The Paris Agreement has opened debate on whether limiting warming to 1.5 °C is compatible with current emission pledges and warming of about 0.9 °C from the mid-nineteenth century to the present decade. We show that limiting cumulative post-2015 CO2 emissions to about 200 GtC would limit post-2015 warming to less than 0.6 °C in 66% of Earth system model members of the CMIP5 ensemble with no mitigation of other climate drivers. We combine a simple climate–carbon-cycle model with estimated ranges for key climate system properties from the IPCC Fifth Assessment Report. Assuming emissions peak and decline to below current levels by 2030, and continue thereafter on a much steeper decline, which would be historically unprecedented but consistent with a standard ambitious mitigation scenario (RCP2.6), results in a likely range of peak warming of 1.2–2.0 °C above the mid-nineteenth century. If CO2 emissions are continuously adjusted over time to limit 2100 warming to 1.5 °C, with ambitious non-CO2 mitigation, net future cumulative CO2 emissions are unlikely to prove less than 250 GtC and unlikely greater than 540 GtC. Hence, limiting warming to 1.5 °C is not yet a geophysical impossibility, but is likely to require delivery on strengthened pledges for 2030 followed by challengingly deep and rapid mitigation. Strengthening near-term emissions reductions would hedge against a high climate response or subsequent reduction rates proving economically, technically or politically unfeasible.
The aim of Paris Agreement is ‘holding the increase in global average temperature to well below 2 °C above pre-industrial levels and pursuing efforts to limit the temperature increase to 1.5 °C’ (ref. 1). The Parties also undertook to achieve this goal by reducing net emissions ‘to achieve a balance between anthropogenic sources and removals by sinks of greenhouse gases in the second half of this century’, and hence implicitly not by geo-engineering planetary albedo. Under what conditions is this goal geophysically feasible?
Human-induced warming reached an estimated 0.93 °C (±0.13 °C; 5–95 percentile range) above mid-nineteenth-century conditions in 2015 and is currently increasing at almost 0.2 °C per decade2. Combined with the effects of El Niño and other sources of natural variability, total warming exceeded 1 °C for the first time in 2015 and again in 20163. Average temperatures for the 2010s are currently 0.87 °C above 1861–80, which would rise to 0.93 °C should they remain at 2015 levels for the remainder of the decade. With a few exceptions4,5, mitigation pathways that could achieve peak or end-of-century warming of 1.5 °C have thus far received little attention. Even the ‘Paris, increased ambition’ scenario of ref. 6 results in CO2 emissions still well above zero in 2100, and hence a low chance of limiting warming to 1.5 °C.
Long-term anthropogenic warming is determined primarily by cumulative emissions of CO2 (refs 7,8,9,10): the IPCC Fifth Assessment Report (IPCC-AR5) found that cumulative CO2 emissions from 1870 had to remain below 615 GtC for total anthropogenic warming to remain below 1.5 °C in more than 66% of members of the 5th Coupled Model Intercomparison Project (CMIP5) ensemble of Earth system models (ESMs)11 (see Fig. 1a). Accounting for the 545 GtC that had been emitted by the end of 201412, this would indicate a remaining budget from 2015 of less than seven years of current emissions, while current commitments under the Nationally Determined Contributions (NDCs) indicate 2030 emissions close to current levels13.
The scenarios and simulations on which these carbon budgets were based, however, were designed to assess futures in the absence of CO2 mitigation, not the very ambitious mitigation scenarios and correspondingly small amounts of additional warming above present that are here of interest. Furthermore, many mitigation scenarios begin reductions in 2010 and are already inconsistent with present-day emissions, complicating the comparison with pledges for 2030.
