Earth:Ocean temperature

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Short description: Physical quantity that expresses hot and cold in ocean water
Graph of different thermoclines (depth versus ocean temperature) based on seasons and latitude.

Several factors cause the ocean temperature to vary. These are depth, geographical location and season. Both the temperature and salinity of ocean water differ. Warm surface water is generally saltier than the cooler deep or polar waters.[1] In polar regions, the upper layers of ocean water are cold and fresh.[2] Deep ocean water is cold, salty water found deep below the surface of Earth's oceans. This water has a uniform temperature of around 0-3 °C.[3] The ocean temperature also depends on the amount of solar radiation falling on its surface. In the tropics, with the Sun nearly overhead, the temperature of the surface layers can rise to over 30 °C (86 °F). Near the poles the temperature in equilibrium with the sea ice is about −2 °C (28 °F). There is a continuous circulation of water in the oceans. Thermohaline circulation (THC) is part of the large-scale ocean circulation. It is driven by global density gradients created by surface heat and freshwater fluxes.[4][5] Warm surface currents cool as they move away from the tropics. This happens as the water becomes denser and sinks. Changes in temperature and density move the cold water back towards the equator as a deep sea current. Then it eventually wells up again towards the surface.

Ocean temperature as a term applies to the temperature in the ocean at any depth. It can also apply specifically to the ocean temperatures that are not near the surface. In this case it is synonymous with "deep ocean temperature").

It is clear that the oceans are warming as a result of climate change and this rate of warming is increasing.[6]:9[7] The upper ocean (above 700 m) is warming fastest, but the warming trend extends throughout the ocean. In 2022, the global ocean was the hottest ever recorded by humans.[8]


Definition and types

Sea surface temperature

This section is an excerpt from Sea surface temperature[ edit ]

Deep ocean temperature

Experts refer to the temperature further below the surface as "ocean temperature" or "deep ocean temperature". Ocean temperatures more than 20 metres below the surface vary by region and time. They contribute to variations in ocean heat content and ocean stratification.[9] The increase of both ocean surface temperature and deeper ocean temperature is an important effect of climate change on oceans.[9]

Deep ocean water is the name for cold, salty water found deep below the surface of Earth's oceans. Deep ocean water makes up about 90% of the volume of the oceans. Deep ocean water has a very uniform temperature of around 0-3 °C. Its salinity is about 3.5% or 35 ppt (parts per thousand).[3]

Relevance

Ocean temperature and dissolved oxygen concentrations have a big influence on many aspects of the ocean. These two key parameters affect the ocean's primary productivity, the oceanic carbon cycle, nutrient cycles, and marine ecosystems.[10] They work in conjunction with salinity and density to control a range of processes. These include mixing versus stratification, ocean currents and the thermohaline circulation.

Ocean heat content

Experts calculate ocean heat content by using ocean temperatures at different depths.

This section is an excerpt from Ocean heat content[ edit ]

Measurements

There are various ways to measure ocean temperature.[11] Below the sea surface, it is important to refer to the specific depth of measurement as well as measuring the general temperature. The reason is there is a lot of variation with depths. This is especially the case during the day. At this time low wind speed and a lot of sunshine may lead to the formation of a warm layer at the ocean surface and big changes in temperature as you get deeper. Experts call these strong daytime vertical temperature gradients a diurnal thermocline.[12]

The basic technique involves lowering a device to measure temperature and other parameters electronically. This device is called CTD which stands for conductivity, temperature, and depth.[13] It continuously sends the data up to the ship via a conducting cable. This device is usually mounted on a frame that includes water sampling bottles. Since the 2010s autonomous vehicles such as gliders or mini-submersibles have been increasingly available. They carry the same CTD sensors, but operate independently of a research ship.

Scientists can deploy CTD systems from research ships on moorings gliders and even on seals.[14] With research ships they receive data through the conducting cable. For the other methods they use telemetry.

