Observations show that Arctic-average surface temperature increased from 1900 to 1940, decreased from 1940 to 1970 and increased from 1970 to present. Here, using new observational data and improved climate models employing observed natural and anthropogenic forcings, we demonstrate that contributions from greenhouse gas and aerosol emissions, along with explosive volcanic eruptions, explain most of this observed variation in Arctic surface temperature since 1900. In addition, climate model simulations without natural and anthropogenic forcings indicate very low probabilities that the observed trends in each of these periods were due to internal climate variability alone. Arctic climate change has important environmental and economic impacts and these results improve our understanding of past Arctic climate change and our confidence in future projections.
Previous studies generally suggest that while the long-term Arctic warming1,2,3 is attributable to increasing greenhouse gas emissions4,5,6,7 the observed multi-decadal variation is primarily associated with internal climate variability4,5,8,9,10. This observed multi-decadal variation was not captured by previous generation climate models4,5,6,7. Early-20th-century warming is also seen in global-average surface temperature which previous single-model simulations indicate could be explained by some combination of human-induced radiative forcing and an unusually large realization of multi-decadal variability11.
Here, we compare Arctic-average (60°N–90°N) annual-average surface temperature from 1900 to 2005 from the HadCRUT412 observational dataset to results from multiple climate models sampled only at locations where corresponding observations exist. Suitable climate simulations with individual forcings extending past 2005 are available from only a few models; hence our period of analysis ends in 2005. Multi-model simulations were obtained from the Coupled Model Intercomparison Project Phase 5 (CMIP5) archive. Three sets of simulations were available from 18 models. The first set of simulations (ALL) is forced by historical anthropogenic increases in greenhouses gases, changes in aerosol and aerosol precursor emissions, anthropogenic ozone changes, changes in land cover and natural forcing. The second set (GHG) is forced by historical increases in anthropogenic greenhouse gases, including anthropogenic ozone forcing in five models. The third set (NAT) is forced only by the historical natural forcing representing solar variability and volcanic aerosol emissions. We estimate the response to anthropogenic forcings other than greenhouse gases (OTH) by subtracting the simulated temperature anomalies in the GHG and NAT simulations from the temperature anomalies in the ALL simulations, based on the assumption of linearly additive responses to the external forcings.
We also employ additional simulations available from one of the CMIP5 models (CanESM2); these additional simulations allow us to separate the responses to changes in aerosols (combined sulphate aerosol, organic carbon and black carbon; AER), black carbon aerosol (BC), land use (LU), solar irradiance (SL), ozone (combined tropospheric and stratospheric ozone; OZ), stratospheric ozone (SOZ) and methane (CH4). All these responses were obtained directly (i.e., calculated from simulations in which only one particular forcing is applied), except for the black carbon and methane responses which were estimated from the difference between the ALL forcing simulations as above and a corresponding ALL simulation with black carbon aerosol or methane concentrations fixed at 1850 values.
The CMIP5 models used in this study are HadGEM2-ES (4,N,Y,B), IPSL-CM5A-LR (3,N,Y,B), MIROC-ESM (3,Y,Y,B), CanESM2 (5,N,Y,B), CSIRO-Mk3-6-0 (5,N,Y,B), MIROC-ESM-CHEM (1,Y,Y,B), NorESM1-M (1,Y,Y), CNRM-CM5 (6,N,Y), GFDL-CM3 (3,Y,Y), CESM1-CAM5-1-FV2 (2,N,Y), CCSM4 (3,N,N), FGOALS-g2 (1,N,Y), GISS-E2-R (5,N,Y,W), GISS-E2-H (5,N,Y,W), GFDL-ESM2M (1,N,N,W), bcc-csm1-1 (1,N,N,W), MRI-CGCM3 (1,Y,Y,W) and BNU-ESM (1,N,N,W). Indicated in parentheses are the number of simulations, whether time-varying ozone is included in the GHG simulations (Y for yes and N for no), whether the indirect aerosol effect is included (i.e. if Y then the first and in some cases, second indirect effect is included) and whether the model is a member of the BEST6 (B) or WRST6 (W) ensemble as defined below. The additional sets of CanESM2 simulations each contain five simulations.
