# Difference between revisions of "The Carbon Cycle"

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==The carbon cycle== | ==The carbon cycle== | ||

− | Changes in atmospheric CO<sub>2</sub> concentration, C, are determined by CO<sub>2</sub> emissions from fossil and industrial sources (< | + | Changes in atmospheric CO<sub>2</sub> concentration, C, are determined by CO<sub>2</sub> emissions from fossil and industrial sources (<math>E_{\rm foss}</math>), other directly human-induced CO<sub>2</sub> emissions from or removals to the terrestrial biosphere (<math>E_{\rm lu}</math>), the contribution from oxidized methane of fossil fuel origin (<math>E_{\rm fCH_4},</math>), the flux due to ocean carbon uptake (<math>F_{\rm ocn}</math>) and the net carbon uptake or release by the terrestrial biosphere (<math>F_{\rm terr}</math>) due to CO<sub>2</sub> fertilization and climate feedbacks. As in the C4MIP generation of carbon cycle models, no nitrogen or sulphur deposition effects on biospheric carbon uptake are included here [[References#Thornton_nitrogenCarbonCycle|Thornton et al., 2006]]. Hence, the budget |

Eq.[[#eq_A1|A1]] for a change in atmospheric CO<sub>2</sub> concentrations is: | Eq.[[#eq_A1|A1]] for a change in atmospheric CO<sub>2</sub> concentrations is: | ||

− | < | + | <math>\Delta C/\Delta t= E_{\rm foss} + E_{\rm lu} + E_{\rm fCH_4}- F_{\rm ocn} - F_{\rm terr}</math><span id="eq_A1"></span><div style="float: right; clear: right;">('''A1''')</div> |

[[file:Fig-A2.jpg|350px|thumb|left|'''Fig-A2''' The terrestrial carbon cycle component in MAGICC with its carbon pools and carbon fluxes. | [[file:Fig-A2.jpg|350px|thumb|left|'''Fig-A2''' The terrestrial carbon cycle component in MAGICC with its carbon pools and carbon fluxes. | ||

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===Terrestrial carbon cycle=== | ===Terrestrial carbon cycle=== | ||

− | The terrestrial carbon cycle follows that in [[References#Wigley_1993_BalancingCarbonBudget|Wigley, 1993]], in turn is based on [[References#Harvey_1989_ManagingAtmCO2|Harvey, 1989]]. It is modeled with three boxes, one living plant box < | + | The terrestrial carbon cycle follows that in [[References#Wigley_1993_BalancingCarbonBudget|Wigley, 1993]], in turn is based on [[References#Harvey_1989_ManagingAtmCO2|Harvey, 1989]]. It is modeled with three boxes, one living plant box <math>P</math> (see Fig.[[#fig_terr_carboncycle|Terrestrial Carbon Cycle]]) and two dead biomass boxes, of which one is for detritus <math>H</math> and one for |

− | organic matter in soils < | + | organic matter in soils <math>S</math>. The plant box comprises woody material, leaves/needles, grass, and roots, but does not include the rapid turnover part of living biomass, which can be assumed to have a zero lifetime on the timescales of interest here (dashed extension of plant box <math>P</math> in Fig.[[#fig_terr_carboncycle|Fig-A2]]. Thus, a fraction of gross primary product (GPP) cycles through the plant box directly back to the atmosphere due to autotrophic respiration and can be ignored (dashed arrows). Only the remaining part of GPP, namely the net primary production (NPP) is simulated. The NPP flux is channeled through the ``rapid turnover´´ part of the plant box and partitioned into carbon fluxes to the remainder plant box (default <math>g_P</math>=35%), detritus (<math>g_H</math>=60%) and soil box<br /> (<math>g_S</math>=1-<math>g_P</math>-<math>g_H</math>=5%). |

− | The plant box has two decay terms, litter production < | + | The plant box has two decay terms, litter production <math>L</math> and a part of gross deforestation <math>D_{\rm gross}^P</math>. Litter production is partitioned |

− | to both the detritus (< | + | to both the detritus (<math>\phi_H</math>=98%) and soil box (<math>\phi_S</math>=1-<math>\phi_H</math>=2%). Thus, the mass balance for the plant box is: |

− | < | + | <math>\Delta P/\Delta t = g_P{\rm NPP} - R - L - D_{\rm gross}^P \label{eq_massbalance_P}</math><span id="eq_A2"></span><div style="float: right; clear: right;">('''A2''')</div> |

− | The detritus box has sources from litter production (< | + | The detritus box has sources from litter production (<math>\phi_HL</math>) and sinks to the atmosphere due to land use (<math>D_{\rm lu}^H</math>), non-land use related oxidation (<math>Q_A</math>), and a sink to the soil box (<math>Q_S</math>). The mass balance for the detritus box is thus |

