# On the time-varying trend in global-mean surface temperature

## Abstract

The Earth has warmed at an unprecedented pace in the decades of the 1980s and 1990s (IPCC in Climate change 2007: the scientific basis, Cambridge University Press, Cambridge, 2007). In Wu et al. (Proc Natl Acad Sci USA 104:14889–14894, 2007) we showed that the rapidity of the warming in the late twentieth century was a result of concurrence of a secular warming trend and the warming phase of a multidecadal (~65-year period) oscillatory variation and we estimated the contribution of the former to be about 0.08°C per decade since ~1980. Here we demonstrate the robustness of those results and discuss their physical links, considering in particular the shape of the secular trend and the spatial patterns associated with the secular trend and the multidecadal variability. The shape of the secular trend and rather globally-uniform spatial pattern associated with it are both suggestive of a response to the buildup of well-mixed greenhouse gases. In contrast, the multidecadal variability tends to be concentrated over the extratropical Northern Hemisphere and particularly over the North Atlantic, suggestive of a possible link to low frequency variations in the strength of the thermohaline circulation. Depending upon the assumed importance of the contributions of ocean dynamics and the time-varying aerosol emissions to the observed trends in global-mean surface temperature, we estimate that up to one third of the late twentieth century warming could have been a consequence of natural variability.

### Keywords

Global warming trend Multidecadal variability Ensemble empirical mode decomposition IPCC AR4## 1 Introduction

^{1}These statistics serve to illustrate the sensitivity of estimates of such linear trends to the choice of start and end points upon which they are based. Short-term linear trends are an amalgamation of the ST and fluctuations with timescales too long to be resolved by conventional time series analysis techniques. The interpretation of the multidecadal variability (MDV) is particularly problematic in this respect.

Distinguishing between cycles and time varying ST of a time series has long been regarded as a daunting problem, as exemplified by the statement of Stock and Watson (1988): “*one economist’s ‘trend’ can be another’s ‘cycle’*”. The most widely used method of determining the trend in a data set is to draw the least squares best fit straight line within prescribed intervals, as was done in IPCC AR4. In reality, the rate of increase of GST in response to the cumulative buildup of long lived greenhouse gases and the changing rates of emission of aerosols is time dependent. Representing secular trends in GST in terms of linear trends is often not physically realistic. A more informative representation is *an intrinsically*-*determined monotonic curve, having at most one extremum**within a given time span* (Huang et al. 1998; Wu et al. 2007).

Using the above definition of the trend is likely to be more true to the observations than fitting data with straight lines within arbitrarily selected time intervals or with other arbitrarily pre-determined curves (e.g., exponential curve, polynomials of various orders). There is no guarantee that the modes recovered using such prescribed analytic functions correspond to physical modes of variability. Hence, it is desirable to have a more objective and non-parametric method of quantifying the low frequency variability of a time series such as GST.

If the cycles and secular trend extracted from the data do reflect the physical processes operating at a given time, then they should be temporally local quantities and the corresponding physical interpretation within specified time intervals should also not change with the addition of new data, for the subsequent evolution of a physical system cannot alter the reality that has already happened. Indeed, temporal locality should be the first principle in guiding all the time series analysis. This requirement reflects the evolution of time series analysis from the Fourier transform, to the windowed Fourier transform (Gabor 1946) and on to wavelet analysis (Daubechies 1992). It can be verified that the linear trends as fitted in AR4 (IPCC 2007) do not satisfy this locality principle, while the adaptive trend defined in Wu et al. (2007) and extracted using the ensemble empirical mode decomposition (EEMD) method (Huang and Wu 2008; Wu and Huang 2009) satisfies it qualitatively at least (as will be shown later), and hence, the ST determined adaptively by the data has a better chance of reflecting the underlying physics and resolving the ambiguity between the trend and the fluctuations superimposed upon it.

