Student or educator? Sign up with your school email and get 6 months of Pro free.
CoChat
Sign Up
Cited by 145

The DOI matches its Crossref record; 3 of the 3 references it cites were found in a registry or an index.

Palaeogeographic controls on climate and proxy interpretation

Lunt, Daniel J., Farnsworth, Alex, Loptson, Claire, Foster, Gavin L., Markwick, Paul, O'Brien, Charlotte L., Pancost, Richard D., Robinson, Stuart A., Wrobel, Neil·2016·Climate of the Past
DOI 10.5194/cp-12-1181-2016

Published version of a preprint

Open this paper in CoChat — free account

Abstract

Abstract. During the period from approximately 150 to 35 million years ago, the Cretaceous–Paleocene–Eocene (CPE), the Earth was in a “greenhouse” state with little or no ice at either pole. It was also a period of considerable global change, from the warmest periods of the mid-Cretaceous, to the threshold of icehouse conditions at the end of the Eocene. However, the relative contribution of palaeogeographic change, solar change, and carbon cycle change to these climatic variations is unknown. Here, making use of recent advances in computing power, and a set of unique palaeogeographic maps, we carry out an ensemble of 19 General Circulation Model simulations covering this period, one simulation per stratigraphic stage. By maintaining atmospheric CO2 concentration constant across the simulations, we are able to identify the contribution from palaeogeographic and solar forcing to global change across the CPE, and explore the underlying mechanisms. We find that global mean surface temperature is remarkably constant across the simulations, resulting from a cancellation of opposing trends from solar and palaeogeographic change. However, there are significant modelled variations on a regional scale. The stratigraphic stage–stage transitions which exhibit greatest climatic change are associated with transitions in the mode of ocean circulation, themselves often associated with changes in ocean gateways, and amplified by feedbacks related to emissivity and planetary albedo. We also find some control on global mean temperature from continental area and global mean orography. Our results have important implications for the interpretation of single-site palaeo proxy records. In particular, our results allow the non-CO2 (i.e. palaeogeographic and solar constant) components of proxy records to be removed, leaving a more global component associated with carbon cycle change. This “adjustment factor” is used to adjust sea surface temperatures, as the deep ocean is not fully equilibrated in the model. The adjustment factor is illustrated for seven key sites in the CPE, and applied to proxy data from Falkland Plateau, and we provide data so that similar adjustments can be made to any site and for any time period within the CPE. Ultimately, this will enable isolation of the CO2-forced climate signal to be extracted from multiple proxy records from around the globe, allowing an evaluation of the regional signals and extent of polar amplification in response to CO2 changes during the CPE. Finally, regions where the adjustment factor is constant throughout the CPE could indicate places where future proxies could be targeted in order to reconstruct the purest CO2-induced temperature change, where the complicating contributions of other processes are minimised. Therefore, combined with other considerations, this work could provide useful information for supporting targets for drilling localities and outcrop studies.

Overview

The claims and statistics of this paper haven’t been checked yet.

Run the check — free, no account needed. It reads the open-access text and checks the sources it cites.

A few free checks a day · papers already verified open instantly · results are public

