The caldera collapse of Deception Island Volcano, Antarctica, was comparable in scale to some of the largest eruptions on Earth over the last several millennia. Despite its magnitude and potential for far-reaching environmental effects, the age of this event has never been established, with estimates ranging from the late Pleistocene to 3370 years before present. Here we analyse nearby lake sediments in which we identify a singular event produced by Deception Island’s caldera collapse that occurred 3980 ± 125 calibrated years before present. The erupted tephra record the distinct geochemical composition of ejecta from the caldera-forming eruption, whilst an extreme seismic episode is recorded by lake sediments immediately overlying the collapse tephra. The newly constrained caldera collapse is now the largest volcanic eruption confirmed in Antarctica during the Holocene. An examination of palaeorecords reveals evidence in marine and lacustrine sediments for contemporaneous seismicity around the Antarctic Peninsula; synchronous glaciochemical volcanic signatures also record the eruption in ice cores spread around Antarctica, reaching >4600 km from source. The widespread footprint suggests that this eruption would have had significant climatic and ecological effects across a vast area of the south polar region.
Large volcanic eruptions can have pervasive climatic, ecological and economic effects1. Climate cooling caused by volcanic aerosols has caused crop failure, starvation, disease and civil unrest and has been linked to the rise and fall of civilisations2,3. Although major climate impacts are often associated with tropical volcanoes, high latitude eruptions may also have wide-ranging environmental consequences and trigger pronounced cooling at hemispheric scales4,5,6. Our understanding of the environmental and climatic impacts of many polar volcanic events, however, is limited by a lack of precision regarding the age of past eruptions as well as by the uncertain provenance of numerous tephra layers in ice and sediment cores7,8.
Deception Island is the largest active volcano in the Antarctic Peninsula region; with a basal diameter of 30 km it is on the scale of the volcanoes responsible for the largest eruptions on Earth over the last several millennia9,10,11,12. It is located in the South Shetland Islands (SSI; Fig. 1), in a volcanically active region that includes nine known volcanoes in the SSI and several more adjacent to the northern Antarctic Peninsula8. The potential of Deception Island eruptions to affect climates around Antarctica and beyond is demonstrated by the identification of its tephra layers in marine and lacustrine sediments situated up to ~1300 km from the volcano8,13,14,15,16 as well as in ice cores from the Antarctic Peninsula and East Antarctica, including at the South Pole8,17,18.
Deception Island has erupted more than twenty times since the 19th Century including three eruptions between 1967 and 1970 and seismic crises in 1992, 1999 and 201510,19,20. Whilst these recent eruptions have been relatively modest in magnitude, the hitherto undated caldera-forming event ejected a dense-rock equivalent (DRE) of 30–60 km3 of magma, comparable in volume to the catastrophic 1815 Tambora eruption that caused global cooling and resulted in “the year without a summer”1,2,10,11,12. The age of this major Deception Island eruption has, however, never been firmly established. Estimates have placed the event between the late Pleistocene and 3370 years before present, with 10000 years ago being the most widely repeated age12,13,21,22. During the collapse, rapid volcano-tectonic subsidence along pre-existing, tectonically-influenced faults resulted in a modern 8–10 km-diameter caldera that is of similar dimensions to those of Santorini and Krakatau (refs10,12 and references therein; Fig. 2). Caldera collapses on this scale are often associated with intense seismic swarms including multiple high-magnitude earthquakes23, and the large volume of magma erupted implies the likelihood of significant, widespread climate impacts.