Carbon budgets and scenarios for ambitious climate goals
The black cross on Fig. 1a shows an estimate of human-induced warming, which excludes the impact of natural fluctuations such as El Niño, in 2015 (0.93 ± 0.13 °C relative to 1861–80; 5–95 percentile range) and pre-2015 cumulative carbon emissions (545 ± 75 GtC since 1870; 1 s.d.). Although both quantities are individually consistent with the CMIP5 ensemble, in the mean CMIP5 response (coloured lines) cumulative emissions do not reach 545 GtC until after 2020, by which time the CMIP5 ensemble-mean human-induced warming is over 0.3 °C warmer than the central estimate for human-induced warming to 2015. In estimating the outstanding carbon budget for 1.5 °C, this is an important discrepancy. IPCC-AR5 also calculated the percentiles of the CMIP5 distribution that exceeded given thresholds of warming relative to the average of 1986–2005 (Table 12.3 of ref. 14), adding a further 0.61 °C to express these relative to 1850–1900. However, this reference period and the GCM ensemble used in this table are not identical to the ESM ensemble used to derive estimates of the carbon budget, for which a volcano-free reference period is preferred, to focus on human-induced warming. Moreover, since the discrepancy in warming between ESMs and observations emerges only after 2000, expressing warming relative to the 1986–2005 reference period does not entirely resolve it and also does not address the small underestimation of cumulative emissions to date. Figure 1b shows an alternative analysis of the CMIP5 ensemble to assess the remaining carbon budget for an additional 0.6 °C of warming beyond the current decade, a possible interpretation of ‘pursuing efforts to limit the temperature increase to 1.5 °C’ in light of estimated human-induced warming to date. The median response of the CMIP5 models indicates allowable future cumulative emissions (threshold-exceedance budget or TEB15) of 223 GtC for a further 0.6 °C warming above the 2010–2019 average, and a 204 GtC remaining TEB from 2015 to keep warming likely below this value (meaning, by the time cumulative emissions from 2015 reach 204 GtC, 66% of CMIP5 models have warmed less than 0.6 °C above the present decade, consistent with the methodology for assessing the 2 °C carbon budget in IPCC-AR516). Given uncertainty in attributable human-induced warming to date, differences between observational products and true global surface air temperature17, and the precise interpretation of the 1.5 °C goal in the Paris Agreement (for example, the choice of pre-industrial reference period which temperatures are defined relative to18), budgets corresponding to a range of levels of future warming should also be considered—see Table 1 and the Supplementary Information.
TEBs are useful because peak CO2-induced warming is a function (shown by the grey plume in Fig. 1) of cumulative CO2 emissions and approximately independent of emission path, although threshold behaviour, such as sudden carbon release from thawing permafrost, might complicate this relationship19. This does not apply to non-CO2 forcing, which is relatively more important for ambitious mitigation scenarios. The rapid warming from the 2000s to the 2030s in CMIP5 arises partly from strong increases in net non-CO2 forcing over this period in the driving RCP scenarios, due to simulated rapid reductions in cooling aerosol forcing. It remains unclear whether this increase in non-CO2 forcing will be observed if future reductions in aerosol emissions occur because present-day effective non-CO2 forcing is still highly uncertain20. Table 2 shows budgets for thresholds of future warming in the CMIP5 ensemble under an RCP2.6 scenario, a stabilization scenario in which non-CO2 forcing across the rest of the century remains closer to the 2010–2019 average than in the RCP8.5 scenario. This should allow more CO2-induced warming for the same total. However, due to the smaller subset of available models in the RCP2.6 scenario, it is not possible to identify any robust shifts in the percentiles of the TEB distribution from the RCP8.5 scenario.
In many current ambitious mitigation scenarios (for example, RCP2.6 (ref. 21), dark blue lines in Fig. 2), substantial CO2 emission reductions begin in 2010, such that both emissions and forcing are already inconsistent with observed climate state and emission inventories to date. The thick dark green lines in Fig. 2 show an amended version of RCP2.6 that is more consistent with current emissions and estimated present-day climate forcing. This scenario, hereafter referred to as RCP2.6-2017, assumes the same proportional rates of change of both CO2 and other anthropogenic forcing components as in the standard RCP2.6 scenario from 2010, but with the mitigation start date delayed by seven years to 2017 (following the RCP8.5 scenario22 between 2010–2017). This is more representative of a possible mitigation pathway from today: many nations are already planning on policy action to reduce emissions over the 2015–2020 period, in anticipation of achieving their NDC commitments in the future. Total anthropogenic radiative forcing peaks in 2050 (at 3.41 W m−2) in RCP2.6-2017, as opposed to in 2043 (at 3.00 W m−2) under RCP2.6. The grey lines represent emissions pathways from the IPCC 430–480 ppm scenario category23,24 but with proportional decreases in radiative forcing also delayed by seven years to start in 2017.
