The mid-Pliocene Warm Period (mPWP) offers an opportunity to understand a warmer-than-present world and assess the predictive ability of numerical climate models. Environmental reconstruction and climate modelling are crucial for understanding the mPWP, and the synergy of these two, often disparate, fields has proven essential in confirming features of the past and in turn building confidence in projections of the future. The continual development of methodologies to better facilitate environmental synthesis and data/model comparison is essential, with recent work demonstrating that time-specific (time-slice) syntheses represent the next logical step in exploring climate change during the mPWP and realizing its potential as a test bed for understanding future climate change.
The Earth is experiencing an unequivocal warming unprecedented over decades to millennia1. The geological record and simulations of past climate provide scientists with the opportunity to understand how Earth system processes operate outside the observational or instrumental record, and are fundamental to our understanding and ability to accurately project future climate and environmental change2. The Pliocene Epoch (5.33–2.58 Ma) is particularly attractive with respect to understanding future climate due to many shared similarities with regards to Earth’s physical characteristics.
Both palaeoenvironmental reconstructions and climate modelling have been pivotal in increasing our understanding of climate and its importance during the mid-Pliocene Warm Period (mPWP: 3.264–3.025 Ma; also referred to as the ‘Pliocene Research, Interpretation and Synoptic Mapping (PRISM) interval’). During warm intervals of the Pliocene, atmospheric CO2 concentration is estimated to have ranged between 350 and 450 p.p.m.v. (refs 3, 4, 5, 6, 7, 8). This is in contrast to the known pre-industrial concentration of 280 p.p.m.v. On the basis of palaeoenvironmental reconstruction, Pliocene surface temperatures over land and oceans were elevated with respect to the pre-industrial9,10. Climate model estimates indicate that the global annual mean surface temperature was 2.7–4.0 °C higher11. A combination of modelling studies and geological data has shown, for example, that during the mPWP the hydrological cycle was enhanced11, ice sheets were smaller12,13, sea level was higher14,15, forest cover was expanded and arid deserts contracted16.
Many parallels can be drawn between the mPWP and observed trends in modern climate, as well as in future climate projections, due to similar continental configurations, land elevations and ocean bathymetries17. Many terrestrial and marine flora and fauna are extant, increasing the validity of approaches that attempt to reconstruct the environment using modern relationships between climate and biogeography18,19. The mPWP20,21 (Fig. 1) provides arguably the best pre-Quaternary example of the synergy between numerical models and proxy data, which has ultimately led to an enhanced understanding of this time period.
Since the late 1980s, scientists have used palaeoenvironmental data to systematically reconstruct ocean temperatures, vegetation cover and ice extent, providing a fundamental understanding of the warm nature of the mPWP. Proxy-based reconstructions alone are unable to tell us about mechanisms for warmth and what might be the main climate drivers of sustained globally higher temperatures during the mPWP. The realization of the potential benefit of including climate modelling led to the design of digital data sets specifically for climate models21.
Over the last 25 years, the relationship between models and data has evolved and become progressively intertwined and complex. The increasingly sophisticated nature of geological reconstruction and climate modelling techniques has driven a continuous process of innovation in combining data and modelling approaches for understanding the mPWP and what it may be able to tell us about future global change11,22,23,24.
Our review begins with an overview of mPWP palaeoenvironmental reconstruction and then discusses the main palaeoclimate modelling efforts focused on this interval. We show how data have progressed from simply providing boundary conditions for numerical models to a means of assessing the efficacy of model simulations of the mPWP climate (for example, data/model comparison). The use of data as a benchmark highlights the complexity of the relationship between data and models, as science demands more statistical rigour and a greater understanding of the potential errors/uncertainty associated with both modelling and data generation. We also use the case study of temperature stability in the tropics to highlight the complexities of this relationship. Finally, we examine recent developments in understanding the mPWP.
Historical perspective of palaeoenvironmental reconstruction
Zubakov and Borzenkova25 were the first to propose that the climate of their Pliocene Optimum (4.3–3.3 Ma) could be considered a past analogue for the mid-Twenty first century when atmospheric CO2 concentrations would reach double their pre-industrial values. They pioneered the earliest efforts towards construction of regional Pliocene palaeoclimate conditions based on the palaeontology of more than 20 continental sections and available marine core sequences. From these data they reconstructed 30 Miocene and Pliocene ‘superclimathems’ defined as cycles of 100,000 to 300,000 years with amplitudes of at least 4 to 5 °C.
With the then generally accepted knowledge that the Pliocene was a time of warm, equable climate, and with growing concern over potential impacts of future global warming as a backdrop, the need for a more precise and less anecdotal assessment of Pliocene climatic conditions became clear. In 1988, the US Geological Survey endeavoured to reconstruct the palaeoenvironment during the mPWP via PRISM. Using lessons learned from earlier efforts to reconstruct the surface of the Ice-Age Earth26, PRISM and its collaborators developed a large-scale data collection project that has grown in size and scope over the past 25 years (Box 1). PRISM remains the only global-scale synoptic reconstruction of the Pliocene. Data are produced from a global distribution of localities; however, work is concentrated on a focused stratigraphic interval (currently 3.264–3.025 Ma)17 (Box 1).
Such an endeavour to understand one stratigraphic interval (time slab) is fundamentally different from efforts that have gone into developing long time series at single locations. When time series intersect the mPWP, we improve our ability to understand the dynamic development and evolution of environment and climate (see also next section). These approaches (time slab and time series) are not mutually exclusive. Rather, each benefits from the perspective only available through the other.
The tools used by the palaeoclimate community have changed over time, and researchers continue to use the most sophisticated techniques available for reconstruction (Fig. 2). Proxies have been developed to reconstruct different aspects of the environment; however, surface ocean and land temperatures are by far the primary variables reconstructed. Techniques include quantitative analysis of faunal and floral assemblages and stable isotopic composition of carbonates and biomarkers. All have strengths and limitations, but each plays an important role in our conceptual understanding of the mPWP.
Stable isotopes of oxygen have been used to estimate palaeotemperatures, and indirectly ice volume, since the pioneering work of Emiliani27. Over time they have become the multitool of palaeoceanographic inquest. Shackleton et al.28 generated the first long benthic δ18O time series spanning the Pliocene, placing limits on potential changes in the cryosphere, the stability of Antarctic ice and sea level. The development of an isotopic composite standard reference section, LR04, is possibly the most unifying development to date in pre-Pleistocene palaeoceanography29. With the LR04 composite, researchers are able to correlate remote sequences to a standardized section tied to orbital chronology. This provides the community with a high-resolution stratigraphic framework within which the temporal and spatial aspects of climate change during the mPWP can be analysed.
