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Tree rings reveal globally coherent signature of cosmogenic radiocarbon events in 774 and 993 CE

Nature Communicationsvolume 9, Article number: 3605 (2018) | Download Citation

Abstract

Though tree-ring chronologies are annually resolved, their dating has never been independently validated at the global scale. Moreover, it is unknown if atmospheric radiocarbon enrichment events of cosmogenic origin leave spatiotemporally consistent fingerprints. Here we measure the 14C content in 484 individual tree rings formed in the periods 770–780 and 990–1000 CE. Distinct 14C excursions starting in the boreal summer of 774 and the boreal spring of 993 ensure the precise dating of 44 tree-ring records from five continents. We also identify a meridional decline of 11-year mean atmospheric radiocarbon concentrations across both hemispheres. Corroborated by historical eye-witness accounts of red auroras, our results suggest a global exposure to strong solar proton radiation. To improve understanding of the return frequency and intensity of past cosmic events, which is particularly important for assessing the potential threat of space weather on our society, further annually resolved 14C measurements are needed.

Introduction

The precise dating of high-precision proxy archives is essential for climate reconstructions, as well as for their comparison with climate forcing agents, climate model simulations, historical sources and archaeological evidence. Extra-tropical wood formation usually generates distinct annual stem growth increments. Consecutive patterns of tree-ring width therefore allow continuous and often well-replicated records of multi-centennial to millennial length to be developed if suitable measurements from living trees are successfully cross-dated against relict wood from historical timbers, archaeological excavations and/or subfossil remains1. The annual dating accuracy of such composite chronologies is not only crucial for (paleo-) climatology and ecology1,2, but also for advancing interdisciplinary research that engages archaeology, history and the environmental sciences3. Although intercontinental assessments reveal a high level of growth coherency between individual ring width chronologies from different parts of the world2, their dating precision has never been independently corroborated at the global scale. Even a 1-year dating offset would prevent any straightforward comparison of tree-growth anomalies with climate forcing agents, output from climate model simulations, climate-induced environmental responses or documented socio-economic and political changes. A prime example of such interdisciplinary cross-comparison is the cluster of large volcanic eruptions identified from ice-core anomalies in 536, 540 and 547 Common Era (CE), which coincided with rapid cooling at the onset of the Late Antique Little Ice Age (LALIA)3, as well as the outbreak of the Justinian Plague in 541 CE and large-scale societal transformation and human migration across much of Eurasia.

If of sufficient amplitude, abrupt changes in the Earth’s atmospheric radiocarbon (14C) abundance4,5 are recorded in tree rings owing to the short mixing time of the atmosphere6, including stratosphere-troposphere exchanges. Often attributed to extreme fluxes of high-energy solar particles7,8, distinct 14C anomalies in 774/5 and 992-4 CE4,5,9,10,11,12,13, as well as possibly much earlier in 660 and 3372/1 BCE14,15 have been identified in local proxy archives. These so-called Cosmic Events also yield anomalies in records of other cosmogenic radionuclides, such as 10Be and 36Cl that are measured in ice cores7. Though proposed as a “paradigm for chronology”16, the extra-terrestrial origin, spatial variation and time-transgressive evolution of cosmogenic tie-points are still unknown because a spatially extensive, well-replicated network of isotopic markers across continents and hemispheres has not hitherto been available.

In an unprecedented voluntary collaboration of the international tree-ring community, the COSMIC initiative gathered wood samples from the majority of the world’s longest tree-ring records, spanning the decades 770–780 and 990–1000 CE. The resulting COSMIC network includes data from 44 disjunct tree-ring width measurement series (Supplementary Note 1), with sampling locations on five continents (Fig. 1; Supplementary Fig. 1). With the individual sites being distributed between 42° S and 72° N, and ranging from around 40 to 4000 m a.s.l., COSMIC represents most of the world’s extra-tropical forest biomes. Covering four atmospheric radiocarbon zones17, our dataset is composed of 13 genera, including 25 coniferous and two broadleaf species (Supplementary Tables 12). Wood fibres from each tree ring, dendrochronologically cross-dated to the period 770–780 CE, or, if not reaching that far back in time, to the interval 990–1000 CE, were manually separated, chemically extracted and automatically graphitized (Methods; Supplementary Table 3). Modern compact tandem accelerator mass spectrometry (AMS) requires 1000-times less material and operates as precisely as some traditional decay counters18 (Methods). Developed and based at ETH-Zurich, the “Mini Radiocarbon Dating System” (MICADAS)18 was used to measure the 14C content of 30–50 mg bulk cellulose for a total of 484 tree rings. A subset of 374 rings in the 770s CE interval originates from 27 records on the Northern Hemisphere (NH) and seven records on the Southern Hemisphere (SH). Another 110 rings that did not reach back into the 8th century CE represent eight NH and two SH records in the 990s CE.