In this paper, we will recalculate the ST of GST using EEMD, which is a major refinement of the original Empirical Mode Decomposition (EMD) method used in Wu et al. (2007). It is expected that the partitioning of a time series into oscillatory variations on various timescales and an ST using an adaptive and temporal local analysis method, such as EEMD, provides an improved means of estimating the global warming trend from a data analysis perspective. In addition, a down-sampling method is devised to estimate the uncertainties of MDV, ST and their instantaneous rates of change. The temporally locality of the extracted modes is examined, with emphasis on the multi-decadal variability and the secular trend. The sensitivity of ST and MDV time series with respect to the different analyses of surface temperature, to the most recent corrections of the surface temperature analysis, to the inclusion or exclusion of the response to volcanic aerosol forcing, and to the presence of noise in the data will be tested.

A closely related question is the degree to which the MDV and the ST components of GST recovered using EEMD correspond, respectively, to the natural and anthropogenically-forced components of the GST variability. ST obtained from EEMD does not capture any anthopogenically-induced global warming that may be present on multi-decadal or shorter timescales and, conversely, it is conceivable that natural variability could project upon the secular trend. That ST and MDV might nonetheless be useful for representing the anthropogenic and natural components of the decadal variability draws support from recent studies of Semenov et al. (2010) and DelSole et al. (2011). Based on an analysis of numerical experiments with a coupled (atmosphere/ocean) model, Semenov et al. showed that the internal variability of Atlantic Meridional Overturning (AMO) circulation “*could have considerably contributed to the Northern Hemisphere surface warming since 1980*”. By projecting observed SST data onto spatial patterns derived from a statistical analysis of Coupled Model Intercomparison Project (CMIP3) simulations, Delsole et al. were able to formally partition the observed variability in 20th century GST into anthropogenically forced and natural components. They concluded that most of the irregularities in the rate of rise on GST on the multidecadal time scale can be attributed to natural (coupled atmosphere/ocean) variability. That our observational results are in agreement with the results of these studies lend credence to the notion that separating the low frequency variability of GST into ST and MDV components using EEMD series may be useful for attribution.

The paper is arranged as the follows: Sect. 2 introduces data and methods used in this study; Sect. 3 presents the major results: including the partitioning of the secular trend and variability on various timescales, their statistical significance, the temporally local warming rate as inferred from the time derivative of ST, an assessment of the robustness of the ST and MDV modes, the global structures of SST variability and change associated with MDV and ST, as well as the link of MDV to the natural variability of Atlantic Meridional Overturning (AMO) circulation. The final section summarizes the main results and provides some caveats relating to this study and some broader conclusions relating to the role of observational studies in the science of global climate change.

## 2 Data and methods

### 2.1 Data

- 1.
Global monthly land and sea surface temperature from HadCRUT3v dataset (Jones et al. 1999; Rayner et al. 2003);

- 2.
Global monthly land and sea surface temperature analyses provided by Goddard Institute for Space Studies (GISTEMP) (Hansen et al. 1999);

- 3.
The surface atmospheric temperature (SAT) dataset, which covers a time span from 1900 to December 2006, from the Global Historical Climatology Network, version 3 (Peterson and Vose 1997). The SST dataset is the NOAA ERSST by Smith et al. (2008);

- 4.
The International Comprehensive Ocean-Atmosphere Data Set (ICOADS), which contains objectively analyzed in-situ observations of SST in 5° × 5° grid boxes (Smith and Reynolds 2005); and

- 5.
An estimate of the variations in global-mean surface temperature variability attributable to volcanic forcing (Thompson et al. 2009).

### 2.2 The ensemble empirical mode decomposition^{2}

To extract trends in real data in accordance with the definition mentioned in the previous section, an adaptive and temporal local analysis method, the recently developed ensemble empirical mode decomposition (EEMD) method (Huang and Wu 2008; Wu and Huang 2009) is used.

EEMD is based on EMD (Huang et al. 1998; Huang and Wu 2008), a method that emphasizes the adaptiveness and temporal locality of the data decomposition. Many traditional decomposition methods, including the Fourier Transform and wavelet decomposition methods, utilize a priori determined basis functions, which may faithfully represent the characteristics of a time series in some segments but not in other segments of a non-stationary time series (Härdle 1990; Fan and Yao 2005). Other methods, including empirical decomposition methods that rely heavily on autocorrelations, involve implicitly global temporal domain integrals and therefore, are non-local and not well suited for extracting physically meaningful information from non-stationary time series. EMD, which uses extrema information of the riding waves in non-stationary time series, is an adaptive and temporally local decomposition method that extracts successively the riding amplitude-frequency modulated oscillatory components, starting with the highest frequencies and proceeding toward the lowest frequencies successively without using any a priori determined basis functions.

