# Well-Mixed Greenhouse Gas Cycles🔗

## Carbon Cycle🔗

### Introduction🔗

The carbon cycle sub-model is adapted from the FREE model (Fiddaman, 1997). While the original FREE structure is based on primary sources that are now somewhat dated, we find that they hold up well against recent data. Calibration experiments against recent data and other models do not provide compelling reasons to adjust the model structure or parameters, though in the future we will likely do so.

Other models in current use include simple carbon cycle representations. Nordhaus’ DICE models, for example, use simple first- and third-order linear models (Nordhaus, 1994, 2000). The first-order model is usefully simple, but does not capture nonlinearities (e.g., sink saturation) or explicitly conserve carbon. The third-order model conserves carbon but is still linear and thus not robust to high emissions scenarios. More importantly for education and decision support, neither model provides a recognizable carbon flow structure, particularly for biomass.

Socolow and Lam (2007) explore a set of simple linear carbon cycle models to characterize possible emissions trajectories, including the effect of procrastination.
The spirit of their analysis is similar to ours, except that the models are linear (sensibly, for tractability) and the calibration approach differs.
Socolow and Lam calibrate to Green’s function (convolution integral) approximations of the 2x CO_{2} response of larger models; this yields a calibration for lower-order variants that emphasizes long-term dynamics.
Our calibration is weighted towards recent data, which is truncated, and thus likely emphasizes faster dynamics.
Nonlinearities in the C-ROADS carbon uptake mechanisms mean that the 4x CO_{2} response will not be strictly double the 2xCO_{2} response.

### Structure🔗

The adapted FREE carbon cycle is an eddy diffusion model with stocks of carbon in the atmosphere, biosphere, mixed ocean layer, and three deep ocean layers. The model couples the atmosphere-mixed ocean layer interactions and net primary production of the Goudriaan and Kettner and IMAGE 1.0 models (Goudriaan and Ketner 1984; Rotmans 1990) with a 5-layer eddy diffusion ocean based on (Oeschger, Siegenthaler et al., 1975) and a 2-box biosphere based on (Goudriaan and Ketner 1984).

The global terrestrial biosphere carbon cycle fluxes and initial biomass and soil stocks are the sum of those by land type as defined in Terrestrial Biosphere Carbon Cycle.

The interaction between the atmosphere and mixed ocean layer involves a shift in chemical equilibria (Goudriaan and Ketner, 1984).
CO_{2} in the ocean reacts to produce HCO–3 and CO=3. In equilibrium,

$$ C_m = C_{\mathrm{m,0}} \biggl( \frac{C_a}{C_{\mathrm{a,0}}} \biggr) ^ { \frac{1}{\zeta} } $$

C_{m} = C in mixed ocean layer

C_{m,0} = reference C in mixed ocean layer

C_{a} = C in atmosphere

C_{a,0} = reference C in atmosphere

ζ = buffer factor

The atmosphere and mixed ocean adjust to this equilibrium with a time constant of 1 year.
The buffer or Revelle factor, ζ, is typically about 10.
As a result, the partial pressure of CO_{2} in the ocean rises about 10 times faster than the total concentration of carbon (Fung, 1991).
This means that the ocean, while it initially contains about 60 times as much carbon as the preindustrial atmosphere, behaves as if it were only 6 times as large.

The buffer factor itself rises with the atmospheric concentration of CO_{2} (Goudriaan and Ketner, 1984; Rotmans, 1990) and temperature (Fung, 1991).
This means that the ocean’s capacity to absorb CO_{2} diminishes as the atmospheric concentration rises.
This temperature effect is another of several possible feedback mechanisms between the climate and carbon cycle.
The fractional reduction in the solubility of CO_{2} in ocean falls with rising temperatures.
Likewise for the temperature feedback on C flux to biomass, we assume a linear relationship, likely a good approximation over the typical range for warming by 2100.
The sensitivity parameter that governs the strength of the effect on the flux to the biomass also governs the strength of the effect on the flux to the ocean.
For both effects, the default sensitivity of 1 yields the average values found in Friedlingstein et al., 2006.

$$ \zeta = \zeta_0 + \delta_b \ln \biggl( \frac{C_a}{C_{\mathrm{a,0}}} \biggr) $$

