Submarine groundwater discharge

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Submarine Groundwater Discharge (SGD) is a hydrological process which commonly occurs in coastal areas. It is described as submarine inflow of fresh-, and brackish groundwater from land into the sea. Submarine Groundwater Discharge is controlled by several forcing mechanisms, which cause a hydraulic gradient between land and sea.[1] Considering the different regional settings the discharge occurs either as (1) a focused flow along fractures in karst and rocky areas, (2) a dispersed flow in soft sediments, or (3) a recirculation of seawater within marine sediments. Submarine Groundwater Discharge plays an important role in coastal biogeochemical processes and hydrological cycles such as the formation of offshore plankton blooms, hydrological cycles, and the release of nutrients, trace elements and gases.[2][3][4][5]

Forcing mechanisms

In coastal areas the groundwater and seawater flows are driven by a variety of factors. Both types of water can circulate in marine sediments due to tidal pumping, waves, bottom currents or density driven transport processes. Meteoric freshwaters can discharge along confined and unconfined aquifers into the sea or the oppositional process of seawater intruding into groundwater charged aquifers can take place.[1] The flow of both fresh and sea water is primarily controlled by the hydraulic gradients between land and sea and differences in the densities between both waters and the permeabilities of the sediments.

According to Badon-Ghijben (1888)[6] and Herzberg (1901)[7] the thickness of a freshwater lens below sea level (z) corresponds with the thickness of the freshwater level above sea level (h) as:

z= ρf/((ρs-ρf))*h

With z being the thickness between the saltwater–freshwater interface and the sea level, h being the thickness between the top of the freshwater lens and the sea level, ρf being the density of freshwater and ρs being the density of saltwater. Including the densities of freshwater (ρf = 1.00 g •cm-3) and seawater (ρs = 1.025 g •cm-3) equation (2) simplifies to:

z=40*h

Together with Darcy's Law, the length of a salt wedge from the shoreline into the hinterland can be calculated:

L= ((ρs-ρf)Kf m)/(ρf Q)

With Kf being the hydraulic conductivity, m the aquifer thickness and Q the discharge rate.[8] Assuming an isotropic aquifer system the length of a salt wedge solely depends on the hydraulic conductivity, the aquifer thickness and is inversely related to the discharge rate. These assumptions are only valid under hydrostatic conditions in the aquifer system. In general the interface between fresh and saline water forms a zone of transition due to diffusion/dispersion or local anisotropy.[9]

Methods

The first study about Submarine Groundwater Discharge was done by Sonrel (1868) who speculated on the risk of submarine springs for sailors. However until the mid-1990s SGD remained rather unrecognized by the scientific community because it was hard to detect and measure the freshwater discharge. The first elaborated method to study SGD was done by Moore (1996)who used radium-226 as a tracer for groundwater. Since then several methods and instruments were developed to attempt to detect and quantify discharge rates.

Radium-226

The first study which detected and quantified Submarine Groundwater Discharge on a regional basis was done by Moore (1996) in the South Atlantic Bight off South Carolina. He measured enhanced radium-226 concentrations within the water column near shore and up to about 100 kilometres (62 mi) from the shoreline. Radium-226 is a decay product of thorium-230, which is produced within sediments and supplied by rivers. However, these sources could not explain the high concentrations present in the study area. Moore (1996) hypothesized that submarine groundwater, enriched in radium-226, was responsible for the high concentrations. This hypothesis has been tested numerous times at sites around the world and confirmed at each site.[10]

Seepage meter

Lee (1977)[11] designed a seepage meter, which consists of a chamber which is connected to a sampling port and a plastic bag. The chamber is inserted into the sediment and water discharging through the sediments is caught within the plastic bag. The change in volume of water which is caught in the plastic bag over time represents the freshwater flux.

Pore water profiles

According to Schlüter et al. (2004)[12] chloride pore water profiles can be used to investigate submarine groundwater discharge. Chloride can be used as a conservative tracer, as it is enriched in seawater and depleted in groundwater. Three different shapes of chloride pore water profiles reflect three different transport modes within marine sediments. A chloride profile showing constant concentrations with depth indicates that no submarine groundwater is present. A chloride profile with a linear decline indicates a diffusive mixing between groundwater and seawater and a concave shaped chloride profile represents an advective admixture of submarine groundwater from below.

References

  1. ↑ 1.0 1.1 William C.Burnett, Bokuniewicz, Henry, Huettel, Markus, Moore, Willard S., Taniguchi, Makoto. "Groundwater and pore water inputs to the coastal zone", Biogeochemistry, Volume 66, 2003, Page 3–33.
  2. ↑ Claudette Spiteri, Caroline P. Slomp, Matthew A. Charette, Kagan Tuncay, Christof Meile. "Flow and nutrient dynamics in a subterranean estuary (Waquoit Bay, MA, USA): Field data and reactive transport modeling", Geochimica et Cosmochimica Acta, Volume 72, Issue 14, 15 July 2008, Pages 3398–3412.
  3. ↑ Caroline P. Slomp, Philippe Van Cappellen. "Nutrient inputs to the coastal ocean through submarine groundwater discharge: controls and potential impact", Journal of Hydrology, Volume 295, Issues 1–4, 10 August 2004, Pages 64–86.
  4. ↑ Willard S. Moore. "Large groundwater inputs to coastal waters revealed by 226Ra enrichments", Nature, Volume 380, 1996
  5. ↑ Matthew A. Charette, Edward R. Sholkovitz. "Trace element cycling in a subterranean estuary: Part 2. Geochemistry of the pore water", Geochimica et Cosmochimica Acta, Volume 70, Issue 4, 15 February 2006, Pages 811–826.
  6. ↑ Badon-Ghijben W., 1888. Nota in verband met de voorgenomen putboring nabij Amsterdam (Notes on the probable results of well drilling near Amsterdam). Tijdschrift van het Koninklinjk Instituut van Ingenieurs. The Hague 1888/9: 8–22
  7. ↑ Herzberg, B. 1901. Die Wasserversorgung einiger Nordseebader. Gasbeleuchtung und Wasserversorgung 44: 815–819, 842–844
  8. ↑ Domenico, E. P. & Schwartz, F. W.; 1998. Physical and chemical hydrogeology. 2nd ed. New York. John Wiley & Sons Inc.: 506
  9. ↑ Stuyfzand, P. J.; 1993. Hydrochemistry and Hydrology of the Coastal Dune area of the Western Netherlands. PhD thesis, Vrije Universiteit Amsterdam: 367.
  10. ↑ Moore, Willard (2010). "The Effect of Submarine Groundwater Discharge on the Ocean". Annual Reviews of Marine Science 2: 345–374. 
  11. ↑ David Robert Lee. "A device to measure seepage flux in estuaries and lakes", Limnology and Oceanography, Volume 22, 1977, pp. 140–147
  12. ↑ Schlüter, M., Sauter, E.J., Andersen, C.E., Dahlgaard, H., Dando, P.R., 2004. "Spatial distribution and budget for submarine groundwater discharge in Eckernforde Bay (Western Baltic Sea)". Limnology and Oceanography 49: 157–167.
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