The paleoclimatic sensitivity to atmospheric greenhouse gases (GHGs) has recently been suggested to be nonlinear, however a GHG threshold value associated with deglaciation remains uncertain. Here, we combine a new sea surface temperature record spanning the last 360,000 years from the southern Western Pacific Warm Pool with records from five previous studies in the equatorial Pacific to document the nonlinear relationship between climatic sensitivity and GHG levels over the past four glacial/interglacial cycles. The sensitivity of the responses to GHG concentrations rises dramatically by a factor of 2–4 at atmospheric CO2 levels of >220 ppm. Our results suggest that the equatorial Pacific acts as a nonlinear amplifier that allows global climate to transition from deglacial to full interglacial conditions once atmospheric CO2 levels reach threshold levels.
Rapidly rising anthropogenic CO2 emissions over the past few decades pose a risk to human society and the biosphere. Relative to pre-industrial levels, the CO2 concentration is projected to double to 560 ppm from 2050–2100, increasing the global mean temperature by 2.0–4.5 °C by the end of the 21st century. This warming is predicted to lead to large-scale ice sheet melting, shifts in rainfall patterns, and sea level rise1. Identifying the interactions among various forcing agents and feedback processes in the projected warming scenario is crucial to our understanding of social/biosystem sustainability and climate change mitigation strategies.
The tropical Pacific Ocean is the most important water vapor and moisture source to middle and high latitudes on the planet2. Accurately estimating tropical sea surface temperature (SST) responses to greenhouse gas (GHG)-induced radiative forcing (RFGHG) is fundamental to reliable predictions. Past climate studies3, 4, however, assumed that the sensitivity of tropical ocean SST to atmospheric GHG content was linear. Physical model simulations were limited by a lack of pre-industrial observational records for climate transitions from low to high GHG levels. The energy budget of the global climate system is, therefore, difficult to precisely evaluate. This severely hinders our understanding of the mechanisms and energy interactions among climatic sub-systems.
The sensitivity of tropical Pacific Ocean SST to RFGHG, mainly contributed by CO2 and <5% by CH4, during the past glacial/interglacial (G/IG) cycles was addressed3,4,5. Linear regression analyses3, 4, 6 were conducted to evaluate the SST response to changes in pCO2 assuming that the RFGHG is the main driver of tropical SST and that the tropical Pacific SST would be 33–36 °C under a doubled CO2 scenario. By comparing the atmospheric pCO2 and SST values of the early Pleistocene to those of the late Pliocene, Martinez-Boti et al.5 found a lower sensitivity under high atmospheric pCO2 conditions, implying that the sensitivity may not respond linearly to the GHG level. Recent transient models7 based on composite paleo-temperature records also revealed nonlinear sensitivity patterns since 800 thousand years ago (kyr BP, before 1950 AD). These variable responses to RFGHG are supported by a conceptual and dynamic-flow box modeling study8 that argues for the existence of possible step-wise and/or different equilibrium climate states during G/IG cycles.
This dispute, linear versus nonlinear climatic sensitivities, hinders our understanding of climate evolution and our ability to evaluate the fidelity of global energy simulations under the current warming stress. Orbital-scale high-resolution SST records are required to clarify this debate. Here, we combine a new record of southern Western Pacific Warm Pool (WPWP) SST anomalies (ΔSST) and previously published equatorial Pacific records4, 9,10,11 for the past four G/IG cycles to document the non-linearity of the relationship between equatorial Pacific SSTs and GHG levels and to identify the specific pCO2 threshold.
A marine sediment core, MD05-2925 (9.3°S, 151.5°E, water depth 1661 m), was retrieved from the Solomon Sea east of Papua New Guinea (Figs 1, S1). The age model for MD05-2925 was established using radiocarbon dates12 and composite benthic foraminiferal oxygen isotopic stratigraphy (Figs S2, S3). The Mg/Ca ratios of planktonic foraminifera, Globigerinoides ruber, were determined using a sector field inductively coupled plasma mass spectrometer (SF-ICP-MS)13 and were used to establish a 360-kyr SST sequence with 200- to 900-year resolution.
Foraminiferal Mg/Ca-inferred Solomon Sea SST
The new reconstructed Solomon Sea SST record shows a large G/IG change of approximately 4 °C, which is supported by a previous study14 (Fig. 2a). The interglacial temperatures of 28–29 °C during Marine Isotope Stage (MIS) 7 and MIS 9 are similar to those of the Holocene and are higher by 1–2 °C than those of MIS 5. Large SST variations of 2–3 °C can be observed during glacial periods, such as MIS 2–4, 6 and 8.