There are other ways of measuring sea surface temperature.[15] At this near-surface layer measurements are possible using thermometers or satellites with spectroscopy. Weather satellites have been available to determine this parameter since 1967. Scientists created the first global composites during 1970.[16]

The Advanced Very High Resolution Radiometer (AVHRR) is widely used to measure sea surface temperature from space.[11]:90

There are various devices to measure ocean temperatures at different depths. These include the Nansen bottle, bathythermograph, CTD, or ocean acoustic tomography. Moored and drifting buoys also measure sea surface temperatures. Examples are those deployed by the Global Drifter Program and the National Data Buoy Center. The World Ocean Database Project is the largest database for temperature profiles from all of the world’s oceans.[17]

A small test fleet of "deep Argo" floats aims to extend the measurement capability down to about 6000 meters. It will accurately sample temperature for a majority of the ocean volume once it is in full use.[18][19]

Mercury thermometers

The most frequent measurement technique on ships and buoys is thermistors and mercury thermometers.[11]:88 Scientists often use mercury thermometers to measure the temperature of surface waters. They can put them in buckets dropped over the side of a ship. To measure deeper temperatures they put them on Nansen bottles.[11]:88

Argo program

This section is an excerpt from Argo (oceanography)[ edit ]

Ocean warming

The illustration of temperature changes from 1960 to 2019 across each ocean starting at the Southern Ocean around Antarctica.[20]
Further information: Earth:Effects of climate change on oceans

Trends

This section is an excerpt from Effects of climate change on oceans#Rising ocean temperature[ edit ]
This section is an excerpt from Sea surface temperature#Recent increase due to climate change[ edit ]

Causes

The root cause of these observed changes is the warming of the Earth due to emissions of greenhouse gases from human causes. These gases include carbon dioxide and methane.[21] The ocean takes up most of the additional heat in the climate system.[7] So this results in ocean warming.

We can express this in another way. The climb in ocean temperatures is the inevitable outcome of Earth's energy imbalance. And this imbalance comes with increasing concentrations of greenhouse gases.[8]

Main physical effects

Increased stratification and lower oxygen levels

Main pages: Earth:Ocean stratification and Earth:Ocean deoxygenation

Higher air temperatures warm the ocean surface. And this leads to greater ocean stratification. Reduced mixing of the ocean layers stabilises warm water near the surface. At the same time it reduces cold, deep water circulation. The reduced up and down mixing reduces the ability of the ocean to absorb heat. This directs a larger fraction of future warming toward the atmosphere and land. Energy available for tropical cyclones and other storms is likely to increase. Nutrients for fish in the upper ocean layers are set to decrease. This is also like to reduce the capacity of the oceans to store carbon.

Warmer water cannot contain as much oxygen as cold water. Increased thermal stratification may reduce the supply of oxygen from the surface waters to deeper waters. This would further decrease the water's oxygen content.[22] This process is called ocean deoxygenation. The ocean has already lost oxygen throughout the water column. Oxygen minimum zones are expanding worldwide.[23]:471

Changing ocean currents

Varying temperatures associated with sunlight and air temperatures at different latitudes cause ocean currents. Prevailing winds and the different densities of saline and fresh water are another cause of currents. Air tends to be warmed and thus rise near the equator, then cool and thus sink slightly further poleward. Near the poles, cool air sinks, but is warmed and rises as it then travels along the surface equatorward. The sinking and upwelling that occur in lower latitudes, and the driving force of the winds on surface water, mean the ocean currents circulate water throughout the entire sea. Global warming on top of these processes causes changes to currents, especially in the regions where deep water is formed.[24]

In the geologic past

Main page: Earth:Geologic temperature record

Scientists believe the sea temperature was much hotter in the Precambrian period. Such temperature reconstructions derive from oxygen and silicon isotopes from rock samples.[25][26] These reconstructdions suggest the ocean had a temperature of 55–85 °C 2,000 to 3,500 million years ago. It then cooled to milder temperatures of between 10 and 40 °C by 1,000 million years ago. Reconstructed proteins from Precambrian organisms also provide evidence that the ancient world was much warmer than today.[27][28]

The Cambrian Explosion approximately 538.8 million years ago was a key event in the evolution of life on Earth. This event took place at a time when scientists believe sea surface temperatures reached about 60 °C.[29] Such high temperatures are above the upper thermal limit of 38 °C for modern marine invertebrates. They preclude a major biological revolution.[30]