Observed interannual to multidecadal variability (i.e. with periods from 2 to 50 years) in Arctic-average surface temperature12,13 is generally within the 5–95% range found in the ALL simulations with natural and anthropogenic forcings (Figure 1a). The evidence, therefore, indicates that the current generation of climate models reproduces the observed level of interannual to multidecadal variability in Arctic surface temperature. Further, at periods of around 50 years, the variability in the ALL simulations is more than twice that in the control simulations (CON) run without natural and anthropogenic forcings (Figure 1b). Here the control power spectral densities are computed using 92 available 106-year long independent segments (i.e. corresponding to the 106-year record from 1900–2005) from 17 of the above climate models with available control simulations (CESM1-CAM5-1-FV2 does not have an available control simulation) and where simulated temperatures are used only where corresponding observations exist.
Figure 2 (top panel) shows observed early-20th-century warming, middle-20th-century cooling and late-20th-century warming. To quantify this behaviour, trends were estimated for the 1900–1939, 1939–1970 and 1970–2005 periods. These trends were obtained from piecewise linear approximations over the period from 1900–2005; with the separation years of 1939 and 1970 having been found to be optimal (see Methods). Figure 2 (top panel) also compares the observed Arctic-average annual-average surface temperature anomalies with those averaged over the six sets of simulations whose piecewise linear approximations in their ALL simulations are closest, in the least squares sense, to the observed piecewise linear approximation (BEST6; see Methods). It should be noted that while the observed variability is similar to variability simulated by the individual models it is larger than the variability in the BEST6 ensemble average owing to the smoothing effect of ensemble averaging. The BEST6 ensemble reproduces the observed multi-decadal variation in Arctic-average surface temperature, with early-20th-century warming, middle-20th-century cooling and late-20th-century warming. In quantitative terms, the linear correlation between the observed and the BEST6-average time series of Arctic surface temperature is 0.65. Here we note that the BEST6 Arctic surface temperature evolution appears to combine impacts from GHG, NAT and OTH forcings (Figure 2, bottom panels).
The six sets of simulations whose piecewise linear approximations are furthest from the observed piecewise linear approximation (WRST6; see Methods) do not capture the observed multi-decadal variation in Arctic surface temperature, particularly the middle-20th-century cooling. Here the linear correlation between the observed and the WRST6-average time series of Arctic-average surface temperature is 0.48. All of the BEST6 models include some representation of the indirect aerosol effect while half of the WRST6 models do not. This suggests that this effect may be important to capturing the observed multi-decadal variation in Arctic-average surface temperature.
Figure 3 shows observed and simulated trends in Arctic-average surface temperature over the early, middle and late periods of the 1900–2005 temperature record (individual observed and model trends are shown in Supplementary Tables S1–S3 online). In the early-20th-century warming period (1900–1939) the observed trend is consistent (it is within the 95% confidence interval) with the trends in the BEST6 ensemble, with the latter clearly due to NAT warming and to a lesser extent to OTH warming. Some of the observed warming during this period may also be associated with part of the rapid rise in black carbon aerosol emissions in the late-19th-century and early-20th-century14, however such a warming impact is not seen in CanESM2 BC simulations. CanESM2 includes representations of the direct and semi-direct effects of black carbon aerosol on climate from scattering and absorption of radiation in the atmosphere. However, the effects of black carbon aerosol on snow and ice albedos, internal mixing of black carbon aerosol with other aerosols and indirect effects are not included and emissions may be underestimated. This leads to a positive radiative forcing in CanESM2 and in many other models, that is likely too low compared to observation-based estimates15. Finally, while the early-20th-century warming in the BEST6 ensemble is consistent with the observed warming, the mean is about 40% less than observed. The WRST6 ensemble does not show a significant average trend in the early-century period, nor does it show a significant GHG, NAT or OTH response.