Primary temperature proxies commonly utilized for mPWP reconstruction include the following: Mg/Ca palaeothermometry, the alkenone unsaturation temperature proxy , the TetraEther index (TEX86) and quantitative analysis of faunal and floral assemblages. These palaeotemperature proxies measure different aspects of temperature by sampling the marine environment at different times of the year as well as at different water depths. While this can provide much insight into the thermal structure of the water column, variations in the timing of production in the past can cause seasonal biases in our interpretations. Likewise, changes in preferred depth habitats would skew palaeoenvironmental reconstruction. Estimates are complicated by effects unique to different signal carriers and methods. For example, the Mg/Ca method depends on assumptions about the composition of seawater at the time calcite was precipitated and can be complicated by post-depositional processes such as dissolution. Faunal assemblage techniques require the assumption of stationarity of ecological preferences and have upper and lower limits based on calibration to present day conditions. , based on extraction of organic molecules (ketones synthesized by haptophyte algae) from sediment, is not affected by seawater chemistry but has an upper limit of ∼28 °C. TEX86 (based on the relative distribution of membrane lipids produced by Crenarchaeota), such as , is not directly affected by seawater composition, has an upper limit close to 38 °C, but can sometimes record subsurface conditions and be complicated by terrestrial input30,31,32,33,34,35,36,37,38,39,40. The use of multiple proxies is of great benefit for gaining more robust and detailed estimates of the palaeoenvironment as long as the relative limitations of various techniques are recognized.
On the basis of these proxy techniques, past studies41 have summarized mPWP oceans as being characterized by a reduced meridional SST gradient, potentially driven by enhanced ocean heat transport42. High-latitude regions were warmer than those of today, and this warming was at least in part related to changes in sea-ice cover. SST increases in the North Atlantic appear to be particularly pronounced (Fig. 5; see also refs 43, 44, 45, 46). In the circum-Antarctic region, the Polar Front Zone was expanded but displaced towards the continent, and sea ice was greatly reduced18,47. Subtropical gyres in all oceans were displaced towards the poles.
To highlight the benefit of using multiple proxies, we focus on efforts to understand the tropics, both in terms of data and climate modelling studies (see sections below for further discussion with regard to data/model comparison).
A clear pattern of tropical SST warming has never been evident in the PRISM reconstructions outside of upwelling regions17,18,20,35,42,48. Tropical upwelling regions are fed by intermediate depth waters that originally form and sink in higher latitudes. Since high-latitude SST reconstructions indicate substantial warming, it is plausible that warmer source waters fed tropical upwelling zones during the mPWP. Given early reconstructions of atmospheric CO2 concentration higher than the pre-industrial3,4,49, which have been supported by more recent studies50, the lack of tropical SST warming in areas outside the upwelling zones has proven puzzling. This was one reason enhanced meridional ocean heat transport was suggested on the basis of reconstructed mPWP SST gradients42. This provided a way to explain higher concentrations of atmospheric CO2 (compared with pre-industrial) while at the same time preserving tropical SST stability outside the upwelling zones.
Understanding the thermal stability of the western equatorial Pacific (WEP) warm pool has been a driver of Pliocene palaeoceanographic research in general for many years. While the focus of these studies has been on the early Pliocene rather than the mPWP, insights may be transferable from one to the other (Box 2).
Wara et al.51 developed Mg/Ca-based sea surface temperature (SST) records from calcareous tests of surface-dwelling planktonic foraminifers. These time series span the Pliocene to Recent at Ocean Drilling Program Sites 847 in the eastern equatorial Pacific (EEP) and 806 in the WEP (Fig. 2). The records suggest stable temperatures in the WEP and a small surface-temperature gradient across the equatorial Pacific, particularly in the early Pliocene, much similar to a modern El Niño event with warmer-than-average SST in the EEP. This led to the concept of a Permanent El Niño-like state during the Pliocene, with concomitant warming in the EEP, suggesting a weak zonal atmospheric circulation51.
One study (ref. 48) used quantitative faunal assemblage techniques to estimate SST and found no compelling evidence that the WEP was different from that of present day. Since faunal techniques (calibrated to present day) have a maximum limit of ∼30 °C, and index becomes fully saturated at 28 °C, neither can document warming above modern warm pool conditions. Some late-Pliocene equatorial assemblages do show small non-analogue increases in thermophilic taxa that could be explained by brief periods with SST in excess of 30 °C (ref. 48).
O’Brien et al.52 and Zhang et al.53 addressed the issue of stability of the tropical warm pool during the early Pliocene by applying Mg/Ca, and TEX86 techniques. They found close agreement between and TEX86 where they could both be applied, giving confidence to the application of TEX86 to the warm pool regions. The TEX86-based estimates of WEP SST were higher than previous studies based on Mg/Ca or faunal assemblages. They concluded that previous WEP Mg/Ca temperatures were underestimated because of changes in the Mg/Ca of Pliocene seawater (see next section for discussion of the Pliocene tropical Pacific and El Niño Southern Oscillation (ENSO)). It is important to note that WEP temperature reconstructions remain highly debated and no clear consensus has yet emerged within the palaeoceanographic community (see comments and counter comments on Zhang et al.53). This is perhaps unsurprising. Elevating atmospheric CO2 concentration to 400 p.p.m.v. (a 120-p.p.m. increase over pre-industrial) would create an additional radiative forcing capable of increasing tropical SSTs by 1–3 °C at most. Hence, the signal of change is small relative to the inherent uncertainties in SST reconstruction resulting in an unfavourable signal to noise ratio. Such scenarios of claim and counterclaim regarding tropical temperatures have been the subjects of significant discussion in other communities studying other time intervals. Overall, this highlights the need for further study, while at the same time anticipating divergent views, given the aforementioned signal to uncertainty ratio.
Besides documenting palaeoceanographic conditions during the mPWP, there have been many studies that focus on the terrestrial environment10,16,19. Work in the terrestrial realm is dependent on the heterogeneous distribution of localities where palaeoclimate signal carriers are preserved. Those outcrops and cores with suitable Pliocene chronology, or that contain continuous sequences, are few in comparison with the quantity of cores containing mPWP marine sediments retrieved by the International Ocean Discovery Program and its predecessors. Terrestrial proxies from near-shore marine cores allow for high-resolution continental–marine correlation of Pliocene palaeoclimate records (for example, refs 54, 55). Salzmann et al.16 summarized vegetation-based estimates of Pliocene (Piacenzian Stage) climate as being generally warmer and moister. Evergreen taiga, temperate forest and grasslands shifted northwards, which resulted in a reduction in tundra vegetation. Warm temperate forests spread in middle and Eastern Europe and tropical savannahs and woodland expanded in Africa and Australia, replacing deserts.
Arguably, the longest and most complete record of late-Pliocene high-latitude continental climate, including the mPWP, comes from Lake El’gygytgyn56, located in Northeast Arctic Russia in a basin formed ∼3.6 Ma by a meteorite impact. The many environmental proxies from the Lake El’gygytgyn core can be correlated to the LR04 stack and thus placed within the same chronostratigraphic framework as marine sequences (Fig. 2). The ability to correlate time series of terrestrial data with time series of marine data is rare in a Pliocene context because of the difficulties in assigning precise chronologies to most available terrestrial data. Lake El’gygytgyn records document polar amplification such as is seen in marine records57 and summer temperatures 8 °C warmer than present day, which persisted until ∼2.2 Ma. This supports other estimates of strong Arctic warming during parts of the late Pliocene, including the mPWP58.
Atmospheric concentration of CO2 during the Pliocene remains only partially constrained. A number of techniques exist to estimate CO2 (alkenones, B/Ca, δ11B, δ13C and leaf stomatal density), but the variability of estimates is high (Fig. 2). The majority of estimates indicate that CO2 concentration during the mPWP was higher than the pre-industrial; however, the increase above pre-industrial levels reconstructed from certain records is small and presents a challenge to attribute mPWP warmth to CO2 forcing alone3,5,6,7,50,59,60.