Byers Peninsula, located ~40 km northwest of Deception Island on Livingston Island, is ideally located to record the eruptive history of the Deception Island volcano due to its proximity and the presence of numerous lakes. In this study, we examined sediments from Byers Peninsula lakes that preserve detailed, long-term environmental records of Deception Island volcanic activity in the form of tephra deposits. We made direct compositional comparisons between Byers Peninsula tephras and those on Deception Island to provide significantly improved age constraints for the caldera-forming eruption. Here we present data from four Byers Peninsula lakes (Escondido, Cerro Negro, Chester and Limnopolar) in which three major tephra horizons – here referred to as T1, T2, and T3 and whose composition indicated a Deception Island provenance – were correlated based on geochemistry and physical properties15 (see Fig. 3 and Supplementary Fig. S1). Our integration of the cumulative evidence derived from geochemical, petrological and palaeolimnological studies provides significant new insights into the chronology and physical and chemical processes that occurred during the Deception Island caldera collapse.
Results and Discussion
Several lines of evidence confirm that tephra T3 in Livingston Island lake sediments was produced by the Deception Island caldera-forming episode. On Deception Island, the Outer Coast Tuff Formation (OCTF; Fig. 2b) is accepted to be the stratigraphic unit that corresponds to the caldera-forming eruption. This formation, the most compositionally distinctive unit on Deception Island, is a sequence of pyroclastic density current deposits of mafic to intermediate composition9,10,12 (Fig. S2). The syn-caldera rocks contain evidence of mingling and co-eruption of two discrete magmas with geochemically distinct compositions, a feature found on Deception Island only in the OCTF. A first group of glass and bulk rock analyses of the OCTF fall within the main geochemical trend for Deception Island defined by the composition of pre- and post-caldera samples (Fig. 4 and Supplementary Fig. S2). By contrast, a second cluster groups at lower TiO2 and FeOt values, and for the same SiO2 have slightly higher concentrations of MgO, Al2O3 and CaO than the pre- and post-caldera rocks in major elements vs. SiO2 Harker diagrams (Fig. 4b and Supplementary Fig. S2). The presence of these two magmas suggests that the explosive eruption leading to caldera formation was triggered by the arrival of hotter and more primitive magmas into an existing reservoir12.
Like the OCTF, the T3 tephra layer’s glass geochemistry also suggests the presence of two magma series (Fig. 5); when T3’s volcanic glasses are compared to those of the OCTF, there is a clear match of all major element relationships as well as locations on the Total Alkali Silica (TAS) diagram (Fig. 5 and Supplementary Fig. S3). Based on these correlations, we conclude that tephra T3 is analogous to the syn-caldera OCTF formation and therefore corresponds to distal fallout from the event shortly before or during the caldera collapse.
Magmatic temperatures and pressures calculated by applying silica-activity geothermobarometry to volcanic glasses (T1: 1094 ± 40 °C, 3.1 ± 0.2 kbar; T2: 1098 ± 40 °C, 3.2 ± 0.2 kbar; T3: 1110 ± 40 °C, 3.2 ± 0.2 kbar) closely reflect the basaltic-andesite source at ca. 10 km depth. Given that tephra T3 contains abundant microlite-poor juvenile sideromelane, while other tephra layers are characterised by more microlite-rich crystalline textures (juvenile tachylite15), we conclude that the magma ascent of T3 was rapid and without prolonged shallow storage and associated late-stage crystallisation prior to eruption. T3 is also the only tephra in Byers Peninsula lakes that contains juvenile clasts coarser than 2 mm in diameter, whose deposition here requires an eruption column tall enough to transport the coarse particles over 40 km against the prevailing wind direction. Their presence is thus indicative of a major eruptive event; the finer grain-size distributions (all particles <250 µm)15 characteristic of all other lacustrine tephra layers are consistent with much smaller eruptions.
