Difference between revisions of "Feedback on Saturation State"

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The ocean has an inbuilt negative feedback process for stabilising the saturation rate with respect to calcium carbonate (Ω), albeit one that takes many millennia to counteract perturbations. This process is called carbonate compensation (Zeebe and Westbroeck, 2003). It involves automatic adjustment of the CaCO<sub>3</sub> [http://en.wikipedia.org/wiki/Lysocline lysocline] in response to any deviations in the CaCO<sub>3</sub> saturation state of seawater. The lysocline is the depth at which significant amounts of calcium carbonate start to dissolve on the seabed. Above the  lysocline, nearly all of the CaCO<sub>3</sub> that falls to the seafloor accumulates in the sediments. Below the calcite lysocline the waters are corrosive to it, leading to dissolving of some or all of the CaCO<sub>3</sub> within the sediments. The CaCO<sub>3</sub> saturation state is equal to ([CO<sub>3</sub><sup>2-</sup>] [Ca<sup>2+</sup>] / ''K''<sub>sp</sub>), where [CO<sub>3</sub><sup>2-</sup>] is the concentration of carbonate ions in seawater, [Ca<sup>2+</sup>] is the concentration of calcium ions and ''K''<sub>sp</sub> is the solubility product.
+
The ocean has an inbuilt negative feedback process for stabilising the saturation rate with respect to calcium carbonate (Ω), albeit one that takes many millennia to counteract perturbations. This process is called carbonate compensation (Zeebe and Westbroeck, 2003). It involves automatic adjustment of the CaCO<sub>3</sub> [http://en.wikipedia.org/wiki/Lysocline lysocline] in response to any deviations in the CaCO<sub>3</sub> saturation state of seawater. The lysocline is the depth at which significant amounts of calcium carbonate start to dissolve on the seabed. Above the  lysocline, nearly all of the CaCO<sub>3</sub> that falls to the seafloor accumulates in the sediments. Below the calcite lysocline the waters are corrosive to it, leading to dissolving of some or all of the CaCO<sub>3</sub> within the sediments. The CaCO<sub>3</sub> saturation state is equal to ([CO<sub>3</sub><sup>2-</sup>] [Ca<sup>2+</sup>] / ''K''<sub>sp</sub>), where [CO<sub>3</sub><sup>2-</sup>] is the concentration of carbonate ions in seawater, [Ca<sup>2+</sup>] is the concentration of calcium ions and ''K''<sub>sp</sub> is the solubility product. In practice, over timescales less than a million years or so, values of both [Ca<sup>2+</sup>] and ''K''<sub>sp</sub>) are bound to remain more or less constant in the ocean.  Variations in the value of Ω are therefore determined by variations in the value of [CO<sub>3</sub><sup>2-</sup>], and stabilising Ω is equivalent to stabilising [CO<sub>3</sub><sup>2-</sup>].
  
[[Image:feedback_on_lowCO3.jpg|right|thumb|200px|Chain of events set in motion by an abnormally low saturation state in seawater, leading to a return towards higher values]]
+
==Response to [CO<sub>3</sub><sup>2-</sup>] Perturbed Downwards==
As illustrated in the diagram to the right, carbonate compensation involves the adjustment of the depth of the CaCO<sub>3</sub> lysocline in the ocean so as to regulate Ω. It acts as follows. As the ocean becomes more acid ([http://en.wikipedia.org/wiki/Ocean_acidification as is happening at present]), carbonate ion concentration ([CO32-]) will drop. Because the vertical profile of the saturating value of [CO32-] for each of aragonite and calcite does not change, the intersection point of the saturating and the actual [CO32-] will move to shallower depths. This will cause a shallowing of the calcite and aragonite saturation horizons (depths at which Ω=1). Jansen et al. (Jansen et al., 2002) give the following equations for calculating the saturating carbonate ion concentration ([CO32-]c(z), μMol kg-1) as a function of depth (z, km):
 
  
(calcite)
+
[[Image:feedback_on_lowCO3.jpg|right|thumb|300px|Chain of events set in motion by an abnormally low saturation state in seawater, leading to a return towards higher values]]
 +
As illustrated in the diagram to the right, carbonate compensation involves the adjustment of the depth of the CaCO<sub>3</sub> lysocline in the ocean in response to changes in Ω. It acts as follows. As the ocean becomes more acid ([http://en.wikipedia.org/wiki/Ocean_acidification as is happening at present]), carbonate ion concentration ([CO<sub>3</sub><sup>2-</sup>]) drops. Because the vertical profile of [CO<sub>3</sub><sup>2-</sup>]c(z) (the saturating value of [CO<sub>3</sub><sup>2-</sup>], i.e. value at which Ω=1 where seawater is neither under- nor super-saturated relative to CaCO<sub>3</sub>) does not change, the intersection point of the saturating and the actual [CO<sub>3</sub><sup>2-</sup>] moves to shallower depths. This causes a shallowing of the saturation horizon (depth at which Ω=1). Although the lysocline does not lie exactly at the saturation horizon, the two are interlinked. The lysocline typically lies somewhat deeper in the water than the saturation horizon, but the two depths change together in response to changing [CO<sub>3</sub><sup>2-</sup>].
  
