the Creative Commons Attribution 3.0 License.
the Creative Commons Attribution 3.0 License.
On the future role of the most parsimonious climate module in integrated assessment
Mohammad M. Khabbazan
Hermann Held
In the following, we test the validity of a onebox climate model as an emulator for atmosphere–ocean general circulation models (AOGCMs). The onebox climate model is currently employed in the integrated assessment models FUND, MIND, and PAGE, widely used in policy making. Our findings are twofold. Firstly, when directly prescribing AOGCMs' respective equilibrium climate sensitivities (ECSs) and transient climate responses (TCRs) to the onebox model, global mean temperature (GMT) projections are generically too high by 0.5 K at peak temperature for peakanddecline forcing scenarios, resulting in a maximum global warming of approximately 2 K. Accordingly, corresponding integrated assessment studies might tend to overestimate mitigation needs and costs. We semianalytically explain this discrepancy as resulting from the information loss resulting from the reduction of complexity. Secondly, the onebox model offers a good emulator of these AOGCMs (accurate to within 0.1 K for Representative Concentration Pathways, RCPs, namely RCP2.6, RCP4.5, and RCP6.0), provided the AOGCM's ECS and TCR values are universally mapped onto effective onebox counterparts and a certain time horizon (on the order of the time to peak radiative forcing) is not exceeded. Results that are based on the onebox model and have already been published are still just as informative as intended by their respective authors; however, they should be reinterpreted as being influenced by a larger climate response to forcing than intended.
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Climate–economy integrated assessment models (IAMs) are used to derive welfareoptimal climate policy scenarios (Kunreuther et al., 2014) or constrained welfareoptimal scenarios that comply with a prescribed policy target (Clarke et al., 2014). Most of them employ relatively simple climate modules emulating sophisticated climate models, atmosphere–ocean general circulation models (AOGCMs). These climate modules (hereafter “simple climate models” – SCMs) offer computational efficiency and hence allow researchers to examine a broader set of scenarios in orders of magnitude less time. For IAMs based on a decisionanalytic framework involving intertemporal welfare optimization, SCMs are in fact indispensable, as these IAMs' numerical solvers may need to access the climate module anywhere from 10 000 to 100 000 times before numerical convergence is flagged.
The need to qualify the degree of accuracy with which SCMs mimic AOGCMs or properly represent ensembles of AOGCMs is increasingly being recognized (Calel and Stainforth, 2017; van Vuuren et al., 2011a), as this aspect might have immediate monetary consequences in connection with derived policy scenarios (Calel and Stainforth, 2017). In previous work, van Vuuren et al. (2011a) found that IAMs tend to underestimate the effects of greenhouse gas emissions.
Due to the centennialscale quasilinear properties of AOGCMs' global mean temperature (GMT) dynamics, SCMs have proven capable of emulating AOGCMs' behavior regarding GMT change, with deviations being a function of spread of forcing, SCM complexity (Meinshausen et al., 2011a), and quality of SCM calibration. The climate component of the Model for the Assessment of Greenhouse Gas Induced Climate Change (MAGICC; Meinshausen et al., 2011a) represents the most complex SCM currently in use. In some sense one could even call MAGICC an Earth system model of intermediate complexity. It has demonstrated its capacity to emulate all AOGCMs' GMT even more precisely than the standard deviation of interannual GMT variability (Meinshausen et al., 2011a), with a fixed set of parameters, utilized for the whole range of Representative Concentration Pathways (RCPs) (see van Vuuren et al., 2011b). This represents the current gold standard of AOGCM emulation using SCMs.
The most extreme opposite end of the scale of complexity within the model category of SCMs is provided by the onebox model as introduced by PetschelHeld et al. (1999) (hereafter “PH99”), converting a radiative forcing time series into a GMT time series. The current role of this model as assessed in the literature is as follows: by fitting PH99 to GMT time series, it can be used as a diagnostic instrument, as Andrews and Allen (2008) have done. However, its main application is as an emulator of AOGCMs. In conjunction with the most parsimonious carbon cycle model (described in PetschelHeld et al., 1999 as well), PH99 has been used to derive “admissible” greenhouse gas emission scenarios in view of prescribed GMT targets (Bruckner et al., 2003; Kriegler and Bruckner, 2004). Furthermore, the following climate–economic IAMs are currently utilizing PH99: FUND (Anthoff and Tol, 2014), MIND (Edenhofer et al., 2005), and PAGE (Hope, 2006) – the last of which was used in the “Stern Review” for the UK government (Stern, 2007). While MIND has since been succeeded by the IAM REMIND (Luderer et al., 2011) when it comes to spatial resolution or representing the energy sector by dozens of technologies, it currently serves as a stateoftheart IAM for decisionmaking under uncertainty (Held et al., 2009; Lorenz et al., 2012; Neubersch et al., 2014; Roth et al., 2015) or joint mitigation–solar radiation management analyses (Roshan et al., 2019; Stankoweit et al., 2015).
Kriegler and Bruckner (2004) validated PH99 in conjunction with a simple carbon cycle model. When diagnosing the effect of the IS92a emissions scenario (Kattenberg et al., 1996) on GMT, they demonstrated deviations of less than 0.2 K for the 21st century (see their Fig. 5). Recently, Calel and Stainforth (2017) highlighted the potential future role of PH99 and hence further validation of its behavior is warranted.
In this article, we ask by what calibration procedure is PH99's temperature response to radiative forcing able to correctly map globally averaged radiative forcing anomalies onto GMT anomalies? In this article, “correctly” refers to an accuracy on the order of magnitude of the standard deviation of natural variability, i.e., ∼0.1 K. Furthermore, in the context of this article we would judge a deviation of 0.5 K as inacceptable because a proclaimed goal of the 2015 Paris Agreement (UNFCCC, 2016) is “… holding the increase in the global average temperature to well below 2 ^{∘}C above preindustrial levels and pursuing efforts to limit the temperature increase to 1.5 ^{∘}C above preindustrial levels …” In the policy domain, a difference of 0.5 K matters.
We believe that further validation of PH99 is necessary and possible, at a higher level of consistency than has been performed previously. Firstly, the respective GMT time series as checked in Kriegler and Bruckner (2004) is convexly increasing. However in the context of scenario generation in keeping with the wellbelow 2 K target (UNFCCC, 2016), validation along GMT stabilization or even peaking scenarios is crucial, as these scenarios display a qualitatively different shape from IS92a. Secondly, in Kattenberg et al. (1996) the forcing was reconstructed by the additional assumption that nonCO_{2} greenhouse gas forcing approximately balances aerosol cooling.
