The instrumental record reveals that tropical cyclone activity is sensitive to oceanic and atmospheric variability on inter-annual and decadal scales. However, our understanding of the influence of climate on tropical cyclone behaviour is restricted by the short historical record and the sparseness of prehistorical reconstructions, particularly in the western North Pacific, where coastal communities suffer loss of life and livelihood from typhoons annually. Here, to explore past regional typhoon dynamics, we reconstruct three millennia of deep tropical North Pacific cyclogenesis. Combined with existing records, our reconstruction demonstrates that low-baseline typhoon activity prior to 1350 ce was followed by an interval of frequent storms during the Little Ice Age. This pattern, concurrent with hydroclimate proxy variability, suggests a centennial-scale link between Pacific hydroclimate and tropical cyclone climatology. An ensemble of global climate models demonstrates a migration of the Pacific Walker circulation and variability in two Pacific climate modes during the Little Ice Age, which probably contributed to enhanced tropical cyclone activity in the tropical western North Pacific. In the next century, projected changes to the Pacific Walker circulation and expansion of the tropics will invert these Little Ice Age hydroclimate trends, potentially reducing typhoon activity in the deep tropical Pacific.
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Grain-size data, median ages by depth, centennial event frequency and the dated material for core LTD3 are available from the National Oceanic and Atmospheric Administration National Centers for Environmental Information (NCEI) paleoclimatology database https://www.ncdc.noaa.gov/paleo/study/31132 and can also be found on the Woods Hole Open Access Server (WHOAS), https://doi.org/10.26025/1912/26159. Much of the data from the existing literature plotted in Fig. 2 can be found on the NCEI paleoclimatology database (https://www.ncdc.noaa.gov/paleo-search/) using the following data set ids: Fig. 2a [noaa-recon-13684], Fig. 2b [noaa-coral-13672], Fig. 2c [noaa-lake-29432], Fig. 2d [noaa-icecore-14174], Fig. 2e [noaa-cave-20530]. Data for Fig. 1b,c are available as tables at https://doi.org/10.1016/j.quascirev.2013.07.01921 and in the supplementary information at https://doi.org/10.1002/2015PA00287020.
The MATLAB code used to analyse the GCM output and the code and data used to plot the figures are available on the Woods Hole Open Access Server (WHOAS), https://doi.org/10.26025/1912/26159.
Peduzzi, P. et al. Global trends in tropical cyclone risk. Nat. Clim. Change 2, 289–294 (2012).
Emanuel, K., DesAutels, C., Holloway, C. & Korty, R. Environmental controls of tropical cyclone intensity. J. Atmos. Sci. 61, 843–857 (2004).
Gray, W. M. Global view of the origin of tropical disturbances and storms. Mon. Weather Rev. 96, 669–700 (1968).
Wu, L., Wen, Z., Huang, R. & Wu, R. Possible linkage between the monsoon trough variability and the tropical cyclone activity over the western North Pacific. Mon. Weather Rev. 140, 140–150 (2012).
Brandon, C. M., Woodruff, J. D., Lane, P. & Donnelly, J. P. Tropical cyclone wind speed constraints from resultant storm surge deposition: a 2500 year reconstruction of hurricane activity from St. Marks, FL. Geochem. Geophys. Geosyst. 14, 2993–3008 (2013).
van Hengstum, J. P. et al. The intertropical convergence zone modulates intense hurricane strikes on the western North Atlantic margin. Sci. Rep. 6, 21728 (2016).
Gao, S., Zhi, L., Zhang, W. & Chen, Z. Strong modulation of the Pacific Meridional Mode on the occurrence of intense tropical cyclones over the western North Pacific. J. Clim. 31, 7739–7749 (2018).
Huang, S. & Oey, L. Y. Land-falling typhoons are controlled by the meridional oscillation of the Kuroshio extension. Clim. Dynam. 52, 2855–2867 (2018).
Woodruff, J. D., Kanamaru, K., Kundu, S. & Cook, T. L. Depositional evidence for the kamikaze typhoons and links to changes in typhoon climatology. Geology 43, 91–94 (2015).