(aragonite)
+
The depths of the saturation horizon and lysocline are very sensitive to deep water [CO<sub>3</sub><sup>2-</sup>]. For instance, even only a 25% drop in average deep water [CO<sub>3</sub><sup>2-</sup>], taking it down from about 90 μMol kg-1 today to 67.5 μMol kg-1 in the future would cause the global saturation horizon to shallow by about 2 km. Much larger decreases in deep [CO<sub>3</sub><sup>2-</sup>] are in fact forecast for the future, depending on future Co2 emissions. A model of ocean acidification predicts, under almost all emissions scenarios, that average lysocline depth will be shallower than 0.5 km by the year 2300, compared to depths of at least several kilometres in most locations at present.
  
The depth of the saturation horizon is obtained by finding the value of z (the depth) at which [CO32-]c(z) is the same as the actual deep ocean [CO32-]. Although the lysocline does not lie exactly at the saturation horizon, the two are interlinked. These equations emphasise the sensitivity of saturation horizons to deep water [CO32-]. For instance, even only a 25% drop in average deep water [CO32-], taking it down from about 90 μMol kg-1 today (Broecker, 2003) to 67.5 μMol kg-1 in the future would, according to the equations, cause the global calcite saturation horizon to shallow from an average depth of 4 km to 2.2 km. Much larger decreases in deep [CO32-] are in fact forecast (section 2.1.1). A model of ocean acidification predicts, under almost all emissions scenarios, that the aver-age calcite lysocline depth will be shallower than 0.5 km by the year 2300 (Caldeira and Wickett, 2005).
+
Shallowing of the lysocline will increase global dissolution and decrease global burial. This will tend to oppose the low [CO<sub>3</sub><sup>2-</sup>] values, by driving an imbalance between the riverine input of dissolved calcium and carbon and their removal in buried calcium carbonate. Rivers continue pouring in 'dissolved carbonate', but the ocean stops (slows down) its burial of CaCO<sub>3</sub>. The chemical equation for calcification is given by:
  
[[Image:feedback_on_highCO3.jpg|right|thumb|200px|Chain of events set in motion by an abnormally high saturation state in seawater, leading to a return towards lower values]]
+
Ca<sup>2+</sup> + 2HCO<sub>3</sub><sup>-</sup>    →    CaCO<sub>3</sub> + CO<sub>2</sub>(aq) + H<sub>2</sub>O
Shallowing of the lysoclines will increase global dissolution and decrease burial. This will tend to oppose the low [CO32-] values of an acid ocean, by driving an imbalance between the riverine input of dissolved calcium and carbon and their removal in buried calcium carbonate. The chemical equa-tion for calcification and/or dissolution  is given by:
 
Ca + 2HCO           CaCO<sub>3</sub> + CO2(aq) + H2O (1)
 
Dissolution of 1 Mole of CaCO<sub>3</sub> (or an equivalent reduction in CaCO<sub>3</sub> burial) therefore leads to ad-dition of 1 Mole of dissolved inorganic carbon to seawater, together with a simultaneous addition of 2 Moles (charge equivalents) of alkalinity. When the carbonate chemistry is calculated out, these changes to DIC and alkalinity induce an increase in the carbonate ion concentration, completing the negative feedback. This increase in ocean carbonate ion concentration will continue until the origi-nal, steady-state, carbonate ion concentration is re-attained. The e-folding response time (the time for the deviation of a variable from its equilibrium value to decrease by a factor of e) for carbonate compensation has variously been estimated at between 6 and 14 ky (Archer et al., 1997, 1998; Sundquist, 1986; Zeebe and Westbroek, 2003).
 
