. ^ "Nutrition study reveals instability in world's most important fishing regions".
  65. ^ a b c d Behrenfeld, Michael J. (2014). "Climate-mediated dance of the plankton". Nature Climate Change. 4 (10): 880–887. Bibcode:2014NatCC...4..880B. doi:10.1038/nclimate2349.
  66. ^ Hutchins, D. A.; Boyd, P. W. (2016). "Marine phytoplankton and the changing ocean iron cycle". Nature Climate Change. 6 (12): 1072–1079. Bibcode:2016NatCC...6.1072H. doi:10.1038/nclimate3147.
  67. ^ De Baar, Hein J. W.; De Jong, Jeroen T. M.; Bakker, Dorothée C. E.; Löscher, Bettina M.; Veth, Cornelis; Bathmann, Uli; Smetacek, Victor (1995). "Importance of iron for plankton blooms and carbon dioxide drawdown in the Southern Ocean". Nature. 373 (6513): 412–415. Bibcode:1995Natur.373..412D. doi:10.1038/373412a0. S2CID 4257465.
  68. ^ Boyd, P. W.; Jickells, T.; Law, C. S.; Blain, S.; Boyle, E. A.; Buesseler, K. O.; Coale, K. H.; Cullen, J. J.; De Baar, H. J. W.; Follows, M.; Harvey, M.; Lancelot, C.; Levasseur, M.; Owens, N. P. J.; Pollard, R.; Rivkin, R. B.; Sarmiento, J.; Schoemann, V.; Smetacek, V.; Takeda, S.; Tsuda, A.; Turner, S.; Watson, A. J. (2007). "Mesoscale Iron Enrichment Experiments 1993-2005: Synthesis and Future Directions" (PDF). Science. 315 (5812): 612–617. Bibcode:2007Sci...315..612B. doi:10.1126/science.1131669. PMID 17272712. S2CID 2476669. Archived from the original (PDF) on 2 November 2020. Retrieved 29 October 2020.
  69. ^ Behrenfeld, Michael J.; o'Malley, Robert T.; Boss, Emmanuel S.; Westberry, Toby K.; Graff, Jason R.; Halsey, Kimberly H.; Milligan, Allen J.; Siegel, David A.; Brown, Matthew B. (2016). "Revaluating ocean warming impacts on global phytoplankton". Nature Climate Change. 6 (3): 323–330. Bibcode:2016NatCC...6..323B. doi:10.1038/nclimate2838.
  70. ^ a b c Behrenfeld, Michael J.; Hu, Yongxiang; o'Malley, Robert T.; Boss, Emmanuel S.; Hostetler, Chris A.; Siegel, David A.; Sarmiento, Jorge L.; Schulien, Jennifer; Hair, Johnathan W.; Lu, Xiaomei; Rodier, Sharon; Scarino, Amy Jo (2017). "Annual boom–bust cycles of polar phytoplankton biomass revealed by space-based lidar". Nature Geoscience. 10 (2): 118–122. Bibcode:2017NatGe..10..118B. doi:10.1038/ngeo2861.
  71. ^ Behrenfeld, Michael J.; o'Malley, Robert T.; Siegel, David A.; McClain, Charles R.; Sarmiento, Jorge L.; Feldman, Gene C.; Milligan, Allen J.; Falkowski, Paul G.; Letelier, Ricardo M.; Boss, Emmanuel S. (2006). "Climate-driven trends in contemporary ocean productivity". Nature. 444 (7120): 752–755. Bibcode:2006Natur.444..752B. doi:10.1038/nature05317. PMID 17151666. S2CID 4414391.
  72. ^ Levitan, O.; Rosenberg, G.; Setlik, I.; Setlikova, E.; Grigel, J.; Klepetar, J.; Prasil, O.; Berman-Frank, I. (2007). "Elevated CO2 enhances nitrogen fixation and growth in the marine cyanobacterium Trichodesmium". Global Change Biology. 13 (2): 531–538. Bibcode:2007GCBio..13..531L. doi:10.1111/j.1365-2486.2006.01314.x. S2CID 86121269.
  73. ^ Verspagen, Jolanda M. H.; Van De Waal, Dedmer B.; Finke, Jan F.; Visser, Petra M.; Huisman, Jef (2014). "Contrasting effects of rising CO2 on primary production and ecological stoichiometry at different nutrient levels" (PDF). Ecology Letters. 17 (8): 951–960. Bibcode:2014EcolL..17..951V. doi:10.1111/ele.12298. hdl:20.500.11755/ecac2c45-7efa-4c90-9e29-f2bafcee1c95. PMID 24813339.