− | < | + | <math> \Delta H/\Delta t = g_H{\rm NPP} + \phi_H L - Q_A - Q_S - D_{\rm lu}^H \label{eq_massbalance_H}</math><span id="eq_A3"></span><div style="float: right; clear: right;">('''A3''')</div> |

− | The soil box has sources from litter production (< | + | The soil box has sources from litter production (<math>\phi_S</math>L), the detritus box (<math>Q_S</math>) and fluxes to the atmosphere due to land use |

− | (< | + | (<math>D_{\rm gross}^S</math>), and non-land use related oxidation (<math>U</math>). The mass balance for the soil box is thus |

− | < | + | <math> \Delta S/\Delta t = g_S{\rm NPP} +\phi_S L + Q_S - U - D_{\rm lu}^S \label{eq_massbalance_S}</math><span id="eq_A4"></span><div style="float: right; clear: right;">('''A4''')</div> |

− | The decay rates (< | + | The decay rates (<math>L</math>, <math>Q</math> and <math>U</math>) of each pool are assumed to be proportional to pool's box masses <math>P</math>, <math>H</math> and <math>S</math>, respectively. The turnover times <math>\tau_P</math>, <math>\tau_H</math> and <math>\tau_S</math> are determined by the initial steady-state conditions for box sizes and fluxes. |

− | < | + | <math>L_0 = P_0/\tau^P_0</math><span id="eq_A5"></span><div style="float: right; clear: right;">('''A5''')</div> |

− | < | + | <math>Q_0 = H_0/\tau^H_0</math><span id="eq_A6"></span><div style="float: right; clear: right;">('''A6''')</div> |

− | < | + | <math>U_0 = S_0/\tau^S_0\label{eq_terrcc_turnovertimes}</math><span id="eq_A7"></span><div style="float: right; clear: right;">('''A7''')</div> |

− | Constant relaxation times < | + | Constant relaxation times <math>\tau</math> ensure that the box masses will relax back to their initial sizes if perturbed by a one-off land use change-related carbon release or uptake -- assuming no changes in fertilization and temperature feedback terms. This relaxation acts as an effective regrowth term so that deforestation <math>\Sigma D_{\rm gross}{=}D_{\rm gross}^P + D_{\rm gross}^H + D_{\rm gross}^S</math> represents the gross land use emissions, related to net land use emissions <math>E_{\rm lu}</math> by regrowth <math>\Sigma G</math>=<math>G^P</math> + <math>G^H</math> + <math>G^S</math> |

− | < | + | <math>\Sigma D_{\rm gross} - \Sigma {\rm G} = E_{\rm lu}</math><span id="eq_A8"></span><div style="float: right; clear: right;">('''A8''')</div> |

− | < | + | <math>D_{\rm gross}^P - {\rm G}^P = d_P E_{\rm lu}</math><span id="eq_A9"></span><div style="float: right; clear: right;">('''A9''')</div> |

− | < | + | <math>D_{\rm gross}^H - {\rm G}^H = d_H E_{\rm lu}</math><span id="eq_A10"></span><div style="float: right; clear: right;">('''A10''')</div> |

− | < | + | <math>D_{\rm gross}^S - {\rm G}^S = d_S E_{\rm lu}\label{eq_grossandnet_deforestation}</math><span id="eq_A11"></span><div style="float: right; clear: right;">('''A11''')</div> |

− | Gross land-use related emissions might be smaller (compared to a case where relaxation times are assumed constant) as some human land use activities, e.g.\ deforestation, can lead to persistent changes of the ecosystems over the time scales of interest, thereby preventing full regrowth to the initial state < | + | Gross land-use related emissions might be smaller (compared to a case where relaxation times are assumed constant) as some human land use activities, e.g.\ deforestation, can lead to persistent changes of the ecosystems over the time scales of interest, thereby preventing full regrowth to the initial state <math>P_0</math>, <math>H_0</math> or <math>S_0</math>. A factor <math>\psi</math> is used to denote the fraction of gross deforestation that does not regrow (0<math>{\leq}{\psi}{\leq}</math>1). Thus, the relaxation times <math>\tau</math> are made time-dependent according to the following equation: |

− | < | + | <math>\tau^P(t) = \left(P_0 - \psi\int_0^t d_PE_{\rm lu}(t')dt'\right)/L_0</math><span id="eq_A12"></span><div style="float: right; clear: right;">('''A12''')</div> |

− | < | + | <math>\tau^H(t) = \left(H_0 - \psi\int_0^t d_HE_{\rm lu}(t')dt'\right)/Q_0</math><span id="eq_A13"></span><div style="float: right; clear: right;">('''A13''')</div> |

− | < | + | <math>\tau^S(t) = \left(S_0 - \psi\int_0^t d_SE_{\rm lu}(t')dt'\right)/U_0 \label{eq_terrcc_turnovertimes_timedep}</math><span id="eq_A14"></span><div style="float: right; clear: right;">('''A14''')</div> |