#### 2.2.1 The empirical mode decomposition

*x*(

*t*) are decomposed in terms of “intrinsic mode functions” (IMFs),

*c*

_{j}, i.e.,

*r*

_{n}is the residual of the data

*x*(

*t*), after

*n*intrinsic mode functions (IMFs) have been extracted. In practice, the EMD is implemented through a sifting process that uses only local extrema. For any data set,

*x*(

*t*) =

*r*

_{j−1}, say, the procedure is as follows: (1) identify all the local extrema (the combination of both maxima and minima) and connect all these local maxima (minima) with a cubic spline as the upper (lower) envelope; (2) obtain the first component

*h*by taking the difference between the data and the local mean of the upper and lower envelopes; and (3) treat

*h*as the data and repeat steps 1 and 2 as many times as is required until the envelopes are symmetric about zero to within a certain tolerance. The final

*h*is designated as

*c*

_{j}. The sifting process is considered to be complete when the residue,

*r*

_{n}, becomes a monotonic function or a function containing only one internal extremum from which no more IMFs can be extracted.

From above algorithm description, it is clear that EMD is not a curve fitting method in which an a priori determined functional form is used, for the piece-wise cubic spline fitting between neighboring maxima (minima) is not sensitive to maxima (minima) far away and is thereby quite local. It has also been tested that using a higher order spline instead of a cubic spline would not change the results significantly (Huang and Wu 2008). By applying EMD, the secular trend of a time series is naturally obtained after all the oscillatory components (riding waves) are removed from the time series. Since its development about 10 years ago, EMD has found numerous successful applications in many different scientific and engineering fields and has accumulated thousands of citations.

#### 2.2.2 Calculation of the instantaneous amplitude and frequency of a component

*c*

_{j}(

*t*), its Hilbert transform

*y*

_{j}(

*t*) is

*y*

_{j}(

*t*) of the function

*c*

_{j}(

*t*), one obtains an analytic function,

*a*

_{j}(

*t*) is the instantaneous amplitude, and

*θ*

_{j}(

*t*) is the instantaneous phase function. The instantaneous frequency is simply

*x*(

*t*).

#### 2.2.3 The ensemble empirical mode decomposition and the direct quadrature method

There have been two major subsequent elaborations of the EMD algorithm that have been motivated by practical problems of EMD. The first problem is that the EMD results are unstable with respect to noise of data for noise can alter the distribution of extrema, thereby leading to the lack of robustness of IMFs obtained using EMD. This drawback leads to difficulty in physical interpretation of IMFs. To solve this problem, EEMD was developed (Wu and Huang 2009). In this method, counter-intuitively, multiple noise realizations are added to the unique time series of “observations” *x*(*t*) to mimic a scenario of multiple realizations from which an ensemble average approach for the corresponding IMFs can be used to extract scale-consistent signals. The major steps in the EEMD method are as follows: (1) add a white noise series to the targeted data; (2) decompose the data with the added white noise into IMFs; (3) repeat step 1 and 2 again and again, but with different white noise series each time; and (4) obtain (ensemble) means of the respective IMFs of the decompositions as the final result.

From observation and intuition, the effects of the decomposition based on EEMD are quite understandable: the added white noise series cancel each other, and the mean IMFs stays within the natural dyadic filter windows as discussed in Flandrin et al. (2004) and Wu and Huang (2004, 2005), significantly improving the dyadic property of the decomposition and leading to stable decompositions. Therefore, this elaboration renders the EMD/EEMD method much more robust, eliminating many side effects formerly caused by unphysical scale mixing due to the presence of noise in the data. This development has also led to the most recent extension to multi-dimensional EEMD (Wu et al. 2009).