Fig. 1
Fig. 1

COSMIC network. Distribution of 44 tree-ring records from which cellulose was extracted for annual 14C measurements during the intervals 770–780 and 990–1000 CE (circles and rectangles) (Supplementary Fig. 1; Supplementary Tables 1-2). Independent 14C evidence from two floating tree-ring chronologies21, 22 (green), and five (quasi) annually resolved ice-core 10Be records23, 24 (yellow). White dashed lines refer to atmospheric radiocarbon zones17. The map reflects knowledge from the authors and was created via software ArcGIS 10.1 SP1 for Desktop by Esri

Results

Cosmogenic radiocarbon signature in 774 CE

The coherent, rapid increase of 14C concentration in NH and SH tree rings reveals the global extent of the cosmogenic signature of extreme fluxes of high-energy solar energetic particles (SEP) in 774 (Fig. 2a). The lower Δ14C values in the SH most likely reflect different ocean circulation, wind and land–ocean–atmosphere exchanges6,19. For the NH, the individual 14C site values, as well as their corresponding hemispheric range, show low levels in 773 (∆∆14C = −0.1%), higher concentrations in 774 (0.4%), a further increase in 775 (0.95%), a relatively small increase in 776 (0.2%), and decreasing concentrations thereafter. Although the overall shape of the 14C time-series through the event is similar for both hemispheres, its amplitude is lower in the SH, and, in contrast to the NH signal, the 14C increase in 774 (0.7%) is comparable to the increase in 775 (0.6%) (Fig. 2a). Collating results from both hemispheres into four meridional bands reveals a similar time-transgressive pattern (Supplementary Fig. 2). The tree ring-based 14C concentrations predominantly reflect tropospheric conditions during wood formation, rather than concentrations of radiocarbon in the stratosphere where it is mostly produced. We therefore employ a global carbon box model to generate mechanistic understanding of the intra-annual course of the radiocarbon cycle (Supplementary Fig. 3). With 95% confidence, the model times the event, presumed to have been ephemeral, within the boreal growing season (June to August) of 774 CE (Supplementary Fig. 4a; Supplementary Table 4). Importantly, this seasonal timing is consistent with the observed ~10% relative difference in radiocarbon amplitude between the NH and SH.

Fig. 2
Fig. 2

COSMIC signature. a Annual 14C content of 374 tree rings formed between 770 and 780 CE at 27 and seven sites across the NH and SH (light blue and red lines), respectively (Supplementary Fig. 2). b 14C content of 110 tree rings from 990–1000 CE at eight and two sites in the NH and SH (blue and red lines), respectively. Thick lines bracket standard uncertainties around hemispheric means, lower box plots reveal year-to-year 14C differences (median, 25th and 75th percentiles), and SH data have been shifted relative to the earlier NH data

Cosmogenic radiocarbon signature in 993 CE

Similar in shape to the 8th century event is a significant, but smaller 14C excursion in 993 (Fig. 2b). The best model/data agreement at the 95% confidence interval suggests it occurred between February and June 993 (Supplementary Fig. 4b; Supplementary Table 4). In contrast to the 8th century excursion, the sharp radiocarbon enrichment in 993, found in both hemispheres, is followed by a moderate increase from 993 to 994 CE. This behaviour is indicative of a late boreal spring event. Although associated with uncertainties, our monthly resolved model assumes that about 2/3 of the total annual wood biomass is produced within 1–2 months in the middle of the vegetation period (Supplementary Fig. 3). Since this rather short window of cell formation and cell wall thickening is synchronized between all sites in each hemisphere, phenological changes in growing season length have no influence on the model outcome. Moreover, only a very small impact is expected from so-called carry-over effects, because <10% of stored carbohydrates from previous year(s) is typically used for cell growth. The model also accounts for seasonal differences in stratosphere–troposphere 14C exchange, and thus simulates the occurrence of both radiocarbon enrichment spikes in the boreal summer (July ± 1 month) of 774 and the boreal spring (April ± 2 months) of 993 (Supplementary Fig. 4) with great confidence. The intra-annual timing of the 14C event in 993 CE translates into a coherent signature across both hemispheres. While the global extent and time-transgressive evolution of the 774 and 993 events are similar, the amplitude of the latter event is about half that of the former. With our box model, an additional 5.3 ± 0.5 (9.6 ± 0.5) 1026 atoms, i.e. 1.8 ± 0.2 (3.2 ± 0.2) times the annual production, are needed to produce the 993 (774) anomaly (Supplementary Fig. 4). Although our findings demonstrate accurate cross-dating of well-replicated tree-ring chronologies from around the world, they still cannot guarantee the annual precision of individual measurements from single trees (Methods). The independent replication of tree-ring width measurement series therefore remains an essential element in dendrochronology, which further distinguishes our discipline from most other proxy archives for which sample size is much more restricted.