====Formulation for CO<sub>2</sub> fertilization==== | ====Formulation for CO<sub>2</sub> fertilization==== | ||

− | CO<sub>2</sub> fertilization indicates the enhancement in net primary production (NPP) due to elevated atmospheric CO<sub>2</sub> concentration. As described in [[References#Wigley_2000_balancingCarbonBudget|Wigley, 2000]], there are two common forms used in simple models to simulate the CO<sub>2</sub> fertilization effect: (a) the logarithmic form (fertilization parameter < | + | CO<sub>2</sub> fertilization indicates the enhancement in net primary production (NPP) due to elevated atmospheric CO<sub>2</sub> concentration. As described in [[References#Wigley_2000_balancingCarbonBudget|Wigley, 2000]], there are two common forms used in simple models to simulate the CO<sub>2</sub> fertilization effect: (a) the logarithmic form (fertilization parameter <math>\beta_m</math>=1) and (b) the rectangular hyperbolic or sigmoidal growth function (<math>\beta_m</math>=2) (see e.g. [[References#Gates_1985_globalbiosphericCCycle|Gates, 1985]]. The rectangular hyperbolic formulation provides more realistic results for both low and high concentrations so that NPP does not rise without limit as CO<sub>2</sub> concentrations increase. Previous MAGICC versions include both formulations, but used the second as default. The code now allows use of a linear combination of both formulations (1<math>{\leq}{\beta_m}{\leq}</math>2). |

− | The classic logarithmic fertilization formulation calculates the enhancement of NPP as being proportional to the logarithm of the change in CO<sub>2</sub> concentrations C above the preindustrial level < | + | The classic logarithmic fertilization formulation calculates the enhancement of NPP as being proportional to the logarithm of the change in CO<sub>2</sub> concentrations C above the preindustrial level <math>C_0</math>: |

− | < | + | <math>\beta_{\rm log}=1 + \beta_s \,{\rm ln}\,({\rm C/C}_0) \label{eq_CO2fertilization_logarithm}</math><span id="eq_A15"></span><div style="float: right; clear: right;">('''A15''')</div> |

The rectangular hyperbolic parameterization for fertilization is given by | The rectangular hyperbolic parameterization for fertilization is given by | ||

− | < | + | <math>N=\frac{{C-C}_b}{1+b({C-C}_b)}</math> |

− | :< | + | :<math>=\frac{{N_0}(1+b(C_0-C_b))({C}-{C_b})}{(C_0-C_b)(1+b({C-C}_b))}\label{eq_CO2fertilization_sigmoidal growth}</math><span id="eq_A16"></span><div style="float: right; clear: right;">('''A16''')</div> |

− | where < | + | where <math>N_0</math> is the net primary production and <math>C_0</math> the CO<sub>2</sub> concentrations at pre-industrial conditions, <math>C_b</math> the concentration value at which NPP is zero (default setting: <math>C_b</math>=31 ppm, see [[References#gifford_1993|Gifford, 1993]]. |

− | For better comparability with models using the logarithmic formulation, following [[References#Wigley_2000_balancingCarbonBudget|Wigley, 2000]], the CO<sub>2</sub> fertilization factor < | + | For better comparability with models using the logarithmic formulation, following [[References#Wigley_2000_balancingCarbonBudget|Wigley, 2000]], the CO<sub>2</sub> fertilization factor <math>\beta_s</math> expresses the NPP enhancement due to a CO<sub>2</sub> increase from 340 ppm to 680 ppm, valid under both formulations. Thus, MAGICC first determines the NPP ratio <math>r</math> for a given <math>\beta_s</math> fertilization factor according to: |

− | < | + | <math>r=\frac{{N}(680)}{{N}(340)}=\frac{{N}_0(1+\beta_s \,{\rm ln}\,(680/{{C}}_0))}{{N}_0(1+\beta_s \,{\rm ln}\, (340/{C}_0))}\label{eq_CO2fertilization_340to640}</math><span id="eq_A17"></span><div style="float: right; clear: right;">('''A17''')</div> |

− | Following from here, < | + | Following from here, <math>b</math> in Eq. [[#eq_A16|A16]] is determined by |

− | < | + | <math>b=\frac{(680-{C}_b)-r(340-{C}_b)}{(r-1)(680-{C}_b)(340-{C}_b)}\label{eq_CO2fertilization_determining b}</math><span id="eq_A18"></span><div style="float: right; clear: right;">('''A18''')</div> |

− | which can in turn be used in Eq. [[#eq_A16|A16]] to calculate the effective CO<sub>2</sub> fertilization factor < | + | which can in turn be used in Eq. [[#eq_A16|A16]] to calculate the effective CO<sub>2</sub> fertilization factor <math>\beta _{\rm sig}</math> at time <math>t</math> as |