Figure 2c shows the implications of these scenarios for future warming, evaluated with a simple climate model that reproduces the response of the CMIP5 models to radiative forcing under ambitious mitigation scenarios (Supplementary Methods). Like other simple climate models, this lacks an explicit physical link between oceanic heat and carbon uptake. It allows a global feedback between temperature and carbon uptake from the atmosphere, but no direct link with net deforestation. It also treats all forcing agents equally, in the sense that a single set of climate response parameters is used in for all forcing components, despite some evidence of component-specific responses25,26. We do not, however, attempt to calibrate the model directly against observations, using it instead to explore the implications of ranges of uncertainty in emissions12, and forcing and response derived directly from the IPCC-AR5, which are derived from multiple lines of evidence and, importantly, do not depend directly on the anomalously cool temperatures observed around 2010. Non-CO2 forcing and the transient climate response (TCR) co-vary within AR5 ranges to consistently reproduce present-day externally forced warming (Methods), and as in Fig. 1b, we quote uncertainties in future temperatures relative to this level.
The limits of the green plume in Fig. 2c show peak warming under the RCP2.6-2017 scenario is likely between 1.24–2.03 °C (1.12–1.99 °C for 2100 warming) given a 2015 externally forced warming of 0.92 °C. The IPCC-AR5 did not propose a ‘best-estimate’ value of the TCR, but using a central value of 1.6 ° C (the median of a log-normal distribution consistent with IPCC-AR5 likely ranges, the typical shape of most reported TCR distributions in ref. 16), RCP2.6-2017 gives a median peak warming of 1.55 °C above pre-industrial (1861–1880 mean) and 1.47 °C in 2100, approximately consistent with as likely as not (50% probability of) warming below 1.5 °C in 2100.
The shaded green bands show the central four probability sextiles of the distribution of responses to RCP2.6-2017 for a log-normal distribution for the TCR (see Supplementary Methods for alternative distributions). Under RCP2.6-2017, peak warming is likely below 2 °C, and well below 2 °C by the end of the century. However, such a scenario cannot exclude a non-negligible probability of peak warming significantly in excess of 2 °C, particularly given the possibility of nonlinear climate feedbacks, for which there is some evidence in more complex GCMs27.
Emissions in Fig. 2a are diagnosed from radiative forcing in Fig. 2b using a version of the IPCC-AR5 carbon-cycle impulse-response function28, with a minimal modification to account for the change in the impulse response between pre-industrial and twenty-first century conditions due to atmospheric CO2 and temperature-induced feedbacks on carbon uptake, as observed in Earth system models29. This simple model reproduces the response of ESMs to ambitious mitigation scenarios (Supplementary Information) including, with best-estimate parameters, near-constant temperatures following a cessation of CO2 emissions. The temperature response of the UVic Earth System Climate Model (UVic ESCM)30,31,32 driven by the diagnosed RCP2.6-2017 emissions scenario and non-CO2 forcing is shown in Fig. 2c (orange line), and is emulated well by the simple carbon-cycle–climate model with equivalent climate response parameters (thin green line, see Methods). Carbon-cycle feedback uncertainties (see Methods) have only limited scope to influence the allowable emissions under scenarios in which concentrations and temperatures peak at a relatively low level.