Liu, K., Shen, C. & Louie, K. A. 1,000-year history of typhoon landfalls in Guangdong, southern China, reconstructed from Chinese historical documentary records. Ann. Assoc. Am. Geogr. 91, 453–464 (2001).
Yu, K. F., Zhao, J. X., Shi, Q. & Meng, Q. S. Reconstruction of storm/tsunami records over the last 4000 years using transported coral blocks and lagoon sediments in the southern South China Sea. Quat. Int. 195, 128–137 (2009).
Donnelly, J. P. et al. Climate forcing of unprecedented intense-hurricane activity in the last 2000 years. Earth’s Future 3, 49–65 (2015).
van Hengstum, P. J. et al. Heightened hurricane activity on the Little Bahama Bank from 1350 to 1650 AD. Cont. Shelf Res. 86, 103–115 (2014).
Lane, P., Donnelly, J. P., Woodruff, J. D. & Hawkes, A. D. A decadally-resolved paleohurricane record archived in the late Holocene sediments of a Florida sinkhole. Mar. Geol. 287, 14–30 (2011).
Gischler, E., Shinn, E. A., Oschmann, W., Fiebig, J. & Buster, N. A. A 1500-year Holocene Caribbean climate archive from the Blue Hole, Lighthouse Reef, Belize. J. Coast. Res. 24, 1495–1505 (2008).
Donnelly, J. P. et al. 700 yr sedimentary record of intense hurricane landfalls in southern New England. Geol. Soc. Am. Bull. 113, 714–727 (2001).
Yan, Q., Wei, T. & Zhang, Z. Variations in large-scale tropical cyclone genesis factors over the western North Pacific in the PMIP3 last millennium simulations. Clim. Dyn. 48, 957–970 (2016).
Zhang, L., Karnauskas, K. B., Donnelly, J. P. & Emanuel, K. Response of the North Pacific tropical cyclone climatology to global warming: application of dynamical downscaling to CMIP5 models. J. Clim. 30, 1233–1243 (2017).
Blumenstock, D. I. Typhoon effects at Jaluit Atoll in the Marshall Islands. Nature 182, 1267–1269 (1958).
Toomey, M. R., Donnelly, J. P. & Tierney, J. E. South Pacific hydrologic and cyclone variability during the last 3000 years. Paleoceanography 31, 491–504 (2016).
Toomey, M. R., Donnelly, J. P. & Woodruff, J. D. Reconstructing mid-late Holocene cyclone variability in the Central Pacific using sedimentary records from Taha’a, French Polynesia. Quat. Sci. Rev. 77, 181–189 (2013).
Kench, P. S., McLean, R. F., Owen, S. D., Tuck, M. & Ford, M. R. Storm-deposited coral blocks: a mechanism of island genesis, Tutaga Island, Funafuti Atoll, Tuvalu. Geology 46, 915–918 (2018).
Kim, H. M., Webster, P. J. & Curry, J. A. Modulation of North Pacific tropical cyclone activity by three phases of ENSO. J. Clim. 24, 1839–1849 (2011).
Patricola, C. M., Camargo, S. J., Klotzbach, P. J., Saravanan, R. & Chang, P. The influence of ENSO flavors on western North Pacific tropical cyclone activity. J. Clim. 31, 5395–5416 (2018).
Denniston, R. F. et al. Extreme rainfall activity in the Australian tropics reflects changes in the El Niño/Southern Oscillation over the last two millennia. Proc. Natl Acad. Sci. USA 112, 4576–4581 (2015).
Emile-Geay, J., Cobb, K. M., Mann, M. E. & Wittenberg, A. T. Estimating central equatorial Pacific SST variability over the past millennium. Part II: reconstructions and implications. J. Clim. 26, 2329–2352 (2013).
Liu, Y. et al. Recent enhancement of central Pacific El Niño variability relative to last eight centuries. Nat. Commun. 8, 15386 (2017).