Discussion

Following the LALIA, the boreal summer of 774 over most of the NH was ~0.7 °C colder than the 1961–90 reference period20, whereas 993 coincided with medieval summer warmth of ~0.6 °C (relative to the 1961–90 mean climatology). Although speculative, slightly lower mean temperatures in the 770 s (compared to the 990 s) may have contributed to a larger, though insignificant (4.0‰ ± 0.4 in 774 versus 3.5‰ ± 0.7 in 993), hemispheric offset in the radiocarbon concentration (Fig. 2). In contrast to previous, model-based assumptions19, we hypothesize that an overall warmer climate in the 990 s might explain the smaller inter-hemispheric 14C difference during high medieval times via reduced atmospheric mixing and/or ocean upwelling in the SH. Our limited understanding of how, if at all, climate change affects the amount of outgassing 14C-depleted CO2 from the proportionally larger SH oceans, however, calls for more research. Moreover, different ecological site conditions and species-specific plant physiological processes, including xylogenesis, may further impact the timing and intensity of cellulose-based 14C anomalies through varying rates of cell formation and carbon sequestration12. Such influences are expected to be particularly strong in multi-biome, global scale tree-ring compilations2, such as the COSMIC network, which contains wood from living trees, historical timbers, archaeological excavations and subfossil remains of 27 species.

Of greater significance than the ~3–4‰ 14C inter-hemispheric offset (Fig. 2), we identify a meridional north–south gradient of declining average 14C values in each 11-year tree-ring record (Fig. 3). Independently of the two cosmogenic events in the 770s and 990s, the mean atmospheric radiocarbon concentration is generally higher at northern latitudes >60° N. The 14C transport to lower latitudes where the growing season of trees is usually lengthening, however, might be altered by stratosphere–troposphere exchanges6. Complex ocean circulations, climate gradients and different growing season lengths are expected to alter further the large-scale distribution of the Earth’s radiocarbon zones. Since the high 14C values at the most northern sites cannot be explained by these processes alone, further research into the role of ocean extent and winds6,19, ocean–atmosphere circulation and coupling, terrestrial and solar magnetism, and the combined effects on the global 14C dispersal, is needed.

Fig. 3
Fig. 3

COSMIC gradient. The 14C content of individual tree-ring site records averaged over 11-year intervals from 770–780 and 990–1000 CE. Horizontal lines indicate atmospheric radiocarbon zones17. Grey lines are standard errors of the tree-ring site records. Linear trends within the NH and across both hemispheres are R2 = 0.29 and 0.71, respectively (not shown)

The global signature of the two cosmogenic excursions independently validates the precise dating of well-replicated tree-ring chronologies from five continents. Moreover, it offers a unique opportunity for assessing and/or correcting records within and between proxy archives, akin to the nuclear Bomb Peak of the 1960s (Methods). This study further emphasizes the accuracy and relevance of using high-resolution 14C measurements in determining the age of floating tree-ring series that have been used to date the eruptions of Katla (Iceland)21 and Changbaishan (China and DPR Korea)22 and (Fig. 1). Quasi-independent evidence of the two radiometric time markers in the 770 and 990 s is also found in high-resolution 10Be deviations in five ice cores from Greenland and Antarctica23,24 (Fig. 1; Supplementary Table 5).