During the later Cretaceous period, from 100 to 66 million years ago, average global temperatures reached their highest level in the last 200 million years or so.[31] This was probably the result of the configuration of the continents during this period. It allowed for improved circulation in the oceans. This discouraged the formation of large scale ice sheet.[citation needed]

Data from an oxygen isotope database indicate that there have been seven global warming events during the geologic past. These include the Late Cambrian, Early Triassic, Late Cretaceous, and Paleocene-Eocene transition. The surface of the sea was about 5-30º warmer than today in these warming period.[10]

See also

References

  1. ↑ "Ocean Stratification". Columbia Univ.. http://eesc.columbia.edu/courses/ees/climate/lectures/o_strat.html. 
  2. ↑ "The Hidden Meltdown of Greenland". NASA. https://science.nasa.gov/science-news/science-at-nasa/2015/28aug_greenland/. 
  3. ↑ 3.0 3.1 "Temperature of Ocean Water". UCAR. http://www.windows.ucar.edu/tour/link=/earth/Water/temp.html. 
  4. ↑ Rahmstorf, S (2003). "The concept of the thermohaline circulation". Nature 421 (6924): 699. doi:10.1038/421699a. PMID 12610602. Bibcode: 2003Natur.421..699R. http://www.pik-potsdam.de/~stefan/Publications/Nature/nature_concept_03.pdf. 
  5. ↑ Lappo, SS (1984). "On reason of the northward heat advection across the Equator in the South Pacific and Atlantic ocean". Study of Ocean and Atmosphere Interaction Processes (Moscow Department of Gidrometeoizdat (in Mandarin)): 125–9. 
  6. ↑ IPCC, 2019: Summary for Policymakers . In: IPCC Special Report on the Ocean and Cryosphere in a Changing Climate [H.-O. Pörtner, D.C. Roberts, V. Masson-Delmotte, P. Zhai, M. Tignor, E. Poloczanska, K. Mintenbeck, A. Alegría, M.  Nicolai, A. Okem, J. Petzold, B. Rama, N.M. Weyer (eds.)]. Cambridge University Press, Cambridge, UK and New York, NY, USA. https://doi.org/10.1017/9781009157964.001.
  7. ↑ 7.0 7.1 Cheng, Lijing; Abraham, John; Hausfather, Zeke; Trenberth, Kevin E. (2019). "How fast are the oceans warming?" (in en). Science 363 (6423): 128–129. doi:10.1126/science.aav7619. ISSN 0036-8075. PMID 30630919. Bibcode: 2019Sci...363..128C. https://www.science.org/doi/10.1126/science.aav7619. 
  8. ↑ 8.0 8.1 Cheng, Lijing; Abraham, John; Trenberth, Kevin E.; Fasullo, John; Boyer, Tim; Mann, Michael E.; Zhu, Jiang; Wang, Fan et al. (2023). "Another Year of Record Heat for the Oceans" (in en). Advances in Atmospheric Sciences 40 (6): 963–974. doi:10.1007/s00376-023-2385-2. ISSN 0256-1530. PMID 36643611.  CC-BY icon.svg Text was copied from this source, which is available under a Creative Commons Attribution 4.0 International License
  9. ↑ 9.0 9.1 Fox-Kemper, B., H.T. Hewitt, C. Xiao, G. Aðalgeirsdóttir, S.S. Drijfhout, T.L. Edwards, N.R. Golledge, M. Hemer, R.E. Kopp, G.  Krinner, A. Mix, D. Notz, S. Nowicki, I.S. Nurhati, L. Ruiz, J.-B. Sallée, A.B.A. Slangen, and Y. Yu, 2021: Chapter 9: Ocean, Cryosphere and Sea Level Change . In Climate Change 2021: The Physical Science Basis. Contribution of Working Group I to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change [Masson-Delmotte, V., P. Zhai, A. Pirani, S.L.  Connors, C. Péan, S. Berger, N. Caud, Y. Chen, L. Goldfarb, M.I. Gomis, M. Huang, K. Leitzell, E. Lonnoy, J.B.R. Matthews, T.K. Maycock, T. Waterfield, O. Yelekçi, R. Yu, and B. Zhou (eds.)]. Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA, pp. 1211–1362, doi:10.1017/9781009157896.011.
