High-resolution, easily accessible paleoclimate data are essential for environmental, evolutionary, and ecological studies. The availability of bioclimatic layers derived from climatic simulations representing conditions of the Late Pleistocene and Holocene has revolutionized the study of species responses to Late Quaternary climate change. Yet, integrative studies of the impacts of climate change in the Early Pleistocene and Pliocene – periods in which recent speciation events are known to concentrate – have been hindered by the limited availability of downloadable, user-friendly climatic descriptors. Here we present PaleoClim, a free database of downscaled paleoclimate outputs at 2.5-minute resolution (~5 km at equator) that includes surface temperature and precipitation estimates from snapshot-style climate model simulations using HadCM3, a version of the UK Met Office Hadley Centre General Circulation Model. As of now, the database contains climatic data for three key time periods spanning from 3.3 to 0.787 million years ago: the Marine Isotope Stage 19 (MIS19) in the Pleistocene (~787 ka), the mid-Pliocene Warm Period (~3.264–3.025 Ma), and MIS M2 in the Late Pliocene (~3.3 Ma).
|Design Type(s)||source-based data transformation objective • data integration objective • observation design|
|Measurement Type(s)||climate change|
|Technology Type(s)||computational modeling technique|
|Factor Type(s)||datatype • temporal_interval • geological epoch|
|Sample Characteristic(s)||Earth (Planet) • planetary atmosphere|
Machine-accessible metadata file describing the reported data (ISA-Tab format)
Background & Summary
Shifts in climate and habitats have key evolutionary and ecological consequences, and are closely associated with contemporary biodiversity patterns1,2. Over the past decade, hundreds of studies have combined data on species occurrences with climate descriptions from interpolated weather-stations to model the distribution of animals and plants worldwide3. When projected into paleo- and future-climatic scenarios, these models are widely used to investigate the historic and future distributions of biodiversity4–7. However, the limited availability of easily accessible climate data for time periods other than the mid-Holocene (6 Ka), the Last Glacial Maximum (LGM, 21 Ka) and the Last Interglacial (130 Ka) has posed a significant impediment to scientists interested in biological responses to past climate change8,9.
Traditionally, those target periods have been the focus of biological investigations largely because they correspond to times of temperature extremes in the northern latitudes1,10. While patterns of climate change between those periods are shown to play a role in biodiversity patterns, there exists considerable spatial variation in their ability to explain the distribution of biological diversity in species-rich and threatened tropical areas4,11–16. Despite the utility of the paleoclimatologies spanning the last 130 Ka, a major impediment to ecological and evolutionary studies is the lack of easily accessible, high spatial resolution paleoclimatic data in a format directly compatible with most GIS software, particularly those describing earlier time periods.
To fill this gap, and given that the most common divergence times between extant sister species have been placed at 1–4 Ma, with relatively few divergence times spanning the last 130 kyrs17,18, we have developed PaleoClim. Our aim is to provide the scientific community with data more reflective of the time periods under which speciation occurs, allowing for a more complete understanding of the drivers of biodiversity processes and patterns. PaleoClim is a free database of downscaled paleomodels at 2.5 arc-minute resolution (~5 km at equator), representing temperature and precipitation estimates output from individual snapshot coupled atmosphere-ocean general circulation models from the Hadley Centre Coupled Model Version 3 (HadCM3). Building from these estimates, we have derived paleo bioclimatic layers that represent annual averages (e.g. mean annual temperature, annual precipitation), seasonality (e.g. annual range in temperature and precipitation), and extreme or limiting environmental factors (e.g. temperature of the coldest and warmest month, and precipitation of the wet and dry quarters), akin to WorldClim19. To date, the database contains high-resolution terrestrial data for three key periods: Marine Isotope Stage 19 (MIS19) in the Pleistocene (ca. 787 Ka), the mid-Pliocene Warm Period (mPWP, ca. 3.264-3.025 Ma) and Marine Isotope Stage M2 (M2), a glacial interval in the Late Pliocene (ca. 3.3 Ma, Fig. 1).