ζ = buffer factor

ζ_{0} = reference buffer factor

δ_{b} = buffer CO_{2} coefficient

C_{a} = C in atmosphere

C_{a,0} = reference C in atmosphere

The deep ocean is represented by a simple eddy-diffusion structure similar to that in the Oeschger model, but with fewer layers (Oeschger, Siegenthaler et al., 1975). Effects of ocean circulation and carbon precipitation, present in more complex models (Goudriaan and Ketner, 1984; Björkstrom, 1986; Rotmans, 1990; Keller and Goldstein, 1995), are neglected. Within the ocean, transport of carbon among ocean layers operates linearly. The flux of carbon between two layers of identical thickness is expressed by:

$$ F_{\mathrm{m,n}} = \frac{ (C_m - C_n) ^ e }{ d^2 } $$

F_{m,n} = carbon flux from layer *m* to layer *n*

C_{k} = carbon in layer *k*

e = eddy diffusion coefficient

d = depth of layers

The effective time constant for this interaction varies with d, the thickness of the ocean layers. To account for layer thicknesses that are not identical, the time constant uses the mean thickness of two adjacent layers. The following table summarizes time constants for the interaction between the layers used in C-ROADS, which employs a 100 meter mixed layer, and four deep ocean layers that are 300, 300, 1300, and 1800 meters, sequentially deeper. Simulation experiments show there is no material difference in the atmosphere-ocean flux between the five-layer ocean and more disaggregate structures, including an 11-layer ocean, at least through the model time horizon of 2100.

Layer Thickness | Time Constant |
---|---|

100 meters | 1 year |

300 meters | 14 years |

300 meters | 20 years |

1300 meters | 236 years |

1800 meters | 634 years |

The sum of carbon removals by non-land based CDR, defined in Carbon Dioxide Removal, is another flux from the carbon in the atmosphere, which increases the stock of carbon sequestered. Carbon captured from CCS also increases that stock. The sum of carbon from that stock that is lost re-enters the atmosphere.

## Other greenhouse gases🔗

### Other GHGs included in CO_{2}equivalent emissions🔗

En-ROADS explicitly models other well–mixed greenhouses gases, including methane (CH_{4}), nitrous oxide (N_{2}O), and the fluorinated gases (PFCs, SF_{6}, and HFCs).
PFCs are represented as CF4-equivalents due to the comparably long lifetimes of the various PFC types.
HFCs, on the other hand, are represented as an array of the nine primary HFC types, each with its own parameters.
The structure of each GHG’s cycle reflects first order dynamics, such that the gas is emitted at a given rate and is taken up from the atmosphere according to its concentration and its time constant.
Initialization is based on 1990 levels of data from GISS for CH_{4} and N_{2}O and according to C-ROADS (2023) for F-gases.
The remaining mass in the atmosphere is converted, according to its molecular weight, to the concentration of that gas.
The multiplication of each gas concentration by the radiative coefficient of the gas yields its instantaneous radiative forcing (RF).
This RF is included in the sum of all RFs to determine the total RF on the system.

For those explicitly modeled GHGs, the CO_{2} equivalent emissions of each gas are calculated by multiplying its emissions by its 100-year Global Warming Potential.
Time constants, radiative forcing coefficients, and the GWP are taken from the IPCCs Fifth Assessment Report (AR5) Working Group 1 Chapter 8.
(Table 8.A.1. Lifetimes, Radiative Efficiencies and Metric Values GWPs relative to CO_{2}).

In addition to the anthropogenic emissions considered as part of the CO_{2} equivalent emissions, CH_{4}, N_{2}O, and PFCs also have a natural component.
The global natural CH_{4} emissions are from the anaerobic respiration of biomass, soil, and oceans.
The global natural N_{2}O emissions are based on MAGICC output, using the remaining emissions in their “zero emissions” scenario.
The global natural PFC emissions are calculated by dividing Preindustrial mass of CF4 equivalents by the time constant for CF4.
The units of each gas are: MtonsCH_{4}, MtonsN_{2}O-N, tonsCF4, tonsSF_{6}, and tonsHFC for each of the primary HFC types.
To calculate the CO_{2} equivalent emissions of N_{2}O, the model first converts the emissions from MtonsN_{2}O-N/year to Mtons N_{2}O/year.

The sensitivity of this release defaults to 0.1% per degree Celsius over a threshold, defaulted to 2 Degrees Celsius; the user may change these assumptions.

### Montréal Protocol Gases🔗

Rather than explicitly modeling the cycles of the Montreal Protocol (MP) gases, whose emissions are dictated by the MP, En-ROADS uses the calculated RF for historical and projected concentrations, inputted as a data variable.

## Cumulative Emissions🔗

En-ROADS calculates the cumulative CO_{2} with the initial value taken as the 1990 C-ROADS value starting in 1870.
Cumulative emissions are determined through the simulation.
The trillionth ton is a marker of cumulative emissions above which a two degree future is far less likely.
Budgets are also presented from 2011 and from 2018, based on IPCC thresholds.