− | < | + | <math>\beta _{\rm sig}(t)=\frac{1/({C}_0 - {C}_b) + b}{1/({C}(t)- {C}_b) + b} \label{eq_CO2fertilization_factor_michaelismenton}</math><span id="eq_A19"></span><div style="float: right; clear: right;">('''A19''')</div> |

− | MAGICC6 allows for an increased flexibility, as any linear combination between the two fertilization parameterizations can be chosen (1< | + | MAGICC6 allows for an increased flexibility, as any linear combination between the two fertilization parameterizations can be chosen (1<math>{\leq}{\beta_m}{\leq}</math>2), so that the effective fertilization factor <math>\beta _{\rm eff}</math> is given by: |

− | < | + | <math>\beta _{\rm eff}(t)=(2-\beta_m)\beta_{\rm log}+(\beta_m-1)\beta_{\rm sig}\label{eq_CO2fertilization_factor_effective}</math><span id="eq_A20"></span><div style="float: right; clear: right;">('''A20''')</div> |

− | The CO<sub>2</sub> fertilization effect affects NPP so that < | + | The CO<sub>2</sub> fertilization effect affects NPP so that <math>\beta_{\rm eff}</math> = NPP - NPP<sub>0</sub>. MAGICC's terrestrial carbon cycle furthermore applies the fertilization factor to one of the heterotrophic respiration fluxes <math>R</math> that cycles through the detritus box, which makes up 18.5 % of the total heterotrophic respiration (<math>\sum {\rm R} {=} R+U_a+Q</math>) at the initial steady-state. |

====Temperature effect on respiration and decomposition==== | ====Temperature effect on respiration and decomposition==== | ||

− | Global-mean temperature increase is taken as a proxy for climate-related impacts on the carbon cycle fluxes induced by regional temperature, cloudiness or precipitation regime changes. Those impacts are commonly referred to as ``climate feedbacks on the carbon cycle´´, or simply, ``carbon cycle feedbacks´´. Here, the terrestrial carbon fluxes NPP, and the heterotrophic respiration/decomposition fluxes < | + | Global-mean temperature increase is taken as a proxy for climate-related impacts on the carbon cycle fluxes induced by regional temperature, cloudiness or precipitation regime changes. Those impacts are commonly referred to as ``climate feedbacks on the carbon cycle´´, or simply, ``carbon cycle feedbacks´´. Here, the terrestrial carbon fluxes NPP, and the heterotrophic respiration/decomposition fluxes <math>R</math>, <math>Q</math> and <math>U</math> are scaled assuming an exponential relationship, |

− | < | + | <math>F_{i}(t)= F_{i}'(t)\cdot {\rm exp}(\sigma_{i}\Delta T(t))\label{eq_CO2feedback_GPP}</math><span id="eq_A21"></span><div style="float: right; clear: right;">('''A21''')</div> |

− | where < | + | where <math>\Delta T(t)</math> is the temperature above a reference year level, e.g. for 1990 or 1900, and <math>F_i'</math> (<math>F_i</math>) stands for the (feedback-adjusted) fluxes ''NPP'', <math>R</math>, <math>Q</math> and <math>U</math>. The parameters <math>\sigma_i</math> (K<math>^{-1}</math>) are their respective sensitivities to temperature changes. In order to model the actual change in <math>Q</math> and <math>U</math>, the relaxation times <math>\tau</math> for the detritus and soil pool are adjusted, respectively. Land use CO<sub>2</sub> emissions in many emissions scenarios ([[References#Nakicenovic_etal_2000_IPCCSRES|e.g SRES, Nakicenovic and Swart, 2000]]) reflect the net directly human-induced emissions. At each time-step, the gross land use emissions are subtracted from the plant, detritus and soil carbon pools. The difference between net and gross land use emissions is the CO<sub>2</sub> uptake due to regrowth. Thus, a separation between directly human-induced (deforestation-related) emissions and indirectly human-induced effects (regrowth) on the carbon cycle is required. As both regrowth and the temperature sensitivity are modeled by adjusting the turnover times, a no-feedback case is computed separately, retrieving the regrowth, then calculating the feedback-case including the formerly calculated regrowth. |

===Ocean carbon cycle=== | ===Ocean carbon cycle=== | ||

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For modeling the perturbation of ocean surface dissolved inorganic carbon, an efficient impulse response substitute for the 3D-GFDL model [[References#Sarmiento_etal_1992_perturbationCO2_ocean_general_circulation_model|Sarmiento et al. (1992)]] is incorporated into MAGICC. The applied analytical representation of the pulse response function is provided in Appendix A.2.2 of [[References#Joos_Bruno_etal_1996_efficient_accurate_carbonuptake|Joos et al. (1996)]]. | For modeling the perturbation of ocean surface dissolved inorganic carbon, an efficient impulse response substitute for the 3D-GFDL model [[References#Sarmiento_etal_1992_perturbationCO2_ocean_general_circulation_model|Sarmiento et al. (1992)]] is incorporated into MAGICC. The applied analytical representation of the pulse response function is provided in Appendix A.2.2 of [[References#Joos_Bruno_etal_1996_efficient_accurate_carbonuptake|Joos et al. (1996)]]. | ||