Since RCP2.6-2017 represents a scenario with ambitious CO2 and non-CO2 mitigation, it currently lies near the lower limit of 2100 anthropogenic forcing available in the literature4,15, as shown by the grey lines in Fig. 2. We have not assumed any additional non-CO2 mitigation beyond RCP2.6, but uncertainties in mitigation technologies and demand reduction measures decades into the future mean that non-CO2 mitigation may yet play a larger role than indicated here.
Adaptive mitigation and carbon budgets
The Paris Agreement establishes a regime of continuously updated commitments informed by on-going scientific and policy developments and the overarching temperature and emission reduction goal. Therefore, we re-estimate carbon budgets, accounting for the present-day climate state and current uncertainty in the climate response, and assuming mitigation efforts are perfectly adapted over time to achieve a warming in 2100 of 1.5 °C for a range of possible realizations of the climate response2,33. Figure 3a shows a distribution of future temperature trajectories, for different climate responses, that are all consistent with observed attributable warming in 2015 and a smooth transition to 1.5 °C in 2100. The limits of the green plume show temperature trajectories associated with IPCC-AR5 likely ranges for the TCR and equilibrium climate sensitivity (ECS), with bands delineating the central four sextiles of the distribution. These temperatures initially follow the responses to the RCP2.6-2017 scenario (the green plumes in Fig. 2c) but are then smoothly interpolated over the coming century to the trajectory given by the best-estimate response (see Supplementary Methods). This provides a simple representation of goal-consistent pathways for a range of possible climate responses34. In contrast to a scenario-driven, forward-modelling approach (for example, ref. 6 and Fig. 2), the temperature trajectories in Fig. 3a define the scenario, from which corresponding CO2 emission pathways (Fig. 3b) are derived, similar to the temperature-tracking approach used by ref. 10. This implicitly assumes that information on the emerging climate response is available and acted upon instantaneously. In reality, both resolving the response and adapting policies will be subject to delay, although the impact can be reduced if policies respond to both observed and decadal predictions of human-induced warming, which are much better constrained than long-term projections of, for example, ECS.
Green bands in Fig. 3b show emissions compatible with the goal-consistent temperature trajectories and climate responses of Fig. 3a, computed using the modified IPCC-AR5 impulse-response function with carbon-cycle feedback uncertainty assumed positively correlated with the TCR (see Methods). Such an assumption may be pessimistic, but uncertainty in these feedbacks may also be underestimated in CMIP5—the impact of thawing permafrost, for example, is generally not represented.
Figure 3c shows cumulative emissions (net carbon budgets) consistent with limiting warming to 1.5 °C warming in 2100 under the climate response uncertainty distribution and these goal-consistent pathways. The median (‘as likely as not’) case corresponds to a cumulative budget of 370 GtC (1,400 GtCO2—all carbon budgets given to two significant figures) from 2015 to 2100, including ∼10 GtC of net negative emissions in the final decades. Compared to this, higher cumulative CO2 emissions budgets are associated with lower climate responses and vice versa (hence the ordering of the coloured bands in 3a, b). Assuming completely successful adaptive CO2 mitigation to achieve a warming of 1.5 °C in 2100 (allowing for mid-century temperature overshoots, assuming non-CO2 forcing following RCP2.6-2017, and imposing no restrictions on the rate of net carbon dioxide removal), the cumulative carbon budget from 2015 to 2100 is unlikely (<33% probability) to be less than 250 GtC (920 GtCO2), about 25% higher than the 204 GtC TEB for the 66th percentile of the CMIP5 distribution for 0.6 °C warming above the 2010–2019 average in the RCP8.5 scenario (Table 1). Conversely, cumulative future emissions from 2015 compatible with a warming of 1.5 °C in 2100 are unlikely to be greater than 540 GtC (the top of the 50–67% band in Fig. 3c) even under such an idealized perfectly responsive mitigation policy. The relationship between CO2-induced future warming compatible with the cumulative emissions shown in Fig. 3c is also broadly consistent with that expected from the IPCC-AR5 likely range of the transient climate response to cumulative carbon emissions, or TCRE (see Supplementary Fig. 4), which, when combined with varying contributions from non-CO2 forcing, informs the all-forcing budgets quoted here.