Emile-Geay, J. et al. Links between tropical Pacific seasonal, interannual and orbital variability during the Holocene. Nat. Geosci. 9, 168–173 (2015).
Denniston, R. F. et al. Expansion and contraction of the Indo-Pacific tropical rain belt over the last three millennia. Sci. Rep. 6, 34485 (2016).
Yan, H. et al. South China Sea hydrological changes and Pacific Walker circulation variations over the last millennium. Nat. Commun. 2, 293 (2011).
Yan, H. et al. Dynamics of the intertropical convergence zone over the western Pacific during the Little Ice Age. Nat. Geosci. 8, 315–320 (2015).
Sachs, J. P. et al. Southward movement of the Pacific intertropical convergence zone AD 1400–1850. Nat. Geosci. 2, 519–525 (2009).
Thompson, L. G. et al. Annually resolved ice core records of tropical climate variability over the past ~1800 years. Science 340, 945–950 (2013).
Kossin, J. P., Emanuel, K. A. & Camargo, S. J. Past and projected changes in western North Pacific tropical cyclone exposure. J. Clim. 29, 5725–5739 (2016).
Sharmila, S. & Walsh, K. J. E. Recent poleward shift of tropical cyclone formation linked to Hadley cell expansion. Nat. Clim. Change 8, 730–736 (2018).
Hong, C. C., Lee, M. Y., Hsu, H. H. & Tseng, W. L. Distinct influences of the ENSO-like and PMM-like SST anomalies on the mean TC genesis location in the western North Pacific: the 2015 summer as an extreme example. J. Clim. 31, 3049–3059 (2018).
Emanuel, K. & Nolan, D. Tropical cyclone activity and global climate. In Proc. 26th Conference on Hurricanes and Tropical Meteorology 240–241 (American Meteorological Society, 2004).
Emanuel, K. Tropical cyclone activity downscaled from NOAA-CIRES reanalysis, 1908–1958. J. Adv. Model. Earth Syst. 2, 1 (2010).
Camargo, S. J., Emanuel, K. A. & Sobel, A. H. Use of a genesis potential index to diagnose ENSO effects on tropical cyclone genesis. J. Clim. 20, 4819–4834 (2007).
Chiang, J. C. H. & Vimont, D. J. Analogous Pacific and Atlantic meridional modes of tropical atmosphere-ocean variability. J. Clim. 17, 4143–4158 (2004).
Chang, P. et al. Pacific meridional mode and El Niño–Southern Oscillation. Geophys. Res. Lett. 34, L16608 (2007).
PAGES Hydro2k Consortium. Comparing proxy and model estimates of hydroclimate variability and change over the Common Era. Clim. Past 13, 1851–1900 (2017).
Ault, T. R., Deser, C., Newman, M. & Emile-Geay, J. Characterizing decadal to centennial variability in the equatorial Pacific during the last millennium. Geophys. Res. Lett. 40, 3450–3456 (2013).
Zanchettin, D., Rubino, A., Matei, D., Bothe, O. & Jungclaus, J. H. Multidecadal-to-centennial SST variability in the MPI-ESM simulation ensemble for the last millennium. Clim. Dyn. 40, 1301–1318 (2013).
Pausata, F. S. R. & Camargo, S. J. Tropical cyclone activity affected by volcanically-induced ITCZ shifts. Proc. Natl Acad. Sci. USA 116, 7732–7737 (2019).
Camargo, S. J. Global and regional aspects of tropical cyclone activity in the CMIP5 models. J. Clim. 26, 9880–9902 (2013).
Chung, E. S. et al. Reconciling opposing Walker circulation trends in observations and model projections. Nat. Clim. Change 9, 405–412 (2019).
Vecchi, G. A. & Soden, B. J. Increased tropical Atlantic wind shear in model projections of global warming. Geophys. Res. Lett. 34, L08702 (2007).
Staten, P. W. et al. Tropical widening: from global variations to regional impacts. Bull. Amer. Meteor. Soc. 101, E897–E904 (2020).
Cobb, K. M. et al. Highly variable El Niño–Southern Oscillation throughout the Holocene. Science 339, 67–70 (2013).