In the middle-20th-century cooling period (1939–1970) the observed trend is also consistent with the BEST6 ensemble, although the BEST6-average cooling is about 30% less than observed. In the BEST6 ensemble, significant cooling impacts from NAT and OTH forcing changes overwhelm a significant GHG warming impact. CanESM2, a member of the BEST6 ensemble, captures the middle-20th-century cooling (see Supplementary Table S2 online) and Figure 3 suggests that aerosol (AER) changes are mainly responsible for the middle-20th-century cooling in CanESM2. An anthropogenic aerosol contribution to middle-20th-century cooling was previously inferred using GHG simulations from earlier generation climate models, none of which simulated middle-20th-century cooling, together with an empirical fit to global temperatures and hemispheric temperature gradient7. However, our results are the first direct confirmation of this impact. The WRST6 ensemble does not show a significant middle-20th-century cooling trend, nor does it capture any significant NAT or OTH cooling impacts.
In the late-20th-century warming period (1970–2005) the observed trend is consistent with the BEST6 ensemble with the BEST6 trends dominated by GHG warming, as is also true of the WRST6 ensemble. In contrast to an earlier study7 using past generation climate models together with an empirical fit to global temperatures we find no evidence in the CMIP5 multi-model ensemble that changes in aerosols since the 1970s (here part of OTH) have contributed to recent Arctic warming.
As for trends over the full period from 1900–2005 (see Supplementary Figure S1 online) we note that observed Arctic warming during this period is highly consistent with the BEST6 ensemble, reflecting GHG warming partially offset by OTH cooling in the BEST6 ensemble and more specifically AER cooling in the CanESM2 ensemble. We also note that long-term changes in anthropogenic ozone has a significant warming impact in the CanESM2 ensemble. The anthropogenic ozone warming impact of about 0.03°C per decade simulated in CanESM2 is consistent with that in the NASA Goddard Institute for Space Studies (GISS) chemistry model16. We find that methane caused a warming impact of about 0.04°C per decade; while we find no significant impact of changes in black carbon aerosol, land use, solar or stratospheric ozone on Arctic-average surface temperature.
Our results suggest that reproducing the observed multi-decadal variation in Arctic surface temperature requires a strong middle-20th-century cooling impact from anthropogenic aerosols. Figure 4a compares the observed sulphate aerosol (SO4) deposition over Greenland derived from ice core records17 with that simulated by three of the BEST6 models (CanESM2, CSIRO-Mk3-6-0 and MIROC-ESM) and three of the WRST6 models (MRI-CGCM3, GISS-E2-R and BNU-ESM), these being the models with available wet and dry SO4 deposition rates. These BEST6 models and CanESM2 in particular, reproduce the change in SO4 deposition whereas the WSRT6 models either grossly underestimate the change (MRI-CGCM3 and BNU-ESM) or overestimate the change (GISS-E2-R), this despite the fact that the same SO2 emissions should have been prescribed in all the models. The fact that the GISS-E2-R model shows too much deposition suggests SO4 removal processes in this model that are too efficient, leaving, as we shall see, too little SO4 in the atmosphere to produce middle-20th-century cooling. Disparities such as these between climate model simulations are the consequence of differing treatments of sulphate aerosol and cloud physical and chemical processing18.
Figure 4b compares the observed climatological monthly variation (1980–2005) in the surface concentration of sulphate aerosol for Alert (83°N, 63°W)19 with that simulated by one of the BEST6 models (CanESM2), two of the WRST6 models (GISS-E2-R and GFDL-ESM2M) and one of the in-between models (GFDL-CM3), these being the models with available SO4 surface concentrations at this time. CanESM2 closely reproduces the monthly variation in SO4 surface concentration whereas the WRST6 models do not. Figure 4c similarly shows that the WRST6 models have much less total SO4 burden in the atmosphere compared to CanESM2; noting that observed values of total SO4 burden are unavailable. As inferred earlier the GISS-E2-R model underestimates the amount of the SO4 in the atmosphere during this period. These results suggest that the BEST6 models mostly reproduce the observed multi-decadal variation of Arctic surface temperature because they reasonably accurately deposit, retain and respond to sulphate aerosols transported into the Arctic from their Northern midlatitude source regions.