Hydrogen (δD) and oxygen (δ18O) isotopes in ejecta record the modification of the original magmatic signal by interaction with meteoric fluids and seawater. The measured isotopic values from Byers Peninsula provide evidence for the pre-collapse characteristics of the T3 magma as well as the evolution of Deception Island magmas during subsequent eruptions (tephras T2 and T1; 2370 ± 100 and 1890 ± 140 cal y BP, respectively; Fig. 3). T3 δD (−51.2‰; Supplementary Fig. S4) reflects its equilibrium with primary magmatic fluids and indicates that the T3 eruption occurred prior to seawater infiltration into the magma chamber and therefore prior to caldera collapse. By contrast, the post-collapse tephra layers T2 and T1 are characterised by progressive δD shifts towards oceanic values (−26.3‰ and −4.4‰, respectively; Supplementary Fig. S4) that document the admixture of seawater into the evacuated magmatic system during subsequent volcanic episodes24. The minimal variation in δ18O between the three tephra layers (range: 5.6–6.1‰) is consistent with limited fractionation typical of such high-T magmas and the relatively small δ18O differences between magmatic and non-magmatic waters.
Whereas geochemical analyses record information about the eruptive process, the stratigraphic setting of lacustrine tephra provides insights into associated palaeoseismicity. Deposits up to 112 cm thick are immediately superposed upon T3 in each of the four studied Byers Peninsula lakes (Fig. 3). The genesis of these beds was determined by characterizing the temporal evolution of several depositional proxies, which included lithology, geochemistry, diatom assemblages and radiocarbon ages. These proxies showed that these were event beds that resulted from rapid mass-wasting of allochthonous sediments. Above and below the deposits, sediments consist of a centimetre-scale alternation of dark brown moss-rich layers and light brown massive lacustrine clays and silty clays. Strikingly different characteristics within the mass-wasting beds include massive lithology, an absence of mosses, and sediment geochemical properties. Radiocarbon ages immediately above and below the beds confirm their rapid deposition. Within the beds, however, anomalous radiocarbon dates that deviate several thousand years from the chronosequence reflect the 14C-depleted carbon associated with the redeposition of catchment material (Fig. 3). Marked differences in organic matter geochemistry provide further evidence for the terrestrial origin of the rapid post-seismic deposition sediments (Fig. 6). The differences in TOC, TN, and δ15N between Lake Escondido sediments within event beds and those of pre- and post-event sediments are significant (p < 0.05) and indicate shifts between long-term organic lacustrine deposition and values that more closely reflect the soils of nearby terrestrial environments25, providing parallel evidence of the catchment origin of the sediments in seismic event beds. Above the event deposits, geochemical characteristics returned to ‘typical’ lacustrine values.
Diatom analysis of the Lake Limnopolar sedimentary record clearly showed that the species present in the mass-wasted sediments were derived from terrestrial and aerophilic assemblages, while those before and after the event were lacustrine taxa. There were three distinct periods in Lake Limnopolar sediments: prior to (Pre-Event), during (Event) and following (Post-Event) the rapid sedimentation event. Diatom assemblages in Pre- and Post-Event sediments were dominated by taxa that are typical of lakes on the Byers Peninsula plateau, as expected with normal lacustrine deposition26. Interestingly, Post-Event assemblages (Supplementary Fig. S5) differed from Event diatoms but also from Pre-Event assemblages, which may indicate an ecological reorganisation due to the perturbation of algal communities by the eruption and its associated post-seismic event. In contrast to abundant deposition in pre- and post-Event sediments, diatoms were scarce in sediments laid down during the rapid deposition event; the minimum threshold for inclusion statistical analyses was not reached in all samples. In all cases, however, event samples were characterised by strikingly different assemblages than those in lacustrine sediments (Supplementary Fig. S5) and were dominated by species observed in soils, mosses and seepage samples in the Antarctic and sub-Antarctic regions (refs26,27, Table S2 and Supplementary Information).