Given the exceptional nature of these two SEP events, we have examined contemporary medieval texts to see if any references might attest to these cosmic events. We recognize that interpretation of such documents is contested and acknowledge the potential for misinterpreting these narratives. The prominent Japanese Buddhist priest Kûkai (Kôbô Dashi), born in 774, was given the official name Henshô Knonô, often translated as “worldwide shining diamond”25. Moreover, “... a person from India presented himself before the Caliph al-Mansur in the year 776 who was well versed in the siddhānta method of calculation related to the movement of the heavenly bodies, ...”26, and in the same year there was a gathering of Mayan mathematicians and astronomers at Copán in Honduras27. Together with other writers, Britton28 refers to an aurora when talking about a red cross that appeared in the heavens after sunset between 773 and 776. Again, the 18th century physician Thomas Short (1690–1772) repeated a record from Chronicon Magdeburgensis29: “993 On the 7th of the Calends of January, at one a Clock in the Night, suddenly Light shined out of the Night like mid-day; it lasted an Hour, but the Sky turning red, the Night returned.”. Some references have been interpreted as aurora28,29,30, but may, alternatively, suggest point-of-light events, such as a gamma ray burst or supernova. Our data, however, suggest globally homogeneous impacts in 774 and 993 that can be best explained by large energy releases from the Sun7, such as SEP events. Historical records from Germany, Ireland and the Korean Peninsula suggest the occurrence of red auroras between late-992 and early-993 CE31, which could be interpreted as great magnetic storms from intense solar activity. While preceding previously reported 14C results from local analyses by one year5,14, the medieval observations are consistent with our findings.

Together with advances in accelerator mass spectrometry and the availability of continuous, multi-millennial tree-ring chronologies from different parts of the world, our results highlight the importance and feasibility of reproducing the decadal-resolved IntCal calibration curve at annual resolution over much of the Holocene and maybe even beyond32. Such an improved high-resolution radiocarbon record would provide unprecedented dating confidence to various fields of the natural sciences and humanities. It would also bring a deeper understanding of the frequency, magnitude and origin of cosmic events, critical to assessments of the threat of space weather to our society33.

Methods

Sample preparation

Although the highest level of caution has been applied in each step throughout the COSMIC project, the final 14C measurements may still contain some degree of uncertainty, because of a wider range of possible biases and errors inherent to such a community wide, voluntary collaboration (Supplementary Note 1).

Once identified, the original data provider, usually an experienced tree-ring researcher either at a university, institute or laboratory, be it private or governmental, delivered the right wood sample that comprises either the 770–780 or 990–1000 interval CE. Although this sounds trivial as individual samples are usually coded after sampling and before archiving, the relevant material often originates from fieldwork campaigns that, in some cases, have been conducted several decades ago. It is important to note, that both samples and scholars may have changed location and workplace throughout the years. A systematic, long-term archiving of wood samples from either extremely long-lived trees, historical timbers, archaeological excavations or subfossil remains, is often complicated because many universities, institutes and laboratories, smaller or larger, simply do not have the appropriate storage capacity. A sustainable archiving of relict wood samples, especially in the case of wet archaeological and subfossil material, poses a serious challenge, and funding for appropriate facilities of such long-term “service” is generally scarce.

Once the right sample was identified and found in one of the many COSMIC-relevant archives around the world (Supplementary Table 1), an accurate, high-resolution re-measurement of the individual tree-ring widths of the two decades of interest (770–780 and 990–1000 CE) was performed to ensure precise cross-dating. Each original data provider was asked to mark the rings in question, sometimes smaller than 0.1 mm if trees were growing at or near their species-specific distribution limit (see above). The labelled (coded) and marked (stitched) wood samples were then packed and sent to the Swiss Federal Research Institute WSL in Birmensdorf (Switzerland), where all material was quality controlled (e.g. wood composition), and further wood preparation steps were performed (see details below).

At WSL, each individual ring boundary from 770–780 or 990–1000 CE was re-identified to guarantee the correct ring width sequence within the two 11-year intervals. All rings were then manually cut with a scalpel and the corresponding wood material was carefully divided and fragmented into similarly sized fibre flakes. Even the smallest contamination either from unclean tools or neighbouring older and younger latewood and early cells, in cases of less defined or irregular ring boundaries, can cause a substantial bias. Contamination is particularly critical when running the high-resolution 14C measurements with the MICADAS18, simply because the total amount of material is only 20–50 mg (see below). Wood samples, ideally representing the interior part of the ring to avoid boundary contamination and seasonal differences in wood formation, were transported to the Laboratory of Ion Beam Physics at ETH Zurich (Switzerland), where all radiocarbon measurements were performed.