Here we employ recently diagnosed forcings for 14 CMIP5 AOGCMs by Forster et al. (2013). As a main finding we diagnose that in the context of 2 K stabilization scenarios, it would be necessary to implement a smaller equilibrium climate sensitivity (ECS) value in PH99 than the diagnosed ECS value of the very AOGCM which PH99 is supposed to emulate. Hence previous work based on PH99 (see Hope, 2006; Anthoff and Tol, 2014, and all the MINDbased work on decisionmaking under ECS uncertainty – see citations above) requires a reinterpretation. Needless to say, we are not claiming that the previously published IAMbased work mentioned above is “worthless”. Rather, we argue that the parameters and probability density distributions need to be interpreted as transformed ones, essentially because a response has been sampled which is higher than that of the corresponding AOGCM. To resolve this, we propose calibrating PH99 by mapping AOGCMs' ECS and TCR to respective effective values, which are suitable for a centennial time horizon, before using them in PH99.
In this way, PH99 could complement the use of increasingly complex climate modules, ranging from DICE's twobox model (Nordhaus, 2013) to the complex upwelling–diffusion climate module used in MAGICC (Meinshausen et al., 2011a). The potential benefits of doing so are twofold: firstly, the most parsimonious SCM, PH99, ensures maximum comprehensibility. Secondly, in the context of numerically solving decisionmaking under climate response uncertainty (Kunreuther et al., 2014), having to simultaneously deal with dozens, hundreds, or even thousands of alternate climate “states of the world” (the economist's term for the uncertain system property) poses a significant challenge for numerical solvers and memory. In this regard, PH99 appears particularly attractive. Keeping the state space as slim as possible proves particularly relevant for decisionmaking under uncertainty with endogenous learning. For that reason, Traeger (2014) utilizes a onebox rather than a twobox model, however with an exogenously given time series somewhat mimicking the existence of a deep ocean layer.
Finally, our article represents a warning: if PH99 is to be used in the future, it should be done in a rescaled manner, adjusted to the time horizon under investigation.
This article is organized as follows. Section 2 introduces the databased part of our analysis. We call for a threestep procedure, including (i) a conventional, though not naïve, calibration of PH99 with regard to climate sensitivity and transient climate response (i.e., the GMT change in response to a 1 % yr^{−1} increase in the CO_{2} concentration until doubling compared to the preindustrial value); (ii) an AOGCMspecific calibration; and (iii) the validation of (ii). In Sect. 3 we first demonstrate that (i) would lead to emulation errors of up to 0.5 K for scenarios approximately compatible with the 2 K target. We then show that this emulation error can be reduced to 0.1 K when choosing AOGCMspecific calibrations of PH99. This calibration is subsequently validated by independent scenarios. Note that, in Sect. 3, we focus on only the RCP2.6 scenario for calibration, use RCP4.5 and RCP8.5 for validation, and leave further analyses, which show that PH99 can be generally calibrated to and validated by a variety of scenarios, to Appendix B. In Sect. 4 we present a scheme of how to calibrate PH99 for a given ECS, thereby avoiding AOGCMspecific calibrations. This results in a larger emulation error than achieved in Sect. 3 but one that would nevertheless suffice for most applications. In Sect. 5 we explain the observed discrepancy between PH99 and AOGCMs as reported for step one of Sect. 2 by pursuing a semianalytical, physically based approach. In Sect. 6 we discuss the implications of our findings for the integrated assessment community, while Sect. 7 presents our conclusions and outlines further research needs.
Before we proceed, a brief note on the role of AOGCM data in our article is in order. We compare PH99 to AOGCM data because we utilize AOGCMs here as the entities closest to “reality” available on the “model market”. We do not, however, claim that IAM modelers were using them or should be using them. AOGCM data are used to demonstrate how ECS and TCR data can skew the calibration of PH99 and how it should be corrected. The same correction should in principle be used for ECS data inferred from any source, e.g., abstract distributions such as those presented in Bindoff et al. (2013). Mirroring PH99 in AOGCM data, however, is currently the most direct way to infer the quality of a (not) recalibrated PH99.
This section introduces the analytic structure of PH99, relates it to ECS and TCR, and then describes a threestep scheme for PH99–AOGCM intercomparison.
PH99 projects the atmospheric GMT anomaly compared to its preindustrial level. PetschelHeld et al. (1999) specified the model for a CO_{2}only forcing scenario and accordingly PH99 reads
Here T denotes the GMT anomaly, c is the CO_{2} concentration in units of its preindustrial level, and α and μ are constant tuning parameters.
From Eq. (1) we can readily read the ECS, the equilibrium temperature anomaly in response to a doubling of the CO_{2} concentration compared to its preindustrial value:
also in line with PetschelHeld et al. (1999) and Kriegler and Bruckner (2004). In Appendix A we briefly derive the TCR (GMT) from a stylized experiment after the CO_{2} concentration has been exponentially increased with the rate γ (of 1 % yr^{−1}) until the concentration has doubled for this model:
In the following we propose a threestep validation approach to clarify PH99's range of applicability.
2.1 Step one
We first check whether simply calibrating PH99 from AOGCMspecific ECS and TCR data would deliver good emulations (i.e., accurate to within 0.1 K) for scenarios compatible with the 2 K target. After a technical derivation, we summarize this method of mapping AOGCMs' ECS and TCR onto PH99's two parameters.
Some difficulty arises due to the fact that AOGCMs have not been run for 2 Ktargetcompatible scenarios for CO_{2}only forcing but solely for a plethora of simultaneous forcings that would add up to a total forcing. Hence we generalize Eq. (1) to its totalforcing counterpart (see Eqs. 4–7) to be driven by total forcing time series as reconstructed in Forster et al. (2013). Accordingly, we utilize scenarios generated by 14 AOGCMs (see Table 1) from CMIP5. From Forster et al. (2013), we also take the ECS and TCR for these 14 models to derive modelspecific α and μ, utilizing Eqs. (2) and (3).
In order to generalize Eq. (1), we recall its derivation from an energy balance approach, as summarized in Kriegler and Bruckner (2004), allowing for a physical interpretation of the model. We start by introducing the general energy balance equation, expressing the change in oceanic heat content as the difference of ingoing (F) and outgoing (λT) radiative flux while h denotes the constant effective oceanic heat capacity (see also Geoffroy et al., 2013, Eqs. 1–4).