− | The sea-to-air flux < | + | The sea-to-air flux <math>F_{\rm ocn}</math> is determined by the partial pressure differential for CO<sub>2</sub> between the atmosphere C and surface layer of the ocean <math>\rho</math>CO<sub>2</sub> |

− | < | + | <math>{\rm F}_{\rm ocn} = k (C-\rho {\rm CO}_2) \label{eq_fluxocean}</math><span id="eq_A22"></span><div style="float: right; clear: right;">('''A22''')</div> |

− | where < | + | where <math>k</math> is the global average gas exchange coefficient ([[References#Joos_Prentice_etal_2001_feedbacks_biosphere_IPCC|Joos et al., 2001]]). This exchange coefficient is here calibrated to the individual C<math>^4</math>MIP carbon cycle models (default value (7.66 yr<sup>-1</sup>). The perturbation in dissolved inorganic carbon in the surface ocean <math>\Delta\Sigma {\rm |

− | CO_2}(t)</ | + | CO_2}(t)</math> at any point t in time is obtained from the convolution integral of the mixed layer impulse response function <math>r_s</math> and the net air-to-sea flux <math>F_{\rm ocn}</math>: |

− | < | + | <math>\label{eq_hilda_pertdissolvedinorgCO2}\Delta\Sigma {\rm CO_2}(t) &=& \frac{c}{hA}\{\int_{t_0}^{t} {F}_{\rm ocn}(t') r_s(t-t')dt')\}</math><span id="eq_A23"></span><div style="float: right; clear: right;">('''A23''')</div> |

− | The impulse response function < | + | The impulse response function <math>r_s</math> is given for the time immediately after the impulse injection (<1 yr) by (see Appendix A.2.4 of [[References#Joos_Bruno_etal_1996_efficient_accurate_carbonuptake|Joos et al., 1996]]): |

− | < | + | <math>r_s(t)&=& 1.0 - 2.2617t + 14.002t^2-48.770t^3+82.986t^4-67.527t^5+21.037t^6 \label{eq_hilda_impulseresponse_below2years}</math><span id="eq_A24"></span><div style="float: right; clear: right;">('''A24''')</div> |

− | and for t< | + | and for t<math>{\geq}</math>1 year is given by: |

− | < | + | <math>r_s(t)= \sum_{i=1}^6 \gamma_i e^{-\tau_i t}\label{eq_oceancc_after_initialphase}</math><span id="eq_A25"></span><div style="float: right; clear: right;">('''A25''')</div> |

− | with the partitioning < | + | with the partitioning <math>\gamma</math> and relaxation <math>\tau</math> coefficients: |

− | < | + | <math>\gamma=\left[\begin{array}{l}0.01481\\0.70367\\0.24966\\0.066485\\0.038344\\0.019439\end{array}\right]\tau=\left[\begin{array}{l}0\\1/0.70177\\1/2.3488\\1/15.281\\1/65.359\\1/347.55\end{array}\right] \label{eq_hilda_impulseresponse_after2years_coefficients}</math><span id="eq_A26"></span><div style="float: right; clear: right;">('''A26''')</div> |

− | The relationship between the perturbation to dissolved inorganic carbon < | + | The relationship between the perturbation to dissolved inorganic carbon <math>\Delta\Sigma</math>CO<math>_2(t)</math> and ocean surface partial pressures <math>\Delta\rho</math>CO<sub>2</sub>(<math>T_0</math>) (expressed in ppm or <math>\mu</math>atm) at the preindustrial temperature level <math>T_0</math> is given by Eq.(A23) in [[References#Joos_Prentice_etal_2001_feedbacks_biosphere_IPCC|Joos et al. (1996)]]. Furthermore, the temperature sensitivity effect on CO<sub>2</sub> solubility and hence oceanic carbon uptake is parameterized with a simple exponential expression. The modeled partial pressure <math>\rho</math>CO<math>_2(t)</math> increases with sea surface temperatures according to: |

− | < | + | <math>\rho {\rm CO}_2(t) = [\rho {\rm CO}_2(t_0) + \Delta\rho {\rm CO}_2(T_0)]\, {\rm exp}(\alpha_T \Delta T)\label{eq_partialpressure_ocn}</math><span id="eq_A27"></span><div style="float: right; clear: right;">('''A27''')</div> |

− | where < | + | where <math>\alpha_T</math> (default <math>\alpha_T</math>=0.0423 K<sup>-1</sup>) is the sensitivity of the sea surface partial pressure to changes in temperature (<math>\Delta T</math>) away from the preindustrial level (see |