Spectral analysis (Fig. S5) shows that the Solomon Sea SST record is characterized by strong obliquity pacing and a good correlation with Antarctic temperature changes during the past four G/IG cycles. The Southern Hemisphere (SH) middle- to high-latitude climate apparently exerts a significant influence on the Solomon Sea, possibly by oceanic tunnel connections11, 12 (Figs S5–S9).
The statistical correlation shown in Figure S7 suggests that the SST changes in the Solomon Sea could be related to SH high-latitude climate variation, similar to the eastern equatorial Pacific (EEP) upwelling region11. The trends in the time series of Antarctic temperature and southern WPWP SST have been similar since 360 ka (R2 = 0.59 or 0.65 if MIS 7 is omitted, Fig. S7). This correlation implies a persistent teleconnection between the two regions (Figs S7–S9)12. Therefore, the southern WPWP and EEP regions are linked to Southern Ocean climate and/or affected directly by the RFGHG 3, 15, 16.
Climate sensitivity and regional comparisons
The relationship between tropical ΔSST and the atmospheric RFGHG anomaly (relative to pre-industrial levels, ΔRFGHG) for the Solomon Sea record is plotted in Figure 3. This comparison expresses a striking nonlinear correlation with a significant change at an atmospheric CO2 threshold of 220 ± 10 ppm (Fig. 3). Southern WPWP ΔSST values increase from −4.1 to −1.2 °C as the ΔRFGHG values increase from −2.75 to −1.55 W m−2, corresponding to a pCO2 range of 170–210 ppm. Thus, the sensitivity is 0.62 ± 0.33 °C (W m−2)−1. Note that all the sensitivity uncertainties are given in 1σ range (Table S3). During the second interval, ΔRFGHG increases from −1.55 to 0 W m−2 (210–280 ppm pCO2). The sensitivity increases to 1.83 ± 0.17 °C (W m−2)−1 as ΔSST increases from −2.1 to 1.8 °C. No significant differences are observed in the SST-RFGHG response among the past four G/IG periods at 1–70, 71–160, 161–270, and 271–360 kyr BP (Fig. S8), indicating that the correlation is independent of the G/IG cycles in this region.
A comparison of ΔSST and pCO2 values over the past 3–4 G/IG cycles at six western and eastern equatorial Pacific sites (Fig. 1) is shown in Figure 4. Five (MD05-2925, ODP 1240, TR163-19, MD97-2140, and ODP 871) of the six sites are characterized by a nonlinear SST-RFGHG relationship with an atmospheric CO2 threshold of 220 ± 10 ppm (Fig. 4). Comparable to the southern WPWP site MD05-2925, the SH-affected EEP upwelling sites of ODP 1240 and TR163-19 also feature similar nonlinearity. Sites ODP 1240 and TR163-19 have low sensitivities of 0.61 ± 0.14 and 0.51 ± 0.14 °C (W m−2)−1, respectively, at pCO2 values of <220 ± 10 ppm and high sensitivities of 2.35 ± 0.17 and 1.29 ± 0.50 °C (W m−2)−1, respectively, at pCO2 values of >220 ± 10 ppm. A similar nonlinearity was also reported in the southern WPWP region over the past 400 kyr BP (Fig. 5 of ref. 15).
MD97-2140, ODP 871, and ODP 806 in the northern WPWP show more complicated patterns. MD97-2140 and ODP 871 have nonlinear relationships and sensitivities of −0.20 ± 0.15 to 1.01 ± 0.57 °C (W m−2)−1, respectively, which are less than the values of the EEP sites and MD05-2925. ODP 806 is the only site characterized by a linear trend due to an absence of statistics-based different sensitivities (Table S3). Its sensitivity is 0.70 ± 0.10 °C (W m−2)−1 (Fig. 4). The nonlinearity observed in the northern WPWP can be attributed to equatorial upwelling, regional oceanic dynamics, and topographic settings4, which might transport high latitude climatic effects to equatorial Pacific17, 18.