Integrity signals

Registry

Crossref · 10.5194/cp-12-1181-2016

Cites

3 of 3 references verified0 citation errors · 0 not checkable

Statistics

Figures

Figure 1 Climate evolution over the last 150 million years, as expressed by the benthic oxygen isotope records of Friedrich et al. (2012) and Cramer et al. (2009) (coloured dots), and a surface temperature record (H13C09) produced by applying the methodologies of Hansen et al. (2013) to the Cramer et al. (2009) 18 O benthic data, and applying a 10-point running average (grey line).
Figure 1 Climate evolution over the last 150 million years, as expressed by the benthic oxygen isotope records of Friedrich et al. (2012) and Cramer et al. (2009) (coloured dots), and a surface temperature record (H13C09) produced by applying the methodologies of Hansen et al. (2013) to the Cramer et al. (2009) 18 O benthic data, and applying a 10-point running average (grey line).CC-BY · From the PDF
Figure 2 The values of solar constant since the earliest Cretaceous, calculated from Gough (1981) and used for the CPE simulations in this paper (green line), and from Caldeira and Kasting (1992) (orange line). Horizontal line shows the modern value.
Figure 2 The values of solar constant since the earliest Cretaceous, calculated from Gough (1981) and used for the CPE simulations in this paper (green line), and from Caldeira and Kasting (1992) (orange line). Horizontal line shows the modern value.CC-BY · From the PDF
Figure 3 CO2 as compiled by Honisch et al. (2012) (small dots). Overlain is the CO 2 concentration in each simulation described in this paper (red dots). The open blue circles show CO 2 concentration in a set of model simulations of the Oligocene and Neogene, which are not discussed in this paper but are provided for reference. Horizontal black lines show 280, 560, and 1120 ppmv.
Figure 3 CO2 as compiled by Honisch et al. (2012) (small dots). Overlain is the CO 2 concentration in each simulation described in this paper (red dots). The open blue circles show CO 2 concentration in a set of model simulations of the Oligocene and Neogene, which are not discussed in this paper but are provided for reference. Horizontal black lines show 280, 560, and 1120 ppmv.CC-BY · From the PDF
Image 4
CC-BY · From the PDF
Image 5
CC-BY · From the PDF
Figure 4 Modelled evolution of global mean ocean temperature [ C] in each CPE simulation at three depths: (a) surface (5 m), (b) 670 m, (c) 2.7 km.
Figure 4 Modelled evolution of global mean ocean temperature [ C] in each CPE simulation at three depths: (a) surface (5 m), (b) 670 m, (c) 2.7 km.CC-BY · From the PDF
Figure 5 The global MAT for each Stage of the CPE at 4 CO2 (black filled circles) plotted over a surface temperature record produced by applying the methodologies of Hansen et al. (2013) to the Cramer et al. (2009) 18 O benthic data, and applying a 10-point running average (grey line). The open circles show model results for the Oligocene and Neogene, with lower CO 2 , which are not discussed in this paper but are provided for reference. The modelled trend (ignoring the outlying Berriasian stage) is shown as a solid line, and the expected trend assuming solar forcing only is shown as a pair of dashed lines which start/end at the beginning/end of the modelled trend.
Figure 5 The global MAT for each Stage of the CPE at 4 CO2 (black filled circles) plotted over a surface temperature record produced by applying the methodologies of Hansen et al. (2013) to the Cramer et al. (2009) 18 O benthic data, and applying a 10-point running average (grey line). The open circles show model results for the Oligocene and Neogene, with lower CO 2 , which are not discussed in this paper but are provided for reference. The modelled trend (ignoring the outlying Berriasian stage) is shown as a solid line, and the expected trend assuming solar forcing only is shown as a pair of dashed lines which start/end at the beginning/end of the modelled trend.CC-BY · From the PDF
Figure 6 (a-r) Annual mean surface air temperature (at 1.5 m) for each geological Stage, expressed as an anomaly relative to the previous Stage. (a) Priabonian-Bartonian, (b) Bartonian-Lutetian, (c) Lutetian-Ypresian, (d) Ypresian-Thanetian (e) Thanetian-Selandian, (f) Selandian-Danian, (g) Danian-Maastrichtian, (h) Maastrichtian-Campanian, (i) Campanian-Santonian, (j) Santonian-Coniacian, (k) Coniacian-Turonian, (l) Turonian-Cenomanian, (m) Cenomanian-Albian, (n) Albian-Aptian, (o) Aptian-Barremian, (p) BarremianHauterivian, (q) Hauterivian-Valanginian, (r) Valanginian-Berriasian. (s) Annual mean surface air temperature (at 1.5 m) for the Berriasian stage.
Figure 6 (a-r) Annual mean surface air temperature (at 1.5 m) for each geological Stage, expressed as an anomaly relative to the previous Stage. (a) Priabonian-Bartonian, (b) Bartonian-Lutetian, (c) Lutetian-Ypresian, (d) Ypresian-Thanetian (e) Thanetian-Selandian, (f) Selandian-Danian, (g) Danian-Maastrichtian, (h) Maastrichtian-Campanian, (i) Campanian-Santonian, (j) Santonian-Coniacian, (k) Coniacian-Turonian, (l) Turonian-Cenomanian, (m) Cenomanian-Albian, (n) Albian-Aptian, (o) Aptian-Barremian, (p) BarremianHauterivian, (q) Hauterivian-Valanginian, (r) Valanginian-Berriasian. (s) Annual mean surface air temperature (at 1.5 m) for the Berriasian stage.CC-BY · From the PDF
Figure 7 Global annual mean surace air temperature (at 1.5 m) in each model simulation (black dots). Also shown as vertical lines is the contribution to temperature difference between each consecutive Stage, from changes over land (green), over ocean (blue), and over regions which switch between land and ocean (red). Also shown are the global mean of all simulations (dotted line), and trend across all simulations except the Berriasian (dashed line, as in Fig. 5).