F also represents the total radiative forcing as applied in Forster et al. (2013). However the equation could still not be integrated as h and λ are yet to be determined. In order to solve the posed problem (CO_{2}only versus total forcing), we note that h and λ represent universal parameters of PH99 in the sense that their numerical values would not depend on the mix of substances (i.e., CO_{2}, other greenhouse gases, aerosols) causing the total radiative forcing. Therefore, h and λ can be determined by considering the CO_{2}only case and, hence, by tracing them back to the already determined α and μ. For the CO_{2}only case, Eq. (4) reads
Q_{2} denotes the additional forcing from the doubling of the CO_{2} concentration compared to its preindustrial value and is listed for all of the AOGCMs (see Forster et al., 2013, Table 1).
If we then divide by h, we obtain
A comparison with Eq. (1) readily reveals
These equations would allow for the determination of $h={Q}_{\mathrm{2}}/\left(\mathit{\mu}\mathrm{ln}\mathrm{2}\right)$ and λ=αh. Utilizing these equations and Eq. (4), we generate PH99's temperature response to the total radiative forcing as specified in Forster et al. (2013).
The derivation displayed so far can be summarized in terms of the following recipe to generate PH99's parameters on the basis of AOGCMs' ECS and TCR:

set PH99's ECS and TCR equal to the selected AOGCM's ECS and TCR;

numerically invert Eq. (3), righthandside expression, to find α (no analytic expression possible);

invert Eq. (2) to find μ;

derive h and λ from Eq. (7), and then utilize Eq. (4), divided by h.
Finally, to avoid differences occurring over the historical period (pre2006 for the RCPs), we need to initialize PH99 with each AOGCM's 2006 temperature anomaly with respect to the preindustrial value. To do this, for each AOGCM we calculate the mean temperature over the period 1881–1910 and set this as the preindustrial value. We then calculate the mean temperature over the period 1991–2020 and use this as an indicator for the 2006 temperature level. The difference between these two values is fixed as the initial temperature anomaly for PH99.
Each temperature trajectory should be compared to the temperature data from the corresponding AOGCM. As for GMTtargetconstrained economic optimizations (Clarke et al., 2014; Edenhofer et al., 2005), the maximum GMT (rather than the whole time series) is of special importance. Hence we use the difference between the respective 2071–2100 GMT time averages of PH99 and the AOGCM as an error metric. If the deviations are tolerable (accurate to within 0.1 K), the climate module is validated; if they are intolerable, we proceed with steps two and three.
2.2 Step two
For each AOGCM, α and μ are tuned such that the difference between PH99 and the AOGCM GMT anomaly for the RCP2.6 scenario in the period 2006–2100 is minimized using a leastsquares approach. For further diagnostics we then determine the new “effective” ECS and TCR from Eqs. (2) and (3). As in step one, the deviations in 2071–2100 means of GMT between PH99 and the respective AOGCM are determined as an accuracy check.
2.3 Step three
Lastly, we validate the PH99 model versions generated in step two. For this purpose, independent temperature and forcing paths must be run as a nontrivial test to check whether the trained climate module can accurately project other temperature data trajectories. To do so, the values for α and μ determined in step two are implemented in PH99, the latter then being driven by the total climate forcing of the RCP4.5 and RCP8.5 scenarios. Similar to steps one and two, the deviations in 2071–2100 means of GMT between PH99 and the respective AOGCM are determined as an accuracy check.
One might be interested in seeing if the calibrated module is capable of mimicking other scenarios such as RCP6.0 or if PH99 was calibrated to RCP4.5 or others. Stating that, in general, the procedure outlined above brings about similar results, for the sake of brevity of the main text, we present the respective results in Appendix B.
Table 1 shows the calculated α and μ together with the feedback response time 1∕α in step one. For all of the indicators we also compute the mean values and standard deviations of the samples. The mean value of the ECS for GCM data is 3.35 K, with a minimum and maximum of 2.11 and 4.67 K, respectively. The mean value of the timescales is roughly 35 years.
Figure 1 represents the projected PH99 temperature evolution for the scenario RCP2.6 of each GCM in 2006–2100, using the data from Table 1 and RCP2.6's forcings. PH99 clearly overestimates the temperature anomaly for all GCMs, especially over the last 30 years. The absolute values of the deviations of mean temperature over the last 30 years (hereafter MTD) from the AOGCM data are shown in Fig. 2. The MTD ranges from 0.22 K for MRICGCM3 to approximately 0.79 K for HadGEM2ES. On average, the deviations are ca. 0.45 K. This is clearly a large error, in both units of annual GMT standard deviation as well as the climate policy dimension. Accordingly, we must proceed with step two.
In step two, for each of the GCMs, we tune α and μ such that the GMT deviations for the whole period 2006–2100 are minimized in a leastsquares manner as represented in Figs. 3 and 4. From the thereby adjusted α and μ we derive the ECS and TCR, which are presented in Table 2. MTDs for the various AOGCMs are shown in Fig. 2.
The results tell us three main things. Firstly, the average of the absolute values of deviations is significantly reduced when α and μ are tuned. Indeed, the MTD average drops to below 0.02 K. Secondly, while the average ECS decreases by 0.9 K (from 3.35 to 2.46 K), the average TCR increases by 0.14 K (from 1.90 to 2.04 K). Thirdly, the mean value of feedback response times decreases significantly, from roughly 35 years to less than 12 years.
For validation we move on to step three. We utilize the RCP4.5 temperature and forcing data as provided by Forster et al. (2013). In Figs. 3 and 4 the respective GMT trajectories for any AOGCM are contrasted with the PH99generated ones, where α and μ are fixed to their values as determined in step two. The MTDs are shown in Fig. 2. The results confirm that the climate module is sufficiently well trained in the second step that it can suitably mimic the actual temperatures (accurate to within 0.1 K) for RCP4.5 and RCP8.5. As shown, the average MTD is approximately 0.05 K for RCP4.5 and about 0.14 K for RCP8.5. For RCP4.5, the deviations for three of the GCMs, namely CCSM4, CNRMCM5, and NorESM1M, are even better than those diagnosed for RCP2.6 in step two. See Appendix B for further analyses.
Finally, we attempt to abstract from fitting PH99 to individual AOGCMs and provide an approximate way to calibrate PH99 within the cloud of AOGCMs simply by knowing the ECS. Then PH99 could be utilized for any ECS in analyses in which the ECS is uncertain.