Radiocarbon measurements

Wood fibres of each tree ring (Supplementary Tables 1-2), putatively dendrochronologically cross-dated to either the 770–780 or 990–1000 CE interval, were manually separated, chemically extracted and automatically graphitized (Supplementary Table 3). All fibres were soaked in NaOH over night at 70 °C, before being washed for 1 h with HCl and again 1 h in NaOH. All fibres were finally bleached in 5% NaClO4 for 2–3 h at 70 °C until they turned white12. A total of 2–3 mg of cellulose per individual ring sample was wrapped in tin capsules and graphitized in the automated graphitization line “AGE”34,35 (see details below). The cellulose-based graphite was then analysed for its radiocarbon concentration with the high-precision compact accelerator mass spectrometer MICADAS18. This modern AMS was developed and is located at ETH Zurich. Subdivided into 10 cycles of 30 s, total measurement time was 1–2 h/sample, with an OX-II standard typically yielding ~500,000 counts or more (12C-ion currents of 50 μA) (see details below). Radiocarbon-dead kauri (Agathis australis) wood from New Zealand and brown coal from Germany12, as well as an absolutely dated historical reference timber from 1515 CE1, were considered for 14C normalization and independent quality control.

The raw wood from each annual tree-ring sample was chemically extracted to holocellulose following a modified version of the BABAB protocol36, i.e. the base-acid-base-acid bleaching method for holocellulose extraction before graphitization37. Sequential steps in the procedure are shown in Supplementary Table 3. Samples were washed at near neutral pH with de-ionized water between each processing step. The combination of sample combustion with an elemental analyser and the subsequent graphitization of the CO2 with H2 on iron powder is widely used to prepare graphite targets for radiocarbon measurement by AMS. Graphitization via “AGE”34,35 considers pre-cleaned iron as a catalyst, for which iron was first baked for three minutes in ambient air, and then reduced under H2 atmosphere (at 80 kPa and 500 °C for 5 min) twice, followed by a third reduction step (80 kPa H2, 500 °C, 20 min). The reaction vessels of the AGE consist of Duran glass tubes that are prebaked (500 °C, 3 h) before use. Wood samples were weighed in tin capsules and combusted in an elemental analyser that transfers only the CO2 in helium to the AGE. The CO2 was trapped on zeolite while the helium carrier gas was removed. The CO2 was thermally released and transferred to the reactors by gas expansion. The amount of CO2 was held constant to maintain stable CO2/H2/Fe ratios for graphitization at 580 °C (0.9 mg carbon, 4.2 mg iron, H2/CO2 ratio = 2.3). Water formed from the reduction was frozen in a Peltier-cooled trap (at about –5 °C). The reaction was stopped automatically when residual gas pressures stabilize.

The 14C measurements were made with a MICADAS tandem accelerator18, which detect atoms of specific elements according to their atomic weights38. The graphite samples are first bombed with Caesium ions, producing negatively ionized carbon atoms before reaching the tandem accelerator where they are accelerated to the positive terminal by a high voltage difference. At this stage, other negatively charged atoms are unstable and cannot reach the detector. The negatively charged carbon atoms, however, move on to the stripper (a gas or a metal foil) where they lose the electrons and emerge as positively charged carbon atoms. Then, they further accelerate away from the positive terminal and pass through a set of focusing devices where mass analysis occurs. If the charged particles have the same velocity but different masses, as in the case of the carbon isotopes, the heavier particles are deflected least. Detectors at different angles of deflection then count the particles. All relevant processing steps are summarized in Supplementary Table 3.

Radiocarbon modelling

The carbon box model developed and introduced by12 was herein expanded and improved by separating the NH and SH data to simulate the interhemispheric offset as revealed by the COSMIC tree-ring network (Fig. 3). In the resulting model, each hemisphere contains 11 boxes (Supplementary Fig. 3; Supplementary Table 4), and the carbon exchange between the NH and SH only takes place in the atmosphere and the ocean. Furthermore, the different distribution of land and ocean, the varying growth seasonality and seasonal variation across the tropopause were considered39. The carbon fluxes between the boxes are balanced and were adapted using bomb peak data40. The model can be fitted simultaneously to two datasets using a X²-fitting routine which evaluates the most likely event date and the additional production needed to reproduce the data (Supplementary Table 4).

Data uncertainty

While the above sections, together with the Supplementary Note 1, outline much of the complexity our COSMIC project was facing in terms of data archiving, identification, preparation and processing, further challenges associated with species-specific tree physiological processes of carbon storage and re-mobilization41, as well as slight differences in growing season lengths42, and climate-induced intra-annual changes in xylogenesis and carbon allocation43 could not be entirely neglected. In addition, intra-annual density fluctuations, so-called false rings, in semi-arid environments44, not only require particular care and time for accurate cross-dating, i.e. matching variations in ring width or other tree-ring parameters and characteristics among several, independent tree-ring measurement series from multiple individual trees to allow the identification of the exact calendar year in which each tree ring was formed45, but may also affect the precise recording of rapid 14C increases.