The small difference that varying TCR makes to warming between 2015 and 2030 (Fig. 3a) highlights both the importance of continuous quantifications of human-induced warming in any stocktake of progress to climate stabilization, and the need for a precautionary approach even under an adaptive mitigation regime34. Although more progress has been made on constraining TCR than ECS, uncertainties are unlikely to be resolved rapidly. Allowing emissions to rise in the hope of a low climate response risks infeasible subsequent reductions should that hope prove ill founded. Conversely, the risk of ‘over-ambitious’ mitigation is low: the darkest green plume in Fig. 3b shows that the difference between a TCR of 1.3 °C and 1 °C has a substantial impact on the allowable carbon budget for 1.5 °C, but the probability of a TCR in that range is already assessed to be low. Since IPCC-AR5 a number of studies have suggested an increase in the lower bound on the TCR towards 1.3 °C (for example, ref. 25), whilst others indirectly support a 1.0 °C lower bound through upward revisions of radiative forcing35,36. Using a TCR likely range of 1.3–2.5 °C and an ECS likely range of 2.0–4.5 °C, the remaining budget for a 1.5 °C warming would be unlikely greater than 400 GtC and unlikely less than 220 GtC (see Supplementary Fig. 18).
Discussion and implications for the ‘emissions gap’
Much recent policy discussion has centred on the ‘emissions gap’ between the NDCs emerging from the Paris Agreement and emission scenarios consistent with 1.5 °C and 2 °C (refs 13,37). The extent of any ‘gap’ depends on the uncertain climate response; the definition of the Paris Agreement goals; the interpretation, delivery and/or revision of the NDCs, and in particular the technical and/or socio-economic feasibility of subsequent emissions reductions.
Considerable uncertainties are associated with the NDCs themselves13,38. Modelling indicates that the NDCs could be consistent with global fossil-fuel and land-use change CO2 emissions in 2030 only slightly above 2015 values6,13 (lower limit of the brown bar in Figs 2a and 3b), close to the RCP2.6-2017 scenario. This would imply that if NDCs are fully implemented (including all conditional elements), with plausible values for Chinese emissions in 2030, and RCP2.6-2017 mitigation rates are maintained after 2030, then the NDCs would still remain inconsistent with future scenarios projected to correspond to a peak warming likely below 2 °C and a 2100 warming as likely as not below 1.5 °C. However, a modest strengthening of the pledges corresponding to an approximate 10% reduction in proposed 2030 emissions could achieve consistency with such scenarios. Hence, the NDCs as they stand do not necessarily imply a commitment to a fundamentally different approach, such as resorting to solar radiation management (SRM), to achieve a warming of 1.5 °C in 2100, if the climate response is close to or less than our central estimate and if emissions can be rapidly reduced after 2030. The RCP2.6-2017 scenario involves a smooth transition to slightly negative net CO2 emissions after 2080, which may require challenging rates of deployment of CO2 removal (CDR). Figure 3b shows that returning warming to 1.5 °C in 2100 under a higher climate response potentially requires very substantial rates of CDR, which may not be technically feasible or socio-economically plausible.
An additional caveat to assessments of a 2030 ‘emissions gap’ is that most NDCs are formulated in terms of CO2-equivalent (CO2e) emissions, a composite metric of warming impact of different gases based on Global Warming Potentials (GWPs) from various IPCC reports. It is therefore impossible to assess precisely the 2030 emissions of CO2 itself that are compatible with these pledges without additional assumptions, because CO2e pledges could be attained through varying combinations of long-lived and short-lived forcer mitigation39,40,41. Separate reporting of long-lived and short-lived greenhouse gases in national pledges would help clarify their long-term implications41,42.