  
Carbonate compensation as described here is brought about purely by changes in lysocline depths in response to changes in Ω. There are likely to be several other changes to oceanic CaCO<sub>3</sub> cycling that will also contribute to restoration of Ω to its equilibrium value:  
+
and dissolution is the reverse reaction.
1. production of CaCO<sub>3</sub> may well decline in a more acidic surface ocean, as discussed above,, lead-ing to a lighter rain of particles out of the surface ocean and hence to a lighter rain to the sea floor;  
+
 
2. CaCO<sub>3</sub> that fell to the seafloor in pre-industrial times, before any ocean acidification, may also be affected. As this CaCO<sub>3</sub>, lying at or near to the surface of the sediments, comes into contact with increasingly acidic deep bottom waters, it is likely that some of it, finding itself now lying beneath a suddenly shallower lysocline, will be chemically eroded via dissolution.
+
Dissolution of 1 Mole of CaCO<sub>3</sub> (or an equivalent reduction in CaCO<sub>3</sub> burial) therefore leads to addition of 1 Mole of dissolved inorganic carbon to seawater, together with a simultaneous addition of 2 Moles (charge equivalents) of alkalinity. When the carbonate chemistry is calculated out, these changes to DIC and alkalinity induce an increase in the carbonate ion concentration, completing the negative feedback.
3. the combination of warming, higher CO2 and increased rainfall in a warmer world may also has-ten the rate of weathering of limestone, dolomite and chalk rocks on land, leading to an increased supply rate of calcium and carbon to the oceans.
+
 
 +
==Response to [CO<sub>3</sub><sup>2-</sup>] Perturbed Upwards==
 +
 
 +
[[Image:feedback_on_highCO3.jpg|right|thumb|300px|Chain of events set in motion by an abnormally high saturation state in seawater, leading to a return towards lower values]]
 +
As illustrated in the diagram to the right, the carbonate compensation response to elevated saturation state is as follows. A rapid elevation of the carbonate ion concentration ([CO<sub>3</sub><sup>2-</sup>]) to higher-than-normal values will be accompanied by a transition to the ocean being more than normally supersaturated. Because the vertical profile of [CO<sub>3</sub><sup>2-</sup>]c(z) (the saturating value of [CO<sub>3</sub><sup>2-</sup>], i.e. value at which Ω=1 where seawater is neither under- nor super-saturated relative to CaCO<sub>3</sub>) does not change, the intersection point of the saturating and the actual [CO<sub>3</sub><sup>2-</sup>] moves to deeper depths. This causes a deepening of the saturation horizon (depth at which Ω=1) and lysocline.
 +
 
 +
Deepening of the lysocline will decrease global dissolution and increase global burial. This will tend to oppose the high [CO<sub>3</sub><sup>2-</sup>] values, by driving an imbalance between the riverine input of dissolved calcium and carbon and their removal in buried calcium carbonate. Rivers continue pouring in 'dissolved carbonate' at the same rate, but are now outweighed by the increased burial of CaCO<sub>3</sub>.
 +
 
 +
CaCO<sub>3</sub> burial leads to removal of 1 Mole of dissolved inorganic carbon from seawater, together with a simultaneous removal of 2 Moles (charge equivalents) of alkalinity. When the carbonate chemistry is calculated out, these changes to DIC and alkalinity induce an decrease in the carbonate ion concentration, completing the negative feedback.
 +
 
 +
==Speed of Carbonate Compensation==
 +
 
 +
The carbonate compensation-induced changes to ocean carbonate ion concentration will continue until the original, steady-state, carbonate ion concentration is re-attained. The [http://en.wikipedia.org/wiki/E-folding e-folding response time] (the time for the deviation of a variable from its equilibrium value to decrease by a factor of e) for carbonate compensation has been estimated in different modelling studies at between 6000 and 14000 years. It will therefore not work quickly enough to prevent ocean acidification (operating over a timescale of centuries) from making dramatic changes to [CO<sub>3</sub><sup>2-</sup>] and Ω. Over longer timescales, however, it buffers their values. It is an important facet of the [[Past_major_events| Earth System response to various upheavals]].
 +
 
 +
==Other Processes Stabilising Ω==
 +
 
 +
Carbonate compensation as described here is brought about purely by changes in lysocline depths in response to changes in Ω. There are several other aspects of oceanic CaCO<sub>3</sub> cycling that most likely also contribute to maintenance of Ω near to its equilibrium value:  
 +
* 1. production of CaCO<sub>3</sub> may well decline in a more acidic surface ocean, leading to a lighter rain of particles out of the surface ocean and hence to a lighter rain to the sea floor;  
 +
* 2. CaCO<sub>3</sub> that fell to the seafloor in pre-industrial times, before any ocean acidification, may also be affected. As this CaCO<sub>3</sub>, lying at or near to the surface of the sediments, comes into contact with increasingly acidic deep bottom waters, it is likely that some of it, finding itself now lying beneath a suddenly shallower lysocline, will be chemically eroded via dissolution.
 +
* 3. the combination of warming, higher CO2 and increased rainfall in a warmer world may also hasten the rate of weathering of limestone, dolomite and chalk rocks on land, leading to an increased supply rate of calcium and carbon to the oceans.
 +
 
 +
These are not incorporated into the carbon model (although the first can be optionally added using the Model Parameters window).
  