The second problem with EMD is associated with using Hilbert transform to calculate the instantaneous frequency. Due to the Hilbert transform being a global domain integral, the instantaneous amplitude and instantaneous frequency obtained using the Hilbert Transform is not “temporally local” or instantaneous. To overcome this problem, the direct quadrature (DQ) algorithm is proposed as a means of obtaining the instantaneous amplitude and instantaneous frequency (Huang et al. 2009a). The principle behind the DQ is very simple: if an IMF *c*_{j}(*t*) is obtained, its amplitude *a*_{j}(*t*) can be obtained simply by connecting the maxima of *c*_{j}(*t*). With known *c*_{j}(*t*) and *a*_{j}(*t*), using Eq. 1b, one can obtain the instantaneous frequency directly without using the Hilbert transform. It has been verified that DQ provides a more accurate calculation of the instantaneous frequency than the traditional method based on the Hilbert transform (Huang et al. 2009a).

### 2.3 Determination of trend uncertainty using down sampling

One issue associated with EMD/EEMD for determining trends in GST must be discussed here: the so called “data end effect”. Any method in current use is subject to uncertainties due to the data end effect. For example, the Fourier transform has the Gibbs effect and the wavelet analysis has its “cone of influence” (Torrence and Compo 1998). For EMD/EEMD, the error related to the data end effect is tied to the determination of values of envelopes at the data ends in every recurrence of the sifting process. When many of the widely used data end treatments in other methods, such as repetitiveness of data (in the Fourier transform) and mirror and anti-mirror extensions (for example, in wavelet analysis) were tested, it was found that EMD has a cone of influence analogous to the one in wavelet analysis but not as serious (Gledhill 2003). This drawback has led us to develop a new data end effect treatment scheme for predicting the values of the ends of the envelopes using information on the nearest two maxima (minima) to a data end for every recursion of the sifting process (Wu et al. 2009). This scheme has been demonstrated to reduce significantly the size of the “cone of influence” in numerous tests with synthetic data and real world data, especially in EEMD in which the added noise perturbation to the data helps to “correct” the predictions of the envelope ends for low frequency components. However, for the case of decomposing GST, the sum of the MDV and ST only has two interior maxima and two interior minima; and the strong amplitude-frequency modulation of the MDV could potentially lead to significant error in the separation of MDV and ST for the linear extension method may not approximate the highly nonlinear amplitude modulation of MDV accurately in this case.

*x*(

*t*) is the recorded data, and

*s*(

*t*) and

*n*(

*t*) are the true signal and noise, respectively. When the noise has a significant portion of its energy at the low frequencies (such as warm color noise), undoubtedly, the determined lower frequency components of the signal will be significantly contaminated by the lower frequency part of noise. Unfortunately, the noise, or even its characteristics, in GST is not a known a priori; and therefore we can not directly separate the noise from the signal. In such a case, if we want to estimate the statistical significance of any component of GST, we need to make a null hypothesis based on our limited understanding of how GST changes, such as in “Appendix” in which a single variable red noise null hypothesis is tested.

To estimate the uncertainties in the determined MDV and ST components of GST in addressing the two issues discussed above, we here devise a down sampling approach that bypasses these two issues. In this new approach, we randomly pick a value of the monthly GST for each calendar year to represent the entire annual average, which leads to a yearly down-sampled GST series. Theoretically, this approach could yield 12^{159} different time series. Among them, we randomly selected one thousand series and decompose each down-sampled GST series. We then obtain the means of the multidecadal variability and of the trend and their spreads (uncertainty) from these decompositions. The results, which will be displayed later, show that the data end effect is minimal and is well within the estimated uncertainty bounds when GST time series is shortened by decades.

It should be noted that this new approach is motivated by Wu et al. (2007) and Huang et al. (2009b), where it was shown that the time series formed by summing the components of the yearly mean GST (resulting from EMD decomposition) with timescales shorter than two decades resembles white noise. The result can be confirmed using Fourier filtering instead of EMD decomposition. As demonstrated in previous studies (Huang and Wu 2008; Wu and Huang 2009), the low frequency components of data resulting from EEMD are not sensitive to temporally local perturbations, which implies that the randomly sampled monthly mean GST data for successive calendar years should contain almost the same MDV and GST signals as the annual mean GST time series if the data end effect and noise inherent in GST are small.