It is increasingly recognized that CO2 is just one agent of radiative forcing and that other greenhouse gases such as methane (CH4) are also important; however, these cannot be reconstructed at the current time for the Pliocene. Changes in continental features (including but not limited to orography and land cover) are also hypothesized to have increased long-term warmth. Furthermore, Unger and Yue61 have demonstrated the potential importance of atmospheric chemistry–climate feedbacks, as well as aerosols, in augmenting surface-temperature warming derived from a given increase in atmospheric CO2.
While palaeoenvironmental reconstructions have contributed greatly to understand the nature of the mPWP, the information available is insufficient to fully explain all aspects of the Earth’s climate during this time.
Palaeoclimate model simulations
Conceptual models of the Pliocene were first used to propose mechanisms and drivers of global and regional climate change demonstrated in proxy-based reconstructions62. For example, Crowley63 showed that the modest CO2 increase reconstructed for the mPWP was capable of producing a radiative forcing of ∼2 Wm−2, which may have been sufficient in explaining the warmth of the Pliocene globally, depending on the chosen Climate Sensitivity (the global mean temperature change in response to a given variation in atmospheric CO2 concentration). As discussed in the section above, such an approach could not explain the regional changes in reconstructed SST (based on planktonic foraminifera) that displayed little or no warming relative to present day in the tropics18,20. Therefore, an additional mechanism(s) working independently or combined with variations in CO2 concentrations in the atmosphere was required to drive and maintain the warmer conditions reconstructed for the mPWP63.
A likely additional driver of Pliocene warmth receiving attention in the early part of the 1990s, and still discussed today, is a change in ocean heat transport. This initially geologically driven hypothesis42 received further impetus from a conceptual modelling study published by Rind and Chandler62. Crowley63,64, based on a conceptual modelling framework, pointed out a paradox: a reduced latitudinal SST gradient implies potentially weaker atmospheric forcing of oceanic circulation, and hence weaker oceanic heat transport. Thus, the total benefit in terms of the ‘global net’ heat transport from enhanced ocean heat transport was lower than would otherwise be expected63. This early conceptually based finding has recently been supported by the investigation of Pliocene ocean circulation and heat transport behaviour in climate models65.
Arguably, the true benefits of the synergy between models and data were first realized in early fully numerical simulations of the mPWP climate using atmosphere-only General Circulation Models (AGCMs). Such models required monthly SSTs and sea ice, as well as vegetation cover, to be prescribed (boundary conditions). The PRISM palaeoenvironmental reconstruction provided the necessary data to underpin these boundary conditions that were held constant for the entire length of the model simulation. While this negated the possibility of examining atmosphere–ocean–vegetation feedbacks, it did provide a way to explore the response of the atmosphere, in isolation, to a given set of geological boundary conditions that at the time represented state-of-the-art knowledge about the mPWP. The first of these simulations used the PRISM0 reconstruction and focused on responses in the Northern Hemisphere22. Subsequent studies simulated the entire globe and used updated boundary conditions as more palaeoenvironmental information became available23,24. The current PRISM reconstruction (PRISM3D17) has been incorporated into a number of AGCMs as part of the Pliocene Model Intercomparison Project (PlioMIP; Box 3 and Figs 3 and 4).
With the evolution of the PRISM data sets and advances in modelling, AGCM simulations forced with PRISM boundary conditions enabled improvements in understanding the nature of the mPWP. AGCM simulations showed an increase in the global annual mean surface air temperature warming of 1.4–3.6 °C, relative to the pre-industrial11. Warming was greatest at high latitudes; consequently, the equator to pole temperature gradient decreased relative to modern. Surface air temperature increases were greatest in winter, as decreased snow and sea ice triggered a positive albedo temperature feedback. At low latitudes, temperatures were mostly unchanged, except for cooling over Northern Africa22,23,24. This model-predicted cooling was supported by palaeobotanical data and, in the simulations, was a response to a weakening and/or broadening of the Hadley Cell, which caused local subtropical clouds and evapotranspiration rates to increase. The hydrological cycle intensified, where regionally annual evaporation, rainfall and soil moisture all increased22,23,24.
Owing to the importance of potential ocean feedbacks on the climate that could not be simulated in AGCMs using prescribed SSTs (and the fact that prescribed SST experiments are often not in energy balance at the top of the atmosphere), modelling strategies quickly evolved to include a simplified slab ocean capable of predicting SST and sea-ice change. Atmosphere-slab ocean models were also employed to explore the sensitivity of Pliocene climate to atmospheric CO2 concentration (Chandler, unpublished data), as well as the sensitivity of climate predictions to orbital forcing66.
A major breakthrough was achieved through the use of fully coupled atmosphere–ocean General Circulation Models (AOGCMs), where the full three-dimensional response of the oceans was, for the first time, predicted. This milestone changed the relationship between models and marine data and moved the use of marine data away from providing model boundary conditions and towards providing verification data for model evaluation. For the first time, researchers explored the relative role of the atmosphere, oceans and cryosphere in contributing towards Pliocene warmth67. In contrast to AGCM experiments, and available geological archives, surface temperatures warmed across the globe, including in the tropics. Analysis of the predicted ocean circulation indicated reduced outflow of Antarctic bottom water, a shallower depth for North Atlantic deep-water formation and slightly weaker thermohaline circulation. Neither the oceans nor the atmosphere transported significantly more heat in the Pliocene scenario, and a significant driver of warmth was the reduced extent of high-latitude terrestrial ice sheets and sea-ice cover, resulting in a strong ice albedo temperature feedback67. This result countered the then-predominant view based on the geological record that there was an increase in ocean heat transport during the mPWP42.
Increasing utilization of AOGCMs unquestionably represented a paradigm shift in climate modelling for the mPWP and underpinned a host of further applications exploring, for example, the sensitivity of climate to greenhouse gas concentrations68,69,70,71, the importance of ocean gateways and ocean bathymetry72,73,74,75, Climate Sensitivity and longer-term sensitivity—Earth System Sensitivity60, the importance of uncertainties in model parameterization76,77, as well as detailed studies exploring the importance of individual boundary conditions in driving the warmth and polar amplification78. These individual studies enhanced our understanding of the mPWP. It is additionally important to understand the degree to which model predictions may differ. To this end, the PlioMIP was initiated in 2008 (Box 3). This provided the framework for multiple models to undertake an experiment with the same boundary conditions and has been a major driver in developing the relationship between data and models (see section on data/model comparison).
In addition, Earth System Models (models capable of including a variety of additional Earth system processes) are allowing entirely new components of the Pliocene climate system to be explored. They present their own unique challenges in terms of providing adequate geological constraints for the models. Earth System components have included interactive vegetation, allowing vegetation/climate feedbacks to be incorporated within simulations (for example, ref. 79).
Ice sheet models are now being used to better understand the validity of ice sheet reconstructions used in climate models13,80,81,82. Geological evidence suggests that the sea level could have been ∼20 m higher than present day during the mPWP15,83,84,85, which implies that there would likely have been a reduction in the size of the Greenland, West Antarctic and potentially the East Antarctic ice sheets. Proximal evidence for ice sheet size86,87 is too sparse around the ice sheet margins to enable detailed reconstructions of the extent of the major ice sheets. Therefore, our current understanding of plausible mPWP ice sheet extents is based on predictions using climate-forcing from a single climate model to force an offline ice sheet model (for example, refs 13, 88, 89, 90, 91, 92, 93, 94, 95). The multitude of reconstructions for mPWP ice sheets has highlighted the key areas of model disagreement. One example surrounding predictions of the East Antarctic ice sheet has sparked much debate, as some results indicate a modern grounding line88, while others imply more wide-scale retreat13,96. There is a general lack of evidence to provide constraints for mPWP ice sheet modelling, although there are interesting new data for the Pliocene, indicating a dynamic behaviour at the margins of East Antarctica12 and also thickening of the Antarctic interior97.