The paleoclimate simulations used here come from the HadCM3 version of the UK Met Office Unified Model General Circulation Model (GCM). This is a well-established coupled ocean atmosphere climate model, having contributed to the last three Intergovernmental Panel on Climate Change (IPCC) Assessment Reports (AR3, AR4 and AR5), and used to simulate climate for nearly 20 years20,21. HadCM3 has a horizontal resolution of 2.5° in latitude and 3.75° in longitude, and a higher resolution ocean of 1.25°×1.25° regular long-lat grid, with 19 vertical levels in atmosphere and 20 in the ocean. The atmospheric component has a time-step of 30 min, and is coupled to the ocean every day. Typically, the climatology is output every month, and the mean annual and monthly climate are calculated from these data. As the name GCM suggests, this class of climate model is able to reproduce the major circulations in the both the atmosphere and ocean, as well as major drivers of inter-annual variability22. The resolution also allows for synoptic weather patterns to be simulated, along with key climate oscillations, but may not simulate well local extremes or regions with high gradients (e.g. extreme convective events23). HadCM3 is in the middle of the range of overall climate sensitivities exhibited by the IPCC-class climate models24,25.
The paleoclimate simulations presented here (Table 1) are intended as an example of what is possible with the techniques employed, and represent significantly different time periods from what is currently broadly available to biologists. Ice cores provide the best possible constraints on past greenhouse gases beyond the instrumental record. This means that paleoclimate simulations of the last 800,000 years have a distinct advantage over those from previous time periods. Marine isotope stage 19 (MIS19) occurs at roughly 787 Ka and is the oldest Pleistocene interglacial covered by the latest EPICA Antarctic ice core26. This allows us to use well-constrained greenhouse gas concentrations of CO226, CH427 and N2O28, as well as accurate orbital parameters29. Prior to 400,000 years ago and MIS11, there are significant differences in the magnitude of glacial-interglacial cycles, both in the greenhouse gas concentrations and temperature responses. However, MIS19 has the most Holocene-like greenhouse gases and ice core temperature proxies of the interglacials that occur between 800,000 and 400,000 years ago. Further paleogeographic boundary condition change must have occurred over these timescales, but as there is no reconstruction currently available, the remaining boundary conditions have been kept as in the pre-industrial simulation.
The mid-Pliocene Warm Period (mPWP) simulation follows the PlioMIP protocols25, is a continuation of the original HadCM3 PlioMIP simulation30, and has been previously published by Hill31. The simulation has elevated atmospheric carbon dioxide concentrations set to 405 parts per million by volume (ppmv), reduced ice sheets32, a Piacenzian vegetation reconstruction33 and altered topography, particularly over the Rockies, Andes and East African Rift system34. As the underlying datasets are not the reconstruction of a specific point in time, but of the environmental conditions typical of a mid-Pliocene warm peak35, a modern orbit is given to the PlioMIP simulations.
The marine isotope stage M2 glacial period is the strongest Pliocene oxygen isotope excursion prior to the beginning of the Plio-Pleistocene transition, which marks the start of the Pleistocene glacial-interglacial cycles36. The magnitude of the oxygen isotope excursion suggests that large ice masses may have covered the Northern Hemisphere for a short time, although the exact locations of these ice sheets remains uncertain37,38. The ice sheets used in the simulations are based on the ice sheets of 116 Ka, which are the 40 m sea level rise volume equivalents from the last glacial cycle37. A reduction in atmospheric CO2 concentration to 220 ppmv39 was implemented in the climate model alongside orbital forcing appropriate for 3.3 Ma, although this is close to the modern orbital configuration24.
We employed the Change-Factor method19,40,41 to downscale the paleoclimatic climatologies. This approach creates high-resolution layers by quantifying the differences between the paleo and current (control) climatologies for each raw variable, at the native model-specific spatial resolution. This functions as a calibration step to measure the raw climate anomalies at the coarser spatial scale climate model. Once this step is completed, the difference layers (commonly called delta layers, change-factor differences, or climate change anomalies) are downscaled to high-resolutions (typically 1–20 km) and summed to a matching high-resolution current climate variable. This method is relatively quick, requiring less than a day of computational time per raster layer, and can be efficiently applied to global datasets. A major benefit of the Change-Factor method relative to other methods of downscaling is its ability to incorporate small-scale topographic nuances in regional climatologies that are often not captured in climate models, but present in the high-resolution current datasets. Examples include climatic differences in mountainous regions such as differences between valleys, mid-elevation ranges, and their peaks.