We hypothesize that this general nonlinear SST response is associated with the sea ice coverage in the Southern Ocean, the related release of ocean-derived CO2, and induced atmospheric radiative forcing during the last four G/IG cycles. Jaccard et al.19 presented sedimentary evidence that sea ice in the Southern Ocean could affect oceanic-atmospheric CO2 exchange by controlling the Subarctic Mode Water (SAMW) and Antarctic Intermediate Water (AAIW) formations during the past one million years. The SH high-latitude impact on the equatorial Pacific hydroclimate and the teleconnection between SAMW/AAIW and South Pacific Tropical Water (SPTW, Fig. 1) have been reported based on evidence from the subtropical gyre and resurfacing processes, such as upwelling and mixing20. The oceanic tunneling process represents the link between the Southern Ocean modulation and the WPWP and EEP. The possible processes are as follows. The gradual melting of sea ice in the Subantarctic Zone and the release of CO2 during the initial phase of glacial termination could cause the first stage of the SST-RFGHG response. Positive latent and sensible heating likely then triggers a sudden retreat of Southern Ocean sea ice and a rapid increase in pCO2, leading to warming and a better ventilated SAMW/AAIW21. A pCO2 level of 220 ± 10 ppm can be considered the critical threshold for runaway melting and is supported by an Earth system model simulation22.
Our hypotheses are supported by previous climate reconstructions23, 24. Taking the last termination as an example, a pCO2 level of 220 ± 10 ppm occurred during Heinrich event 1, when meridional circulation shut down, the Southern Ocean warmed, and releases from the major deep-sea carbon reservoir began23. Benthic foraminiferal δ13C and SST data from the southwestern Pacific also suggest that the SAMW/AAIW experienced periods of relatively strong and weak ventilation24.
The responses of the WPWP and EEP thermal conditions to GHGs imply that the Southern Ocean–tropical ocean link acts as a nonlinear amplifier during glacial terminations via ocean circulation and atmospheric energy feedbacks. Once the pCO2 level exceeded 220 ppm, the southern WPWP SSTs increased by 1.83 °C (W m−2)−1, a rate that is three times higher than that associated with pCO2 levels of <220 ppm. The higher SST and increased latent heating may also have acted as a positive feedback mechanism, contributing to the collapse of high-latitude ice sheets25. Rapid warming in the equatorial Pacific possibly further weakened Hadley circulation12 and strengthened the SH westerlies. The enhanced Southern Ocean upwelling was then able to release more CO2 into the atmosphere23. Similar climatic threshold behavior during the past one million years of G/IG oscillations has been reported19. The teleconnection between the southern and northern hemisphere climates via WPWP and EEP SSTs during past G/IG cycles suggests that the tropical climate system plays a crucial role in rapid climatic transitions on Earth.
The clear relationship between equatorial Pacific SSTs and RFGHG provides an important reference for understanding past and future climate dynamics. First, the mechanism that controls the nonlinearity in different oceans needs to be confirmed to improve predictions of the responses to increases in pCO2. Second, the potential existence of another higher CO2 threshold should be determined. Martinez-Boti et al.5 reported that the climate sensitivity could be similar or greater at higher pCO2 levels. The spatial variability in climate sensitivity during the Pliocene, with pCO2 levels of 300–500 ppm, remains unknown. More spatial and temporal high-resolution SST records and accurate GHG concentration reconstructions are required to clarify the complexity of the tropical ocean thermal response to RFGHG changes and potential high-latitude teleconnections and to understand the linkages between tropical and high-latitude climate systems at different timescales.
A marine sediment core was obtained at site MD05-2925 during the 2005 PECTEN (Past Equatorial Climate: Tracking El Niño) cruise, which was supported by the International Marine and Climate Changes (IMAGES) Project, on the research vessel Marion Dufresne. This site is located on the Woodlark rise, Solomon Sea, which is close to Papua New Guinea (PNG). The main route of the South Equatorial Current (SEC) traverses the Solomon Sea. The SEC originates in the mid-latitudes and travels to the equator. The annual average SST is 28.5 °C (ref. 26) and the seasonal variations are from 27.4 to 29.4 °C from the closest observational site at 8°S (ref. 27).
The MD05-2925 age model was established using accelerator mass spectrometry radiocarbon (AMS 14C) dates and benthic foraminiferal oxygen isotope stratigraphic correlation. The compiled benthic foraminiferal δ18O data were correlated to the global benthic foraminiferal δ18O stack (LR04, ref. 28) (Figs S2, S3). All benthic foraminiferal tests were >250 μm in size, and 2–5 tests were used to measure δ18O values. Our group has reported the first 282-kyr age model12, 29 and adopt the interspecies δ18O offset constants from previous studies29. All oxygen isotope age control points are summarized in Table S1.