It is important to quantify the extent to which model predictions for ice sheets in the mPWP differ and as such the period has been used as a test bed for understanding the model dependency of ice sheet predictions during a warm interval in Earth History. Results from the Pliocene Ice Sheet Model Intercomparison Project (PLISMIP98) have shown that simulations using the same climate-forcing fields but different ice sheet models are relatively similar over Greenland93; however, the predicted details of ice configuration over West Antarctica and the subglacial basins of East Antarctica can differ99. A priori assumptions necessary to initiate a climate model (for example, ice configuration) and also the choice of model have the largest impact on the simulated Greenland ice sheet for the mPWP81,93. Important steps towards understanding model dependency have been made, and this has informed future iterations of palaeogeographic boundary conditions for PlioMIP Phase 2 (ref. 100). Using a compilation from the PLISMIP results and taking into account available geological constraints, the latest Pliocene palaeogeography contains ice sheet configurations where there is highest confidence in the possibility of ice presence during the warmest parts of the Pliocene. The PRISM4 palaeogeography is more internally consistent than the previous PRISM3 topographic reconstruction101 as it also takes into account the glacial isostatic response of loading specific Pliocene ice sheets (for example, ref. 102) and includes components such as the contribution of dynamic topography caused by changes in the mantle flow (for example, ref. 103).
Earth System Models incorporating representations of atmospheric chemistry are being used to simulate the effects of altered vegetation patterns on dust and aerosol emissions and the radiative forcing of such agents that have little or no expression within geological archives. For example, Unger and Yue101 calculated terrestrial ecosystem emissions and atmospheric chemical composition for the mPWP and the pre-industrial era. Tropospheric ozone and aerosol precursors from vegetation and wildfire were ∼50% and ∼100% higher in the mPWP because of the spread of the tropical savanna and deciduous biomes, respectively. The chemistry–climate feedbacks contributed to a net global warming that is +30–250% of the carbon dioxide effect, and a net aerosol global cooling masked 15–100% of the carbon dioxide effect. Although an exciting development, this realization presents a huge challenge to the palaeoclimate data community to develop proxies for atmospheric chemistry and aerosols. Such studies highlight the emergence of new unknowns in terms of atmospheric forcing in the Pliocene that are potentially more important than the currently known uncertainty in CO2 forcing, which from a modelling point of view can be investigated through CO2 sensitivity experiments.
Rapid progress has been made since the emergence of palaeoclimate model simulations for the mPWP. Models have incorporated geological data in the form of boundary conditions, but have also been used in isolation to understand particular climate mechanisms. We suggest that modelling results are most powerful when they are constrained by geological data.
When performing any kind of climate model simulation, it is important that the model be compared and evaluated against available data. Where data and models agree on the degree of temperature change (for example), there can be more confidence in the performance of that model. The utilization of AOGCMs in the context of the mPWP rapidly transformed the role of geological archives of surface temperature from providing model boundary conditions to providing the means to independently evaluate model performance. This was an important step as it facilitated a new way to use the Pliocene to evaluate the same models that are used to predict future climate change (Fig. 5).
To date, all mPWP data/model comparisons have used surface-temperature data from the PRISM palaeoenvironmental reconstructions. These data, representative of a time slab, have been compared with equilibrium (snapshot style) climate model simulations (for example, refs 9, 10, 11, 41, 57, 67). Published data/model comparisons for the mPWP have identified many regions of agreement between data and model predictions, such as in the Southern Ocean (for example, ref. 11; Fig. 5). They have highlighted potential inconsistencies between data and models in the tropics, where models may predict surface temperatures that are too warm compared with data11,16,50,104,105 (Fig. 5). Comparison with SSTs has suggested that the magnitude of warming predicted by models in the North Atlantic may be insufficient10,57, and that polar amplification may be too weak10,57,58 (Fig. 5). As discussed in Box 1, the averaging of geological ‘interglacial’ climate signals across the mPWP makes these initial observations regarding model performance unclear.
At present, an assessment of suggested model shortcomings against uncertainties in the interpretation of surface-temperature records from geological data can only conclude that the implications of these patterns of data/model discord remain uncertain, and there are several reasons to support this view.
PlioMIP has shown a substantial spread in model predictions (Box 3). Therefore, previous studies that have analysed the performance of a single model and have suggested that data/model comparison is able to demonstrate a structural weakness in climate models may be too simplistic11. Forcings and model experimental design are at best incomplete, or at worst incorrect. This covers an uncertainty in the agents of radiative forcing (including atmospheric greenhouse gas composition, chemistry/climate feedbacks)61, ice sheet configuration81 and the likelihood that similarities drawn between modern and mPWP topography, drainage and bathymetry are overstated. Finally, the interpretation of surface-temperature patterns derived from geological archives are evolving (for example, refs 52, 53; Box 1).
The current debate regarding mPWP (and Pliocene in general) stability of tropical SSTs is a key illustration of this point. Recent re-evaluations of the Mg/Ca data incorporate the effects of changing concentrations of Mg/Ca in the water column through time. This, as well as the application of a newer proxy (TEX86), has indicated that surface ocean temperatures in the WEP warm pool may have been 1–2 °C higher than modern52. If true, this would effectively resolve the mismatch between tropical Pacific Ocean temperature data and predictions of AOGCMs for the mPWP52 (Fig. 5).
We have learned much about the environment of the mPWP and our ability to reproduce it with climate models. Data/model comparison is complex and requires a full and open discussion of (a) the inherent strengths and weaknesses of climate models, (b) uncertainties in geological boundary conditions used within models to facilitate simulations of the mPWP and (c) uncertainties in the geological archives and their interpretation. A key challenge for the future is to quantify and reduce uncertainty in both palaeoenvironmental reconstruction and climate modelling. In this way, the mPWP can achieve its potential in terms of informing us about processes and the key mechanisms associated with global warming, and will be better placed to inform us about the likely long-term environmental and climate effects of higher than pre-industrial concentrations of atmospheric CO2 (through more accurate assessments of Climate and Earth System Sensitivity).
We have provided evidence that synthesis of observations and models has enhanced understanding of the mPWP. We also maintain that one of the fundamental lessons from previous data/model comparisons (see Box 1) is the need to make palaeoenvironmental reconstructions and climate model simulations more consistent in time.
Our ability to correlate and date multiple marine records using the LR04 timescale has limits. There is uncertainty in correlation of particular events (for example, Marine Isotope Stages) primarily because of the character of the local isotopic record and the assumption of linear sedimentation rates. In addition, ice sheet response times, tuning errors and uncertainty in the Laskar106 orbital solution are all potential sources of error. Thus, near 3.0 Ma temporal uncertainty could be as much as 6–15 ky (ref. 29). Global average sediment accumulation rates vary, on average, between 3 and 5 cm ky−1. Bioturbation effect (mixing of sediment due to biologic activity) generally ranges between 4 and 8 cm depth from the sediment–water interface. Consequently, the benthic δ18O signal (and any other palaeoclimate signal recorded in deep-ocean sediments) is time-averaged and temporal homogenization could range from 0.8 to 2.5 ky.