  10. ↑ 10.0 10.1 Song, Haijun; Wignall, Paul B.; Song, Huyue; Dai, Xu; Chu, Daoliang (2019). "Seawater Temperature and Dissolved Oxygen over the Past 500 Million Years" (in en). Journal of Earth Science 30 (2): 236–243. doi:10.1007/s12583-018-1002-2. ISSN 1674-487X. http://link.springer.com/10.1007/s12583-018-1002-2. 
  11. ↑ 11.0 11.1 11.2 11.3 "Introduction to Physical Oceanography" (in en). 2008. https://open.umn.edu/opentextbooks/textbooks/20. 
  12. ↑ Vittorio Barale (2010). Oceanography from Space: Revisited. Springer. p. 263. ISBN 978-90-481-8680-8. https://books.google.com/books?id=hH2NkL_318wC&pg=PA263. 
  13. ↑ "Conductivity, Temperature, Depth (CTD) Sensors - Woods Hole Oceanographic Institution" (in en-US). https://www.whoi.edu/what-we-do/explore/instruments/instruments-sensors-samplers/conductivity-temperature-depth-ctd-sensors/. 
  14. ↑ Boyd, I.L; Hawker, E.J; Brandon, M.A; Staniland, I.J (2001). "Measurement of ocean temperatures using instruments carried by Antarctic fur seals" (in en). Journal of Marine Systems 27 (4): 277–288. doi:10.1016/S0924-7963(00)00073-7. https://linkinghub.elsevier.com/retrieve/pii/S0924796300000737. 
  15. ↑ Alexander Soloviev; Roger Lukas (2006). The near-surface layer of the ocean: structure, dynamics and applications. シュプリンガー・ジャパン株式会社. xi. ISBN 978-1-4020-4052-8. Bibcode: 2006nslo.book.....S. https://books.google.com/books?id=tZary8a4HMwC. 
  16. ↑ P. Krishna Rao; W. L. Smith; R. Koffler (January 1972). "Global Sea-Surface Temperature Distribution Determined From an Environmental Satellite". Monthly Weather Review 100 (1): 10–14. doi:10.1175/1520-0493(1972)100<0010:GSTDDF>2.3.CO;2. Bibcode: 1972MWRv..100...10K. 
  17. ↑ "World Ocean Database Profiles the Ocean". National Centers for Environmental Information. 14 June 2017. https://www.ncei.noaa.gov/news/world-ocean-database-profiles-ocean. 
  18. ↑ Administration, US Department of Commerce, National Oceanic and Atmospheric. "Deep Argo" (in EN-US). https://oceantoday.noaa.gov/deepargo/welcome.html. 
  19. ↑ "Deep Argo: Diving for Answers in the Ocean's Abyss". 24 December 2021. https://www.climate.gov/news-features/climate-tech/deep-argo-diving-answers-ocean%E2%80%99s-abyss. 
  20. ↑ Cheng, Lijing; Abraham, John; Zhu, Jiang; Trenberth, Kevin E.; Fasullo, John; Boyer, Tim; Locarnini, Ricardo; Zhang, Bin et al. (2020). "Record-Setting Ocean Warmth Continued in 2019" (in en). Advances in Atmospheric Sciences 37 (2): 137–142. doi:10.1007/s00376-020-9283-7. ISSN 1861-9533. Bibcode: 2020AdAtS..37..137C. 
  21. ↑ Doney, Scott C.; Busch, D. Shallin; Cooley, Sarah R.; Kroeker, Kristy J. (2020-10-17). "The Impacts of Ocean Acidification on Marine Ecosystems and Reliant Human Communities" (in en). Annual Review of Environment and Resources 45 (1): 83–112. doi:10.1146/annurev-environ-012320-083019. ISSN 1543-5938.  CC-BY icon.svg Text was copied from this source, which is available under a Creative Commons Attribution 4.0 International License