Aside from scientific uncertainties and the interpretation of the NDCs, a crucial issue is the feasibility of achieving sufficient rates and levels of decarbonization required by these ambitious mitigation scenarios. Rapid decarbonization relies on societies being able to swiftly replace existing capital with new investments at massive scales. Inertia within the economic system is an important constraint on realizable mitigation pathways43. RCP2.6-like scenarios imply decarbonization at over 0.3 GtC yr−1 yr−1 in the 2030s and 2040s—or 4–6% per year sustained for multiple decades. If applied to gross CO2 emissions, such rates of reduction have historically been observed globally only for short periods, such as in the 1930s Great Recession and the Second World War, and regionally in the collapse of the former Soviet Union44. Sustained decarbonization at these rates, and the associated capital displacement (run-down and replacement of fossil-fuel infrastructure), would be historically unprecedented, although the parallel between intentional policy-driven decarbonization in the future and historical rates remains unclear.
Longer-term deep decarbonization also relies on many energy system innovations, including development and deployment on an unprecedented scale of renewable energy as well as, as yet undemonstrated, amounts of carbon capture and storage and CDR45. Given possible limits to rates of decarbonization, near-term mitigation ambition and delays in mitigation start dates may strongly influence peak and 2100 warming. The purple dashed lines in Fig. 2 illustrate this point with a simple scenario in which CO2 emissions reduce linearly (at 0.17 GtC yr−1 yr−1, about 0.6 GtCO2 yr−1 yr−1) from 2020 to achieve approximately the same warming as RCP2.6-2017 in 2100. Under this scenario, maximum rates of decarbonization are much lower than in RCP2.6-2017, in both absolute and percentage terms, demonstrating the potential advantage of more ambitious near-term mitigation given the risk that subsequent RCP2.6-like rates of decarbonization may be unachievable.
More ambitious near-term mitigation may be more feasible than previously thought. The rapid growth of global emissions from 2000 to 2013 was dominated by increases in Chinese emissions46, driven, at least in part, by unprecedented levels of debt-fuelled investment in carbon-intensive industries and capital stock47. Sustaining such expansion is likely to be neither necessary (the infrastructure is now built) nor feasible (the debt levels are likely to prove unsustainable)47. For these reasons, the possibility that both Chinese and global emissions are at or near their peak46,48, and could reduce from 2020, seems less far-fetched than it once did. This could allow for the required strengthening of the NDCs in the 2020 review towards an RCP2.6-2017 trajectory or beyond, more readily consistent with a 1.5 °C goal.
Regular review of commitments is built in to the Paris Agreement. This stocktake should be extended to relate commitments directly to the long-term temperature goal. As human-induced warming progresses, the question must be asked: ‘Are we on track to reduce net emissions to zero to stabilize climate well below 2 °C as agreed in Paris’? Regular updates of human-induced warming based on a standard and transparent methodology would allow countries to adapt commitments to the emerging climate response. Our analysis suggests that ‘pursuing efforts to limit the temperature increase to 1.5 °C’ is not chasing a geophysical impossibility, but is likely to require a significant strengthening of the NDCs at the first opportunity in 2020 to hedge against the risks of a higher-than-expected climate response and/or economic, technical or political impediments to sustained reductions at historically unprecedented34 rates after 2030.
We refer to ‘climate response’ as a specified combination of the TCR and ECS throughout this paper. Our median estimate climate response (TCR = 1.6 °C, ECS = 2.6 °C) is defined as the median of log-normal distributions consistent with IPCC-AR5 likely bounds on the TCR and ECS (TCR: 1.0–2.5 °C; ECS: 1.5–4.5 °C). From this, the likely above/below values are found from the 33rd and 67th percentiles of the distribution (TCR: 1.3–1.9 °C; ECS: 2.0–3.3 °C). The median TCR of this log-normal distribution is significantly lower than in the IPCC-AR5 ESM ensemble but is more consistent with observed warming to date than many ensemble members (see Supplementary Methods), indicative of the multiple lines of evidence used to derive the IPCC-AR5 uncertainty ranges. Although IPCC-AR5 did not explicitly support a specific distribution, there is some theoretical justification50 for a log-normal distribution for a scaling parameter like the TCR. Reconciling the IPCC-AR5 best estimate of attributable warming trend over 1951–2010 with the best-estimate effective radiative forcing requires a best-estimate TCR near to 1.6 °C under the simple climate model used here, consistent with a log-normal distribution. As a sensitivity study, we also assume a Gaussian distribution for the TCR (see Supplementary Methods) that raises the 2015 attributable warming to 1.0 °C but only marginally affects the remaining carbon budget for a 1.5 °C warming above pre-industrial (the likely below budget is reduced to 240 GtC).