Terrestrial sequences are generally more difficult to date. Age determination relies on the presence of materials compatible with isotopic dating systems, magnetic reversals and/or faunal and floral zonations calibrated to age. Lake settings sometimes show near continuous sedimentation, and geophysical logs (for example, magnetic susceptibility) can often be tuned to orbital forcing, providing an age model as accurate as the marine records, allowing direct marine–terrestrial correlation. These records are generally scarce, and the terrestrial realm is in all but a few unique sedimentary settings not going to be as completely reconstructed as the marine palaeoenvironment. Thus, terrestrial reconstructions are going to carry a greater degree of diachrony than marine reconstructions.
A recent study107 demonstrated that orbitally forced changes in surface air temperature during interglacial events within the mPWP can be substantial and differ from one interglacial to another. Thus, uncertainties in correlation could easily contribute to patterns of apparent data/model disagreement. This is especially likely if geological archives (for example, the higher latitudes) preserve a growing season signal rather than the mean annual temperature (discussed in palaeoenvironmental reconstruction section). Climate model results indicate that peak surface temperatures associated with MIS KM5c and K1 interglacials were not globally synchronous, highlighting leads and lags in temperature in different regions. Furthermore, variability of surface temperature ±20 kyr surrounding MIS KM5c was 2–3 °C, but for K1 locally exceeded 5 °C. This indicates that the choice of the time interval is critical to the potential success of data/model comparison (Fig. 6).
The development of high-resolution proxy data time series within the mPWP (see Box 1) is an important step in characterizing climate variability at a local level over orbital timescales. Recognition and careful evaluation of stratigraphic factors described above will be necessary to objectively choose those marine sequences that can be confidently correlated to events such as KM5c. Performing sensitivity experiments with climate models, in which characteristics of orbital forcing are changed appropriately to any given time point, will be important in examining patterns of climate change recorded in geological time series. With complex and more computationally demanding climate models, this is likely to take the form of a series of snapshot-style experiments where the orbital forcing is varied appropriately to the time point in question and run to equilibrium. Another approach towards characterizing mPWP climate variability is to use computationally efficient, although lower (spatial) resolution-transient simulations. Experiments with time-dependent orbital forcing as well as dynamic ice sheets and vegetation108 provide estimates of the mean annual global warming and insight into feedbacks.
Not every warm peak within the mPWP has equal relevance in understanding future climate change, since specific warm intervals ‘interglacials’ occurred under conditions of orbital forcing, unlike today. Therefore, it is important to either separate out the effect of orbital forcing on Climate Sensitivity or target a time period in which the orbital configuration is similar to modern within the mPWP. In the context of longer-term Climate Sensitivity (Earth System Sensitivity11,108,109), we must acknowledge that the effect of prior orbital forcing would continue to be present in parts of the Earth system, such as the ice sheets and deep-ocean temperatures because of their response times and memory effects.
Climate modelling is enabling the mPWP community to consider, in a more robust way, new intervals for data acquisition and reconstruction, at the same time narrowing the relevant time window. In the near future, models and data will be more ‘time consistent’, meaning that models can be given more appropriate forcings to better represent the narrower time interval being reconstructed by geologists110. This means that orbitally induced surface-temperature variability will have a reduced potential to bias data/model comparisons. Even so, limitations in correlation will continue and climate variability at suborbital timescales will remain an important factor.
In the future, the integration of mPWP data and climate model simulations will be enhanced by (1) establishing a more precise chronology of the proxy data, (2) creating holistic regional and locality-based palaeoenvironmental reconstructions, which can be compared directly to simulated environments produced through proxy-modelling components (for example, isotope-enabled AOGCMs, predictive plankton and vegetation models and so on) of Earth System models, (3) providing climate models with boundary conditions that are more consistent with the intervals of time studied for environmental reconstruction (including more confident greenhouse gas-forcing calculations) and (4) producing climate ensembles and transient climate simulations that more adequately capture orbital and environmental variability around any studied interval of the mPWP.
How to cite this article: Haywood, A. M. et al. Integrating geological archives and climate models for the mid-Pliocene warm period. Nat. Commun. 7:10646 doi: 10.1038/ncomms10646 (2016).
IPCC. Climate Change 2013: The Physical Science Basis Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change (eds Stocker T. F.et al. 1535Cambridge University Press (2013).
Valdes, P. Built for stability. Nat. Geosci. 4, 414–416 (2011).
Raymo, M., Grant, B., Horowitz, M. & Rau, G. Mid-Pliocene warmth: stronger greenhouse and stronger conveyor. Mar. Micropaleontol. 27, 313–326 (1996).
Kürschner, W. M., van der Burgh, J., Visscher, H. & Dilcher, D. L. Oak leaves as biosensors of late Neogene and early Pleistocene paleoatmospheric CO2 concentrations. Mar. Micropaleontol. 27, 299–312 (1996).
Seki, O. et al. Alkenone and boron-based Pliocene pCO2 records. Earth Planet. Sci. Lett. 292, 201–211 (2010).
Pagani, M., Liu, Z., LaRiviere, J. & Ravelo, A. C. High Earth-system climate sensitivity determined from Pliocene carbon dioxide concentrations. Nat. Geosci. 3, 27–30 (2010).
Bartoli, G., Honisch, B. R. & Zeebe, R. E. Atmospheric CO2 decline during the Pliocene intensification of Northern Hemisphere glaciations. Paleoceanography 26, PA4213 (2011).
Badger, M. P. S., Schmidt, D. N., Mackensen, A. & Pancost, R. D. High resolution alkenone palaeobarometry indicates relatively stable pCO2 during the Pliocene (3.3 to 2.8 Ma). Philos. Trans. A Math. Phys. Eng. Sci. 371, 20130094 (2013).
Dowsett, H. J. et al. Assessing confidence in Pliocene sea surface temperatures to evaluate predictive models. Nat. Climate Change 2, 365–371 (2012).
Salzmann, U. et al. Challenges in reconstructing terrestrial warming of the Pliocene revealed by data-model discord. Nat. Climate Change 3, 969–974 (2013).
Haywood, A. M. et al. Large-scale features of Pliocene climate: results from the Pliocene Model Intercomparison Project. Clim. Past 9, 191–209 (2013) Summary of the outcomes from the first co-ordinated model intercomparison project for the Pliocene .
Cook, C. P. et al. Sea surface temperature control on the distribution of far-traveled Southern Ocean ice-rafted detritus during the Pliocene. Paleoceanography 29, 533–548 (2014).
Dolan, A. M. et al. Sensitivity of Pliocene ice sheets to orbital forcing. Palaeogeogr. Palaeoclimatol. Palaeoecol. 309, 98–110 (2011).
Dowsett, H. J. & Cronin, T. M. High eustatic sea level during the middle Pliocene: evidence from the southeastern U.S. Atlantic Coastal Plain. Geology 18, 435–438 (1990).
Miller, K. G. et al. High tide of the warm Pliocene: implications of global sea level for Antarctic deglaciation. Geology 40, 407–410 (2012).
Salzmann, U., Haywood, A. M., Lunt, D. J., Valdes, P. J. & Hill, D. J. A new global biome reconstruction and data-model comparison for the Middle Pliocene. Global Ecol. Biogeogr. 17, 432–447 (2008).
