Eustatic sea level

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The eustatic sea level is the distance from the center of the earth to the sea surface.[1][2] An increase of the eustatic sea level can be generated by decreasing glaciation, increasing spreading rates of the mid-ocean ridges or more mid-oceanic ridges. Conversely, increasing glaciation, decreasing spreading rates or fewer mid-ocean ridges lead to a fall of the eustatic sea level.

Changes in the eustatic sea level lead to changes in accommodation and therefore affect the deposition of sediments in marine environments.

Eustatic (global) sea level refers to the sea level change of the volume of Earth’s oceans.[3] This is not a physical level but instead represents the sea level if all of the water in the oceans were contained in a single basin.[4] Eustatic sea level is not relative to local surfaces, because relative sea level is dependent on many factors including tectonics, continental rise and subsidence. Eustatic sea level follows the ‘bathtub approach’ which describes the ocean as a single bathtub. One can add or remove water and Earth’s oceans will gain or lose water globally. Differences of eustatic sea level are caused by three main factors:

  • Changes in total ocean water mass, for instance, by ice sheet runoff. When an ice sheet such as Greenland begins to lose its ice mass due to melt, the liquid water is transported to the ocean.[5] According to the ‘bathtub approach’, ice sheet runoff from Greenland will affect eustatic sea level in all areas of the world, whether nearby or distant. [3] Ocean water mass may also shrink in size if the continental ice sheets grow in size, thereby removing liquid water from oceans and converting them to grow ice sheets [6]
  • Changes in the size of the ocean basin, for instance, by tectonic seafloor spreading or by sedimentation. These slow processes can cause the total volume of the oceanic basin to change.[7]
  • Density changes of the water, for instance, by thermal expansion. One driver of thermal expansion is a rise in greenhouse gases such as carbon dioxide, methane, and ozone. These gases cause surface temperatures to increase, which in turn increases ocean temperatures.[3] This warming will cause water to experience greater molecular motion, thus increasing the volume a molecule will occupy. A decrease in atmospheric greenhouse gases will cause surface temperatures to drop.[3] Expansion of water may also be caused by changes in ocean salinity.[3] As continental ice accumulates, the ocean water freezes onto land but the salt it carried will mostly remain in the ocean. Thus, as ice sheets increase, ocean salinity also increases (and vice versa). An increase in salinity will increase the density of the ocean basin. Melting of ice sheets and a decrease of ocean salinity will effectively decrease the density of the water. These two effects together are called the steric sea level. The thermal part is called the thermosteric sea level, whereas the salinity part is called the halosteric sea level.[8]

References[edit]

  1. ^ Patzkowsky, Mark E.; Holland, Steven M. (2012). Stratigraphic Paleobiology. Chicago: University of Chicago University Press. p. 30.
  2. ^ Schlager, Wolfgang (2005). Carbonate Sedimentology and Sequence Stratigraphy. Tulsa: Society for Sedimentary Geology. p. 92. ISBN 978-1-56576-116-2.
  3. ^ a b c d e Rovere, A., Stocchi, P., & Vacchi, M. (2016). Eustatic and Relative Sea Level Changes. Current Climate Change Reports,2(4), 221-231. doi:10.1007/s40641-016-0045-7
  4. ^ CU Sea Level Research Group, Sea Level Research Group
  5. ^ Ahlstrøm, A. P., Petersen, D., Langen, P. L., Citterio, M., & Box, J. E. (2017). Abrupt shift in the observed runoff from the southwestern Greenland ice sheet. Science Advances,3(12). doi:10.1126/sciadv.1701169
  6. ^ Penn State 2018
  7. ^ Rovere, Alessio; Stocchi, Paolo; Vacchi, Matteo (2016). "Eustatic and Relative Sea Level Changes". Current Climate Change Reports.
  8. ^ Piecuch, Christopher; Ponte, Rui (2014). "Mechanisms of Global-Mean Steric Sea Level Change". Journal of Climate. 27 (2): 824–834. doi:10.1175/JCLI-D-13-00373.1.