The ECS distribution used here is derived directly from IPCC-AR5 likely bounds that drew on multiple lines of evidence, so our conclusions are not directly affected by uncertainties in the efficacy of ocean heat uptake that affect purely observational constraints on ECS51. We are not here arguing for the revision of uncertainty estimates on any climate response parameters, although any such revision would of course affect our conclusions. The implications of an increased lower bound on the climate response are shown in Supplementary Fig. 18.
Reproducing present-day temperatures with differing values for both the TCR and ECS requires these parameters to co-vary with present-day net anthropogenic radiative forcing52. In the best-estimate forcing case (Fig. 2b), past and future effective radiative forcing components are individually scaled (multiplicatively) to match the respective best-estimate values for each component in 2011 as given in IPCC-AR525. Figures 2 and 3 scale past and future anthropogenic aerosol effective radiative forcing (the most uncertain forcing component28), along with accounting for combined uncertainty in the non-CO2 effective radiative forcing components that were assessed to have Gaussian-distributed uncertainty in IPCC-AR5 (draws from this distribution are anti-correlated with TCR). The aerosol radiative forcing scaling factor is chosen to give externally forced warming above 1861–1880 equal to that under the median climate response (that is, 0.92 °C in 2015) for all draws from the climate response distribution. In all cases shown the scaled 2011 aerosol forcing is within IPCC-AR5 assessed uncertainty bounds. A summary of climate system properties used is given in Supplementary Table 1: in only one case (the TCRE value implied by the lowest, 17th, percentile) are these outside the AR5 ‘likely’ ranges, and this parameter combination is used only in the figures, not our headline conclusions.
Temperature anomalies are computed using a two-timescale impulse-response model from refs 28,29, in which surface temperatures adjust to an imposed radiative forcing with a fast and slow timescale characterizing the uptake of heat into the upper and deep ocean (set at 8.4 and 409.5 years, respectively, as in ref. 28). The lower limit of the TCR likely range requires a total anthropogenic forcing of 3.54 W m−2 in 2011, slightly greater than the upper bound of the IPCC-AR5 confidence interval (3.33 W m−2). Natural forcing is taken as given at http://www.pik-potsdam.de/∼mmalte/rcps and is smoothed with a 10-year standard deviation Gaussian filter beyond 2015 in all scenarios.
In constructing temperature trajectories in Fig. 3a, a smooth cosine interpolation of the CO2-induced warming is applied over the period 2017 to 2117 between the response for a specific climate response parameter set to RCP2.6-2017 and the total warming under the RCP2.6-2017 median climate response (which meets the goal of 1.5 °C in 2100). Non-CO2 warming remains as originally simulated under the climate response parameter set for RCP2.6-2017, and only CO2-induced warming is adapted to force the total warming to asymptote towards the median response of RCP2.6-2017, corresponding to a scenario in which only CO2 policy responds to the emerging signal.
CO2 emissions in Figs 2a and 3b are derived using the simple carbon-cycle impulse-response formulation in ref. 28, modified to make airborne fraction a linear function of both warming and cumulative carbon uptake by terrestrial and ocean sinks29. Emissions in all figures are smoothed with a Gaussian filter with a standard deviation of two years: note that our use of an acausal filter implies that emissions are continuously adjusted to projected human-induced warming over this timescale in addition to warming to date. Cumulative emissions (Fig. 3c) are more robust than emission rates in any given year, since rates depend on the method used to construct these goal-consistent pathways.