Figure 7 Global annual mean surace air temperature (at 1.5 m) in each model simulation (black dots). Also shown as vertical lines is the contribution to temperature difference between each consecutive Stage, from changes over land (green), over ocean (blue), and over regions which switch between land and ocean (red). Also shown are the global mean of all simulations (dotted line), and trend across all simulations except the Berriasian (dashed line, as in Fig. 5).CC-BY · From the PDF
Figure 8 Plots showing the relationship between Stage-Stage changes in (a) ocean near-surface (1.5 m) air temperature (SAT) and continental SAT, (b) continental area and global mean SAT, (c) global mean orography and continental SAT, (d) surface temperature due to emissivity change and global mean surface temperature, and (e) surface temperature due to albedo change and global mean surface temperature. Note that the continental and ocean SAT values are the relative contribution to the global mean values.
Figure 8 Plots showing the relationship between Stage-Stage changes in (a) ocean near-surface (1.5 m) air temperature (SAT) and continental SAT, (b) continental area and global mean SAT, (c) global mean orography and continental SAT, (d) surface temperature due to emissivity change and global mean surface temperature, and (e) surface temperature due to albedo change and global mean surface temperature. Note that the continental and ocean SAT values are the relative contribution to the global mean values.CC-BY · From the PDF
Figure 9 (a) The palaeolocation of seven key sites used for reconstructing climate of the CPE. Large black dots represent the modern location. Small black dots represent the location at each Stage post the CPE, and coloured dots represent the location at each Stage during the CPE, for those Stages that the modern ocean crust was present. (b) Climate evolution across the CPE, simulated by the model, as experienced at the same seven sites. Filled (open) symbols indicate that a particular site is marine (terrestrial) at a particular Stage.
Figure 9 (a) The palaeolocation of seven key sites used for reconstructing climate of the CPE. Large black dots represent the modern location. Small black dots represent the location at each Stage post the CPE, and coloured dots represent the location at each Stage during the CPE, for those Stages that the modern ocean crust was present. (b) Climate evolution across the CPE, simulated by the model, as experienced at the same seven sites. Filled (open) symbols indicate that a particular site is marine (terrestrial) at a particular Stage.CC-BY · From the PDF
Figure 10 (a) Proxy temperature data (black asterixes) at Falkland plateau (Site 511) from TEX 86 . Eocene data are from Liu et al. (2009), and Cretaceous data from Jenkyns et al. (2012). Black line shows the line of best fit. Also shown is the modelled temperature evolution at Falkland plateau (green line), i.e. the adjustment factor. In (b) , the proxy data have been adjusted using the model output, relative to either the earliest (light blue) or latest (red) proxy data point. Blue and red lines show the respective lines of best fit. TEX 86 temperatures are calculated using the TEX H 86 -SST calibration of Kim et al. (2010).
Figure 10 (a) Proxy temperature data (black asterixes) at Falkland plateau (Site 511) from TEX 86 . Eocene data are from Liu et al. (2009), and Cretaceous data from Jenkyns et al. (2012). Black line shows the line of best fit. Also shown is the modelled temperature evolution at Falkland plateau (green line), i.e. the adjustment factor. In (b) , the proxy data have been adjusted using the model output, relative to either the earliest (light blue) or latest (red) proxy data point. Blue and red lines show the respective lines of best fit. TEX 86 temperatures are calculated using the TEX H 86 -SST calibration of Kim et al. (2010).CC-BY · From the PDF
Figure 11 (a) Total temperature change across the CPE (maximum temperature in the CPE minus minimum temperature in the CPE, C) for all modern locations, due to changes in palaeogeography and solar constant. Missing data (white) is where the Getech Plc plate model indicates that the modern location was not present across all the CPE. Also shown as black dots are the seven locations in Fig. 9. CPE is defined as from the early Cretaceous (Berriasian) to the late Eocene (Priabonian). (b-d) are similar, but show the change (b) from the late Cretaceous (Cenomanian) to the late Eocene (Priabonian), (c) from the early Paleocene (Danian) to the late Eocene (Priabonian), (d) from the early Eocene (Ypresian) to the late Eocene (Priabonian).
Figure 11 (a) Total temperature change across the CPE (maximum temperature in the CPE minus minimum temperature in the CPE, C) for all modern locations, due to changes in palaeogeography and solar constant. Missing data (white) is where the Getech Plc plate model indicates that the modern location was not present across all the CPE. Also shown as black dots are the seven locations in Fig. 9. CPE is defined as from the early Cretaceous (Berriasian) to the late Eocene (Priabonian). (b-d) are similar, but show the change (b) from the late Cretaceous (Cenomanian) to the late Eocene (Priabonian), (c) from the early Paleocene (Danian) to the late Eocene (Priabonian), (d) from the early Eocene (Ypresian) to the late Eocene (Priabonian).CC-BY · From the PDF