 
==Other related pages==
 
==Other related pages==
 
* [[Carbon model]]
 
* [[Carbon model]]
 
* [[Carbonate Compensation worksheet]]
 
* [[Carbonate Compensation worksheet]]
 +
* [[Past_major_events| Earth System response to various upheavals]]
 +
* [[Ocean acidification]]
  
 
==Further reading==
 
==Further reading==
* R.E. Zeebe & P. Westbroek (2003) [http://www.agu.org/journals/gc/gc0312/2003GC000538/ A simple model for the CaCO3 saturation state of the ocean: The "Strangelove", the "Neritan", and the "Cretan" Ocean]. ''Geochemistry, Geophysics, Geosystems'', 4: article number 1104.
+
* Zeebe RE & Westbroek P (2003) [http://www.agu.org/journals/gc/gc0312/2003GC000538/ A simple model for the CaCO3 saturation state of the ocean: The "Strangelove", the "Neritan", and the "Cretan" Ocean]. ''Geochemistry, Geophysics, Geosystems'', 4: article number 1104.
 +
* Broecker WS & Peng T-H (1987) The role of CaCO3 compensation in the glacial to interglacial atmospheric CO2 change, ''Global Biogeochem. Cycles'', '''1''': 15–29.
  
 
==External links==
 
==External links==
Line 37: Line 58:
 
* [http://en.wikipedia.org/wiki/Carbonate_Compensation_Depth carbonate compensation depth in the oceans], [[Wikipedia]]
 
* [http://en.wikipedia.org/wiki/Carbonate_Compensation_Depth carbonate compensation depth in the oceans], [[Wikipedia]]
 
* [http://en.wikipedia.org/wiki/Saturation_%28chemistry%29 Saturation] (first meaning), [[Wikipedia]]
 
* [http://en.wikipedia.org/wiki/Saturation_%28chemistry%29 Saturation] (first meaning), [[Wikipedia]]
 +
* [http://en.wikipedia.org/wiki/Carbonate Carbonate], [[Wikipedia]]
  
 
[[Category:Stabilisation]]
 
[[Category:Stabilisation]]
 
[[Category:Carbon model]]
 
[[Category:Carbon model]]
 
[[Category:Negative Feedback]]
 
[[Category:Negative Feedback]]

Latest revision as of 11:54, 16 April 2008

Carbonate Compensation.

The ocean has an inbuilt negative feedback process for stabilising the saturation rate with respect to calcium carbonate (Ω), albeit one that takes many millennia to counteract perturbations. This process is called carbonate compensation (Zeebe and Westbroeck, 2003). It involves automatic adjustment of the CaCO3 lysocline in response to any deviations in the CaCO3 saturation state of seawater. The lysocline is the depth at which significant amounts of calcium carbonate start to dissolve on the seabed. Above the lysocline, nearly all of the CaCO3 that falls to the seafloor accumulates in the sediments. Below the calcite lysocline the waters are corrosive to it, leading to dissolving of some or all of the CaCO3 within the sediments. The CaCO3 saturation state is equal to ([CO32-] [Ca2+] / Ksp), where [CO32-] is the concentration of carbonate ions in seawater, [Ca2+] is the concentration of calcium ions and Ksp is the solubility product. In practice, over timescales less than a million years or so, values of both [Ca2+] and Ksp) are bound to remain more or less constant in the ocean. Variations in the value of Ω are therefore determined by variations in the value of [CO32-], and stabilising Ω is equivalent to stabilising [CO32-].

Response to [CO32-] Perturbed Downwards

Chain of events set in motion by an abnormally low saturation state in seawater, leading to a return towards higher values

As illustrated in the diagram to the right, carbonate compensation involves the adjustment of the depth of the CaCO3 lysocline in the ocean in response to changes in Ω. It acts as follows. As the ocean becomes more acid (as is happening at present), carbonate ion concentration ([CO32-]) drops. Because the vertical profile of [CO32-]c(z) (the saturating value of [CO32-], i.e. value at which Ω=1 where seawater is neither under- nor super-saturated relative to CaCO3) does not change, the intersection point of the saturating and the actual [CO32-] moves to shallower depths. This causes a shallowing of the saturation horizon (depth at which Ω=1). Although the lysocline does not lie exactly at the saturation horizon, the two are interlinked. The lysocline typically lies somewhat deeper in the water than the saturation horizon, but the two depths change together in response to changing [CO32-].