4.1 An existing mapping for PH99
Before diving into our suggestions, we examine one of the existing options (a reader solely interested in our improved method of utilizing PH99 can move straight on to Sect. 4.2). We inspect the curve suggested by Lorenz et al. (2012), which correlates α and μ to ECS. Using a sample from Frame et al. (2005) and assuming a strict relationship between 1∕μ and ECS, Lorenz et al. (2012) suggest the following approximation:
where $\stackrel{\mathrm{\u203e}}{\mathit{\mu}}$ is the mean value of μ in the sample (see Fig. 7 in Lorenz et al., 2012; all quantities measured in the units utilized in Kriegler and Bruckner, 2004). Knowing μ, Eq. (2) is used to determine α. In turn, Eqs. (2) and (8) have been repeatedly used in studies employing MIND and concerning uncertainties and ECS (Neubersch et al., 2014; Roshan et al., 2019; Roth et al., 2015).
We employ Eqs. (2) and (8) for all ECSs from Table 1 and show the MTDs for the RCP2.6 scenario in Fig. 5. Note that TCR can readily be calculated using Eq. (3). Clearly, on average, employing Lorenz's curve does not result in a better situation than step one. However, this might not necessarily be a case of comparing like with like. At the time of Frame et al. (2005), the twodimensional uncertainty information was obtained by reconstructing the 20th century's warming signal from fingerprinting by means of a single AOGCM and then using these observational data as a constraint. It is well known that observational constraints may lead to different distributions than ensembles of AOGCMs do (Andrews and Allen, 2008). Nevertheless we include this piece of information here for the sake of completeness.
4.2 A multiple AOGCMbased mapping for PH99
Given the inferred estimates in Table 2, one can directly relate α and μ to the ECS. To do so, we generate polynomial fits (of orders of 2 and 3) of α and μ against all AOGCMs' ECSs. Predicting a twodimensional manifold from ECS alone implicitly exploits the fact that AOGCMs' TCRs can be predicted well using ECSs (see e.g., Meinshausen et al., 2009) in a statistical sense. Another option would be to derive α and μ analytically (like in the first step) when the inferred ECS and TCR are correlated to the ECS and TCR of AOGCMs.
Figure 6 relates α and μ (from Table 2) to the ECS (from Table 1), using linear, quadratic, and cubic polynomial approximations. For the case of a linear approximation, we put the model GISS_E2_R out as an outlier. Figure 5 indicates that on average all approximations mimic the actual temperature paths better than a nonfitted one. The cubic estimation projects significantly smaller deviations compared to the quadratic approximation and slightly smaller deviations compared to the linear approximation. The maximum MTD in the cubic approximation is 0.3 K for IPSLCM5ALR, which is roughly a third of the maximum in the quadratic approximation that is revealed for CSIROMk360.
We also consider alternative ways to map ECS and TCR from the 14 utilized AOGCMs onto PH99intrinsic properties, going beyond the scheme displayed in Fig. 6. As one option, shown in Fig. 7, we linearly regress the ECS and TCR values inferred from step two against their original AOGCM counterparts and obtain
with a=0.5846, b=0.5095 K, and R^{2}=0.8158, as long as ECS_{PH99} < ECS_{AOGCM} and
with c=0.9763, d=0.1829 K, and R^{2}=0.667.
The other option consists in using Eq. (9) along with a linearly regressed TCR_{PH99} over ECS_{AOGCM}, that is
with m=0.4582, n=0.5044 K, and R^{2}=0.7876.
The respective MTDs are shown in Fig. 5. Although both approximations mimic the actual temperature paths better than a nonfitted one, regressing both the inferred effective ECS and TCR solely against AOGCMs' ECS (hereafter ETE) clearly offers the best overall approximation.
Using the ETE has four major advantages over all other options dealt with here, especially for the IAM community. Firstly, its approximation is better than all options but the cubic fit. Secondly the ETE still has an advantage over the cubic fit because one can easily use a broader range of climate sensitivities, for example, from 1 to 9 K, which may not be accurately determined by the cubic fit. Even though the cubic fit may yield a better approximation, in our analysis it is only better by 0.03 K at the expense of a nonintuitive shape that might result in even worse deviations for outofsample data. Thirdly, prior knowledge regarding the TCR is no longer a decisive factor. Note that prior knowledge regarding the TCR can make approximations better. However, as we tested, for example, in the case of linearly regressing both the inferred effective ECS and TCR against both AOGCMs' ECS and TCR, the R squares for Eqs. (9) and (11) only improve by 6 % and 7 % respectively, and the MTD is no better than the ETE. Finally, in the case of ETE, we do not need to reevaluate our sample and possibly drop any model as an outlier. Given the explorations already carried out and their performance, we leave explorations beyond the linear approximation for future research.
In the following, we explain why PH99 systematically overestimates maximum GMT for peaking scenarios when fitted for exponentially growing scenarios. As an AOGCM is analytically not accessible, we investigate an intermediate step of model replacement by moving from a onebox to a twobox SCM (as utilized in DICE; Nordhaus, 2013). In fact we qualitatively trace back the effects reported so far to the information loss incurred by replacing a twobox SCM with a onebox SCM like PH99. We then also investigate the quality of alternative fitting schemes based on our semianalytic analysis, which complements our previously mentioned AOGCMbased validation.
Following Geoffroy et al. (2013) we introduce a twobox SCM as a more universal emulator of AOGCMs' mapping from radiative forcing onto temperature.
T_{2B} denotes the twobox analogue of the onebox temperature T in Eq. (1). The upper and the lower equations represent the upper and the lower ocean, respectively.
In order to contrast PH99 with this twobox model, we search for analytic approximations of generic shapes of the forcing F(t) and examine the longterm projections under various RCPs as depicted in Meinshausen et al. (2011b) – an excerpt is included in Fig. 8 for the reader's convenience. Particularly in view of the peaking, mitigationoriented lowest forcing scenario, we approximate forcing paths in three phases: zero forcing, linear increase, and linear decrease, under a continuity assumption.