The strength of carbon-cycle feedbacks (a single scaling factor applied to default rT and rC coefficients in ref. 29) varies from 0 to 2, consistent with the CMIP5 RCP2.6 ensemble (Supplementary Information). We assume that this scaling factor range corresponds to the 5th–95th percentiles of a Gaussian distribution. In Fig. 3, draws from this carbon-cycle feedback scaling factor distribution are taken at an equal percentile to that from the TCR distribution. This correlation between the TCR and carbon-cycle feedback distribution is chosen to maximize the range of carbon budgets calculated from Fig. 3. For each carbon-cycle feedback strength, total airborne fraction is adjusted (via the r0 parameter in ref. 29) to reproduce observed CO2 emissions in 2014, and leads to a range of historical cumulative CO2 emissions of 467–598 GtC (17th–83rd percentile of distribution), with a median estimate of 542 GtC, under carbon-cycle-only uncertainty.
Figures 2c and 3a show a version of the simple carbon-cycle–climate model (thin green lines) with thermal climate response parameters as represented in the UVic Earth System Climate Model (version 2.9; TCR = 1.9 °C and ECS = 3.5 °C)31,32 and default carbon-cycle parameters given in ref. 29. These parameters achieve a good emulation of the UVic ESCM response when driven with the RCP4.5 scenario (see Supplementary Methods). In Fig. 2c, UVic ESCM and the UVic ESCM-emulation simple carbon-cycle–climate model version are driven by RCP2.6-2017 emissions, diagnosed from the simple climate–carbon-cycle model using the median climate response and carbon-cycle parameters (dark green line in Fig. 2a) and RCP2.6-2017 non-CO2 radiative forcing scaled as discussed previously, for a 1.9 °C TCR. In Fig. 3a, UVic ESCM and the UVic ESCM-emulation simple carbon-cycle–climate model version are driven by diagnosed emissions corresponding to an interpolated temperature pathway at a 1.9 °C TCR, consistent with the method described previously.
We add an estimate of the 2030 land-use emissions in RCP2.6-2017 (2023 in RCP2.6), as derived from the MAGICC model53 (http://www.pik-potsdam.de/∼mmalte/rcps), to the fossil-fuel and industry emissions consistent with the NDCs from ref. 12 for the brown bars in Figs 2 and 3.
In analysis of the CMIP5 ensemble budgets given in Tables 1 and 2, budgets are calculated in an identical fashion to ref. 54 (both in terms of models and initial condition ensemble members used). Budgets are TEBs and are derived from percentiles of the distribution of decadal means of CMIP5 RCP8.5 integrations, linearly interpolating between adjacent rank-ordered ensemble members. In Table 2, where insufficient models cross a particular future warming threshold to calculate a particular percentile of the total model distribution at that threshold, no value is reported. For the grey (1% yr−1 CO2 increase) plume in Fig. 1, cumulative emissions and temperatures are expressed from the beginning of the increase (Fig. 1a) and relative to a ten-year period centred around the year in which concentrations reach the 2015 value of 398 ppm (Fig. 1b). Scenarios that peak and decline emissions were excluded from the red plume in Fig. 1b.
Code will be available on request to the corresponding author.
RCP forcing data used in this study are available at http://www.pik-potsdam.de/∼mmalte/rcps.
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The authors would like to thank E. Hawkins, R. Pierrehumbert, G. Peters, R. Knutti, D. van Vuuren, K. Riahi and E. Kriegler for useful discussions and/or comments on an earlier draft. R.J.M. and P.F. acknowledge support from the Natural Environment Research Council project NE/P014844/1; R.J.M. and M.R.A. from the Oxford Martin Net Zero Carbon Investment Initiative (co-I Cameron Hepburn); M.R.A. from the Oxford Martin Programme on Resource Stewardship; and J.S.F. and R.B.S. from the Research Council of Norway through projects 235548 and 261728. H.D.M. acknowledges support from the Natural Sciences and Engineering Research Council of Canada. D.J.F. acknowledges support from the Deep South National Science Challenge and an internal grant from Victoria University of Wellington.