A reduced amplitude, possibly due to species- and site-specific biological carry-over effects, was observed in a Mountain hemlock (Tsuga mertensiana) sample from the Great Nunatak Mountain region near the Prince William Sound in Alaska (USA10). A similarly dampened signal was exhibited by a Douglas-fir (Pseudotsuga menziesii) sample from the El Malpais National Monument in New Mexico (USA07). Furthermore, repeated measurements along different radii of an individual Scots pine (Pinus sylvestris) sample from the Torneträsk region in northern Sweden suggested a one-year inconsistency. The Torneträsk 14C measurements herein used, however, precisely detected the cosmic signal in either 993 or 774 CE (depending on the material used). A similar, 1-year dating irregularity was found in an individual kauri (Agathis australis) from northern New Zealand. The kauri samples herein used, however, confirm both of the events in 993 and 774 CE. It is important to note at this stage that in the temperate regions of the SH, tree growth starts in the spring of a certain year and ends in the summer of the following year. Following Schulman’s (1956) convention46, which assigns to each tree ring the date of the year in which tree growth started, year 774 in our paper refers to the spring-summer of the NH and November 774 until March 775 on the SH

On top of biological carry-over effects and wood anatomical features, several biotic and abiotic disturbance factors, such as insect outbreaks, fungal diseases and severe climate anomalies, cannot be ignored, especially if datasets are less replicated. Due to the frequent occurrence of severe defoliation patterns following massive outbreaks of the pandora moth (Coloradia pandora Blake), our ponderosa pine (Pinus ponderosa Dougl. ex Laws.) sample from a lava flow in central Oregon (USA16) indicated one missing ring. At that time, the sample was not part of a finally crossdated and published chronology. In addition, we detected a missing ring in a dead Bosnian pine (Pinus heldreichii) from central Albania (ALB01), as well as in a subfossil Norway spruce (Picea abies) remain from the Italian Alps (ITA09). Again, both samples were previously not included in published chronologies. It should be noted in this regard, that the earliest portion of species-specific site chronologies, often truncated and excluded from publications, may rely on the ring width measurements of one or two individual trees only. During such periods of very low sample size, cross-dating cannot be entirely validated. Even if well-replicated composite ring width chronologies are precisely dated at annual resolution, individual measurements of single trees therefore may still sporadically deviate due to missing rings and other reasons described above.

Finally, we suggest that the relatively small amplitude of the 14C event in 993 CE, especially when considering limited accuracy in radiocarbon measurements from less precise AMS systems, together with the possible effects of biological memory and even sample contamination in the case of very narrow tree rings and their irregular boundaries, appears less suitable for independent proxy archive dating, especially when compared to the much stronger event in 774 CE.

Data availability

All data will be freely available via https://www.ams.ethz.ch/research.html.

Additional information

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Acknowledgements

We thank everyone who participated in fieldwork, sample preparation, cross-dating and/or chronology development. This study was funded by the WSL-internal COSMIC project (5233.00148.001.01), the ETHZ (Laboratory of Ion Beam Physics), the Swiss National Science Foundation (SNF Grant 200021L_157187/1), and as the Czech Republic Grant Agency project no. 17-22102s.

Author information

Affiliations

  1. Department of Geography, University of Cambridge, Cambridge, CB2 3EN, UK

    • Ulf Büntgen
    • , Fredrik Charpentier Ljungqvist
    • , Alexander Kirdyanov
    • , Paul J. Krusic
    •  & Clive Oppenheimer
  2. Swiss Federal Research Institute WSL, CH-8903, Birmensdorf, Switzerland

    • Ulf Büntgen
    • , J. Diego Galván
    • , Paolo Cherubini
    • , Fritz H. Schweingruber
    • , Kerstin Treydte
    •  & Jan Wunder
  3. Global Change Research Institute CAS, 603 00, Brno, Czech Republic

    • Ulf Büntgen
    • , Tomáš Kolář
    • , Tomáš Kyncl
    •  & Michal Rybníček
  4. Department of Geography, Masaryk University, 611 37, Brno, Czech Republic

    • Ulf Büntgen
  5. Laboratory for Ion Beam Physics, ETH Zürich, CH-8093, Zurich, Switzerland

    • Lukas Wacker
    • , Stephanie Arnold
    • , Marcus Christl
    •  & Hans-Arno Synal
  6. Département de biologie, chimie et géographie, University of Québec in Rimouski, QC, G5L 3A1, Canada