We approximately identify t_{1} with the year 2035 and t=0 with 100 years earlier, i.e., we assume a rampup time t_{1} for the forcing of roughly 100 years. Furthermore, k_{2}<0 and ${k}_{\mathrm{2}}/{k}_{\mathrm{1}}=:\mathit{\epsilon}\ll \mathrm{1}$. From Fig. 8 we approximate a generic value of ε=0.2. For $\mathrm{0}\le t\le {t}_{\mathrm{1}}$ we draw on Geoffroy et al. (2013 – see their Eq. 14):
This represents two linear modes of amplitudes a_{f} and a_{s} (with a sum equal to 1), delayed by the characteristic timescales of a fast and a slow mode, τ_{f} and τ_{s}, respectively, and continuously matched to the initial condition “0” by an exponential. In Geoffroy et al. (2013) the twobox model is fitted to 16 AOGCMs. After having reviewed their results, we can make the following two simplifying assumptions: (i) both amplitudes a_{f} and a_{s} approximately equal 1∕2 (see their Fig. 3a – amplitudes range from 0.35 to 0.65) and (ii) τ_{f}≈0 (values range from 1 to 5.5 years; see their Table 4; for centennial effects, this mode would nearly match the equilibrium response). Furthermore we can see that τ_{s} ranges from 100 to 300 years for 15 out of 16 AOGCMs. Hence the twobox model is characterized by a marked timescale separation between the two linear modes. With the aid of these two approximations, the last equation can be simplified to
We then extend the analytic range of that formula, given the two approximations above, for t>t_{1} (for a derivation; see Appendix C):
The analogous expressions for the onebox model read
and
5.1 Explaining the PH99–AOGCM discrepancy for equal ECS and TCR values
We are now prepared to mimic step one in Sect. 2: we calibrate the onebox model such that it is characterized by the same ECS and TCR as the twobox model. As $\mathit{\lambda}={Q}_{\mathrm{2}}/{\mathrm{ECS}}_{\mathrm{2}\mathrm{B}}$, equal ECS values for both models deliver λ=λ_{2B}.
Determining the second degree of freedom of PH99 (e.g., as expressed by θ) from some transient property proves more intricate. We choose
where we introduce t_{TCR} as the moment in time when T needs to be evaluated in order to determine TCR. In Appendix A we note, by definition, that ${t}_{\mathrm{TCR}}=\left(\mathrm{ln}\mathrm{2}\right)/\mathit{\gamma}\approx \mathrm{70}$ years for a growth rate γ=1 % yr^{−1} of the carbon dioxide concentration; hence $\mathrm{0}<{t}_{\mathrm{TCR}}<{t}_{\mathrm{1}}$. Therefore, when exploiting Eq. (20), Eqs. (16) and (18) (rather than Eqs. 17 and 19) apply and result in the expression
with h denoting the auxiliary function (see Fig. 9)
where
From this, we can already get a first impression of the scale of θ, prior to numerical inversion: as τ is generically markedly larger than t_{TCR}, the righthand side of the defining equation above approximates 1∕2. Further, if we boldly assume a slight timescale separation between θ and t_{TCR}, the former being smaller than the latter, then the linear approximation of h would apply and $\mathit{\theta}\approx {t}_{\mathrm{TCR}}/\mathrm{2}\approx \mathrm{35}$ years. For a centered value of τ=250 years, this approximation is confirmed in a direct numerical treatment of Eq. (21).
Hence from the twin timescale separation of “the onebox model mode”, “defining timescale for TCR”, and the “slow mode of the twobox model” we have explained why TCRoriented fitting exercises of the onebox model would generically result in timescales of roughly 30 to 40 years (see e.g., Anthoff and Tol, 2014; Kriegler and Bruckner, 2004). The factor 1∕2 between the onebox model's timescale and the TCRdefining timescale goes back to the observation of Geoffroy et al. (2013) that the fast and the slow modes both enter the superposition result with approximately equal weights of 1∕2. The slow mode is then too slow to be of much relevance for TCR – a phenomenon not revealed by the onebox model.
We are now equipped to compare the two models' temperature projections and apply the threephase forcing as defined above for ε=0.2. a_{1}∕λ is chosen such that peak temperatures enter the 2 K regime for illustrative purposes. We exploit the coincidence that t_{TCR} just happens to approximately correspond to our starting year 2006 for PH99 (because $\mathrm{2035}\mathrm{100}+\mathrm{70}=\mathrm{2005}$). Hence the formulas for the onebox model do not need to be adapted for an explicit initial condition for this purpose. Figure 10 shows that by construction, both temperature responses match at t_{TCR}≈70 years, although the onebox model's maximum exceeds the maximum by 0.5 K. This phenomenon can be explained as follows. As the onebox model responds with a finite timescale, its derivative must be continuous in response to a continuous forcing. Hence the leading term is quadratic when the forcing starts. In contrast, the twobox model contains a virtually degenerate timescale (the fast one); hence its leading term is linear. If the two curves are to nevertheless match at t_{TCR}, the onebox model's derivative at t_{TCR} must transcend the twobox model's derivative. This, together with the rightbending kink in the twobox model's response at t_{1}, leads to a larger maximum in the onebox model. In summary, on timescales much smaller than the slow mode, the slow mode, compared to the fast mode, cannot develop yet; hence the fast mode will dominate the slow mode. As such, fitting a onemode model in a convex regime is likely to yield poor predictions of a temperature maximum for mitigationbased forcings.
This explains the discrepancies found in our PH99–AOGCM comparison when directly transferring AOGCMs' ECS and TCR onto PH99. Figure 10 further suggests that if PH99 were used to predict correct maxima and emulate AOGCMs in this time regime, it would need to be used with a markedly smaller timescale. However, a simple reduction in timescale would lead to a new intermodel discrepancy before the kink; hence the overall amplitude of PH99's response would need to be reduced as well. The latter scales with the ECS. Thus the ECS must be reduced by a certain factor towards a new “effective ECS”, which could also be called a “transient climate sensitivity”.
5.2 Testing the validity of a recalibrated PH99 for a twobox model
In Sect. 5.1 we derived an analytic explanation for why a naïve transfer of an AOGCM's ECS and TCR to PH99 results in a maximum GMT, which is too large when driven by a mitigation forcing scenario. However we show in Sects. 3 and 4 that PH99 in fact is a good emulator of an AOGCM within 0.1 K if it were either directly fitted to that AOGCM or if the AOGCM's ECS and TCR were transformed into effective quantities for PH99. Hereby “good emulator” expresses the fact that the same parameter set can be utilized for any RCP (2.6, 4.5, 6.0, 8.5). From a practical point of view, we could stop our analysis here and suggest that this type of validation might be sufficient to generate trust in PH99 as an emulator for any forcing scenario.