## 3 ST and MDV in GST

### 3.1 ST and MDV of GST and their instantaneous rates of change

Correlations between corresponding components of SST and SAT

C | C | C | C | C | C | C | C | |
---|---|---|---|---|---|---|---|---|

SST&SAT | 0.08 | 0.21 | 0.26 | 0.45 | 0.70 | 0.61 | 0.70 | 0.57 |

_{2}input to the atmosphere by the fossil fuel burning (figure not shown). Therefore, the estimated global warming due to human activities over the past 25 years ranges from about 0.10 K to about 0.15 K per decade, depending on the assumed partitioning of the MDV between natural and anthropogenic aerosol-forced variability: if variations in the circulation of the Atlantic Ocean play a prominent role in causing MDV, then the value should lie toward the lower end of this range. On the other hand, if a slowdown or reversal in the buildup of aerosols was primarily responsible for the increased rate of global warming toward the end of the twentieth century, then the human contribution should lie closer to the top end of the range.

Mean slopes (°C/decade) of trends over different temporal spans

Last 150 years | Last 100 years | Last 50 years | Last 25 years | |
---|---|---|---|---|

AR4 | 0.045 ± 0.012 | 0.074 ± 0.018 | 0.128 ± 0.026 | 0.177 ± 0.052 |

ST and MDV | 0.051 ± 0.040 | 0.086 ± 0.039 | 0.105 ± 0.041 | 0.148 ± 0.051 |

ST | 0.050 ± 0.014 | 0.067 ± 0.014 | 0.086 ± 0.018 | 0.096 ± 0.024 |

The time derivative of ST, indicated by the red curve in Fig. 1, provides an indication of the rate at which global warming induced by the buildup of greenhouse gases and long-term aerosol change in the atmosphere has been proceeding, irrespective of the MDV associated with variations in the oceanic circulation and the relatively short-term changes in the rate of emission of aerosols. It is evident from the red curve in Fig. 1 that this rate has been increasing with time. The instantaneous warming rate is largest at the end of GST with a value of 0.10 ± 0.03 K per decade. The instantaneous warming rates of ST calculated based on different periods of record of GST all stay within ± 0.03 K per decade of the warming rate of the mean ST calculated based on GST for 1850–2008.

The time derivative of ST + MDV, indicated by the blue curve in Fig. 1, replicates the step-like character of the 25-year running mean trends (the black curve) and it also captures the recent slowdown in the rate of warming.

### 3.2 Robustness of MDV and ST

In this section, we examine the robustness of the results, with emphasis on the sensitivity of MDV and ST with respect to (a) a spurious discontinuity in the GST time series in 1945, (b) the inclusion or removal of the cool episodes following major volcanic eruptions, and (c) the presence of noise in the GST time series. All these calculations use the down-sampling approach described in Sect. 2.3.

#### 3.2.1 Effect of the spurious temperature discontinuity in 1945

A spurious temperature drop in the GST time series derived from HadCRUT3v data, with an amplitude of about 0.3°C occurs starting in August 1945, when the U.S. Naval fleet, which was measuring sea surface temperature (SST) using thermometers embedded in the condenser intake returned to port and British ships, which were taking bucket measurements of SST, replaced them as the dominant source of SST data (Thompson et al. 2008, 2009). This problem was discovered in 2008; efforts are underway to correct it, but as of this time, it is known only that the correction required to eliminate the biases associated with the use of different measurement methods aboard ships operated by different nations will be negative prior to 1945 and positive thereafter and that these corrections will probably extend over one to as much as a few decades (Thompson et al. 2008).

*e*-folding time for both exponential functions is 15 years. The original GST, the GST correction function, and corrected GST are displayed in the top panel of Fig. 6.

It is clear from the bottom two panels of Fig. 6 that the MDVs of the original and “corrected” GST exhibit some differences between 1925 and 1975. The peak in the 1940s occurs a few years earlier in the “corrected” data and the minimum that appears in the original data in the 1960s is slightly shallower and shifted forward in time by about 10 years. The effect of the correction on the ST is barely discernible. Hence, unless the forthcoming real correction to the GST time series extends over time intervals substantially longer than assumed in designing this synthetic correction, it is not likely to qualitatively affect the results presented in this paper.