Blauuw, M. & Christen, J. A. Flexible paleoclimate age-depth models using an autoregressive gamma process. Bayesian Anal. 6, 457–474 (2011).
Reimer et al. IntCal13 and Marine13 radiocarbon age calibration curves 0–50,000 years cal BP. Radiocarbon 55, 1869–1887 (2013).
Hua, Q., Barbetti, M. & Rakowski, A. Z. Atmospheric radiocarbon for the period 1950–2010. Radiocarbon 55, 2059–2072 (2013).
Weisler et al. Marine reservoir correction for the southern Marshall Islands for the past 2500 years. Radiocarbon 60, 333–348 (2018).
Knapp, K. R., Kruk, M. C., Levinson, D. H., Diamond, H. J. & Neumann, C. J. The international best track archive for climate stewardship (IBTrACS) unifying tropical cyclone data. Bull. Am. Meteorol. Soc. 91, 363–376 (2010).
Sueyoshi et al. Set-up of the PMIP3 paleoclimate experiments conducted using an earth system model, MIROC-ESM. Geosci. Model Dev. 6, 819–836 (2013).
Emanuel, K. A., Sundararajan, R. & Williams, J. Hurricanes and global warming: results from downscaling IPCC AR4 simulations. Bull. Am. Meteorol. Soc. 89, 347–367 (2008).
Bister, M. & Emanuel, K. A. Dissipative heating and hurricane intensity. Meteorol. Atmos. Phys. 65, 233–240 (1998).
Emanuel, K. A. Downscaling CMIP5 climate models shows increased tropical cyclone activity over the 21st century. Proc. Natl Acad. Sci. USA 110, 12219–12224 (2013).
Korty, R. L., Camargo, S. J. & Galewsky, J. Tropical cyclone genesis factors in simulations of the Last Glacial Maximum. J. Clim. 25, 4348–4365 (2012).
Hu, J., Emile-Geay, J. & Partin, J. Correlation-based interpretations of paleoclimate data – where statistics meet past climates. Earth Planet. Sci. Lett. 459, 362–371 (2017).
We thank student intern D. Carter for extensive labwork on core LTD3. This work was supported by the Strategic Environmental Research and Development Program (SERDP RC-2336). C.C.U. acknowledges support from NSF under AGS-1602455. We acknowledge the WCRP’s Working Group on Coupled Modelling, which is responsible for CMIP, and we thank the climate modelling groups for producing and making available their model output. CMIP5 model output was provided by the WHOI CMIP5 Community Storage Server via their website: http://cmip5.whoi.edu/. Any use of trade, firm or product names is for descriptive purposes only and does not imply endorsement by the US Government.
The authors declare no competing interests.
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Maps of the reconstruction site: a, Map of the tropical western Pacific, with the storm tracks of every tropical cyclone in the IBTrACS dataset to pass within 100 km of Jaluit Atoll; b, map of the site showing location of cores as green asterisks; c, bathymetric profile of the basin from which the sediment cores were extracted, with a salinity profile; d, map of the tropical Pacific with locations of the reconstructions referenced in this study.
Profiles of sediment cores collected from the Jaluit Atoll blue hole. a, BACON age model for LTD3 and b, coarse fraction profiles of LTD2 and LTD3. BACON-calibrated radiocarbon dates are displayed as green triangles. A tie point used in the age models and to establish core top depth by comparing drives are indicated with a blue dashed line. Storm beds were identified as those samples that exceeded 1.5 standard deviations above an 11-cm moving average, where both statistics were calculated while ignoring >2 standard deviation outliers.
Extended Data Fig. 3 Illustration of the method used to calculate centennial event frequency from coarse fraction.
Illustration of the method used to calculate centennial event frequency from coarse fraction. c, Coarse fraction anomaly is used to identify event deposits as in Methods. b, The annually-binned probability distribution function (PDF, blue shading) of each event deposit is extracted from the age model and summed for each year (black line). a, The sum of annual PDFs is summed over a 100-year moving window to construct a time series of centennial event frequency incorporating age model uncertainty.