Role of natural climate variability
We have shown that most but not all of the multi-decadal variation in Arctic surface temperature is due to the responses to external forcings. We now consider the role of natural climate variability. Using an established multivariate statistical technique20,21 (see Methods) we estimate the natural signals in Arctic-average monthly-average surface temperature associated with dynamically-induced atmospheric variability, the El Niño-Southern Oscillation (ENSO) and major explosive volcanic eruptions in the HadCRUT4 dataset and in the ALL simulations. The observed signals of dynamically-induced atmospheric variability and explosive volcanic eruptions are significant and together explain 30% of the standard deviation of Arctic-average monthly-average surface temperature (see Supplementary Table S4 online). Importantly, we note a warming impact in the early-20th-century associated with the eruption of Santa Maria in 1902 and a cooling impact in the middle-20th-century associated with the eruption on Agung in 1963 (see Supplementary Figure S2 online). The simulated signals of dynamically-induced atmospheric variability and explosive volcanic eruptions are also generally significant and on average explain about 24% of the standard deviation of simulated Arctic-average monthly-average surface temperature (see Supplementary Table S4 online). The simulated volcanic signals contribute, as observed, to the early-period warming and middle-period cooling of Arctic-average surface temperature (see Supplementary Figure S2 online).
Based on earlier results regarding variations in Arctic temperature connected with heat transported from the Atlantic Ocean into Arctic Ocean9 we explore the connection to the Atlantic Multidecadal Oscillation22 (AMO). We obtain the AMO signal in Arctic surface temperature by regression of its index23 (defined here as the average North Atlantic sea surface temperature minus the global average) against Arctic-average monthly-average surface temperature after removing the signals of dynamically-induced atmospheric variability, ENSO and explosive volcanic activity (see Methods). The observed AMO signal (see Supplementary Figure S2 online) is statistically significant and explains about 16% of the standard deviation of Arctic-average monthly-average surface temperature (see Supplementary Table S4 online). Figure 5 shows that the observed AMO signal accounts for about 15%, 30% and 10% of the early-20th-century warming, middle-20th-century cooling and late-20th-century warming in Arctic-average surface temperature, respectively. Two recent studies24,25 similarly indicate that the AMO contributed to early-20th-century warming, middle-20th-century cooling and late-20th-century warming in global-average surface temperature.
Neither the CMIP5 models, as a group, nor the BEST6 models, as a subset, show a significant signal of the AMO in Arctic-average surface temperature in their ALL simulations (see Supplementary Figure S2 and Table S4 online), hence their AMO signals do not contribute to early-20th-century warming, middle-20th-century cooling or late-20th-century warming (Figure 5). As an aside, it is worth noting that an anthropogenic aerosol influence on the AMO in HadGEM2-ES has been previously reported26, however this is not seen in other CMIP5 models27 and is at odds with observations of North Atlantic upper-ocean heat content28. Finally, Figure 5 shows that with the observed and simulated AMO signals removed (ALL-AMO) there is an even closer overall agreement between the observed and BEST6 Arctic-average surface temperature trends than found with the AMO signal included. The evidence, therefore, indicates that the observed multi-decadal variation of Arctic-average surface temperature is the consequence of anthropogenic forcing, explosive volcanic eruptions and AMO influence.
Observed global-average surface temperature similarly shows a multi-decadal variation, albeit with much smaller amplitude than in the Arctic, which the BEST6 ensemble captures (see Supplementary Figure S3 online). Here we note that the BEST6 models, while optimal in describing observed Arctic-average variation, are as a group no better or no worse than the other members of the CMIP5 ensemble in describing the observed global-average variation. This said, reproducing the observed temporal variations in surface temperature across all regions of the globe and in the global-average, is a challenge for climate models7.