Eq.(A24) in [[References#Joos_Prentice_etal_2001_feedbacks_biosphere_IPCC|Joos et al. (1996)]], based on [[References#Takahashi_etal_1993_surfaceOceans_CO2|Takahashi et al. (1993)]]). | Eq.(A24) in [[References#Joos_Prentice_etal_2001_feedbacks_biosphere_IPCC|Joos et al. (1996)]], based on [[References#Takahashi_etal_1993_surfaceOceans_CO2|Takahashi et al. (1993)]]). |

## Latest revision as of 17:09, 17 June 2013

## Contents

## The carbon cycle

Changes in atmospheric CO_{2} concentration, C, are determined by CO_{2} emissions from fossil and industrial sources (<math>E_{\rm foss}</math>), other directly human-induced CO_{2} emissions from or removals to the terrestrial biosphere (<math>E_{\rm lu}</math>), the contribution from oxidized methane of fossil fuel origin (<math>E_{\rm fCH_4},</math>), the flux due to ocean carbon uptake (<math>F_{\rm ocn}</math>) and the net carbon uptake or release by the terrestrial biosphere (<math>F_{\rm terr}</math>) due to CO_{2} fertilization and climate feedbacks. As in the C4MIP generation of carbon cycle models, no nitrogen or sulphur deposition effects on biospheric carbon uptake are included here Thornton et al., 2006. Hence, the budget
Eq.A1 for a change in atmospheric CO_{2} concentrations is:

**A1**)

### Terrestrial carbon cycle

The terrestrial carbon cycle follows that in Wigley, 1993, in turn is based on Harvey, 1989. It is modeled with three boxes, one living plant box <math>P</math> (see Fig.Terrestrial Carbon Cycle) and two dead biomass boxes, of which one is for detritus <math>H</math> and one for
organic matter in soils <math>S</math>. The plant box comprises woody material, leaves/needles, grass, and roots, but does not include the rapid turnover part of living biomass, which can be assumed to have a zero lifetime on the timescales of interest here (dashed extension of plant box <math>P</math> in Fig.Fig-A2. Thus, a fraction of gross primary product (GPP) cycles through the plant box directly back to the atmosphere due to autotrophic respiration and can be ignored (dashed arrows). Only the remaining part of GPP, namely the net primary production (NPP) is simulated. The NPP flux is channeled through the ``rapid turnover´´ part of the plant box and partitioned into carbon fluxes to the remainder plant box (default <math>g_P</math>=35%), detritus (<math>g_H</math>=60%) and soil box

(<math>g_S</math>=1-<math>g_P</math>-<math>g_H</math>=5%).

The plant box has two decay terms, litter production <math>L</math> and a part of gross deforestation <math>D_{\rm gross}^P</math>. Litter production is partitioned to both the detritus (<math>\phi_H</math>=98%) and soil box (<math>\phi_S</math>=1-<math>\phi_H</math>=2%). Thus, the mass balance for the plant box is:

<math>\Delta P/\Delta t = g_P{\rm NPP} - R - L - D_{\rm gross}^P \label{eq_massbalance_P}</math>**A2**)

The detritus box has sources from litter production (<math>\phi_HL</math>) and sinks to the atmosphere due to land use (<math>D_{\rm lu}^H</math>), non-land use related oxidation (<math>Q_A</math>), and a sink to the soil box (<math>Q_S</math>). The mass balance for the detritus box is thus

<math> \Delta H/\Delta t = g_H{\rm NPP} + \phi_H L - Q_A - Q_S - D_{\rm lu}^H \label{eq_massbalance_H}</math>**A3**)

The soil box has sources from litter production (<math>\phi_S</math>L), the detritus box (<math>Q_S</math>) and fluxes to the atmosphere due to land use (<math>D_{\rm gross}^S</math>), and non-land use related oxidation (<math>U</math>). The mass balance for the soil box is thus

<math> \Delta S/\Delta t = g_S{\rm NPP} +\phi_S L + Q_S - U - D_{\rm lu}^S \label{eq_massbalance_S}</math>**A4**)

The decay rates (<math>L</math>, <math>Q</math> and <math>U</math>) of each pool are assumed to be proportional to pool's box masses <math>P</math>, <math>H</math> and <math>S</math>, respectively. The turnover times <math>\tau_P</math>, <math>\tau_H</math> and <math>\tau_S</math> are determined by the initial steady-state conditions for box sizes and fluxes.