Verification

Claims the paper makes

The claims and statistics of this paper haven’t been checked yet.

Run the check — free, no account needed. It reads the open-access text and checks the sources it cites.

A few free checks a day · papers already verified open instantly · results are public

Claims other papers make about this one

Each is checked against this paper’s own text: does it say what the citing paper says it does?

Self-check

Percentages, sums and reported differences re-computed from the paper’s own numbers.

The self-check needs the paper’s full text.

Citations

Cites

Show all 3 references

Research works printed but not linked: 65

  1. Barrera, E. and Huber, B. T.: Evolution of Antarctic waters during the Maestrichtian: Foraminifer oxygen and carbon isotope ratios, ODP Leg 113, in Barker, P. F., Kennett, J. P., et al., Proceedings of the Ocean Drilling Program, scientific results: College Station, Texas, Ocean Drilling Program, 113, 813–823, 1990. · DOI
  2. Barron, E. J. and Peterson, W. H.: Mid-Cretaceous ocean circulation: results from model sensitivity studies, Paleoceanography, 5, 319–337, 1990. · DOI
  3. Barron, E. J. and Washington, W. M.: The role of geographic variables in explaining paleoclimates: results from Cretaceous Climate Model sensitivity studies, J. Geophys. Res., 89, 1267–1279, 1984. · DOI
  4. Barron, E. J., Sloan II, J. L., and Harrison, C. G. A.: Potential significance of land-sea distribution and surface albedo variations as a climatic forcing factor; 180 M.Y. to the present, Palaeogeogr. Palaeocl., 30, 17–40, 1980. · DOI
  5. Barron, E. J., Fawcett, P. J., Peterson, W. H., Pollard, D., and Thompson, S. L.: A `simulation' of mid-Cretaceous climate, Paleoceanography, 10, 953–962, 1995. · DOI
  6. Beerling, D. and Royer, D.: Convergent Cenozoic CO2 history, Nat. Geosci., 4, 418–420, 2011. · DOI
  7. Beerling, D. J., Fox, A., Stevenson, D. S., and Valdes, P. J.: Enhanced chemistry-climate feedbacks in past greenhouse worlds, P. Natl. Acad. Sci. USA, 108, 9770–9775, 2011. · DOI · Paper page
  8. Bice, K. L. and Marotzke, J.: Could changing ocean circulation have destabilized methane hydrate at the Paleocene/Eocene boundary?, Paleoceanography, 17, 1018, https://doi.org/10.1029/2001PA000678, 2002. · DOI
  9. Bice, K. L., Huber, B. T., and Norris, R. D.: Extreme polar warmth during the Cretaceous greenhouse? Paradox of the late Turonian δ18O record at Deep Sea Drilling Project Site 511, Paleoceanography, 18, 1031, https://doi.org/10.1029/2002PA000848, 2003. · DOI
  10. Bice, K. L., Birgel, D., Meyers, P. A., Dahl, K. A., Hinrichs, K.-U., and Norris, R. D.: A multiple proxy and model study of Cretaceous upper ocean temperatures and atmospheric CO2 concentrations, Paleoceanography, 21, PA2002, https://doi.org/10.1029/2005PA001203, 2006. · DOI
  11. Bornemann, A., Norris, R., Friedrich, O., Beckmann, B., Schouten, S., Sinninghe-Damsté, J., Vogel, J., Hofmann, P., and Wagner, T.: Isotopic evidence for glaciation during the Cretaceous supergreenhouse, Science, 319, 189–192, 2008. · DOI
  12. Bradshaw, C. D., Lunt, D. J., Flecker, R., Salzmann, U., Pound, M. J., Haywood, A. M., and Eronen, J. T.: The relative roles of CO2 and palaeogeography in determining late Miocene climate: results from a terrestrial model-data comparison, Clim. Past, 8, 1257–1285, https://doi.org/10.5194/cp-8-1257-2012, 2012. · DOI
  13. Caballero, R. and Huber, M.: State-dependent climate sensitivity in past warm climates and its implications for future climate projections, P. Natl. Acad. Sci. USA, 110, 14162–14167, 2013. · DOI
  14. Caldeira, K. and Kasting, J. F.: The life span of the biosphere revisited, Nature, 360, 721–723, 1992. · DOI
  15. Cox, P., Betts, R., Bunton, C., Essery, R., Rowntree, P. R., and Smith, J.: The impact of new land-surface physics on the GCM simulation and climate sensitivity, Clim. Dynam., 15, 183–203, 1999. · DOI