However for further validation, in this subsection we would like to exploit the fact that for a twobox–onebox intercomparison we can validate PH99 for an order of magnitude larger set of forcing scenarios. We systematically test the previously suggested adjustment formulas Eqs. (9) to (11) for a range of t_{1} and ε values, hence varying mitigation scenarios, given the alternative ECS and slow mode's timescale τ for the twobox model. We find numerically that θ is on the order of 10 years, and the ECS needs to be reduced by 1∕4 to 1∕3. We test for the centered ECS values of 3 and 4 K and a slow mode's timescale, ranging from 100 to 300 years (see Geoffroy et al., 2013).
In principle, for any forcing scenario characterized by varying t_{1} and ε, we would need to compare GMT as calculated by Eqs. (18) and (19) vs. Eqs. (16) and (17). However all of these equations derive GMT for the boundary condition of zero temperature at t=0. Conversely, our validation scheme as utilized in Sects. 3 and 4 fix PH99 to the AOGCM at the year 2006. The latter point in time we denote by t_{0}(≈t_{TCR}). Having transformed ECS and TCR according to Eqs. (9)–(11), we cannot expect that T(t_{0})=T_{2B}(t_{0}) any longer. Therefore we have to force the solution of PH99 to match the solution of the twobox model at t_{0} and call the thereby initialized solution of PH99 “T_{init}”:
We generate T_{init}(t) from T(t) (see Eqs. 18 and 19) by adding a suitably scaled solution of the homogenous counterpart of Eq. (4):
Figure 11 shows the relative deviations of the GMT maxima of the onebox and the twobox model for the extrapolation scheme ETE (Eqs. 9 and 11). In a certain regime, the extrapolation delivers sufficiently accurate results, however, not everywhere. When utilizing the mapping scheme represented by Eqs. (9) and (10), the results look similar. The overall impression is that the mapping removes the bias. However, it does not deliver a universal correction as found for the direct intercomparison between PH99 and AOGCMs. Hence we cannot exclude the possibility that AOGCMs are easier to emulate as they contain many more timescales than the twobox model and their effects might in part cancel.
While we observe a qualitative gain, Fig. 11 reveals there is still room for improvement. Accordingly, we further transform the ECS to request perfect matching for t_{1}=100 years, ε=0.2; the results can be seen in Fig. 12. The fit is much further improved such that a major fraction of (t_{1}, ε) values would lead to a relative error of <5 %, and another large fraction would lead to a relative error of <10 %. As the standard deviation of annual GMT is between 0.1 and 0.2 ^{∘}C and a typical application might be a costeffectiveness analysis of the 2 ^{∘}C target, such errors might still seem tolerable. However we observe structural problems for very small values of ε, the latter implying very late assumption of a maximum. In this case, the slow mode becomes more relevant, and hence the quality of the calibration deteriorates. We find that the calibration is valid for a time horizon on the order of t_{1} to 2 t_{1}, i.e., on the order of the time to peak forcing.
The previous section offers a key mechanism to explain why, for given ECS and TCR, GMT responses generated by PH99 in response to peakanddecline forcing scenarios are biased towards higher temperatures. How does this relate to the observation that PH99 tends to underestimate the effect of greenhouse gas emissions (van Vuuren et al., 2011a) as mentioned in our introduction? In fact, van Vuuren et al. (2011a) describe a different forcing experiment: a step function (see their Fig. 3). Here FUND, based on PH99, displays a GMT lower than that of MAGICC4 by more than 0.8 K at certain times during the most transient phase, although both models share the same ECS. This can be explained by the lack of timescales faster than 35 years (the latter characterizing PH99 in standard calibrations) within PH99. Whether PH99 over or underestimates GMT is hence a strong function of the functional shape of forcing. Our article highlights the effects of naïvely calibrating PH99 when assessing mitigation scenarios.
Additional mechanisms are also possible. Firstly, the statistical errors in determining AOGCMs' ECS, TCR, and Q_{2} may lead, mediated through the nonlinear mapping to PH99's parameters, to an overall bias in PH99's GMT. Furthermore, diagnosing the total radiative forcing active in an AOGCM is a complex undertaking (see, e.g., Meinshausen et al., 2011a, for a discussion). A bias to the high end here would also result in inaccurately large GMT responses by PH99.
However, in the context of this article, we contend that the information loss when moving from a twobox to a onebox model is the key source of the observed discrepancy – we find Fig. 10 compelling in this regard. Complying with the latter interpretation raises a key question: can PH99 be seen as a “physical model” and if so, what are the implications for users? It is readily apparent that a onebox model cannot mimic a twobox model, characterized by a marked timescale separation for all forcings at all times. However it is equally clear that the simplest temperature equation is in fact the one that treats the ocean as a single box. It would still explain warming with forcing in a quasilinear manner, though with some delay. If we are willing to accept that the calibration of PH99 is time horizon specific, then PH99 still holds some semiphysical meaning. If, however, this is seen as unacceptable, then we would have to recognize that PH99 is more an efficient emulator than a physical model. In this context we would like to recall that virtually every model has a limited range of validity – and as such, PH99 is no different from most other models.
When investigating the onebox and twobox models' differences, our research also suggests that within the class of peakanddecline scenarios PH99 provides a good emulation (accurate to within 0.2 K for a generic AOGCM setting such as ECS = 4 K, a peaking of forcing between 2020 and 2100, and a ratio of slopes of pre and postpeaking forcing of 0.1 to 0.4). For the AOGCM–PH99 intercomparison, PH99 performs even better: for RCP2.6, RCP4.5, RCP6.0 (∼0.1 K) and approximately 0.2 K for RCP8.5.
What are the ramifications of our findings for previous publications based on PH99? Those authors who claimed to have worked with PH99 in conjunction with ECS = 3 K have effectively worked with a more complex model in conjunction with ECS ≈ 4 K for the centennial time horizon. Much of the work performed based on MIND in conjunction with PH99 and the lognormal distribution for ECS by Wigley and Raper (2001) has essentially been based on a lognormal distribution shifted to larger ECS values. The 5 %, 50 %, and 95 % quantiles of the lognormal distribution by Wigley and Raper (2001) are 1.2, 2.6, and 5.8 K, respectively. When interpreting these values as PH99 values, as they have in fact been utilized in PH99 for the MIND model since Lorenz et al. (2012), in the sense of a rough estimate one could ask what the corresponding effective ECS values of a more complex model according to our Fig. 7 were. The respective values are 1.2, 3.6, and 9.0 K. From Fig. 13, which reflects IPCC AR5's synopsis of current knowledge regarding ECS (Bindoff et al., 2013), we can see that these are still in line with the range spanned by instrumental studies. Hence the results obtained by PH99 in conjunction with the distribution by Wigley and Raper (2001) are not erroneous but simply need to be reinterpreted as rather highend representatives within the collection of ranges as seen in IPCC AR5.