<math>L_0 = P_0/\tau^P_0</math>**A5**)

**A6**)

**A7**)

Constant relaxation times <math>\tau</math> ensure that the box masses will relax back to their initial sizes if perturbed by a one-off land use change-related carbon release or uptake -- assuming no changes in fertilization and temperature feedback terms. This relaxation acts as an effective regrowth term so that deforestation <math>\Sigma D_{\rm gross}{=}D_{\rm gross}^P + D_{\rm gross}^H + D_{\rm gross}^S</math> represents the gross land use emissions, related to net land use emissions <math>E_{\rm lu}</math> by regrowth <math>\Sigma G</math>=<math>G^P</math> + <math>G^H</math> + <math>G^S</math>

<math>\Sigma D_{\rm gross} - \Sigma {\rm G} = E_{\rm lu}</math>**A8**)

**A9**)

**A10**)

**A11**)

Gross land-use related emissions might be smaller (compared to a case where relaxation times are assumed constant) as some human land use activities, e.g.\ deforestation, can lead to persistent changes of the ecosystems over the time scales of interest, thereby preventing full regrowth to the initial state <math>P_0</math>, <math>H_0</math> or <math>S_0</math>. A factor <math>\psi</math> is used to denote the fraction of gross deforestation that does not regrow (0<math>{\leq}{\psi}{\leq}</math>1). Thus, the relaxation times <math>\tau</math> are made time-dependent according to the following equation:

<math>\tau^P(t) = \left(P_0 - \psi\int_0^t d_PE_{\rm lu}(t')dt'\right)/L_0</math>**A12**)

**A13**)

**A14**)

#### Formulation for CO_{2} fertilization

CO_{2} fertilization indicates the enhancement in net primary production (NPP) due to elevated atmospheric CO_{2} concentration. As described in Wigley, 2000, there are two common forms used in simple models to simulate the CO_{2} fertilization effect: (a) the logarithmic form (fertilization parameter <math>\beta_m</math>=1) and (b) the rectangular hyperbolic or sigmoidal growth function (<math>\beta_m</math>=2) (see e.g. Gates, 1985. The rectangular hyperbolic formulation provides more realistic results for both low and high concentrations so that NPP does not rise without limit as CO_{2} concentrations increase. Previous MAGICC versions include both formulations, but used the second as default. The code now allows use of a linear combination of both formulations (1<math>{\leq}{\beta_m}{\leq}</math>2).

The classic logarithmic fertilization formulation calculates the enhancement of NPP as being proportional to the logarithm of the change in CO_{2} concentrations C above the preindustrial level <math>C_0</math>:

**A15**)

The rectangular hyperbolic parameterization for fertilization is given by

<math>N=\frac{{C-C}_b}{1+b({C-C}_b)}</math>

- <math>=\frac{{N_0}(1+b(C_0-C_b))({C}-{C_b})}{(C_0-C_b)(1+b({C-C}_b))}\label{eq_CO2fertilization_sigmoidal growth}</math>(
**A16**)

where <math>N_0</math> is the net primary production and <math>C_0</math> the CO_{2} concentrations at pre-industrial conditions, <math>C_b</math> the concentration value at which NPP is zero (default setting: <math>C_b</math>=31 ppm, see Gifford, 1993.

For better comparability with models using the logarithmic formulation, following Wigley, 2000, the CO_{2} fertilization factor <math>\beta_s</math> expresses the NPP enhancement due to a CO_{2} increase from 340 ppm to 680 ppm, valid under both formulations. Thus, MAGICC first determines the NPP ratio <math>r</math> for a given <math>\beta_s</math> fertilization factor according to:

**A17**)

Following from here, <math>b</math> in Eq. A16 is determined by

<math>b=\frac{(680-{C}_b)-r(340-{C}_b)}{(r-1)(680-{C}_b)(340-{C}_b)}\label{eq_CO2fertilization_determining b}</math>**A18**)

which can in turn be used in Eq. A16 to calculate the effective CO_{2} fertilization factor <math>\beta _{\rm sig}</math> at time <math>t</math> as

**A19**)

MAGICC6 allows for an increased flexibility, as any linear combination between the two fertilization parameterizations can be chosen (1<math>{\leq}{\beta_m}{\leq}</math>2), so that the effective fertilization factor <math>\beta _{\rm eff}</math> is given by:

<math>\beta _{\rm eff}(t)=(2-\beta_m)\beta_{\rm log}+(\beta_m-1)\beta_{\rm sig}\label{eq_CO2fertilization_factor_effective}</math>**A20**)

The CO_{2} fertilization effect affects NPP so that <math>\beta_{\rm eff}</math> = NPP - NPP_{0}. MAGICC's terrestrial carbon cycle furthermore applies the fertilization factor to one of the heterotrophic respiration fluxes <math>R</math> that cycles through the detritus box, which makes up 18.5 % of the total heterotrophic respiration (<math>\sum {\rm R} {=} R+U_a+Q</math>) at the initial steady-state.