Here, we created global delta layers by subtracting the raw temperature and precipitation values of each snapshot paleoclimatic simulation from corresponding HadCM3 control simulations that represent the pre-industrial era. The delta layer represents the pixel-by-pixel changes from pre-industrial conditions, within the constraints of each snapshot climate simulation. The delta layers were downscaled 60-fold from 2.5 arc-degrees to 2.5 arc-minutes (ca. 5 km) using a tensioned spline in ArcGIS 10.5 (sampling = 12 nearest observations to a focal point, weight of 0.1, ESRI 2018). A spline is a deterministic interpolation method that has been shown to deliver similar results when compared to kriging41–46, and it has been commonly considered as appropriate for interpolation environmental variables44. We used a tensioned spline (instead of a regularized spline) to avoid extraneous inflection points, and more generally to preserve shape properties, such as monotonicity and convexity, of a set of data points - and to do so without sacrificing smoothness47. Spline approaches are based on requirement that the interpolation function passes through the data points, but also yield the smoothest transition as possible.
The high-resolution delta layers were then summed to a corresponding current monthly temperature or precipitation climate layers from the Climatologies at High-Resolution for the Earth’s Land Surface Areas (CHELSA) database48 at the same resolution. Though rare in our analyses, negative precipitation values were converted to zero. To reduce pixel-depth and file sizes of final products, all monthly temperature raster layers were multiplied by 10 and converted to integers. Prior to the creation of bioclimate layers, final monthly layers were adjusted to the mean sea-level of paleoclimatic period, based on adjustments to a contemporary bathymetry dataset49.
We also explored the use of ratios of anomalies (ROAs), instead of raw differences, to downscale precipitation. A major caveat to the Change-Factor method regards transferring the generalized spatial patterns in the climate model simulations to the regional mosaic of habitats in the high-resolution climates, as the model predicted climate patterns are uniformly applied to the latter. Other studies using the Change-Factor approach have advocated the use of ROAs to the corresponding baseline conditions for downscaling precipitation (vs. raw differences used here, and for temperatures universally elsewhere). Those studies argue that the use of the raw difference method40 may result in inaccurate inferences in regions of strong rainfall gradients, and state that ROAs are more robust to maintaining original patterns in downscaling when managing larger values40,41.
At a coarse level, all paleoclimatic layers account for topographic shifts incurred between now and the past. For instance, the global topography used in the Pliocene simulations, derived from the Pliocene Research, Interpretation and Synoptic Mapping (PRISM3) dataset, are largely, but not entirely, similar to the modern topography32. Notable exceptions include: 1) the mountains of the western Cordillera of western North America and the Andean mountains in South America, which were then, in a few regions, lower than modern altitudes50,51, 2) the elevation of some of the regions now covered by the Greenland and Antarctica Ice Sheets, which then experienced a net decrease caused by a reduction in the size of the ice sheets themselves, 3) the east African rift zone, which then reached higher elevations than at present, as indicated in the literature50,51. All topographic changes were incorporated into HadCM3, and the simulated climates are reflective of those differences. However, because we downscaled the final datasets with modern climatologies, results in these particular areas should be carefully evaluated.
Unlike for the mid-Pliocene simulation, the M2 glacial climate simulation only has changes to topography resulting from changes in the ice sheets. Over Antarctica, Greenland and North America, changes over the ice sheet regions generally led to uplift in surface topography of between 50 and 500 meters compared with present day, but glacioisostatic rebound leads to reductions in the topography of neighbouring regions37. Regions outside those impacted by ice sheets were kept at modern topography. The MIS19 simulation use identical topography to the pre-industrial simulation.
From the high-resolution monthly temperature and precipitation values, we calculated a set of derived parameters broadly used in ecological applications. These bioclimatic variables are derived from the monthly mean temperature (or minimum and maximum temperature, depending on their availability) and precipitation values. They are specifically developed for species distribution modelling and related ecological applications (see Table 2 for a list and common nomenclature). For some paleo simulations (e.g. mPWP), the monthly maximum and minimum temperatures were not available. In these instances, the bioclimatic layers that represent annual averages (mean annual temperature, annual precipitation), seasonality (annual range in temperature and precipitation), and extreme or limiting environmental factors (temperature of the coldest and warmest quarters, and precipitation of the wet and dry quarters) could not be created (Bio_2, Bio_3, Bio_5, Bio_6, and Bio_7). In this transformation, a quarter is defined as the period of three months (1/4 of the year). Output bioclimate layers were saved as individual GeoTiffs (*tif) and projected in the WGS 1984 projection.