  22. ↑ Chester, R.; Jickells, Tim (2012). "Chapter 9: Nutrients oxygen organic carbon and the carbon cycle in seawater". Marine geochemistry (3rd ed.). Chichester, West Sussex, UK: Wiley/Blackwell. ISBN 978-1-118-34909-0. OCLC 781078031. https://www.wiley.com/en-us/Marine+Geochemistry%2C+3rd+Edition-p-9781118349090. 
  23. ↑ Bindoff, N.L., W.W.L. Cheung, J.G. Kairo, J. Arístegui, V.A. Guinder, R. Hallberg, N. Hilmi, N. Jiao, M.S. Karim, L. Levin, S. O'Donoghue, S.R. Purca Cuicapusa, B. Rinkevich, T. Suga, A. Tagliabue, and P. Williamson, 2019: Chapter 5: Changing Ocean, Marine Ecosystems, and Dependent Communities . In: IPCC Special Report on the Ocean and Cryosphere in a Changing Climate [H.-O. Pörtner, D.C. Roberts, V. Masson-Delmotte, P. Zhai, M. Tignor, E. Poloczanska, K. Mintenbeck, A. Alegría, M. Nicolai, A. Okem, J. Petzold, B. Rama, N.M. Weyer (eds.)]. In press.
  24. ↑ Trenberth, K; Caron, J (2001). "Estimates of Meridional Atmosphere and Ocean Heat Transports". Journal of Climate 14 (16): 3433–43. doi:10.1175/1520-0442(2001)014<3433:EOMAAO>2.0.CO;2. Bibcode: 2001JCli...14.3433T. https://zenodo.org/record/1234671. 
  25. ↑ Knauth, L. Paul (2005). "Temperature and salinity history of the Precambrian ocean: implications for the course of microbial evolution". Palaeogeography, Palaeoclimatology, Palaeoecology 219 (1–2): 53–69. doi:10.1016/j.palaeo.2004.10.014. Bibcode: 2005PPP...219...53K. 
  26. ↑ Shields, Graham A.; Kasting, James F. (2006). "A palaeotemperature curve for the Precambrian oceans based on silicon isotopes in cherts". Nature 443 (7114): 969–972. doi:10.1038/nature05239. PMID 17066030. Bibcode: 2006Natur.443..969R. 
  27. ↑ Gaucher, EA; Govindarajan, S; Ganesh, OK (2008). "Palaeotemperature trend for Precambrian life inferred from resurrected proteins". Nature 451 (7179): 704–707. doi:10.1038/nature06510. PMID 18256669. Bibcode: 2008Natur.451..704G. 
  28. ↑ Risso, VA; Gavira, JA; Mejia-Carmona, DF (2013). "Hyperstability and substrate promiscuity in laboratory resurrections of Precambrian b-lactamases". J Am Chem Soc 135 (8): 2899–2902. doi:10.1021/ja311630a. PMID 23394108. 
  29. ↑ Wotte, Thomas; Skovsted, Christian B.; Whitehouse, Martin J.; Kouchinsky, Artem (2019). "Isotopic evidence for temperate oceans during the Cambrian Explosion" (in en). Scientific Reports 9 (1): 6330. doi:10.1038/s41598-019-42719-4. ISSN 2045-2322. PMID 31004083. Bibcode: 2019NatSR...9.6330W.  CC-BY icon.svg Text was copied from this source, which is available under a Creative Commons Attribution 4.0 International License
  30. ↑ Wotte, Thomas; Skovsted, Christian B.; Whitehouse, Martin J.; Kouchinsky, Artem (2019). "Isotopic evidence for temperate oceans during the Cambrian Explosion" (in en). Scientific Reports 9 (1): 6330. doi:10.1038/s41598-019-42719-4. ISSN 2045-2322. PMID 31004083. Bibcode: 2019NatSR...9.6330W. 
  31. ↑ Renne, Paul R.; Deino, Alan L.; Hilgen, Frederik J.; Kuiper, Klaudia F.; Mark, Darren F.; Mitchell, William S.; Morgan, Leah E.; Mundil, Roland et al. (7 February 2013). "Time Scales of Critical Events Around the Cretaceous-Paleogene Boundary". Science 339 (6120): 684–687. doi:10.1126/science.1230492. PMID 23393261. Bibcode: 2013Sci...339..684R. 



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