For future applications we can conclude that PH99 must be applied and interpreted with greater care – utilizing transformed values for ECS and TCR – than in the past, if it is not to be replaced by at least a twobox model as suggested by Geoffroy et al. (2013) and implemented in DICE (Nordhaus, 2013). Onebox models like PH99 can be crucial for modeling decisionmaking under uncertainty and anticipated future learning. As an illustration, execution of the MIND model currently demands between hours and days for 20 different values of climate sensitivity in conjunction with one learning step (Elnaz Roshan, personal communication, 2018). The execution time needed will grow exponentially with the number of learning steps and at least linearly with the number of state variables influenced by uncertainty. For endogenous learning in a recursive design, computation time scales factorially with the numerical resolution per state variable. The change from a onebox to a twobox model might hence imply an order of magnitude larger execution time (Christian Traeger, personal communication, 2018, in conjunction with Traeger, 2014). So a onebox model will remain an attractive alternative in numerical applications addressing decisionmaking under anticipated future learning. Users who would like to go that road might, however, also consider the augmented onebox model by Traeger (2014) as an alternative to PH99, employing an additional exogenous forcing of that single box to somewhat emulate two boxes.
We utilize recent data on total radiative forcing (Forster et al., 2013) from 14 stateoftheart CMIP5 atmosphere ocean general circulation models (AOGCMs) in order to test the validity of the onebox climate module by PetschelHeld et al. (1999, “PH99”) for scenarios approximately compatible with the 2^{∘} target. PH99 is currently utilized within the integrated assessment models FUND, MIND, and PAGE.
We find that when prescribing the equilibrium climate sensitivity (ECS) and transient climate response (TCR) of these AOGCMs to the emulator PH99, global mean temperature (GMT) is generically projected 0.5 K higher by PH99 than by the corresponding AOGCM. In contrast, by directly fitting PH99 to the RCP2.6 time series and validating with the RCP4.5 and RCP6.0 series, we find that PH99 can emulate AOGCMs to a degree of accuracy better than 0.1 K. Even for RCP8.5 the error is on the same order of magnitude, although somewhat larger (up to 0.2 K).
We numerically demonstrate that PH99 can be used to excellently emulate AOGCMs (accurate to within 0.1 K on average) within centennialscale integrated assessment of the 2 K target, provided its ECS and TCR are reinterpreted as effective values and mapped from original ECS and TCR values. We suggest such a mapping.
Furthermore we explain the observed discrepancies and the need to reduce PH99's ECS compared to the AOGCM's ECS as being due to the information loss produced by approximating a twoboxbased energy balance model with a oneboxbased model. The key point is that PH99 has a fundamentally different response shape to an AOGCM and hence ECS alone does not allow one to easily move between the two. The transformation we propose adjusts PH99's ECS, sacrificing agreement in the longterm response in order to gain agreement in the centennial response (which is useful given it is more often than not the timescale of interest).
In fact the slow mode of the twobox model is so slow that in a climatepolicyrelevant context it can unfold only up to a relatively small extent; hence for practical purposes the twobox model's ECS cannot fully develop. Accordingly, adjusting the ECS to lower values also proves to be compatible with reducing PH99's response time. When comparing PH99 and AOGCMs, the match is even better – a phenomenon for which the explanation is beyond the scope of this article.
Hence older work based on PH99, executed within FUND, MIND, and PAGE, may need to be reinterpreted in the sense that a response had been sampled that is higher than that of the corresponding AOGCM. This effect, in turn, proves equivalent to utilizing higher ECS values in the more complex model. Even when having dealt with distributions of ECS as for the MIND model, ECS values reinterpreted in that sense are still within the range outlined by IPCC AR5 (see Fig. 13). Accordingly, we see this reinterpretation as a mere numerical fix. In terms of the underlying physics, we stress that using ECS alone to characterize climate response on a timescale of a few hundred years is fundamentally flawed, given that ECS takes on the order of 1000 years to emerge.
For future work, we propose the following steps: (i) by comparison with more sophisticated, multibox climate modules it should be tested again whether the effect of a transient climate sensitivity (and TCR) alone could explain our observed PH99–AOGCM discrepancy; (ii) future discussions with the AOGCM community should illuminate to what extent the further explanations we suggested might also apply, thereby potentially reducing the need to correct for PH99; (iii) an AOGCM and scenario classindependent yet centennialtimescalespecific twodimensional mapping from ECS and TCR on to ECS and TCR and designed for PH99 should be derived in conjunction with twodimensional distributions inferred from observations as performed in Frame et al. (2005). The IAM community could then be offered both options for emulation: the one presented here, trained by AOGCMs, and one based on observational data and mediated by more complex SCMs.
In summary, PH99 could continue to be used as the most parsimonious emulator of AOGCMs and is especially efficient for decisionmaking under climate response uncertainty. However its calibration proves to be much more involved than previously assumed. Future users should carefully consider whether they actually want to use PH99 or whether they prefer a less parsimonious solution.
For data sets please contact the corresponding author for Forster et al. (2013).
We rearrange Eq. (1) as
TCR is defined as the temperature change in response to a 1 % yr^{−1} increase in CO_{2} concentration, starting from preindustrial conditions. Hence the concentration, expressed in units of the preindustrial concentration, reads
with γ denoting the above rate of change. As Eq. (A1) represents a linear ordinary differential equation with constant coefficients, and the initial temperature anomaly is to vanish, its solution reads
Temperature should be evaluated at t_{2} when the concentration is doubled. t_{2} is determined by $c\left({t}_{\mathrm{2}}\right)=\mathrm{2}\Rightarrow {t}_{\mathrm{2}}=\mathrm{ln}\mathrm{2}/\mathit{\gamma}$. From this and Eq. (A3) we conclude Eq. (3). (In fact we find the same result using an expression provided in Andrews and Allen (2008) when we plug in our expression for t_{2} into theirs, which is phrased in terms of ECS.)
As further validation of the trained PH99 calibrated to RCP2.6, Fig. B1 shows the respective GMT trajectories of AOGCMs for the RCP6.0 scenario contrasted with its respective PH99generated ones for which α and μ are fixed to their value as determined in step two. MTDs are shown in the third columns of Table B1. The missing models are due to either lack of temperature trajectories for AOGCM or lack of total forcing. Notice that first, second, and fourth columns are exactly the numbers related to Fig. 2. The results confirm that the climate module is so well trained in the second step that it can appropriately mimic the actual temperatures (accurate to within 0.1 K) for RCP6.0. As shown, the average value of MTD is about 0.06 K for RCP6.0.