The Paleoclim data depict records for monthly mean temperature in °C and precipitation values in mm/month, and derived bioclimatic variables for a 30-year simulation period in the form of GeoTIFF files. The high resolution paleoclimatic bioclimatic variables and the original raw HadCM3 GCM monthly paleoclimate variables are freely available at Figshare (Data Citation 1). The latest versions of paleoclimate bioclimatic data are also freely available at http://www.paleoclim.org. See Table 2 for naming conventions and specific details for each provided variable.
We carefully explored the use of raw differences vs. ratios of anomalies to calibrate downscaled precipitation data under the Change Factor method. Understanding how the ‘raw difference’ and ROA calibration methods can dramatically change output paleoclimatic patterns is straightforward. Imagine an observed rainfall at a specific location to be 2.0 m/mo and 1.0 m/mo in the paleo- and current simulations, respectively. In this situation, the raw difference of precipitation is +1 m, while ROA is 2. Now let us assume that the precipitation values in the high-resolution modern dataset used to downscale the delta layers ranges, within that same area, from 0.25 m to 4.0 m. The raw difference method would yield paleoclimatic rainfall estimates, in the corresponding high-resolution dataset, that range from 1.25–5.0 m. In contrast, the ROA method would yield values ranging from 0.5–8.0 m, a much wider interval. It is important to also point out that this example oversimplifies the Change-Factor process, because delta layers are downscaled prior to summation or multiplication, which results in intermediate values between input delta layer points and the final high-resolution values, accordingly.
When using raw differences in precipitation, we found no evidence of illogical transitions in our datasets in areas of high rainfall (Fig 2). In contrast, the use of ROA (vs. raw differences) resulted in inferior results (Fig. 2). For illustration purposes, we show the downscaled high-resolution layers of the mid-Pliocene Warm Period, in an area of a high range of rainfall, the region of the Himalayan Mountains (Fig 2). For the month of June, for instance, the use of the raw differences calibration method resulted in a total precipitation estimate ranging between 0 and 2.8 m/mo. The use of the ROA, in turn, yielded a much larger range, between 0 and 5.7 m/mo. For this same region, the raw values from the original paleoclimate simulation ranged from 0.85 to 0.69 m/mo, from 0.65 to 0.59 m/mo for the pre-industrial control simulations, and from 0 to 2.5 m for the current high-resolution layers. The resulting differences in the ROA-derived high-resolution paleolayer is hence over a 2-fold difference in maximum precipitation values.
Similarly, when the hi-resolution data are aggregated to 2.5 degrees (by calculating the mean value per area), and correlated to the raw Pliocene values from HadCM3, we observe a Pearson correlation coefficient of 0.810 in the raw change method and 0.667 in ratio of anomalies - for the same corresponding region and time. At a global level, we measured a Pearson correlation coefficient of 0.823 in the raw change method, and 0.612 in the ratio of anomalies. These results are also matched by the visualization of both high-resolution layers compared to the raw climate model values (Fig 2, comparing A & G vs. A. & F). Though this is just one example, these observations were consistent among all months evaluated and between different climate model simulations.
A second concern regards the extent by which areas of low current rainfall change as a result of ROA downscaling, particularly those with zero modern rainfall. When the modern value is zero, the downscaling values cannot change, as any number multiplied against zero will be zero. Therefore, when using the ROA method, areas of the eastern Sahara Desert, for instance, will never possess rainfall amounts above zero for many months, despite the fact we know this is historically inaccurate53, and potentially reflected in the climate model simulations. Furthermore, if the rainfall value is small in the current high-resolution dataset, values change only slightly when using ROA, even if the ROA value is high. Given the profound ecological impacts of precipitation in water-limited ecosystems, the two different calibration methods dramatically impact downscaled precipitation in these habitats. We recommend avoiding ROA in this case.