Dowsett, H. et al. The PRISM3D paleoenvironmental reconstruction. Stratigraphy 7, 123–139 (2010).
Dowsett, H., Barron, J. & Poore, R. Middle Pliocene sea surface temperatures: a global reconstruction. Mar. Micropaleontol. 27, 13–25 (1996) First global scale syntheses of mid Pliocene sea surface temperature .
Thompson, R. S. & Fleming, R. F. Middle Pliocene vegetation: reconstructions, paleoclimatic inferences, and boundary conditions for climatic modeling. Mar. Micropaleontol. 27, 13–26 (1996) First global scale syntheses of mid Pliocene vegetation .
Dowsett, H. J. et al. Middle Pliocene Pal eoenvironmental Reconstruction: PRISM 2. Open File Report 99–535 (U.S. Geological Survey, Reston, VA, USA 1999).
Dowsett, H. J. in Deep-time Perspectives on Climate Change: Marrying the Signal from Computer Models and Biological Proxies eds Williams M., Haywood A. M., Gregory J., Schmidt D. N. 459–480Micropalaeontological Society (Special Publication)), Geological Society of London (2007).
Chandler, M., Rind, D. & Thompson, R. Joint investigations of the middle Pliocene climate II: GISS GCM Northern Hemisphere results. Glob. Planet. Change 9, 197–219 (1994) The first use of PRISM boundary conditions in a model simulation .
Sloan, L. C., Crowley, T. J. & Pollard, D. Modeling of middle Pliocene climate with the NCAR GENESIS general circulation model. Mar. Micropaleontol. 27, 51–61 (1996).
Haywood, A. M., Valdes, P. J. & Sellwood, B. W. Global scale palaeoclimate reconstruction of the middle Pliocene climate using the UKMO GCM: initial results. Glob. Planet. Change 25, 239–256 (2000).
Zubakov, V. A. & Borzenkova, I. I. Pliocene palaeoclimates: past climates as possible analogues of mid-twenty-first century climate. Palaeogeogr. Palaeoclimatol. Palaeoecol. 65, 35–49 (1988) Early discussion of Pliocene climates as an analog for future climate conditions .
CLIMAP. The surface of the ice-age Earth. Science 191, 1131–1137 (1976).
Emiliani, C. Pleistocene temperature. J. Geol. 63, 538–578 (1955).
Shackleton, N. J., Hall, M. A. & Pate, D. Pliocene stable isotope stratigraphy of Site 846. Proceedings of the Ocean Drilling Program, Scientific Results 138, 337–355 (1995).
Lisiecki, L. E. & Raymo, M. E. A Pliocene-Pleistocene stack of 57 globally distributed benthic δ18O records. Paleoceanography 20, PA1003 (2005) Seminal contribution providing a chronologic framework within which Pliocene palaeoceanographic sequences could be compared .
Lea, D. W., Mashiotta, T. A. & Spero, H. J. Controls on magnesium and strontium uptake in planktonic foraminifera determined by live culturing. Geochim. Cosmochim. Acta 63, 2369–2379 (1999).
Barker, S. & Elderfield, H. Foraminiferal Calcification response to glacial-interglacial changes in atmospheric CO2 . Science 297, 833–836 (2002).
Rosenthal, Y., Lohmann, G. P., Lohmann, K. C. & Sherrell, R. M. Incorporation and preservation of Mg in Globigerinoides sacculifer: implications for reconstructing the temperature and 18O/16O of seawater. Paleoceanography 15, 135–145 (2000).
Imbrie, J. & Kipp, N. G. in The Late Cenozoic Glacial Ages Vol. 3, (ed. Truekian, K. K.) 71–181Yale University (1971) The factor analytic method of temperature reconstruction which was the basis for the CLIMAP initiative .
Dowsett, H. J. & Poore, R. Z. A new planktic foraminifer transfer function for estimating Pliocene—Holocene paleoceanographic conditions in the North Atlantic. Mar. Micropaleontol. 16, 1–23 (1990).
Dowsett, H. J. & Poore, R. Z. Pliocene sea surface temperatures of the North Atlantic Ocean at 3.0 Ma. Quat. Sci. Rev. 10, 189–204 (1991).
Sachs, J. P., Pahnke, K., Smittenberg, R. & Zhang, Z. Biomarker Indicators of Past Climate. in Encyclopedia of Quaternary Science 2nd edn (eds Elias, S., Mock C.) 775–779 (Elsevier Science, 2013).
Volkman, J. K., Eglinton, G., Corner, E. D. & Forsberg, T. Long-chain alkenes and alkenones in the marine coccolithophorid Emiliania huxleyi. Phytochemistry 19, 2619–2622 (1980).
Conte, M. H., Thompson, A. & Eglinton, G. Primary production of lipid biomarker compounds by Emiliania huxleyi: results from an experimental mesocosm study in fjords of southern Norway. Sarsia 79, 319–332 (1994).
Prahl, F. G., Muehlhausen, L. A. & Zahnle, D. L. Further evaluation of long-chain alkenones as indicators of paleoceanographic conditions. Geochim. Cosmochim. Acta 52, 2303–2310 (1988).
Müller, P. J., Kirst, G., Ruhland, G., von Storch, I. & Rosell-Melé, A. Calibration of the alkenone paleotemperature index based on core-tops from the eastern South Atlantic and the global ocean (60° N-60° S). Geochim. Cosmochim. Acta 62, 1757–1772 (1998).
Dowsett, H. J. et al. Sea surface temperatures of the mid-Piacenzian warm period: a comparison of PRISM3 and HadCM3. Palaeogeogr. Palaeoclimatol. Palaeoecol. 309, 83–91 (2011).
Dowsett, H. J. et al. Micropaleontological evidence for increased meridional heat transport in the North Atlantic Ocean during the Pliocene. Science 258, 1133–1135 (1992).
Groeneveld, J. Effect of the Pliocene Closure of the Panamanian Gateway on Caribbean and East Pacific Sea Surface Temperatures and Salinities by Applying Combined Mg/Ca and δ18O Measurements (5.6-2.2 Ma) (PhD thesis, Univ. Kiel, (2005).
Herbert, T. D., Peterson, L. C., Lawrence, K. T. & Liu, Z. Tropical ocean temperatures over the past 3.5 million years. Science 328, 1530–1534 (2010).
Sarnthein, M. et al. Mid-Pliocene shifts in ocean overturning circulation and the onset of Quaternary-style climates. Clim. Past 5, 269–283 (2009).
Lawrence, K. T., Sosdian, S., White, H. E. & Rosenthal, Y. North Atlantic climate evolution through the Plio-Pleistocene climate transitions. Earth Planet. Sci. Lett. 300, 329–342 (2010).
Barron, J. A. Diatom constraints on the position of the Antarctic Polar Front in the middle part of the Pliocene. Mar. Micropaleontol. 27, 195–213 (1996).
Dowsett, H. J. Faunal re-evaluation of Mid-Pliocene conditions in the western equatorial Pacific. Micropaleontology 53, 447–456 (2007).
Van Der Burgh, J., Visscher, H., Dilcher, D. & Kurschner, M. Paleoatmospheric signatures in Neogene fossil leaves. Science 260, 1788–1790 (1993).