#### 3.2.2 Inclusion or exclusion of the response to volcanic eruptions

Sulfur injected into the stratosphere by volcanic eruptions, condenses, forming long-lived layers of sulfate aerosols that reduce the shortwave solar radiation reaching the Earth’s surface. Because of the thermal inertia of the oceans, the resulting cooling of GST persists much longer than the aerosol layers that produce it. Since the volcanic eruptions occur intermittently throughout the GST record and the cool episodes following major eruptions in low latitudes can persist for up to 5–10 years, it is conceivable that volcanic forcing could affect the estimated MDV and ST.

From the results shown in Fig. 7, it is evident that the removal of the response to volcanic eruptions in the GST time series has very little effect on the estimated ST. However, the effect on the MDV is quite significant: when the response to volcanic eruptions is removed, the MDV exhibits a pronounced peak around the year 2000, with a rapid dropoff after that time that is not present in the original GST time series. But regardless of whether the response to volcanic eruptions is included or excluded, MDV exhibits a pronounced warming trend throughout most of the 1970s, the 1980s and the 1990s.

#### 3.2.3 The choice of dataset

Although various versions of HadCRUT (Jones et al. 1999; Rayner et al. 2003) are the most widely used surface temperature analysis, there are other analyses, such as those provided by Goddard Institute for Space Studies (GISTEMP) (Hansen et al. 2009), and by the NOAA National Climate Data Center (Smith et al. 2008). Since the different analyses have used different methods to homogenize the observed surface air temperature and sea surface temperature observations, each of these products is slightly different. For example, 1998 is the warmest year based on HadCRUT, while in GISTEMP, 2005 is as warm as 1998. Furthermore, each of these analyses contains a different level of noise. Since there is not enough information to assess which of these products is the most accurate, we will restrict ourselves to assessing whether the results obtained by performing EEMD on the GST time series are sensitive to the choice of dataset.

In the sensitivity experiments described in this section, we have demonstrated that the secular trend (ST or C9) mode recovered from EEMD is robust with respect to several prescribed perturbations in the input time series. The multidecadal variability (MDV or C8) mode exhibits some sensitivity with respect to the timing of the extrema, but the character of the variations is qualitatively similar in all cases and, in particular, all variants of the analysis exhibit a strong upward temperature trend in the late twentieth century that is reflected in both MDV and ST.

### 3.3 Spatial structures of ST and MDV

A noticeable feature of our regression pattern for MDV is that the dominant signals are restricted to high latitudes of the Northern Hemisphere and they appear to be more clearly defined over the ocean than over land (despite the fact that the amplitudes of surface temperature variation tend to be larger over land) and the sea surface temperature variations associated with MDV are particularly large over the Gulf Stream extension. These results are also consistent with the results of Semenov et al. (2010) which indicate that the North Atlantic-Arctic sector explains over 60% of the total Northern Hemisphere SAT response to surface flux anomalies of multidecadal timescale in their model experiments.

Both recent observational diagnoses (Zhang et al. 2007; Zhang 2008; Polyakov et al. 2009) and modeling evidence (Knight et al. 2005; Latif et al. 2006; Keenlyside et al. 2008; Semenov et al. 2010) suggest that variations in the intensity of the Atlantic meridional overturning circulation on the multidecadal time scale can give rise to episodes of rising and falling SST over the extratropical North Atlantic. In the SST pattern for the MDV shown in Fig. 9, the positive regression coefficients over the extratropical North Atlantic are accompanied by patches of negative coefficients over the Southern Ocean, a configuration reminiscent of the so-called “bi-polar seesaw” pattern inferred from paleoclimate proxies (Seidov and Maslin 2001; EPICA Community Members 2006), which is believed to be a consequence of variations in the strength of the Atlantic meridional overturning circulation. Another potential source of MDV that projects upon C8 derived from the EEMD analysis is the change in the Northern Hemisphere wintertime circulation that contributed to the rise in surface air temperature over the continents poleward of 40°N during the late twentieth century (Wallace et al. 1995; Quadrelli and Wallace 2004, Fig. 16).

The two representations of the Southern Ocean time series closely parallel one another after 1930, during which time they exhibit a pronounced out-of-phase relationship with the North Atlantic time series on the multidecadal time scale. The correlation coefficient between C8 of the North Atlantic ERSST and the ERSST (ICOADS) representation of the Southern Hemisphere time series is −0.77 (−0.57). The length of these time series is not sufficient to establish the statistical significance of these multidecadal correlations, but at least it is evident that they are strong and the sign of them is consistent with the notion that the Atlantic multidecadal variability involves cross-equatorial heat fluxes associated with the thermohaline circulation, as demonstrated in Semenov et al. (2010).