Overall, the use of ROAs (vs. raw differences) resulted in inferior paleoclimatic outputs due to multiplication of ratios in the delta layers against a high-resolution current climatology (vs. summing in the raw difference method). Hence, we suggest that users apply the raw difference method to precipitation data or utilize the raw difference-based paleoclimate outputs in their environmental, ecological, and evolutionary analyses. This approach is more sensitive to changes in low precipitation environments, more reflective of the raw paleoclimate values from HadCM3, and not as confounded by modern precipitation levels (i.e. areas with zero monthly precipitation). In the future releases, we plan to evaluate a hybrid approach that averages the outputs from both calibration methods.
When citing data from Paleoclim.org, please cite both this manuscript and the original manuscript(s) that generated to each climatology (see Table 1). This supports the continued generation of these derivative works, the primary research of the groups generating them, and promotes collaboration among PaleoClim and other researchers. PaleoClim reduces the amount of time that would be spent developing common solutions and provides data in a consistent nomenclature and common format, making data easier to use. We plan to regularly expand the PaleoClim database: providing additional paleoclimate time-periods, and new or improved GCMs of existing datasets with paleoclimate variability (vs. a mean simulation value). For questions, collaborative inquires, or suggestions regarding PaleoClim, go to our Google Group (https://groups.google.com/forum/#!forum/paleoclim) or email firstname.lastname@example.org. Data are feely available under the Creative Commons License: CC BY.
How to cite this article: Brown, J. L. et al. PaleoClim, high spatial resolution paleoclimate surfaces for global land areas. Sci. Data. 5:180254 doi: 10.1038/sdata.2018.254 (2018).
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Hewitt, G. The genetic legacy of the Quaternary ice ages. Nature 405, 907–913 (2000).
Carnaval, A. C., Hickerson, M. J., Haddad, C. F., Rodrigues, M. T. & Moritz, C. Stability predicts genetic diversity in the Brazilian Atlantic forest hotspot. Science 323, 785–789 (2009).
Graham, C. H., Ferrier, S., Huettman, F., Moritz, C. & Peterson, A. T. New developments in museum-based informatics and applications in biodiversity analysis. Trends in Ecology & Evolution 19, 497–503 (2004).
Prates, I. et al. Inferring responses to climate dynamics from historical demography in neotropical forest lizards. Proceedings of the National Academy of Sciences 113, 7978–7985 (2016).
Brown, J. L. et al. Predicting the genetic consequences of future climate change: The power of coupling spatial demography, the coalescent, and historical landscape changes. American Journal of Botany 103, 153–163 (2016).
Knowles, L. L. & Alvarado‐Serrano, D. F. Exploring the population genetic consequences of the colonization process with spatio‐temporally explicit models: insights from coupled ecological, demographic and genetic models in montane grasshoppers. Molecular Ecology 19, 3727–3745 (2010).
He, Q., Edwards, D. L. & Knowles, L. L. Integrative testing of how environments from the past to the present shape genetic structure across landscapes. Evolution 67, 3386–3402 (2013).
Brown, J. L. & Knowles, L. L. Spatially explicit models of dynamic histories: examination of the genetic consequences of Pleistocene glaciation and recent climate change on the American Pika. Molecular Ecology 21, 3757–3775 (2012).
Knowles, L. L., Carstens, B. C. & Keat, M. L. Coupling genetic and ecological-niche models to examine how past population distributions contribute to divergence. Current Biology 17, 940–946 (2007).
Carstens, B. C. & Richards, C. L. Integrating coalescent and ecological niche modeling in comparative phylogeography. Evolution 61, 1439–1454 (2007).
Batalha-Filho, H., Fjeldså, J., Fabre, P.-H. & Miyaki, C. Y. Connections between the Atlantic and the Amazonian forest avifaunas represent distinct historical events. Journal of Ornithology 154, 41–50 (2013).
Smith, B. T. et al. The drivers of tropical speciation. Nature 515, 406–409 (2014).
Brown, J. L., Cameron, A., Yoder, A. D. & Vences, M. A necessarily complex model to explain the biogeography of the amphibians and reptiles of Madagascar. Nature Communications 5 (2014).
Thomas, C. D. et al. Biodiversity conservation: uncertainty in predictions of extinction risk/Effects of changes in climate and land use/Climate change and extinction risk (reply). Nature 430, 34 (2004).