Fedorov, A. et al. Patterns and mechanisms of early Pliocene warmth. Nature 496, 43–49 (2013).
Wara, M. W., Ravelo, A. C. & Delaney, M. L. Permanent El Niño-like conditions during the Pliocene warm period. Science 309, 758–761 (2005) Established the concept of permanent El Niño conditions during the Pliocene .
O'Brien, C. L. et al. High sea surface temperatures in tropical warm pools during the Pliocene. Nat. Geosci. 7, 606–611 (2014).
Zhang, Y. G., Pagani, M. & Liu, Z. A 12-million-year temperature history of the Tropical Pacific Ocean. Science 344, 84–87 (2014).
Rea, D. K., Snoeck, H. & Joseph, L. H. Late Cenozoic eolian deposition in the North Pacific: Asian drying, Tibetan uplift, and cooling of the Northern Hemisphere. Paleoceanography 13, 215–224 (1998).
deMenocal, P. B. African climate change and faunal evolution during the Pliocene-Pleistocene. Earth Planet. Sci. Lett. 220, 3–24 (2004).
Brigham-Grette, J. et al. Pliocene warmth, polar amplification, and stepped Pleistocene cooling recorded in NE Arctic Russia. Science 340, 1421–1427 (2013) A unique high resolution record of Pliocene-Pleistocene terrestrial palaeoclimate conditions .
Dowsett, H. J. et al. Sea surface temperature of the mid-Piacenzian ocean: a data-model comparison. Sci. Rep. 3, 1–8 (2013).
Ballantyne, A. P. et al. Significantly warmer Arctic surface temperatures during the Pliocene indicated by multiple independent proxies. Geology 38, 603–606 (2010).
Tripati, A. K., Roberts, C. D. & Eagle, R. A. Coupling of CO2 and ice sheet stability over major climate transitions of the last 20 million years. Science 326, 1394–1397 (2009).
Lunt, D. J. et al. Earth system sensitivity inferred from Pliocene modelling and data. Nat. Geosci. 3, 60–64 (2010) First constraint on Pliocene Earth System Sensitivity .
Unger, N. & Yue, X. Strong chemistry-climate feedback in the Pliocene. Geophys. Res. Lett. 41, 527–533 (2014).
Rind, D. & Chandler, M. A. Increased ocean heat transports and warmer climate. J. Geophys. Res. 96, 7437–7461 (1991).
Crowley, T. J. Pliocene climates: the nature of the problem. Mar. Micropaleontol. 27, 3–12 (1996).
Crowley, T. J. Modeling Pliocene warmth. Quat. Sci. Rev. 10, 272–282 (1991).
Zhang, Z.-S. et al. Mid-pliocene Atlantic meridional overturning circulation not unlike modern. Clim. Past 9, 1495–1504 (2013) Multi-model assessment of ocean and thermohaline circulation behaviour during the mid-Pliocene .
Haywood, A. M., Valdes, P. J. & Sellwood, B. W. Magnitude of climate variability during middle Pliocene warmth: a palaeoclimate modelling study. Palaeogeogr. Palaeoclimatol. Palaeoecol. 188, 1–24 (2002).
Haywood, A. M. & Valdes, P. J. Modelling Pliocene warmth: contribution of atmosphere, oceans and cryosphere. Earth Planet. Sci. Lett. 218, 363–377 (2004) First simulation of Pliocene climate using a coupled ocean-atmosphere GCM .
Haywood, A. M. et al. Are there pre-Quaternary geological analogues for a future greenhouse gas-induced global warming? Philos. Trans. R Soc. Lond. A 369, 933–956 (2011).
Hill, D. J., Csank, A. Z., Dolan, A. M. & Lunt, D. J. Pliocene climate variability: Northern annular mode in models and tree-ring data. Palaeogeogr. Palaeoclimatol. Palaeoecol. 309, 118–127 (2011).
Bonham, S. G., Haywood, A. M., Lunt, D. J., Collins, M. & Salzmann, U. El Niño-Southern Oscillation, Pliocene climate and equifinality. Philos. Trans. A Math. Phys. Eng. Sci. 367, 127–156 (2009).
Brierley, C. M. Interannual climate variability seen in the Pliocene Model Intercomparison Project. Clim. Past 11, 605–618 (2015).
Lunt, D. J., Valdes, P. J., Haywood, A. & Rutt, I. C. Closure of the Panama Seaway during the Pliocene: implications for climate and Northern Hemisphere glaciation. Clim. Dyn. 30, 1–18 (2008).
Karas, C., Nürnberg, D., Tiedemann, R. & Garbe-Schönberg, D. Pliocene climate change of the Southwest Pacific and the impact of ocean gateways. Earth Planet. Sci. Lett. 301, 117–124 (2011).
Schneider, B. & Schmittner, A. Simulating the impact of the Panamanian seaway closure on ocean circulation, marine productivity and nutrient cycling. Earth Planet. Sci. Lett. 246, 367–380 (2006).
Robinson, M. M. et al. Bathymetric controls on Pliocene North Atlantic and Arctic sea surface temperature and deepwater production. Palaeogeogr. Palaeoclimatol. Palaeoecol. 309, 92–97 (2011).
Pope, J. O. et al. Quantifying uncertainty in model predictions for the Pliocene (Plio-QUMP): initial results. Palaeogeogr. Palaeoclimatol. Palaeoecol. 309, 128–140 (2011).
Howell, F. W. et al. Can uncertainties in sea ice albedo reconcile patterns of data-model discord for the Pliocene and 20th/21st centuries? Geophys. Res. Lett. 41, 2011–2018 (2014).
Lunt, D. J. et al. On the causes of mid-Pliocene warmth and polar amplification. Earth. Planet. Sci. Lett. 321-322, 128–138 (2012).
Haywood, A. M. & Valdes, P. J. Vegetation cover in a warmer world simulated using a dynamic global vegetation model for the Mid-Pliocene. Palaeogeogr. Palaeoclimatol. Palaeoecol. 237, 412–427 (2006).
Hill, D. J., Haywood, A. M., Hindmarsh, R. C. A. & Valdes, P. J. in Deep Time Perspectives on Climate Change: Marrying the Signals from Computer Models and Biological Proxies eds Williams M., Haywood A. M., Gregory D., Schmidt D. N. 517–538Micropalaeontological Society, Special Publication, Geological Society of London (2007).
Dolan, A. M. et al. Using results from the PlioMIP ensemble to investigate the Greenland Ice Sheet during the mid-Pliocene Warm Period. Clim. Past. 11, 403–424 (2015).
Naish, T. R. & Wilson, G. S. Constraints on the amplitude of Mid-Pliocene (3.6–2.4 Ma) eustatic sea-level fluctuations from the New Zealand shallow-marine sediment record. Philos. Trans. A Math. Phys. Eng. Sci. 367, 169–187 (2009).
Masson-Delmotte, V. et al. in: Climate Change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change (eds Stocker T. F.et al. 383–464Cambridge University Press (2013).
Rovere, A. et al. The Mid-Pliocene sea-level conundrum: glacial isostasy, eustasy and dynamic topography. Earth Planet. Sci. Lett. 387, 27–33 (2014).
Rohling, E. J. et al. Sea-level and deep-sea temperature variability over the past 5.3 million years. Nature 508, 477–482 (2014).
Funder, S. et al. Late Pliocene Greenland—The Kap København Formation in North Greenland. Bull. Geol. Soc. Den. 48, 117–134 (2001).