Observations show that Arctic-average surface temperature increased from 1900 to 1940, decreased from 1940 to 1970 and increased from 1970 to present. Our results show that this multi-decadal variation in Arctic-average surface temperature is better simulated in an ensemble of current climate models that reasonably accurately simulate the transport, deposition and retention of anthropogenic sulphate aerosol into and within the Arctic. Using an ensemble of models run with natural forcings only, as one set of simulations and anthropogenic-only-forcings, as another set of simulations, we have shown that these multi-decadal variations can be largely explained by local responses to large-scale climate forcings together with a smaller contribution from internal climate variability, notably variability associated with sea surface temperature fluctuations in the North Atlantic. More specifically, we have concluded that the observed Arctic-average surface warming from 1900 to 1939 was likely the combined surface response to rising black carbon aerosol emissions, recovery from the eruption of Santa Maria (1902) at the beginning of the period and transition of the AMO to its positive phase. We have also argued that observed Arctic-average surface cooling from 1939–1970 was due to anthropogenic sulphate aerosol cooling, the eruption of Agung (1963) towards the end of the period and the transition of the AMO to its negative phase – a combined cooling effect that overwhelmed a significant GHG warming impact during this period. Arctic-average surface warming from 1970–2005 was dominated by GHG warming with a smaller contribution from the transition of the AMO to its positive phase. Our analysis has also identified a number of deficiencies in many current climate models, most notably the incomplete representation of the effects of anthropogenic sulphate aerosols and black carbon aerosols on climate, which together contribute to the inability of some models to reproduce observed Arctic surface temperature trends and to the inter-model spread in trends across all models.
Finally, using this set of current climate models run without natural and anthropogenic forcings it is possible to estimate the probability that the observed variation in Arctic-average surface temperature was due to internal climate variability alone. To accomplish this we have taken all available 106-year long independent segments from 17 of the above climate models with available control (i.e. externally-unforced) simulations. In total this yielded 92 such segments which were each masked with the observational coverage before computing piecewise linear approximations as above. Figure 6 shows that only one such segment, or realization, has early-20th-century warming as large as observed and that only two realizations have middle-20th-century cooling as large as observed – no realizations have late-20th-century warming as large as observed. The evidence, therefore, suggests that internal climate variability cannot account for the observed trends and this is supported by statistical tests of the null hypothesis that observed trends are consistent with zero29. Differences between observed and control–average trends in the early-20th-century and middle-20th-century periods have p-values equal to 0.01 and 0.02, respectively and near zero for the late-20th-century period (assuming the models are exchangeable with each other29). Here we note that the smaller the p-value is, the stronger the evidence against the null hypothesis. On this basis, we reject the null hypothesis that the observed trends are due to internal climate variability. In contrast, differences between the observed and BEST6–average trends in the early-20th-century, middle-20th-century and late 20th-century-periods have p-values equal to 0.08, 0.17 and 0.30, respectively. Hence, only with simulations that combine natural and anthropogenic (aerosol) forcings can we explain the observed variation in Arctic-average surface temperature from 1900–2005.
Since observations of internal climate variability are unavailable (reliable paleo-observations of Arctic wide surface temperature do not exist) we have used climate model control (i.e. externally-unforced) simulations to estimate this variability. To judge the sensitivity of results to our model-based estimate of internal climate variability we note that doubling the variance of this estimate (i.e. by multiplying the control trends in Figure 6 by the square root of 2) does not affect our conclusion that internal climate variability cannot explain the variation in Arctic-average surface temperature variability from 1900–2005.
Piecewise linear approximations
We approximate Arctic-average annual-average surface temperature T(t) using piecewise linear functions in three pieces between t1 = 1900 and t4 = 2005:
For fixed separation points t2 and t3, values of Ti are obtained by setting ∂Q/∂Ti = 0 where Q = ∑i (T−F)2 and solving the resulting system of four linear equations. The separation points t2 = 1939 and t3 = 1970 produce the best such approximation to the observed time series given pieces each with length greater than 10 years and these separation points are used in all cases. Trends in each piece are for i = 1, 2, 3.
BEST6 and WRST6 ensembles
These ensembles were selected by first computing the sum of square errors between the observed piecewise linear approximation and the piecewise linear approximations of each simulated ALL time series, i.e. for each of 51 simulations from 18 models. The models were then ranked based on the least sum of square errors over the available simulations for each model, e.g. the sum of square errors was computed for each of CanESM2's five simulations and the smallest of these values determined its ranking relative to the other 17 models. Our conclusions were found to be insensitive to reasonable variations in this procedure including removing the AMO signal before ranking.