  16. Cox, P. M., Betts, R. A., Jones, C. D., Spall, S. A., and Totterdell, I. J.: Modelling vegetation and the carbon cycle as interactive elements of the climate system, in: Meteorology at the Millennium, edited by: Pearce, R., Academic Press, San Diego CA, USA, 259–279, 2001. · DOI
  17. Cramer, B. S., Toggweiler, J. R., Wright, J. D., Katz, M. E., and Miller, K. G.: Ocean overturning since the Late Cretaceous: inferences from a new benthic foraminiferal isotope compilation, Paleoceanography, 24, PA4216, https://doi.org/10.1029/2008PA001683, 2009. · DOI
  18. Donnadieu, Y., Pierrehumbert, R., Jacob, R., and Fluteau, F.: Modelling the primary control of paleogeography on Cretaceous climate, Earth Planet. Sc. Lett., 248, 426–437, 2006. · DOI
  19. Donnadieu, Y., Goddéris, Y., and Bouttes, N.: Exploring the climatic impact of the continental vegetation on the Mezosoic atmospheric CO2 and climate history, Clim. Past, 5, 85–96, https://doi.org/10.5194/cp-5-85-2009, 2009. · DOI
  20. Donnadieu, Y., Pucéat, E., Moiraud, M., Guillocheau, F., and Deconinck, J.: A better-ventilated ocean triggered by Late Cretaceous changes in continental configuration, Nature Communications, 7, 10316, https://doi.org/10.1038/ncomms10316, 2016. · DOI
  21. Erbacher, J., Friedrich, O., Wilson, P., Lehmann, J., and Weiss, W.: Short-term warming events during the boreal Albian (mid-Cretaceous), Geology, 39, 223–226, 2011. · DOI
  22. Forster, A., Schouten, S., Baas, M., and Sinninghe Damste, J. S.: Mid-Cretaceous (Albian–Santonian) sea surface temperature record of the tropical Atlantic Ocean, Geology, 35, 919–922, 2007. · DOI
  23. Foster, G. L., Lunt, D. J., and Parrish, R. R.: Mountain uplift and the glaciation of North America – a sensitivity study, Clim. Past, 6, 707–717, https://doi.org/10.5194/cp-6-707-2010, 2010. · DOI
  24. Franks, P. J., Royer, D. L., Beerling, D. J., de Water, P. K. V., Cantrill, D. J., Barbour, M. M., and Berry, J. A.: New constraints on atmospheric CO2 concentration for the Phanerozoic, Geophys. Res. Lett., 41, 4685–4694, https://doi.org/10.1002/2014GL060457, 2014. · DOI
  25. Friedrich, O., Erbacher, J., Moriya, K., Wilson, P., and Kuhnert, H.: Warm saline intermediate waters in the Cretaceous tropical Atlantic Ocean, Nat. Geosci., 1, 453–457, 2008. · DOI
  26. Friedrich, O., Herrle, J. O., Wilson, P. A., Cooper, M. J., Erbacher, J., and Hemleben, C.: Early Maastrichtian carbon cycle perturbation and cooling event: Implications from the South Atlantic Ocean, Paleoceanography, 24, PA2211, https://doi.org/10.1029/2008PA001654, 2009. · DOI
  27. Friedrich, O., Norris, R. D., and Erbacher, J.: Evolution of middle to Late Cretaceous oceans – a 55 m.y. record of Earth's temperature and carbon cycle, Geology, 40, 107–110, 2012. · DOI
  28. Gordon, C., Cooper, C., Senior, C. A., Banks, H., Gregory, J. M., Johns, T. C., Mitchell, J. F. B., and Wood, R. A.: The simulation of SST, sea ice extents and ocean heat transports in a version of the Hadley Centre coupled model without flux adjustments, Clim. Dynam., 16, 147–168, 2000. · DOI
  29. Honisch, B., Ridgwell, A., Schmidt, D. N., Thomas, E., Gibbs, S. J., Sluijs, A., Zeebe, R., Kump, L., Martindale, R. C., Greene, S. E., Kiessling, W., Ries, J., Zachos, J. C., Royer, D. L., Barker, S., Marchitto, T. M., Moyer, R., Pelejero, C., Ziveri1, P., Foster, G. L., and Williams, B.: The geological record of ocean acidification, Science, 335, 1058–1063, 2012. · DOI
  30. Huber, B. T., Hodell, D. A., and Hamilton, C. P.: Middle-Late Cretaceous climate of the southern high latitudes: stable isotopic evidence for minimal equator-to- pole thermal gradients, Geol. Soc. Am. Bull., 107, 1164–1191, 1995. · DOI
  31. Huber, B. T., Norris, R. D., and MacLeod, K. G.: Deep-sea paleotemperature record of extreme warmth during the Cretaceous, Geology, 30, 123–126, 2002. · DOI
  32. Huber, M. and Caballero, R.: The early Eocene equable climate problem revisited, Clim. Past, 7, 603–633, https://doi.org/10.5194/cp-7-603-2011, 2011. · DOI