Bennike, O. et al. A multi-proxy study of Pliocene sediments from Île de France, North-East Greenland. Palaeogeogr. Palaeoclimatol. Palaeoecol. 186, 1–23 (2002).
Pollard, D. & DeConto, R. M. Modelling West Antarctic ice sheet growth and collapse through the past five million years. Nature 458, 329–332 (2009).
Lunt, D. J., Haywood, A. M., Foster, G. L. & Stone, E. J. The Arctic cryosphere in the Mid-Pliocene and the future. Philos. Trans. R Soc. A 367, 49–67 (2009).
Hill, D. J., Dolan, A. M., Haywood, A. M., Hunter, S. J. & Stoll, D. K. Sensitivity of the Greenland Ice Sheet to Pliocene sea surface temperatures. Stratigraphy 7, 111–122 (2010).
Koenig, S., DeConto, R. & Pollard, D. Late Pliocene to Pleistocene sensitivity of the Greenland Ice Sheet in response to external forcing and internal feedbacks. Clim. Dyn. 37, 1247–1268 (2011).
Koenig, S. J., DeConto, R. M. & Pollard, D. Impact of reduced Arctic sea ice on Greenland ice sheet variability in a warmer than present climate. Geophys. Res. Lett. 41, 3933–3942 (2014).
Koenig, S. J. et al. Ice sheet model dependency of the simulated Greenland Ice Sheet in the mid-Pliocene. Clim. Past. 11, 369–381 (2015).
Contoux, C., Dumas, C., Ramstein, G., Jost, A. & Dolan, A. M. Modelling Greenland ice sheet inception and sustainability during the Late Pliocene. Earth Planet. Sci. Lett. 424, 295–305 (2015).
Yan, Q., Zhang, Z., Wang, H. & Zhang, R. Simulation of Greenland ice sheet during the mid-Pliocene warm period. Chin. Sci. Bull. 59, 201–211 (2014).
Hill, D. J., Haywood, A. M., Hindmarsh, R. C. M. & Valdes, P. J. in Deep-Time Perspectives on Climate Change: Marrying the Signal from Computer Models and Biological Proxies eds Williams M., Haywood A. M., Gregory F. J., Schmidt D. N. 517–538The Micropalaeontological Society, Special Publications, The Geological Society (2007).
Yamane, M. et al. Exposure age and ice-sheet model constraints on Pliocene East Antarctic ice sheet dynamics. Nat. Commun. 6, 7016 (2015).
Dolan, A. M., Koenig, S. J., Hill, D. J., Haywood, A. M. & DeConto, R. M. Pliocene Ice Sheet Modelling Intercomparison Project (PLISMIP)—experimental design. Geosci. Model Dev. 5, 963–974 (2012).
de Boer, B. et al. Simulating the Antarctic ice sheet in the Late-Pliocene warm period: PLISMIP-ANT, an ice-sheet model intercomparison project. Cryosphere 9, 881–903 (2015).
Haywood, A. M. et al. Pliocene Model Intercomparison (PlioMIP) Phase 2: scientific objectives and experimental design. Clim. Past Disc. 11, 4003–4038 (2015).
Sohl, L. E. et al. PRISM3/GISS Topographic Reconstru ction. Geological Survey Data Series 419, 6 (U.S. Geological Survey, Reston, Virginia, USA, 2009).
Raymo, M. E., Mitrovica, J. X., O/'Leary, M. J., DeConto, R. M. & Hearty, P. J. Departures from eustasy in Pliocene sea-level records. Nat. Geosci. 4, 328–332 (2011).
Rowley, D. B. et al. Dynamic topography change of the Eastern United States since three million years ago. Science 340, 1560–1563 (2013).
Haywood, A. M., Dekens, P., Ravelo, A. C. & Williams, M. Warmer tropics during the mid-Pliocene? Evidence from alkenone paleothermometry and a fully coupled ocean-atmosphere GCM. Geochem. Geophys. Geosyst. 6, Q03010 (2005).
Dowsett, H. J. & Robinson, M. M. Mid-Pliocene equatorial Pacific sea surface temperature reconstruction: a multi-proxy perspective. Philos. Trans. A Math. Phys. Eng. Sci. 367, 109–125 (2009).
Laskar, J. et al. A long-term numerical solution for the insolation quantities of the Earth. Astron. Astrophys. 428, 261–285 (2004).
Prescott, C. L. et al. Assessing orbitally-forced interglacial climate variability during the mid-Pliocene Warm Period. Earth Planet. Sci. Lett. 400, 261–271 (2014).
Willeit, M., Ganopolski, A. & Feulner, G. On the effect of orbital forcing on mid-Pliocene climate, vegetation and ice sheets. Clim. Past 9, 1749–1759 (2013).
Martínez-Botí, M. A. et al. Plio-Pleistocene climate sensitivity evaluated using high-resolution CO2 records. Nature 518, 49–54 (2015).
Haywood, A. M. et al. On the identification of a Pliocene time slice for data-model comparison. Philos. Trans. A Math. Phys. Eng. Sci. 371, 20120515 (2013).
Haug, G., Tiedemann, R., Zahn, R. & Ravelo, A. Role of Panama uplift on oceanic freshwater balance. Geology 29, 207–210 (2001).
Dowsett, H. J. et al. Joint investigations of the Middle Pliocene climate I: PRISM paleoenvironmental reconstructions. Global Planet. Change 9, 169–195 (1994).
Rosenbloom, N. A., Otto-Bliesner, B. L., Brady, E. C. & Lawrence, P. J. Simulating the mid-Pliocene Warm Period with the CCSM4 model. Geosci. Model Dev. 6, 549–561 (2013).
Dowsett, H. J., Robinson, M. M. & Foley, K. M. Pliocene three-dimensional global ocean temperature reconstruction. Clim. Past 5, 769–783 (2009).
Dowsett, H. J. et al. The PRISM (Pliocene Palaeoclimate) reconstruction: time for a paradigm shift. Philos. Trans. R Soc. 371, 20120524 (2013).
Fedorov, A. V., Burls, N. J., Lawrence, K. T. & Peterson, L. C. Tightly linked zonal and meridional sea surface temperature gradients over the past five million years. Nat. Geosci. 8, 975–980 (2015) Discusses changes to zonal temperature gradients in the tropical Pacific, Walker circulation, ENSO and climate dynamics .
Hill, D. J. et al. Evaluating the dominant components of warming in Pliocene climate simulations. Clim. Past 10, 79–90 (2014).
H.J.D. acknowledges support from the US Geological Survey Climate and Land Use Change Research and Development Program and the John Wesley Powell Center for Analysis and Synthesis. A.M.H. and A.M.D. acknowledge that this review was completed in receipt of funding from the European Research Council under the European Union’s Seventh Framework Programme (FP7/2007–2013)/ERC grant agreement no. 278636. H.J.D., A.M.H. and A.M.D. thank Marci Robinson, Fergus Howell, Lynn Wingard, Caroline Prescott and Danielle Stoll Dowsett for comments and discussions on a previous version of the review.
The authors declare no competing financial interests.
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Haywood, A., Dowsett, H. & Dolan, A. Integrating geological archives and climate models for the mid-Pliocene warm period. Nat Commun 7, 10646 (2016). https://doi.org/10.1038/ncomms10646
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