The results of a climate model simulations by Semenov et al. (2010), the statistical analysis of CMIP 3 forced and unforced runs by DelSole et al. (2011) and our analysis of observational data sets all points to the MDV being largely a reflection of internal variability of the climate system. However, the possibility that shorter term variations in aerosol forcing has contributed to the MDV cannot be ruled out. For example, the leveling off of sulfate concentrations around 1970 projects positively on that segment of the MDV curve (Murphy et al. 2009); indeed, it has been argued that the MDV in the second half of the twentieth century is dominated by this feature (Mann and Emanuel 2006).

## 4 Summary and discussion

In the previous sections, we have presented the results of EEMD analysis, which indicate that the secular warming trend during the 1980s and 1990s was not as large as the linear trends of the observation-based GST estimated in AR4 (IPCC 2007); and that the unprecedented rate of warming in the late twentieth century was a consequence of the concurrence of the upward swing of the multidecadal variability, quite possibly caused at least in part by an increase in the strength of the thermohaline circulation, and a secular warming trend due to the buildup of greenhouse gases. We estimate that as much as one third the warming of the past few decades as reported in Fig. TS.6 of the Summary for Policymakers of AR4 (IPCC 2007) may have been due to the speeding up of the thermohaline circulation. Other researchers have reached a similar conclusion: Keenlyside et al. (2008), Semenov et al. (2010) and DelSole et al. (2011) on the basis of numerical experiments with a climate model capable of representing the variability of the Atlantic meridional overturning circulation; Wild et al. (2007) on the basis of long term trends in the character of the diurnal temperature cycle at the Earth’s surface; and Swanson et al. (2009) based on an analysis of the partitioning of the GST trends using linear discriminant analysis. Furthermore, by analyzing the temporal derivatives of ST, we have demonstrated that the secular warming trend in GST has not accelerated sharply in the past few decades.

- 1.
The time derivative of ST of GST in the later twentieth century, as estimated by EEMD, is subject to future adjustments depending on how rapidly the atmosphere warms over the next decade or two.

- 2.
The contribution of aerosol forcing to ST remains uncertain, as are the relative contributions of aerosol forcing and Atlantic MDV to the observed MDV of GST.

These caveats notwithstanding, the results presented here further substantiate the reality of human-induced global warming, as evidenced by the similarity between the secular trend curve recovered from EEMD of GST and the buildup of atmospheric greenhouse gas concentrations and by the near-global extent of the temperature increases associated with the secular trend. Our results also serve to highlight the importance of Atlantic multidecadal variability in mediating the rate of global warming, and they suggest that these variations deserve more explicit consideration in twentieth century climate simulations and in attribution studies based on recent observations of the rate of change of GST.

## Footnotes

- 1.
In contrast, the 25-year running linear trend of AR4 multimodel ensemble does not contain stepwise fashion; rather, it varies little for the periods before 1963 or after 1963 which coincided with Agung volcano eruption. The linear trend is about 0.06°C/decade for the period 1900–1963 and about 0.19°C/decade for the period after 1963.

- 2.
The Matlab code of EEMD and a simple tutorial for how to use the code can be found in http://www.rcada.ncu.edu.tw/research1.htm.

## Notes

### Acknowledgments

The authors are benefited from the discussions with E. S. Sarachik, K.-K. Tung of U. Washington, E. K. Schneider of George Mason U., I. Fung of UC Berkeley, P. Chang of Texas A&M U, and R. Zhang of GFDL. NEH would like to acknowledge the support of a TSMC endowed chair at NCU, and also the support in part by a National Research Council of Taiwan grant NSC 95-2811-M-008-027, and a (USA) Federal Highway Administration grant DTFH61-08-C-00028. ZW was sponsored by the NSF grants ATM-0917743 and the First Year Asst Prof Award of Florida State University. JMW and BVS by NSF grant ATM-0812802. XC was supported by the National Basic Research Program of China 2007CB816002, National Science Foundation of China 40776018, and by National Key Technology R&D Program 2006BAB18B02.

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