Natural signals of Arctic surface temperature variability
Indices in Arctic-average monthly-average surface temperature of dynamically-induced variability, ENSO and volcanic variability were estimated as follows20,21. Dynamically-induced indices were found on a month-by-month basis by regressing sea level pressure anomaly maps onto normalized land-ocean surface temperature difference time series for the Northern Hemisphere. The coefficient time series of these sea level pressure regression patterns define the index of dynamically-induced variability. ENSO indices were estimated using a simple ocean mixed layer model using estimates of monthly anomalous flux of sensible and latent heat in the eastern tropical Pacific and optimal estimates of linear damping and effective heat capacity. Volcanic indices were estimated from the oceanic mixed layer model as above with observed aerosol optical thickness data and optimal estimates of linear damping and effective heat capacity. AMO indices were estimated using monthly sea surface temperature anomalies averaged over the North Atlantic (75°W–7°W, 25°N–60°N) after subtracting anomalies of global-average surface temperature. Natural signals of dynamically-induced variability, ENSO and volcanic variability in Arctic surface temperature were obtained using a multivariate linear regression of their indices, in addition to a term linear in time, upon Arctic-average monthly-average surface temperature assuming a first order autoregressive, AR(1), model for the noise. The natural signal of the AMO in Arctic surface temperature was obtained by regression of the AMO index against Arctic-average monthly-average surface temperature after first removing the signals of dynamically-induced variability, ENSO and volcanic variability as above. As a final step these natural signals of variability were annually averaged.
ACIA, Arctic Climate Impact Assessment. Cambridge University Press, 1042p (2005).
Trenberth, K. E. et al. Observations: Surface and Atmospheric Climate Change. In: Climate Change 2007: The Physical Science Basis. Contribution of Working Group I to the Fourth Assessment Report of the Intergovernmental Panel on Climate Change Solomon S., Qin D., Manning M., Chen Z., Marquis M., Averyt K. B., Tignor M. & Miller H. L. (Eds.). Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA (2007).
Polyakov, I. V. et al. Variability and trends of air temperature and pressure in the maritime Arctic. J. Climate 16, 2067–2077 (2003).
Johannessen, O. M. et al. Arctic climate change: Observed and modelled temperature and sea ice variability. Tellus A 56, 328–341 (2004).
Wang, M. et al. Intrinsic versus forced variation in Coupled Climate Model simulations over the Arctic during the Twentieth Century. J. Climate 20, 1093–1107 (2007).
Gillett, N. P. et al. Attribution of polar warming to human influence. Nat. Geosci. 1, 750–754 (2008).
Shindell, D. & Faluvegi, G. Climate response to regional radiative forcing during the twentieth century. Nat. Geosci. 2, 294–300 (2009).
Wood, K. R. & Overland, J. E. Early 20th century Arctic warming in retrospect. Int. J. Climatol. 30(9), 1269–1279 (2009) 10.1002/joc.1973.
Bengtsson, L., Semenov, V. A. & Johannessen, O. M. The early twentieth-century warming in the Arctic - a possible mechanism. J. Climate 17, 4045–4057 (2004).
Moritz, R. E., Bitz, C. M. & Steig, E. J. Dynamics of recent climate change in the Arctic. Science 297, 1497–1502 (2002).
Delworth, T. L. & Knutson, T. R. Simulation of early 20th century global warming. Science 287, 2246–2250 (2000).
Morice, C. P., Kennedy, J. J., Rayner, N. A. & Jones, P. D. Quantifying uncertainties in global and regional temperature change using an ensemble of observational estimates: The HadCRUT4 data set. J. Geophys. Res. 117 (2012) 10.1029/2011JD017187.
Bekryaev, R. V., Polyakov, I. V. & Alexeev, V. A. Role of polar amplification in long-term surface air temperature variations and modern Arctic warming. J. Climate 2, 3888–3906 (2010).