    • Dominique Arseneault
  7. School of Natural and Built Environment, Queen’s University, Belfast, BT7 1NN, Northern Ireland, UK

    • Michael Baillie
  8. Swiss Federal Institute of Aquatic Science and Technology Eawag, CH-8600, Dübendorf, Switzerland

    • Jürg Beer
  9. CNR-IVALSA, Trees and Timber Institute, 38010, San Michele all′Adige, TN, Italy

    • Mauro Bernabei
  10. Competence Center for Underwater Archaeology and Dendrochronology, Office for Urbanism, City of Zurich, 8008, Zürich, Switzerland

    • Niels Bleicher
  11. School of Environment, University of Auckland, 1010, Auckland, New Zealand

    • Gretel Boswijk
    • , Anthony M. Fowler
    •  & Jan Wunder
  12. Institute of Geography, Friedrich-Alexander-University Erlangen-Nürnberg (FAU), 91058, Erlangen, Germany

    • Achim Bräuning
    •  & Jussi Grießinger
  13. Department Territorio e Sistemi Agro-Forestali, University of Padova, 35020, Legnaro (PD), Italy

    • Marco Carrer
  14. Department of History, Stockholm University, SE-10691, Stockholm, Sweden

    • Fredrik Charpentier Ljungqvist
  15. Bolin Centre for Climate Research, Stockholm University, SE-10691, Stockholm, Sweden

    • Fredrik Charpentier Ljungqvist
    •  & Björn E. Gunnarson
  16. Laboratorio de Dendrocronología y Cambio Global, Universidad Austral de Chile, Casilla 567, Valdivia, Chile

    • Duncan A. Christie
    • , Antonio Lara
    •  & Carlos LeQuesne
  17. Center for Climate and Resilience Research, Blanco Encalada 2002, 8370449, Santiago, Chile

    • Duncan A. Christie
    •  & Antonio Lara
  18. Rubenstein School of Environment and Natural Resources, University of Vermont, Burlington, Vermont, 05405, USA

    • Peter W. Clark
  19. Tree-Ring Laboratory, Lamont-Doherty Earth Observatory of Columbia University, Palisades, NY, 10964-8000, USA

    • Edward R. Cook
    • , Rosanne D’Arrigo
    • , Nicole Davi
    •  & Rob Wilson
  20. Department of Environmental Science, William Paterson University, Wayne, NJ, 07470, USA

    • Nicole Davi
  21. Icelandic Forest Research Mógilsá, 116, Reykjavik, Iceland

    • Ólafur Eggertsson
  22. Department of Geography, Johannes Gutenberg University, 55099, Mainz, Germany

    • Jan Esper
  23. Department of Geography, University of Guelph, ON, N1G 2W1, Canada

    • Ze’ev Gedalof
  24. AgroParisTech, INRA, Université de Lorraine, 54000, Nancy, France

    • Fabio Gennaretti
  25. Department of Geography, University of Tennessee, Knoxville, TN, 37996-0925, USA

    • Henri Grissino-Mayer
  26. Swedish Polar Research Secretariat, SE-104 05, Stockholm, Sweden

    • Håkan Grudd
  27. Department of Physical Geography, Stockholm University, SE-106 91, Stockholm, Sweden

    • Björn E. Gunnarson
    •  & Paul J. Krusic
  28. Institute of Plant and Animal Ecology, Ural Branch of the Russian Academy of Sciences, Ekaterinburg, 620144, Russia

    • Rashit Hantemirov
    •  & Vladimir Kukarskih
  29. Bavarian State Office for Monument Protection, 80539, München, Germany

    • Franz Herzig
  30. Department of Geology and Geography, West Virginia University, WV, 26505-6300, USA

    • Amy Hessl
  31. German Archaeological Institute, 14195, Berlin, Germany

    • Karl-Uwe Heussner
  32. Department of Geosciences, University of Arizona, Tucson, AZ, 85721, USA

    • A. J. Timothy Jull
  33. AMS Laboratory, University of Arizona, Tucson, AZ, 85721, USA

    • A. J. Timothy Jull
  34. Isotope Climatology and Environmental Research Centre, Institute of Nuclear Research, H-4001, Debrecen, Hungary

    • A. J. Timothy Jull
  35. Sukachev Institute of Forest SB RAS, 660036, Krasnoyarsk, Russia

    • Alexander Kirdyanov
  36. Department of Humanities, Siberian Federal University, 660041, Krasnoyarsk, Russia