Biological, geochemical and radiochronological data thus showed significant differences between the mass-wasted beds and adjacent sediments, indicating that event beds contained rapidly deposited terrestrial material. We propose that this deposition was triggered by an extreme seismic episode associated with the Deception Island caldera collapse. Distinctive mass-wasting deposits have been generated in lake sediments due to the extreme seismic activity that has accompanied other caldera collapse eruptions; analogous, meter-thick event beds are found in lakes hundreds of kilometres from the 1960 magnitude 9.5 Chilean earthquake, the largest ever recorded23,28. Numerous earthquakes up to Magnitude 7 were recorded in association with the Mt. Katmai caldera collapse in 1912 (caldera diameter 4 km)23 and, given its much greater size, it is reasonable to infer that seismic events of similar or superior magnitude were associated with the collapse of the Deception Island caldera. Seismic seiches, which have been observed in lakes located hundreds to thousands of kilometres from the epicentres of high magnitude earthquakes, are known to cause rapid post-seismic remobilisation of large volumes of terrestrial material from catchments to lake sediments, and are the likely mechanism for the deposition of the Byers Peninsula mass-wasting beds28,29.
To establish a rigorous chronology, we constrained the tephrostratigraphy with a total of 54 AMS 14C dates based on aquatic moss samples and three thermoluminescence ages (refs30,31, Fig. 3 and Supplementary Table 1). Bayesian age-depth models indicate that the caldera collapse eruption occurred 3980 cal y BP. We specifically avoided dating bulk sediment samples, given their well-demonstrated problems in providing reliable dates in Antarctic lake and ocean samples14,32, with the exception of samples taken within the rapid deposition event where no mosses were present. Twenty-nine radiocarbon dates encompassing five cores and three lakes (Escondido, Chester and Cerro Negro) were used to determine the age of the caldera collapse event based on calibrated ages immediately above the rapid sedimentation event and immediately below T3 (Fig. 3). Lake Escondido served as the basis for our chronology given the abundance of moss remains, the availability of suitable dating material immediately above and below collapse event sediments, and its robust age-depth model. In this lake, moss from 0.5 cm below T3 returned an age of 4060 ± 50 cal y BP, while moss 1.3 cm above the rapid deposition event was aged 3890 ± 50 cal y BP. Bayesian age-depth modelling further constrained this age, placing the caldera collapse at 3980 cal y BP, with a 95% confidence age range of 3860–4110 cal y BP30. Chester Lake sediments confirmed the timing of the caldera collapse, with moss radiocarbon ages in sediments above the termination of the rapid deposition event indicating that it occurred just prior to 3930 ± 25 cal y BP (Core CH12-0501G, 0.6 cm above event sediments), 3940 ± 30 cal y BP (Core CH12-0401; 9.4 cm above) and 3960 ± 50 cal y BP (Core CH12-0801; 0.5 cm above) (Fig. 3). Due to a lack of datable material, no older bounding age was available from Chester Lake; heavily folded sediments below the termination of the rapid deposition event and limited overlap between cores prevented the construction of a robust composite age model30.
In Lake Cerro Negro, the radiocarbon age nearest to event sediments was aged 3130 ± 50 cal y BP, however this age was 8.6 cm above the event’s termination. No material suitable for radiocarbon dating was found below this horizon, either above or below T3. Bayesian age-depth modelling indicated a minimum age for the caldera collapse event of 3635 ± 440 cal y BP, however the Lake Cerro Negro model was based on five moss ages (vs. 17 in the Escondido model) and before 3130 cal y BP was based entirely on a single thermoluminescence age30. Although the modelled collapse event age in Lake Cerro Negro is broadly consistent with those determined in the other cores, we gave primacy to the ages from lakes Escondido and Chester due to the stronger age model and the position of radiocarbon samples in stratigraphic proximity to event beds and tephra. Lake Limnopolar ages were not used to constrain the collapse event as our data suggest that they were subject to large and variable reservoir effect due to ancient carbon contamination most likely stored in catchment soils (see Supplementary Information for details).