McConnell, J. R. et al. 20th century industrial black carbon emissions altered Arctic climate forcing. Science 317, 1381–1384 (2007).
Bond, T. C. et al. Bounding the role of black carbon in the climate system: A scientific assessment. J. Geophys. Res. 118, 5380–5552 (2013).
Shindell, D., Faluvegi, G., Lacis, A., Hansen, J., Ruedy, R. & Aguilar, E. Role of tropospheric ozone increases in 20th century climate change. J. Geophys. Res. 111 (2006) 10.1029/2005JD006348.
McConnell, J. R. New Directions: Historical black carbon and other ice core aerosol records in the Arctic for GCM evaluation. Atmos. Environ. 44, 2665–2666 (2010).
Shindell, D. T. et al. A multi-model assessment of pollution transport to the Arctic. Atmos. Chem. Phys. 8, 5353–5372 (2008).
Sharma, S., Lavoue, D., Cachier, H., Barrie, L. A. & Gong, S. L. Long-term trends of the black carbon concentrations in the Canadian Arctic. J. Geophys. Res. 109 (2004) 10.1029/2003JD004331.
Thompson, D. W. J., Wallace, J. M., Jones, P. D. & Kennedy, J. J. Identifying signatures of natural climate variability in time series of global mean surface temperature: Methodology and insights. J. Climate 22, 6120 (2009).
Fyfe, J. C., Gillett, N. P. & Thompson, D. W. J. Comparing variability and trends in observed and modelled global-mean surface temperature. Geophys. Res. Lett. 37 (2010) 10.1029/2010GL044255.
Schlesinger, M. E. & Ramankutty An oscillation in the global climate system of period 6570 years. Nature 367, 723–726 (1994).
van Oldenborgh, G. J., te Raa, L. A., Dijkstra, H. A. & Philip, S. Y. Frequency- or amplitude-dependent effects of the Atlantic meridional overturning on the tropical Pacific Ocean. Ocean Sci. 5, 293–301 (2009).
Tung, K. K. & Zhou, J. Using data to attribute episodes of warming and cooling in instrumental records. P. Natl. Acad. Sci. USA 110, 2058–2063 (2013).
Zhou, J. & Tung, K. K. Deducing Multidecadal Anthropogenic Global Warming Trends Using Multiple Regression Analysis. J. Atmos. Sci. 70, 3–8 (2013).
Booth, B. B., Dunstone, N. J., Halloran, P. H., Andrews, T. & Bellouin, N. Aerosols implicated as a prime driver of twentieth-century North Atlantic climate variability. Nature 484, 228–232 (2012).
Chiang, J. C. H., Chang, C. Y. & Wehner, M. F. Long-term trends of the Atlantic Interhemispheric SST gradient in the CMIP5 historical simulations. J. Climate (2013) 10.1175/JCLI-D-12-00487.1.
Zhang, R. et al. Have aerosols caused the observed Atlantic multi-decadal variability? J. Atmos. Sci. 70, 1135–1144 (2013).
Fyfe, J. C., Gillett, N. P. & Zwiers, F. W. Overestimated global warming in the past 20 years. Nat. Clim. Chang. 3, 767–769 (2013).
We thank Bill Merryfield, Slava Kharin and Michael Sigmond for their comments. We are very grateful to Sangeeta Sharma for providing the Alert sulphate aerosol concentration data and to Igor Polyakov for providing the NPA surface temperature timeseries. We acknowledge the modelling groups, the Program for Climate Model Diagnosis and Intercomparison (PCMDI) and the World Climate Research Programme's (WCRP's) Working Group on Coupled Modeling for their roles in making available WCRP CMIP5 multi-model data. The Greenland ice cores were collected under various NSF and NASA grants and were recently reanalyzed as part of NSF grants 0909541 and 0856845.
The authors declare no competing financial interests.
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Fyfe, J., von Salzen, K., Gillett, N. et al. One hundred years of Arctic surface temperature variation due to anthropogenic influence. Sci Rep 3, 2645 (2013). https://doi.org/10.1038/srep02645
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