Column 5 thereafter in Table B1 shows MTDs in the situations when PH99 is calibrated to the other RCP scenarios and is validated against the others.
We start by rewriting Eq. (15) in a way that it is most consequently decomposed into the contributions from the two modes i∈{f, s} (for “slow” and “fast” modes, respectively).
One could derive Eq. (17) from an intuitive perspective by noticing that for any of the modes i, its contribution to the temperature response would consist of an equilibrium response, delayed by τ_{i}, and a summand of exponential decay that would ensure continuity with respect to the initial condition. This very principle can be followed again for the time horizon beyond t_{1}.
However, for those readers who would like to see a more formal derivation, we provide the following ansatz: for t>t_{1}, we decompose T_{2B} into three contributions, according to the superposition principle for linear differential equations.

T_{1} is induced by a forcing k_{2}(t−t_{1}) with T_{1}(t_{1})=0. This contribution can be treated analogously to ${T}_{\mathrm{2}\mathrm{B}}(\mathrm{0}<t<{t}_{\mathrm{1}}$) when noticing the replacements k_{1}→k_{2}, $t\to t{t}_{\mathrm{1}}$. From Eq. (C1) we infer
$$\begin{array}{}\text{(C2)}& {\displaystyle}{\displaystyle}{T}_{\mathrm{1}}\left(t\ge {t}_{\mathrm{1}}\right)={\displaystyle \frac{{k}_{\mathrm{2}}}{{\mathit{\lambda}}_{\mathrm{2}\mathrm{B}}}}\sum _{i}{a}_{i}\left(t{\mathit{\tau}}_{i}+{\mathit{\tau}}_{i}{\mathrm{e}}^{\frac{\left(t{t}_{\mathrm{1}}\right)}{{\mathit{\tau}}_{i}}}\right).\end{array}$$ 
T_{2} is induced by a constant forcing k_{1}t_{1} with T_{2}(t_{1})=0. This problem has also been solved by Geoffroy et al. (2013) in terms of their Eq. (9), which we rewrite in our notation:
$$\begin{array}{}\text{(C3)}& {\displaystyle}{\displaystyle}{T}_{\mathrm{2}}\left(t\ge {t}_{\mathrm{1}}\right)={\displaystyle \frac{{k}_{\mathrm{1}}{t}_{\mathrm{1}}}{{\mathit{\lambda}}_{\mathrm{2}\mathrm{B}}}}\sum _{i}{a}_{i}\left(\mathrm{1}{\mathrm{e}}^{\frac{\left(t{t}_{\mathrm{1}}\right)}{{\mathit{\tau}}_{i}}}\right).\end{array}$$ 
T_{3} is the decaying initial condition at t=t_{1}. For reasons of continuity, this initial condition is identical to the terminal condition according to Eq. (C1). Hence,
$$\begin{array}{}\text{(C4)}& {\displaystyle}{\displaystyle}{T}_{\mathrm{3}}\left(t\ge {t}_{\mathrm{1}}\right)={\displaystyle \frac{{k}_{\mathrm{1}}}{{\mathit{\lambda}}_{\mathrm{2}\mathrm{B}}}}\sum _{i}{a}_{i}\left({t}_{\mathrm{1}}{\mathit{\tau}}_{i}+{\mathit{\tau}}_{i}{\mathrm{e}}^{\frac{{t}_{\mathrm{1}}}{{\mathit{\tau}}_{i}}}\right){\mathrm{e}}^{\frac{\left(t{t}_{\mathrm{1}}\right)}{{\mathit{\tau}}_{i}}}.\end{array}$$
When we add these three components, we receive
Allowing for the limit τ_{f}→0 and noticing that ${k}_{\mathrm{2}}=\mathit{\epsilon}{k}_{\mathrm{1}}$, we verify Eq. (17) by a summandbysummand comparison.
Allowing for ${\mathit{\tau}}_{\mathrm{f}}={\mathit{\tau}}_{\mathrm{s}}=\mathit{\theta}$ (i.e., simulating a onebox setting by a twobox approach), we obtain Eq. (18) from Eq. (C1) and Eq. (19) from Eq. (C5).
MMK performed the statistical analysis. HH provided the analytic analysis. MMK suggested and developed the alternative scheme. Both participated in the writing of the article.
The authors declare that they have no conflicts of interest.
The authors would like to thank Jochem Marotzke for drawing their attention to
the Forster et al. (2013) article, discussing these results on total forcing
and providing the relevant data. In addition, the authors would like to
thank Chao Li for supporting the data handling process and making the authors
aware of Geoffroy et al. (2013), who discuss negligible AOGCM drift. The
authors are also grateful to Elnaz Roshan for her help with the visualizations
and providing quantiles of the distribution of Wigley and Raper (2001) on ECS.
We thank Matt Fentem for proofreading the second version of our paper
from a native speaker's perspective as well as Benjamin Blanz and
Manuel Wifling for further proofreading. All remaining errors are ours. Mohammad M. Khabbazan was supported by
the Cluster of Excellence “Integrated Climate System Analysis and
Prediction” (CliSAP, DFGEXC177). Finally, the authors would like to thank the
three anonymous referees for their valuable criticism and constructive suggestions.
Edited by: Fubao Sun
Reviewed by: three anonymous referees
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 Abstract
 Introduction
 Method
 Results
 A mapping of ECS onto their PH99specific counterparts α and μ
 An analytic interpretation of the AOGCM–PH99 intercomparison
 Discussion
 Summary and conclusion
 Data availability
 Appendix A: An analytic expression of TCR in PH99
 Appendix B: Further analysis on calibration and validation
 Appendix C: Derivation of Eqs. (16)–(18)
 Author contributions
 Competing interests
 Acknowledgements
 References
 Abstract
 Introduction
 Method
 Results
 A mapping of ECS onto their PH99specific counterparts α and μ
 An analytic interpretation of the AOGCM–PH99 intercomparison
 Discussion
 Summary and conclusion
 Data availability
 Appendix A: An analytic expression of TCR in PH99
 Appendix B: Further analysis on calibration and validation
 Appendix C: Derivation of Eqs. (16)–(18)
 Author contributions
 Competing interests
 Acknowledgements
 References