  33. Inglis, G. N., Farnsworth, A., Lunt, D., Foster, G., Hollis, C., Pagani, M., Jardine, P., Pearson, P., Markwick, P., Raynman, L., Galsworthy, A., and Pancost, R.: Descent towards the icehouse: Eocene sea surface cooling inferred from GDGT distributions, Paleoceanography, 30, 1000–1020, https://doi.org/10.1002/2014PA002723, 2015. · DOI
  34. Irvine, P. J., Gregoire, L. J., Lunt, D. J., and Valdes, P. J.: An efficient method to generate a perturbed parameter ensemble of a fully coupled AOGCM without flux-adjustment, Geosci. Model Dev., 6, 1447–1462, https://doi.org/10.5194/gmd-6-1447-2013, 2013. · DOI
  35. Jenkyns, H. C., Schouten-Huibers, L., Schouten, S., and Sinninghe Damsté, J. S.: Warm Middle Jurassic-Early Cretaceous high-latitude sea-surface temperatures from the Southern Ocean, Clim. Past, 8, 215–226, https://doi.org/10.5194/cp-8-215-2012, 2012. · DOI
  36. Kennedy, A., Farnsworth, A., Lunt, D., and Lear, C.: Palaeogeographic control on the atmospheric and oceanic impacts of Antarctic glaciation at the Eocene–Oligocene boundary, Philos. T. R. Soc. A, 373, 20140419, https://doi.org/10.1098/rsta.2014.0419, 2015. · DOI · Paper page
  37. Kim, J. H., Van Der Meer, J., Schouten, S., Helmke, P., Willmott, V., Sangiorgi, F., Koç, N., Hopmans, E. C., and Sinninghe Damsté, J. S.: New indices and calibrations derived from the distribution of crenarchaeal isoprenoid tetraether lipids: Implications for past sea surface temperature reconstructions, Geochim. Cosmochim. Ac., 74, 4639–4654, 2010. · DOI
  38. Lauderdale, J. M., Naveira Garabato, A. C., Oliver, K. I., Follows, M. J., and Williams, R. G.: Wind-driven changes in Southern Ocean residual circulation, ocean carbon reservoirs and atmospheric CO2, Clim. Dynam., 41, 2145–2164, 2013. · DOI
  39. Linnert, C., Robinson, S., Lees, J., Bown, P., Perez-Rodriguez, I., Petrizzo, M., Falzoni, F., Littler, K., Arz, J., and Russell, E.: Evidence for global cooling in the Late Cretaceous, Nature Communications, 5, 4194, https://doi.org/10.1038/ncomms5194, 2014. · DOI
  40. Littler, K., Robinson, S., Bown, P., Nederbragt, A., and Pancost, R.: High sea-surface temperatures during the Early Cretaceous Epoch, Nat. Geosci., 4, 169–172, 2011. · DOI
  41. Loptson, C. A., Lunt, D. J., and Francis, J. E.: Investigating vegetation-climate feedbacks during the early Eocene, Clim. Past, 10, 419–436, https://doi.org/10.5194/cp-10-419-2014, 2014. · DOI
  42. Lunt, D. J., Valdes, P. J., Dunkley Jones, T., Ridgwell, A., Haywood, A. M., Schmidt, D. N., Marsh, R., and Maslin, M.: CO2-driven ocean circulation changes as an amplifier of Paleocene–Eocene thermal maximum hydrate destabilization, Geology, 38, 875–878, 2010. · DOI
  43. Lunt, D. J., Dunkley Jones, T., Heinemann, M., Huber, M., LeGrande, A., Winguth, A., Loptson, C., Marotzke, J., Roberts, C. D., Tindall, J., Valdes, P., and Winguth, C.: A model-data comparison for a multi-model ensemble of early Eocene atmosphere-ocean simulations: EoMIP, Clim. Past, 8, 1717–1736, https://doi.org/10.5194/cp-8-1717-2012, 2012. · DOI
  44. Luyendyk, B. P., Forsyth, D., and Phillips, J. D.: Experimental approach to the palecirculation of the oceanic surface waters, Geol. Soc. Am. Bull., 83, 2649–2664, 1972. · DOI
  45. MacLeod, K., Huber, B., Berrocoso, A., and Wendler, I.: A stable and hot Turonian without glacial δ18O excursions is indicated by exquisitely preserved Tanzanian Foraminifera, Geology, 41, 1083–1086, 2013. · DOI
  46. Markwick, P. J. and Valdes, P. J.: Palaeo-digital elevation models for use as boundary conditions in coupled ocean–atmosphere GCM experiments: a Maastrichtian (late Cretaceous) example, Palaeogeogr. Palaeocl., 213, 37–63, 2004. · DOI
  47. Markwick, P. J.: The palaeogeographic and palaeoclimatic significance of climate proxies for data-model comparisons, in Deep time perspectives on climate change: marrying the signal from computer models and biological proxies, edited by: Williams, M., Haywood, A. M., Gregory, J. F., and Schmidt, D. N., The Micropalaeontological Society Special Publications, Geological Society of London, London, 251–312, 2007. · DOI