    • Alexander Kirdyanov
    • , Vladimir S. Myglan
    •  & Olga Churakova (Sidorova)
  37. Department of Wood Science, Mendel University in Brno, 61300, Brno, Czech Republic

    • Tomáš Kolář
    •  & Michal Rybníček
  38. Navarino Environmental Observatory, GR-24001, Messinia, Greece

    • Paul J. Krusic
  39. Department of Earth Sciences, University of Gothenburg, 405 30, Gothenburg, Sweden

    • Hans W. Linderholm
  40. Department of Geography, Swansea University, Swansea, SA2 8PP, Wales, UK

    • Neil J. Loader
    •  & Giles H. F. Young
  41. Department of Geography, University of Western Ontario, London, ON, N6A 3K7, Canada

    • Brian Luckman
  42. Institute for Space-Earth Environmental Research, Nagoya University, Nagoya, 464-8601, Japan

    • Fusa Miyake
  43. Institute of Geography, University of Innsbruck, 6020, Innsbruck, Austria

    • Kurt Nicolussi
  44. Palaeontology, Geobiology and Earth Archives Research Centre, and ARC Centre of Excellence for Australian Biodiversity and Heritage, School of Biological, Earth and Environmental Sciences, The University of New South Wales, Sydney, NSW, 2052, Australia

    • Jonathan Palmer
  45. Laboratory of Tree-Ring Research, University of Arizona, Tucson, AZ, 85721, USA

    • Irina Panyushkina
  46. Harvard Forest, Harvard University, Petersham, MA, 01366, USA

    • Neil Pederson
  47. Chair of Forest Growth and Dendroecology, Institute of Forest Sciences, University of Freiburg, Freiburg, Germany

    • Andrea Seim
    •  & Willy Tegel
  48. Laboratory of Environmental Chemistry, Paul Scherrer Institute, 5232, Villigen, Switzerland

    • Michael Sigl
  49. Institute for Environmental Sciences, University of Geneva, 1205, Geneva, Switzerland

    • Olga Churakova (Sidorova)
  50. Department of Earth and Environmental Systems, Indiana State University, Terre Haute, IN, 47809, USA

    • James H. Speer
  51. Archaeological Service Kanton Thurgau (AATG), 8510, Frauenfeld, Switzerland

    • Willy Tegel
  52. Instituto Argentino de Nivología, Glaciología y Ciencias Ambientales, IANIGLA - CONICET, Mendoza, CP 330, 5500, Argentina

    • Ricardo Villalba
  53. Department of of Earth Sciences, The College of Wooster, OH, 44691, USA

    • Greg Wiles
  54. School of Geography and Geosciences, University of St Andrews, St Andrews, KY16 9AJ, Scotland, UK

    • Rob Wilson
  55. School of Natural Science, Hampshire College, Amherst, MA, 01002, USA

    • Lawrence J. Winship
  56. Key Laboratory of Desert and Desertification, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences, 730000, Lanzhou, China

    • Bao Yang

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Contributions

U.B. and L.W. designed the study with input from J.D.G. Radiocarbon measurements and analyses were performed by J.D.G. and L.W., with the involvement of J.W. Additional radiocarbon measurements and analyses were performed by A.J.T.J., I.P. and F.M. S.A., M.Chr. and L.W. modelled the 14-C. M.B. compiled the historical documentary evidence. The paper was written by U.B., together with P.J.K., C.O., J.E., M.B., F.C.L. and L.W. Further editorial contributions were obtained from J.B., P.C., M.Chr., R.H., F.H., F.H.S., H.-A.S., J.H.S. and R.W. Wood samples were collected, prepared and provided by D.A., M.B, N.B., G.B., A.B., M.Car., D.A.C., P.W.C., E.R.C., R.D’A., N.D., Ó.E., J.E., A.M.F., Z.G., F.G., J.G., H.G.-M., H.G., B.E.G., R.H., F.H., A.H., K.-U.H., V.K., A.K., T.Kol., P.J.K., T.Kyn., A.L., C.L.Q., H.W.L., N.J.L., B.L., V.S.M., K.N., J.P., N.P., M.R., A.S., O.C.(S.), J.H.S., W.T., K.T., R.V., G.W., L.J.W., B.Y. and G.H.F.Y. Ice core data were provided and discussed by M.S.

Competing interests

The authors declare no competing interests.

Corresponding authors

Correspondence to Ulf Büntgen or Lukas Wacker.

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DOI

https://doi.org/10.1038/s41467-018-06036-0

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