Now firmly established as a Holocene event, the erupted volume of 30–60 km3 and volcanic explosivity index (VEI) of 69,10,12 make the Deception Island caldera-forming eruption the largest eruption documented in Antarctica during the Holocene, exceeding the Hudson Mountains Subglacial Volcano (VEI 3-4; ref.33) by several orders of magnitude. Although an event of this magnitude would be expected to have widespread environmental consequences, until now, the lack of firm chronological constraint for the Deception Island caldera collapse had precluded an evaluation of the scope of its impacts. We therefore examined Antarctic ice cores, and lacustrine and marine sediments throughout the SSI and the Antarctic Peninsula, in search of contemporaneous volcanogenic layers and comparable event beds, revealing at least 18 such sites around Antarctica that preserve a record of the caldera collapse eruption (Fig. 1 and Supplementary Table 3). The distribution suggests that volcanic ejecta were transported by a predominantly westerly airstream and deposited across a wide region of the sub-Antarctic, with deflection onto the Antarctic continent mediated by the polar vortex, as indicated by modelling of recent Deception Island eruptions34. Glaciochemical signatures record a major volcanic event in Antarctic ice cores reaching >4600 km from Deception Island, with modelled ice ages that closely matched the Deception Island caldera-forming event. These included Talos Dome (3998 ± 130 y BP); Dome C (4004 ± 200 y BP); Dronning Maud Land (3995 ± 200 y BP); and Vostok (3942 ± 600 y BP)35,36,37,38,39,40, as well as Plateau Remote (3969 ± 100 y BP)41, whilst a tephra tentatively aged 3910 ± 200 y BP was deposited in a James Ross Island ice core18, although the correlations remain tenuous until they can be confirmed by geochemical composition data for these tephra. Tephra layers that we correlated to the Deception Island caldera collapse by a combination of chronology and/or geochemistry were also found in sediment cores and terrestrial sites situated across the SSI, James Ross Island and the Antarctic Peninsula, as well as in palaeoceanographic records from Bransfield Strait and the Scotia Sea (Fig. 1 and Supplementary Information). Several lakes from the Barton, Fildes and Potter peninsulas of King George Island, ~120–130 km downwind of Deception Island, contain eruptive-seismic depositional sequences with tephra, gravity flows and rapid-deposition events that in some instances reach 1.5 m thickness (Fig. 1 and Supplementary Table S3; refs42,43). The sedimentary record of another two King George Island lakes record tephra and periods of accelerated sedimentation, combined with the deposition of terrestrial diatoms and reductions in organic matter content due to inputs of allochthonous material, that are consistent with our event chronology44. These singular, largely unexplained stratigraphic features mirror those on Livingston Island and underline the magnitude of both the Deception Island eruption and the seismic episode.
Taken together, our study reveals conclusive, multidisciplinary evidence for a major volcanic episode with far-reaching effects at 3980 cal y BP. Ejecta from the caldera-forming eruption were deposited widely across the Antarctic, whilst a major coeval earthquake affected the Antarctic Peninsula region. In addition to resolving the long-lasting controversy regarding the timing of this major volcanic episode, these findings provide a valuable tie point for the calibration of ice and sediment core chronologies and will therefore contribute to an improved understanding of past Antarctic environmental change. Much remains to be elucidated about the effects of large eruptions on climate, and the data available at present are insufficient to provide a detailed characterisation of the climatic and ecological response to this and other profound but short-lived Antarctic events1,7. However, our study establishes a precise chronology for the Deception Island caldera collapse, a volcano-climatic event with a likely hemispheric impact. Future, high-resolution re-examination of ice and sediment records should help to clarify the influence of such volcanic forcing on Antarctic climate.
Sites, coring and subsampling
During Austral summer 2008 (Limnopolar Lake, 62° 37′ 23.65″S, 61° 06′ 23.67″W) and 2012 (Escondido Lake, 62° 37′ 06.57″S, 61° 03′ 36.51″W; Chester Lake, 62° 36′ 41.10″S, 61° 06′ 02.28″W; and Cerro Negro Lake, 62° 37′ 47.30″S, 61° 00′ 19.99″W) lakes were cored until the underlying glacial till was reached using a 90 mm diameter UWITEC piston corer mounted on a tripod as well as a 60 mm diameter UWITEC gravity corer to recover the undisturbed sediment-water interface, using the lake ice covers as platforms. Limnopolar Lake sediments were extruded, cut in 60 cm sections, and sealed for shipping, whilst the sediments of the other four lakes were sealed for shipping directly in the plastic core liners. All cores were stored in a cold room at 4 °C until they were opened in the laboratory, when they were split longitudinally and subsamples were taken from the centres of cores.