  48. Martinez-Boti, M., Foster, G., Chalk, T., Rohling, E., Sexton, P., Lunt, D., Pancost, R., Badger, M., and Schmidt., D.: Plio–Pleistocene climate sensitivity evaluated using high-resolution CO2 records, Nature, 518, 49–54, 2015. · DOI
  49. Otto-Bliesner, B. L., Brady, E. C., and Shields, C.: Late Cretaceous ocean: Coupled simulations with the National Center for Atmospheric Research Climate System Model, J. Geophys. Res., 107, 4019, https://doi.org/10.1029/2008PA001654, 2002. · DOI
  50. Pagani, M., Huber, M., Liu, Z., Bohaty, S. M., Henderiks, J., Sijp, W., Krishnan, S., and DeConto, R. M.: The role of carbon dioxide during the onset of Antarctic glaciation, Science, 334, 1261–1264, 2011. · DOI
  51. Pearson, P. N., Foster, G. L., and Wade, B. S.: Atmospheric carbon dioxide through the Eocene–Oligocene climate transition, Nature, 461, 1110–1113, 2009. · DOI
  52. Poulsen, C. J., Barron, E. J., Arthur, M. A., and Peterson, W. H.: Response of the mid-Cretaceous global oceanic circulation to tectonic and CO2 forcings, Paleoceanography, 16, 1–17, 2001. · DOI
  53. Poulsen, C. J., Gendaszek, A. S., and Jacob, R. L.: Did the rifting of the Atlantic Ocean cause the Cretaceous thermal maximum?, Geology, 31, 115–118, 2003. · DOI
  54. Poulsen, C. J., Pollard, D., and White, T. S.: General circulation model simulation of the δ18O content of continental precipitation in the middle Cretaceous: a model–proxy comparison, Geology, 35, 199–202, 2007. · DOI
  55. Raymo, M. E., Ruddiman, W. F., and Froelich, P. N.: Influence of late Cenozoic mountain building on ocean geochemical cycles, Geology, 16, 649–653, 1988. · DOI · Paper page
  56. Royer, D., Pagani, M., and Beerling, D. J.: Geobiological constraints on Earth system sensitivity to CO2 during the Cretaceous and Cenozoic, Geobiology, 10, 298–310, 2012. · DOI · Paper page
  57. Ruddiman, W. F. and Kutzbach, J. E.: Forcing of Late Cenozoic Northern Hemisphere climate by plateau uplift in southern Asia and the American West, J. Geophys. Res.-Atmos., 94, 18409–18427, 1989. · DOI
  58. Scotese, C.: Atlas of Earth History, University of Texas, Arlington, available at: http://www.academia.edu/9730874/Atlas_of_Earth_History, ISBN: 0-9700020-0-9, 2001.
  59. Sellwood, B. W., Price, G. D., and Valdes, P. J.: Cooler estimates of Cretaceous temperatures, Nature, 370, 453–455, 1994. · DOI
  60. Spicer, R. A., Ahlberg, A., Herman, A. B., Hofmann, C.-C., Raikevich, M., Valdes, P. J., and Markwick, P. J.: The Late Cretaceous continental interior of Siberia: a challenge for climate models, Earth Planet. Sc. Lett., 267, 228–235, 2008. · DOI
  61. Upchurch, G. R., Kiehl, J., Shields, C., Scherer, J., and Scotese, C.: Latitudinal temperature gradients and high-latitude temperatures during the latest Cretaceous: Congruence of geologic data and climate models, Geology, 43, 683–686, 2015. · DOI
  62. Winguth, A., Shellito, C., Shields, C., and Winguth, C.: Climate response at the Paleocene–Eocene thermal maximum to greenhouse gas forcing – a model study with CCSM3, J. Climate, 23, 2562–2584, 2010. · DOI
  63. Zhang, Y., Pagani, M., Liu, Z., Bohaty, S. M., and DeConto, R.: A 40-million-year history of atmospheric CO2, Philos. T. R. Soc. A, 371, 20130096, https://doi.org/10.1098/rsta.2013.0096, 2013. · DOI
  64. Zhang, Z., Nisancioglu, K. H., Flatøy, F., Bentsen, M., Bethke, I., and Wang, H.: Tropical seaways played a more important role than high latitude seaways in Cenozoic cooling, Clim. Past, 7, 801–813, https://doi.org/10.5194/cp-7-801-2011, 2011. · DOI
  65. Zhou, J., Poulsen, C. J., Rosenbloom, N., Shields, C., and Briegleb, B.: Vegetation-climate interactions in the warm mid-Cretaceous, Clim. Past, 8, 565–576, https://doi.org/10.5194/cp-8-565-2012, 2012. · DOI