Planktonic foraminiferal δ18O and Mg/Ca ratio
In total, 40–60 planktonic foraminifera G. ruber (white, s.s., 250–300 μm) were picked for oxygen isotopic measurements and Mg/Ca determinations. Each of the paired δ18O-Mg/Ca measurements, 20–30 tests were crashed and mixed for clearing procedure. For the oxygen isotope measurements, the samples were ultrasonicated 3–4 times, immersed in NaOCl for 24 hours, and dried. The cleaned samples were measured using an isotope ratio mass spectrometer (IRMS) at the National Taiwan Normal University. Analytical reproducibility is ±0.60‰ (2 RSD, N = 701)12 with respect to the Vienna Pee Dee Belemnite (VPDB). For the Mg/Ca measurements, the shells were gently crushed and placed in Teflon vials. The cleaning procedure followed that of Lo et al.13. Cleaned samples were dissolved in 5% HNO3 and measured using a Thermo-Finngan Element II sector field inductive coupled plasma mass spectrometer (SF-ICP-MS) at the High-Precision Mass Spectrometry and Environment Change Laboratory (HISPEC), Department of Geosciences, National Taiwan University. The external uncertainty is ± 0.60% (2 RSD). G. ruber δ18O and Mg/Ca values during the last termination (23-10 kyr BP) were previously reported12.
SSTs inferred from G. ruber Mg/Ca ratios
The average Solomon Sea G. ruber Mg/Ca ratios vary from approximate 3.5 mmol mol−1 during the glacial periods to 4.5–5.0 mmol mol−1 during the interglacial periods (Fig. S4b). We adapted composite equation Mg/Ca = 0.38 x e(0.09 x SST) to calculate the corresponding SST values30, 31. The average G. ruber shell weight during glacial periods (11.37 ± 1.11 μg, 1RSD, n = 20) does not differ from that during interglacial periods (11.46 ± 0.78 μg, 1RSD, n = 21) (Fig. S4d). The coarse fraction weight percentage shows no clear G/IG changes, which is reported to be linked with the carbonate preservation condition in the eastern equatorial Pacific region32 (Fig. S4c). Accordingly, no additional dissolution correction needs to be applied to the MD05-2925 Mg/Ca ratios, similar to the SST record reported in the northern PNG region15.
ΔSST is defined as the difference between past temperatures (SSTi) and the modern annual average temperature (SST0, 28.5 °C)26. ΔRFGHG is defined as the difference between a certain past GHG level ([CO2] and [CH4]) and the pre-industrial greenhouse gas level ([CO2]0 = 280 ppm, [CH4]0 = 700 ppb)33. Although CH4 contributes only <5%, we calculated the ΔRFGHG using both CO2 and CH4. The negative feedback from N2O is negligible with respect to RF26. The equation used to determine ΔRFGHG is as follows:
Regional sensitivity comparison
We summarized the updated G. ruber Mg/Ca records, which included at least three G/IG cycles, and calculated the relationships between ΔSST and ΔRFGHG. The records of ODP 806 (0.3°N, 159.4°E, water depth 2520 m)9, MD97-2140 (2.0°N, 141.7°E, water depth 2547 m)10, ODP 871 (5.6°N, 172.3°E, water depth 1255 m)4, TR163-19 (2.3°N, 91°W, water depth 2348 m)9, and ODP 1240 (0.0°N, 86.5°E, water depth 2921 m)11 were used. The Mg/Ca records of ODP 806 and TR163-19 have been recently calibrated using the dissolution correction equation4. We resampled ODP 806, ODP 871, TR163-19, and MD97-2140 at a 4-kyr interval and ODP 1240 at a 1-kyr interval and compared them to the contemporaneous resampled Antarctica ΔT and pCO2 records with the AICC2012 age model34, 35, following the methods of previous studies4, 9. No significant lead-lag difference is observed between the Antarctic and Solomon Sea ΔSST records (Table S2).
Statistical methods to identify nonlinearity
Non-overlapping binned method
A non-overlapping binned method, used by the compilation of tropical SSTs (ref. 12), was applied to calculate the average trend of ΔSST versus ΔRFGHG. A radiative forcing window corresponding to 10 ppm pCO2 was used to calculate the average value of ΔSST and standard deviation of the mean for each of the SST data locations with different time resolutions.
K-means clustering analysis36 is widely used in diverse fields37,38,39 to statistically determine inflection points from separated k groups of any dataset with a non-linear trend. The data shown in all panels of Figures 3 and 4 were divided into two groups by k-means analysis. The regression lines with a 95% confidence interval of the two groups were calculated.
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The authors would like to thank the chief scientists Luc Beaufort and Min-Te Chen of the 2005 PECTEN cruise, which was supported by the IMAGES group. This project was supported by Taiwan ROC MOST (104-2119-M-002-003, 104-2917-I-564-046, 105-2119-M-002-001, 105-2116-M-002-026-MY3), National Taiwan University (105R7625), State Key Laboratory of Isotope Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences (SKLaBIG-QD-16-04) and Academia Sinica.