Stratigraphic ages were determined throughout cores in order to understand overall trends in sedimentation. In order to constrain event chronologies, particular attention was paid to samples immediately above and below tephra and the rapid, deposition event that was clearly distinguishable from the otherwise regular alternation of organic and mineral sedimentation. Fifty-four AMS radiocarbon measurements were performed, almost exclusively on large moss fragments, with samples from Limnopolar dated at the Poznań Radiocarbon Lab (Poznań, Poland) and those from the other four lakes prepared at the Université Laval Laboratoire de Radiochronologie (Quebec, Canada) and measured at the Keck Carbon Cycle Accelerator Mass Spectrometry Laboratory (Irvine, USA), respectively, along with three thermoluminescence ages measured at the base of cores in order to corroborate 14C data30,31. All radiocarbon ages were calibrated using the SHCal13 curve for the Southern Hemisphere45 and are listed in calibrated years before present (cal y BP), with the present indicating the year 1950 AD. A full list of 14C samples, accession numbers and data as well as other details about the chronology can be found in the Supplementary Information.
Bulk organic geochemistry and sediment stable isotope analysis
Samples were taken throughout two cores for sediment organic matter (total organic carbon: TOC; and total nitrogen: TN) and stable isotope analysis of N (δ15N) and C (δ13C). Samples were dried at 60 °C for 48 h and ground by hand using an agate mill. TOC, TN, δ13C and δ15N were determined using a Finnigan DELTAplus elemental analyser-continuous flow-isotope ratio mass spectrometer (EA-CF-IRMS) at the Centres Científics i Tecnològics of the Universitat de Barcelona (CCiTUB). The relative standard deviation (RSD) for TOC and TN measurements was 5% whilst the analytical precision for δ13C and δ15N was 0.2‰. Stable isotope ratios are reported in δ notation using parts per thousand units (‰) and are defined as δ = [(Rsample/Rstandard) − 1] × 1000.
Tephra geothermobarometry, geochemistry and stable isotope analysis
Magmatic temperatures and pressures were calculated by applying silica-activity geothermobarometry to volcanic glasses. Because the water content was not constrained, we assigned an H2O content range from 1 to 4%, just sufficient to achieve saturation, and utilised the silica-activity (in glass) geothermobarometer of Albarède46, which precisely matches with the formation conditions of basalt-andesite shield-volcanoes. Water variations gave negligible P-T fluctuations.
The composition of tephra samples from T1, T2, and T3 was determined by electron microprobe analysis at the Centres Científics i Tecnològics Universitat de Barcelona and the University of Bristol. Byers Peninsula tephra samples (0.5–2 g) were cleaned in an ultrasonic bath for five minutes and dried overnight at 80 °C. Dried samples were then sieved into individual size fractions at phi (φ) intervals from −1φ to <3φ (corresponding to >2 mm, 1–2 mm, 500–1000 µm, 250–500 µm, 125–250 µm, and <125 µm; φ = −log2d, where d is the particle diameter in mm). Matrix glass major element compositions (as oxides) were measured on carbon-coated polished grain mounts of the 0–1φ, 1–2φ, and 2–3φ size fractions using the Cameca SX100 electron microprobe at the University of Bristol. Analyses were performed under operating conditions of 15 kV accelerating voltage and 4 nA beam current using a defocused beam (10 μm) to minimise sodium mobility. A combination of mineral and glass standards were used for calibration. Typical 1σ standard deviation of counts was between 0.5 and 1%. Analyses of secondary standards (KK1, BCR2 and diopside) were repeated each day to identify any instrumental drift, for which no corrections were necessary. Counting times were 10 s for Na, Si, Al, K and Ca, and 30 s for Mg, S, P, Ti, Fe and Mn, over a total analysis time of 60 s. A total of 40–50 glassy crystal-poor grains within the 125–250 µm (2–3φ) size fraction was analysed for each tephra layer, with each grain analysed once. Analyses that were contaminated by crystal phases were excluded. All compositions are shown normalised to anhydrous composition.