Extended Data Fig. 4 Sensitivity analysis of the procedure used to identify event beds in Jaluit Atoll core LTD3 grain size data, using the 250–2000 μm coarse fraction.
Sensitivity analysis of the procedure used to identify event beds in Jaluit Atoll core, LTD3 grain size data, using the 250–2000 μm coarse fraction. Coarse fraction variance over the entire core was calculated a, with a moving-average window-size of 11 cm and exclusion of outliers, b, with a moving average window size of 11 cm and inclusion of outliers, c, with a moving average window size of 31 cm and exclusion of outliers, and d, with a moving average window size of 31 cm and inclusion of outliers. For each of these four cases, event beds were flagged with 1.5 standard deviation and 2 standard deviation cutoffs. The active interval thresholds for each of these cutoffs represents the 97.5 percentile frequency for a Poisson distribution with the core’s mean event frequency. Active intervals were identified as intervals lasting at least a century in which those thresholds were exceeded. Passive intervals were identified as intervals with zero events that were less than 2.5% likely to occur according to a gamma distribution. P-values are the cumulative frequency distribution values for a gamma distribution defined by a Poisson process defined by the cores centennial event frequency and the number of events contained in an active or passive interval, evaluated for the length of time between the first and last event in that interval.
Same as Extended Data Fig. 4, but using the >250 μm coarse fraction.
Extended Data Fig. 6 Ensemble median relative anomaly in tropical cyclone genesis indexes during the Little Ice Age (1400–1700 CE).
Ensemble median relative anomaly in tropical cyclone genesis indexes during the LIA (1400–1700 CE). Relative anomaly was calculated as Δ = (LIA - MCA) / MCA × 100%. The a, Genesis Potential Index41 is calculated from four variables: b, low level vorticity, η (s−1), c, vertical wind shear (ms−1), d, potential intensity (ms−1), and e, the mid-troposphere saturation deficit, χ (dimensionless)57. The colour palettes are aligned so red always indicates increasing cyclogenesis potential. The sign of relative vorticity in the southern hemisphere in b) was reversed so positive change indicates more cyclonic vorticity. Percent change values were calculated from storm season averages for the two time periods. In the northern hemisphere, the WNP storm season (JASON) was used. No data is shown for 1°S-1°N to indicate the different months used for averaging in each hemisphere. Black stippling indicates grid cells in which at least five of seven models agreed on the direction of change. The green symbols represent the locations of storm reconstructions (Extended Data Fig. 1).
Extended Data Fig. 7 Spearman rank correlation between mean storm season vertical wind shear and Pacific Meridional Mode for each of the CMIP5 models.
Spearman rank correlation between mean storm season vertical wind shear and Pacific Meridional Mode for each of the CMIP5 models. Correlation coefficients were calculated for Last Millennium experiment results for the period 1000–1850 CE. Black stippling indicates statistical significance as determined by a two-tailed Student t-test after taking into account multiple hypothesis testing using the false discovery rate procedure and setting q = 2.5%61.
Hadley circulation anomalies during the Little Ice Age (1400–1700 CE). Zonal (100–180°E) mean vertical pressure velocity associated with meridional overturning circulation (shading, vectors) and non-divergent meridional wind velocity (vectors) a,b, averaged over 1000–1850 CE and c,d, the LIA (1400–1700 CE) anomaly relative to 1000–1850 CE. The dashed vertical lines indicate the equator. Negative (positive) vertical pressure velocity values indicate ascending (descending) motion. Black stippling in c,d) indicates pressure/latitude coordinates where at least 5 of the 7 models agreed on the direction of change.
Sediment core radiocarbon dates.
Summary of CMIP5 models from which monthly mean data were used in the last millennium analysis.
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Bramante, J.F., Ford, M.R., Kench, P.S. et al. Increased typhoon activity in the Pacific deep tropics driven by Little Ice Age circulation changes. Nat. Geosci. 13, 806–811 (2020). https://doi.org/10.1038/s41561-020-00656-2