#### Temperature effect on respiration and decomposition

Global-mean temperature increase is taken as a proxy for climate-related impacts on the carbon cycle fluxes induced by regional temperature, cloudiness or precipitation regime changes. Those impacts are commonly referred to as ``climate feedbacks on the carbon cycle´´, or simply, ``carbon cycle feedbacks´´. Here, the terrestrial carbon fluxes NPP, and the heterotrophic respiration/decomposition fluxes <math>R</math>, <math>Q</math> and <math>U</math> are scaled assuming an exponential relationship,

<math>F_{i}(t)= F_{i}'(t)\cdot {\rm exp}(\sigma_{i}\Delta T(t))\label{eq_CO2feedback_GPP}</math>**A21**)

where <math>\Delta T(t)</math> is the temperature above a reference year level, e.g. for 1990 or 1900, and <math>F_i'</math> (<math>F_i</math>) stands for the (feedback-adjusted) fluxes *NPP*, <math>R</math>, <math>Q</math> and <math>U</math>. The parameters <math>\sigma_i</math> (K<math>^{-1}</math>) are their respective sensitivities to temperature changes. In order to model the actual change in <math>Q</math> and <math>U</math>, the relaxation times <math>\tau</math> for the detritus and soil pool are adjusted, respectively. Land use CO_{2} emissions in many emissions scenarios (e.g SRES, Nakicenovic and Swart, 2000) reflect the net directly human-induced emissions. At each time-step, the gross land use emissions are subtracted from the plant, detritus and soil carbon pools. The difference between net and gross land use emissions is the CO_{2} uptake due to regrowth. Thus, a separation between directly human-induced (deforestation-related) emissions and indirectly human-induced effects (regrowth) on the carbon cycle is required. As both regrowth and the temperature sensitivity are modeled by adjusting the turnover times, a no-feedback case is computed separately, retrieving the regrowth, then calculating the feedback-case including the formerly calculated regrowth.

### Ocean carbon cycle

For modeling the perturbation of ocean surface dissolved inorganic carbon, an efficient impulse response substitute for the 3D-GFDL model Sarmiento et al. (1992) is incorporated into MAGICC. The applied analytical representation of the pulse response function is provided in Appendix A.2.2 of Joos et al. (1996).

The sea-to-air flux <math>F_{\rm ocn}</math> is determined by the partial pressure differential for CO_{2} between the atmosphere C and surface layer of the ocean <math>\rho</math>CO_{2}

**A22**)

where <math>k</math> is the global average gas exchange coefficient (Joos et al., 2001). This exchange coefficient is here calibrated to the individual C<math>^4</math>MIP carbon cycle models (default value (7.66 yr^{-1}). The perturbation in dissolved inorganic carbon in the surface ocean <math>\Delta\Sigma {\rm
CO_2}(t)</math> at any point t in time is obtained from the convolution integral of the mixed layer impulse response function <math>r_s</math> and the net air-to-sea flux <math>F_{\rm ocn}</math>:

**A23**)

The impulse response function <math>r_s</math> is given for the time immediately after the impulse injection (<1 yr) by (see Appendix A.2.4 of Joos et al., 1996):

<math>r_s(t)&=& 1.0 - 2.2617t + 14.002t^2-48.770t^3+82.986t^4-67.527t^5+21.037t^6 \label{eq_hilda_impulseresponse_below2years}</math>**A24**)

and for t<math>{\geq}</math>1 year is given by:

<math>r_s(t)= \sum_{i=1}^6 \gamma_i e^{-\tau_i t}\label{eq_oceancc_after_initialphase}</math>**A25**)

with the partitioning <math>\gamma</math> and relaxation <math>\tau</math> coefficients:

<math>\gamma=\left[\begin{array}{l}0.01481\\0.70367\\0.24966\\0.066485\\0.038344\\0.019439\end{array}\right]\tau=\left[\begin{array}{l}0\\1/0.70177\\1/2.3488\\1/15.281\\1/65.359\\1/347.55\end{array}\right] \label{eq_hilda_impulseresponse_after2years_coefficients}</math>**A26**)

The relationship between the perturbation to dissolved inorganic carbon <math>\Delta\Sigma</math>CO<math>_2(t)</math> and ocean surface partial pressures <math>\Delta\rho</math>CO_{2}(<math>T_0</math>) (expressed in ppm or <math>\mu</math>atm) at the preindustrial temperature level <math>T_0</math> is given by Eq.(A23) in Joos et al. (1996). Furthermore, the temperature sensitivity effect on CO_{2} solubility and hence oceanic carbon uptake is parameterized with a simple exponential expression. The modeled partial pressure <math>\rho</math>CO<math>_2(t)</math> increases with sea surface temperatures according to:

**A27**)

where <math>\alpha_T</math> (default <math>\alpha_T</math>=0.0423 K^{-1}) is the sensitivity of the sea surface partial pressure to changes in temperature (<math>\Delta T</math>) away from the preindustrial level (see
Eq.(A24) in Joos et al. (1996), based on Takahashi et al. (1993)).