Thomas, C. D. et al. Extinction risk from climate change. Nature 427, 145–148 (2004).
Raxworthy, C. J. et al. Predicting distributions of known and unknown reptile species in Madagascar. Nature 426, 837–841 (2003).
Rull, V. Speciation timing and neotropical biodiversity: the Tertiary–Quaternary debate in the light of molecular phylogenetic evidence. Molecular Ecology 17, 2722–2729 https://doi.org/10.1111/j.1365-294X.2008.03789.x (2008).
Rull, V. Neotropical biodiversity: timing and potential drivers. Trends in Ecology & Evolution 26, 508–513 https://doi.org/10.1016/j.tree.2011.05.011 (2011).
Hijmans, R. J., Cameron, S. E., Parra, J. L., Jones, P. G. & Jarvis, A. Very high resolution interpolated climate surfaces for global land areas. International Journal of Climatology 25, 1965–1978 (2005).
Gordon, C. et al. The simulation of SST, sea ice extents and ocean heat transports in a version of the Hadley Centre coupled model without flux adjustments. Climate Dynamics 16, 147–168 (2000).
Pope, V., Gallani, M., Rowntree, P. & Stratton, R. The impact of new physical parametrizations in the Hadley Centre climate model: HadAM3. Climate Dynamics 16, 123–146 (2000).
Randall, D. A. et al. Climate Models and Their Evaluation (2007).
Kendon, E. J. et al. Do convection-permitting regional climate models improve projections of future precipitation change? Bulletin of the American Meteorological Society 98, 79–93 (2017).
Haywood, A. M. et al. Large-scale features of Pliocene climate: results from the Pliocene Model Intercomparison Project. Climate of the Past 9, 191–209 https://doi.org/10.5194/cp-9-191-2013 (2013).
Haywood, A. et al. Pliocene Model Intercomparison Project (PlioMIP): experimental design and boundary conditions (experiment 1). Geoscientific Model Development 3, 227–242 (2010).
Lüthi, D. et al. High-resolution carbon dioxide concentration record 650,000–800,000 years before present. Nature 453, 379 (2008).
Loulergue, L. et al. Orbital and millennial-scale features of atmospheric CH 4 over the past 800,000 years. Nature 453, 383 (2008).
Spahni, R. et al. Atmospheric methane and nitrous oxide of the late Pleistocene from Antarctic ice cores. Science 310, 1317–1321 (2005).
Laskar, J. et al. A long-term numerical solution for the insolation quantities of the Earth. Astronomy and Astrophysics 428, 261–285 (2004).
Bragg, F., Lunt, D. & Haywood, A. Mid-Pliocene climate modelled using the UK hadley centre model: PlioMIP experiments 1 and 2. Geoscientific Model Development 5, 1109 (2012).
Hill, D. J. The non-analogue nature of Pliocene temperature gradients. Earth and Planetary Science Letters 425, 232–241 (2015).
Dowsett, H. et al. The PRISM3D paleoenvironmental reconstruction. Stratigraphy 7, 123–139 (2010).
Salzmann, U., Haywood, A., Lunt, D., Valdes, P. & Hill, D. A new global biome reconstruction and data‐model comparison for the middle Pliocene. Global Ecology and Biogeography 17, 432–447 (2008).
Sohl, L. et al. PRISM3/GISS topographic reconstruction: US Geological Survey Data Series 419. US Geological Survey, Reston VA (2009).
Haywood, A. M. et al. On the identification of a Pliocene time slice for data–model comparison. Philosophical Transactions of the Royal Society A 371, 20120515 (2013).
Lisiecki, L. E. & Raymo, M. E. A Pliocene‐Pleistocene stack of 57 globally distributed benthic δ18O records. Paleoceanography 20 (2005).
Dolan, A. M. et al. Modelling the enigmatic Late Pliocene Glacial Event—Marine Isotope Stage M2. Global and Planetary Change 128, 47–60 (2015).
Tan, N. et al. Exploring the MIS M2 glaciation occurring during a warm and high atmospheric CO2 Pliocene background climate. Earth and Planetary Science Letters 472, 266–276 (2017).
Bartoli, G., Hönisch, B. & Zeebe, R. E. Atmospheric CO2 decline during the Pliocene intensification of Northern Hemisphere glaciations. Paleoceanography 26 (2011).