Oxygen isotope analyses were performed on whole-rock powders by laser fluorination47, using a Synrad 25 W CO2 laser48 and ClF3 as reagent (cf. ref.49). Isotope ratios were measured on a VG-Isotech SIRA-II dual-inlet mass spectrometer at the Servicio de Isótopos Estables (Nucleus, University of Salamanca). The preparation systems included both a conventional and a laser fluorination line (δ18O determination in silicates), a D/H high-vacuum line for hydrogen extraction from hydrated minerals with a uranium-depleted reduction system, and a step-heating device for the fractional extraction and purification of fluids (liquid, gas) from potential presence of glass inclusions. Both internal and international reference standards (NBS-28, NBS-30) were run to check accuracy and precision. Results are reported in δ18O notation relative to the Vienna Standard Mean Ocean Water (V-SMOW) standard, using a δ18O value of 9.6‰ for NBS-28 (quartz) for the mass spectrometer calibration. Long-term reproducibility for repeated determination of reference samples was better than ± 0.2‰ (1σ).
D/H ratios were determined on a second SIRA-II mass spectrometer on H2 gas obtained by reduction over hot depleted-U of the water released by induction heating of samples, using a vacuum line, following the procedures described in Godfrey50 with modifications51. Samples were loaded into degassed platinum crucibles that were placed in quartz reaction tubes and heated under vacuum to 125 °C overnight to remove any adsorbed H2O. The yield of evolved gas was used to determine the amount of structural water contained in the sample. Results are reported in δD notation relative to the V-SMOW standard, using a δD = −66.7‰ for NBS-30 (biotite) for the mass spectrometer calibration. Long-term reproducibility for repeated determination of reference samples was better than ± 2‰ (1σ).
Samples for diatom analysis were taken at regular intervals from Lake Limnopolar (core LIM08). Organic matter was oxidised by treatment with hydrogen peroxide (33% H2O2) and samples were mounted in Naphrax following methods described in ref.27. Three hundred diatom valves from each sample were identified and enumerated on random transects at 1000x magnification under oil immersion using a Zeiss Axio Imager A1 microscope equipped with differential interference contrast optics. See Supplementary information for further details about diatom identification and statistical analyses.
The tephra datasets generated during and/or analysed during the current study are available in Supplementary Information File 2.
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Field work for this study was supported by the Spanish (2007; MEC grant POL2006-06635/CGL) and Portuguese (2012; grant PTDC/CTE-GIX/119582/2010) Polar programs. D.A. thanks the Natural Sciences and Engineering Research Council of Canada’s Discovery Grants program and the Instituto Antártico Uruguayo for logistical support. A.M.A-V. acknowledges funding from the Programa Propio I (Usal-2014), and the assistance of the Ramón y Cajal research program (RYC-2011-07584). A.G. thanks the MICINN grants CTM2009-05919-E, CGL2010-22022-C02-02, CGL2015-72629-EXP, CTM2016-79617-P (AEI/FEDER-UE) and the support provided by the Ramón y Cajal research program (RYC-2012-11024). MICINN grant CTM2009-07869-E/ANT supported laboratory analyses. M.O. also thanks the Ramón y Cajal research program (RYC-2015-17597) EJL acknowledges support from a Leverhulme Early Career Fellowship. This study is a contribution to ANTALP - Antarctic, Arctic, Alpine Environments (2017 SGR 1102), Generalitat de Catalunya.