  74. ^ Holding, J. M.; Duarte, C. M.; Sanz-Martín, M.; Mesa, E.; Arrieta, J. M.; Chierici, M.; Hendriks, I. E.; García-Corral, L. S.; Regaudie-De-Gioux, A.; Delgado, A.; Reigstad, M.; Wassmann, P.; Agustí, S. (2015). "Temperature dependence of CO2-enhanced primary production in the European Arctic Ocean". Nature Climate Change. 5 (12): 1079–1082. Bibcode:2015NatCC...5.1079H. doi:10.1038/nclimate2768. hdl:10754/596052.
  75. ^ Boyce, Daniel G.; Lewis, Marlon R.; Worm, Boris (2010). "Global phytoplankton decline over the past century". Nature. 466 (7306): 591–596. Bibcode:2010Natur.466..591B. doi:10.1038/nature09268. PMID 20671703. S2CID 2413382.
  76. ^ MacKas, David L. (2011). "Does blending of chlorophyll data bias temporal trend?". Nature. 472 (7342): E4 – E5. Bibcode:2011Natur.472E...4M. doi:10.1038/nature09951. PMID 21490623. S2CID 4308744.
  77. ^ Rykaczewski, Ryan R.; Dunne, John P. (2011). "A measured look at ocean chlorophyll trends". Nature. 472 (7342): E5 – E6. Bibcode:2011Natur.472E...5R. doi:10.1038/nature09952. PMID 21490624. S2CID 205224535.
  78. ^ McQuatters-Gollop, Abigail; Reid, Philip C.; Edwards, Martin; Burkill, Peter H.; Castellani, Claudia; Batten, Sonia; Gieskes, Winfried; Beare, Doug; Bidigare, Robert R.; Head, Erica; Johnson, Rod; Kahru, Mati; Koslow, J. Anthony; Pena, Angelica (2011). "Is there a decline in marine phytoplankton?". Nature. 472 (7342): E6 – E7. Bibcode:2011Natur.472E...6M. doi:10.1038/nature09950. PMID 21490625. S2CID 205224519.
  79. ^ Boyce, Daniel G.; Lewis, Marlon R.; Worm, Boris (2011). "Boyce et al. Reply". Nature. 472 (7342): E8 – E9. Bibcode:2011Natur.472E...8B. doi:10.1038/nature09953. S2CID 4317554.
  80. ^ Antoine, David (2005). "Bridging ocean color observations of the 1980s and 2000s in search of long-term trends". Journal of Geophysical Research. 110 (C6): C06009. Bibcode:2005JGRC..110.6009A. doi:10.1029/2004JC002620.
  81. ^ Wernand, Marcel R.; Van Der Woerd, Hendrik J.; Gieskes, Winfried W. C. (2013). "Trends in Ocean Colour and Chlorophyll Concentration from 1889 to 2000, Worldwide". PLOS ONE. 8 (6): e63766. Bibcode:2013PLoSO...863766W. doi:10.1371/journal.pone.0063766. PMC 3680421. PMID 23776435.
  82. ^ Rousseaux, Cecile S.; Gregg, Watson W. (2015). "Recent decadal trends in global phytoplankton composition". Global Biogeochemical Cycles. 29 (10): 1674–1688. Bibcode:2015GBioC..29.1674R. doi:10.1002/2015GB005139.
  83. ^ Sea Ice Index National Snow and Ice Data Center. Accessed 30 October 2020.
  84. ^ Kirchman, David L.; Morán, Xosé Anxelu G.; Ducklow, Hugh (2009). "Microbial growth in the polar oceans – role of temperature and potential impact of climate change". Nature Reviews Microbiology. 7 (6): 451–459. doi:10.1038/nrmicro2115. PMID 19421189. S2CID 31230080.
  85. ^ Benedetti, Fabio; Vogt, Meike; Elizondo, Urs Hofmann; Righetti, Damiano; Zimmermann, Niklaus E.; Gruber, Nicolas (1 September 2021). "Major restructuring of marine plankton assemblages under global warming". Nature Communications. 12 (1): 5226. Bibcode:2021NatCo..12.5226B. doi:10.1038/s41467-021-25385-x. ISSN 2041-1723. PMC 8410869. PMID 34471105.

Further reading

[edit]
[edit]
Retrieved from "https://en.wikipedia.org/w/index.php?title=Phytoplankton&oldid=1262745047"