Wilby, R. et al. Guidelines For Use of Climate Scenarios Developed From Statistical Downscaling Methods (2004).
Lima-Ribeiro, M. et al. EcoClimate: a database of climate data from multiple models for past, present, and future for macroecologists and biogeographers. Biodiversity Informatics 10, 1–21 (2015).
Laslett, G. M. Kriging and Splines: An Empirical Comparison of Their Predictive Performance in Some Applications. Journal of the American Statistical Association 89, 391–400 https://doi.org/10.2307/2290837 (1994).
Dubrule, O. Comparing splines and kriging. Computers & Geosciences 10, 327–338 https://doi.org/10.1016/0098-3004(84)90030-X (1984).
Hutchinson, M. F. Interpolating mean rainfall using thin plate smoothing splines. International Journal of Geographical Information Systems 9, 385–403 https://doi.org/10.1080/02693799508902045 (1995).
Hutchinson, M. F. & Gessler, P. E. Splines — more than just a smooth interpolator. Geoderma 62, 45–67 https://doi.org/10.1016/0016-7061(94)90027-2 (1994).
Laslett, G. M., McBratney, A. B., Pahl, P. J. & Hutchinson, M. F. Comparison of several spatial prediction methods for soil pH. Journal of Soil Science 38, 325–341 https://doi.org/10.1111/j.1365-2389.1987.tb02148.x (1987).
Renka, R. J. Interpolatory Tension Splines with Automatic Selection of Tension Factors. SIAM Journal on Scientific and Statistical Computing 8, 393–415 https://doi.org/10.1137/0908041 (1987).
Karger, D. N. et al. Climatologies at high resolution for the earth’s land surface areas. Scientific Data 4, 170122 https://doi.org/10.1038/sdata.2017.122 (2017).
Weatherall, P. et al. A new digital bathymetric model of the world’s oceans. Earth and Space Science 2, 331–345 https://doi.org/10.1002/2015EA000107 (2015).
Thompson, R. S. & Fleming, R. F. Middle Pliocene vegetation: reconstructions, paleoclimatic inferences, and boundary conditions for climate modeling. Marine Micropaleontology 27, 27–49 https://doi.org/10.1016/0377-8398(95)00051-8 (1996).
Markwick, P. J. The palaeogeographic and palaeoclimatic significance of climate proxies for data-model comparisons, The Geological Society (2007).
Hijmans, R. J., Phillips, S. J., Leathwich, J. & Elith, J. dismo: Species Distribution Modelling https://CRAN.R-project.org/package=dismo (2018).
Tierney, J. E., Pausata, F. S. R. & deMenocal, P. B. Rainfall regimes of the Green Sahara. Science Advances 3 https://doi.org/10.1126/sciadv.1601503 (2017).
De Boer, B., Van de Wal, R., Bintanja, R., Lourens, L. & Tuenter, E. Cenozoic global ice-volume and temperature simulations with 1-D ice-sheet models forced by benthic δ 18 O records. Annals of Glaciology 51, 23–33 (2010).
Brown, J. L., Hill, D. J., Dolan, A. M., Carnaval, A. C., & Haywood, A. M. Figshare https://doi.org/10.6084/m9.figshare.c.4126292 (2018)
We are grateful to Dan Sears and Skye Steiner for assistance at early stages of this project. This work was co-funded by the National Science Foundation (NSF) Grant DEB 1343578, the National Aeronautics and Space Administration, and the São Paulo State Research Foundation (FAPESP) Grant BIOTA 2013/50297-0, through the Dimensions of Biodiversity Program, start-up provided by Southern Illinois University to J.L.B, and through the University of Leeds International Research Collaboration Award (IRCA). A.M.H and A.M.D acknowledge funding from the European Research Council under the European Union’s Seventh Framework Programme (FP7/2007-2013)/ERC grant agreement no 278636. A.M.D. and D.J.H. also acknowledge the University of Leeds’ High Performance Computing System (ARC).
The authors declare no competing interests.
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Brown, J., Hill, D., Dolan, A. et al. PaleoClim, high spatial resolution paleoclimate surfaces for global land areas. Sci Data 5, 180254 (2018). https://doi.org/10.1038/sdata.2018.254
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