The depths of the saturation horizon and lysocline are very sensitive to deep water [CO32-]. For instance, even only a 25% drop in average deep water [CO32-], taking it down from about 90 μMol kg-1 today to 67.5 μMol kg-1 in the future would cause the global saturation horizon to shallow by about 2 km. Much larger decreases in deep [CO32-] are in fact forecast for the future, depending on future Co2 emissions. A model of ocean acidification predicts, under almost all emissions scenarios, that average lysocline depth will be shallower than 0.5 km by the year 2300, compared to depths of at least several kilometres in most locations at present.

Shallowing of the lysocline will increase global dissolution and decrease global burial. This will tend to oppose the low [CO32-] values, by driving an imbalance between the riverine input of dissolved calcium and carbon and their removal in buried calcium carbonate. Rivers continue pouring in 'dissolved carbonate', but the ocean stops (slows down) its burial of CaCO3. The chemical equation for calcification is given by:

Ca2+ + 2HCO3- → CaCO3 + CO2(aq) + H2O

and dissolution is the reverse reaction.

Dissolution of 1 Mole of CaCO3 (or an equivalent reduction in CaCO3 burial) therefore leads to addition of 1 Mole of dissolved inorganic carbon to seawater, together with a simultaneous addition of 2 Moles (charge equivalents) of alkalinity. When the carbonate chemistry is calculated out, these changes to DIC and alkalinity induce an increase in the carbonate ion concentration, completing the negative feedback.

Response to [CO32-] Perturbed Upwards

Chain of events set in motion by an abnormally high saturation state in seawater, leading to a return towards lower values

As illustrated in the diagram to the right, the carbonate compensation response to elevated saturation state is as follows. A rapid elevation of the carbonate ion concentration ([CO32-]) to higher-than-normal values will be accompanied by a transition to the ocean being more than normally supersaturated. Because the vertical profile of [CO32-]c(z) (the saturating value of [CO32-], i.e. value at which Ω=1 where seawater is neither under- nor super-saturated relative to CaCO3) does not change, the intersection point of the saturating and the actual [CO32-] moves to deeper depths. This causes a deepening of the saturation horizon (depth at which Ω=1) and lysocline.

Deepening of the lysocline will decrease global dissolution and increase global burial. This will tend to oppose the high [CO32-] values, by driving an imbalance between the riverine input of dissolved calcium and carbon and their removal in buried calcium carbonate. Rivers continue pouring in 'dissolved carbonate' at the same rate, but are now outweighed by the increased burial of CaCO3.

CaCO3 burial leads to removal of 1 Mole of dissolved inorganic carbon from seawater, together with a simultaneous removal of 2 Moles (charge equivalents) of alkalinity. When the carbonate chemistry is calculated out, these changes to DIC and alkalinity induce an decrease in the carbonate ion concentration, completing the negative feedback.

Speed of Carbonate Compensation

The carbonate compensation-induced changes to ocean carbonate ion concentration will continue until the original, steady-state, carbonate ion concentration is re-attained. The e-folding response time (the time for the deviation of a variable from its equilibrium value to decrease by a factor of e) for carbonate compensation has been estimated in different modelling studies at between 6000 and 14000 years. It will therefore not work quickly enough to prevent ocean acidification (operating over a timescale of centuries) from making dramatic changes to [CO32-] and Ω. Over longer timescales, however, it buffers their values. It is an important facet of the Earth System response to various upheavals.

Other Processes Stabilising Ω

Carbonate compensation as described here is brought about purely by changes in lysocline depths in response to changes in Ω. There are several other aspects of oceanic CaCO3 cycling that most likely also contribute to maintenance of Ω near to its equilibrium value.  :

  • 1. production of CaCO3 may well decline in a more acidic surface ocean, leading to a lighter rain of particles out of the surface ocean and hence to a lighter rain to the sea floor;
  • 2. CaCO3 that fell to the seafloor in pre-industrial times, before any ocean acidification, may also be affected. As this CaCO3, lying at or near to the surface of the sediments, comes into contact with increasingly acidic deep bottom waters, it is likely that some of it, finding itself now lying beneath a suddenly shallower lysocline, will be chemically eroded via dissolution.
  • 3. the combination of warming, higher CO2 and increased rainfall in a warmer world may also hasten the rate of weathering of limestone, dolomite and chalk rocks on land, leading to an increased supply rate of calcium and carbon to the oceans.

These are not incorporated into the carbon model (although the first can be optionally added using the Model Parameters window).

Other related pages

Further reading

External links