Cited by

Metadata

Authors
Lunt, D. J., Farnsworth, A., Loptson, C., Foster, G. L., Markwick, P., O'Brien, C. L., Pancost, R. D., Robinson, S. A., & Wrobel, N.
ORCID
Venue
Climate of the Past
Publisher
Copernicus GmbH
Published
2016-05-20
Volume
12
Issue
5
Pages
1181-1198
ISSN
1814-9332
DOI
10.5194/cp-12-1181-2016
Cited by
145
References
3
Language
en
Licence
creativecommons.org/licenses/by/3.0/ (vor)
Funders
Natural Environment Research Council (NE/K014757/1, NE/I005714/1, NE/I005501/2, NE/K012479/1)

About these checks

Registry, retraction, Cites and statistics results are computed, not judged, with one exception: a printed reference that no index lists is read once by a model before it counts as a citation error. Claims are extracted by a model and kept only when their quote appears verbatim in the text; each cited source is then checked, with a model’s help, for whether it says what the claim relies on. Those verdicts can be wrong — read the claim’s quote and the cited source before relying on one.

Statistics and arithmetic are recomputed, not judged.

Confidence bands are shown only for fields calibrated on our annotated test set. None is calibrated yet, so no band is shown.

What counts as a claim ›How we measure confidence ›How we check this ›

Are you an author, or do you see a problem with this page? Request a review