The volcanic eruption of Santorini in the Bronze Age left detectable debris across the Mediterranean, serving as an anchor in time for the region, synchronizing chronologies of different sites. However, dating the eruption has been elusive for decades, as radiocarbon indicates a date about a century earlier than archaeological chronologies. The identification of annual rings by CT in a charred olive branch, buried alive beneath the tephra on Santorini, was key in radiocarbon dating the eruption. Here, we detect a verified annual growth in a modern olive branch for the first time, using stable isotope analysis and high-resolution radiocarbon dating, identifying down to the growing season in some years. The verified growth is largely visible by CT, both in the branch’s fresh and charred forms. Although these results support the validity of the Santorini branch date, we observed some chronological anomalies in modern olive and simulated possible date range scenarios of the volcanic eruption of Santorini, given these observed phenomena. The results offer a way to reconcile this long-standing debate towards a mid-sixteenth century BCE date.
The volcanic eruption of Santorini in the Bronze Age was one of the largest in historical time1,2, spewing volcanic ash and sending pumice across the Mediterranean3. This debris found in stratified layers in archaeological sites serves as an absolute anchor in time, deeming layers beneath as “pre-eruption” and layers above as “post-eruption,” along with the artifacts they contain. According to the archaeological evidence synchronizing the Aegean with Egypt, the eruption should have occurred after the beginning of the New Kingdom in Egypt4. Based on extensive radiocarbon dating of dynastic Egypt, this date should fall between 1570–1544 BCE5.
However, radiocarbon dating places the eruption in the late seventeenth century BCE6,7, nearly a century in disagreement, generating a long-standing debate8 which has not been settled to this day9,10,11,12. The radiocarbon date is based on multiple samples of short-lived organic material from the destruction layer at Akrotiri6, as well as an olive branch, buried alive by tephra from the eruption13. The weighted average of the radiocarbon dates from 25 short-lived samples from Akrotiri (3345 ± 8)6 calibrated using the updated IntCal20 calibration curve14 provides a date range of 1630–1548 BCE (at 68.2% probability) or 1681–1542 BCE (at 95.4% probability). This date range spans more than a century, and thus is not very helpful in settling the debate.
The significance of wood buried alive as a sample for radiocarbon dating, as opposed to short-lived organic material such as an olive pit, is that wood is built over a number of years, providing a sequence in time rather than just one point. Matching multiple radiocarbon measurements to the radiocarbon calibration curve (termed “wiggle matching”15) generally gives a narrower date range compared to one radiocarbon measurement, which could potentially be matched to several areas on the calibration curve, resulting in a broader possible date range. The radiocarbon date for the eruption based on the olive branch, considering only that the samples taken from the branch are a sequence, is 1625–1567 BCE, at 1σ (68.2%) confidence interval7. This result is obtained by calibrating the radiocarbon age against the updated standard calibration curve, IntCal2014. This date range just barely includes the earliest possible date for the beginning of the New Kingdom.
Tree rings can store environmental data at an annual resolution and are thus an invaluable source for environmental as well as chronological data16. However, many trees do not form distinguishable annual growth rings, and the olive tree (Olea europaea) is thought to be among them17. This is most unfortunate as the olive is a long-lived fruit tree, one of the most common and characteristic species of the Mediterranean climate18,19,20, and the key piece of evidence for dating the Bronze Age eruption of Santorini. The debate surrounding the dating of the eruption sparked a renewed interest in determining whether or not olive trees produce annual growth rings17, as the first work published on the olive branch from Santorini relied on X-ray tomography for ring count, and subsequent modelling of radiocarbon dates13. It has previously been shown that subjective visual identification of olive growth rings is unreliable17,21.
Previous studies have shown an intra-annual fluctuation pattern of δ13C for numerous tree species22,23,24,25,26,27. These fluctuations are thought to be linked not only to δ13C fluctuations of atmospheric CO2 but also to changing environmental conditions, such as moisture, light, and temperature, which in turn affect the ratio of the partial pressure of CO2 in the intercellular spaces and that of atmospheric CO2, leading to a fractionation effect between the stable carbon isotopes. In addition, the exploitation of δ13C enriched energy reserves, such as starch during times of decreased photosynthetic activity, can lead to intra-annual variations in δ13C24,28,29.
We take advantage of this phenomenon and combine it with detailed structural studies of olive wood using micro-CT and chronological studies at a resolution of 1–2 years using radiocarbon dating. Dating at such high resolution is possible for a unique period of time beginning in the early 1960s, due to massive nuclear weapon testing in the atmosphere. This testing resulted in a sharp and nearly twofold increase in atmospheric radiocarbon levels, termed the “bomb peak”. This was followed by a gradual decrease, as atmospheric nuclear tests were banned30. Only in recent years has the atmospheric radiocarbon level approached “pre-bomb” levels. As the change in radiocarbon levels was relatively fast and dramatic, the difference between one year and another during the “bomb peak” is significant, which allows for a sequence of samples from this specific period to be radiocarbon dated at a nearly-annual (but sometimes sub-annual) resolution30.
High-resolution radiocarbon dating of modern olive wood
Numerous radiocarbon dates were obtained from a cross-section of a modern olive wood branch (Fig. 1), which was growing in northern Israel. Based on these dates, a 6 cm long segment was selected which contained the “bomb peak” years between 1957–1972 (red frame in Fig. 1). This segment was then cut with a microtome and divided into 96 contiguous samples, collected as pools of 30 µm thick sections of wood. A parallel segment was used for high-resolution micro-CT imaging.
Following α-cellulose extraction of all contiguous samples, aliquots were taken for 14C measurement and for δ13C composition determination. Radiocarbon results, presented as percent modern carbon (pMC), were calibrated and modeled with OxCal31. The pMC values obtained followed the radiocarbon “bomb peak” calibration curve closely and in a continuous manner (Fig. 2A), indicating consistent annual growth of the tree. A nearby growing pine (Pinus halepensis), a species known to have visibly distinguishable and reliable annual rings, was used as a reference. The pine ring widths were measured and cross-dated with a pine regional master chronology32 using standard dendrochronological methods. These dates were further verified by radiocarbon, measured from eight selected latewood α-cellulose samples (Fig. 2A), confirming the bomb peak curve shape and ruling out any considerable time lag in this region.
Stable carbon isotopes ratio (δ13C) reveals sub-annual signal
Most significantly, δ13C values of the contiguous cellulose samples from the olive wood segment revealed a recurring cyclic pattern (Fig. 2B). Radiocarbon dates support the assignment of each minimum point of δ13C values to the border between growth years (Fig. 2B,C). This shows that indeed, olive trees do produce new wood annually and that this wood can be identified by the δ13C pattern, making this 15-year segment the first sequence of verified annual growth rings in olive wood. It should also be noted that it is anchored in time, thanks to the pine rings, and is not in a significant lag relative to the “bomb peak”.
Seasonal cambial activity
Comparing the radiocarbon data from the olive wood with the raw data of the calibration curve (as described in30 for northern hemisphere zone 2 which is based on33,34,35,36,37,38) enables an even higher resolution placement in time. We posit that the minimum points of δ13C values (Fig. 2B) indicate the beginning of the growing season. The corresponding radiocarbon values for all minimum δ13C values are marked as green in Fig. 3, such that each green data point represents the start of a new growing season. Arbitrarily setting these data points to a certain month within the previously established year, based on radiocarbon dating, would move all data points either left (earlier) or right (later) compared to the “bomb peak”. The best fit we found for our data and the “bomb peak” calibration curve was when we arbitrarily assigned these minimum δ13C points to April of the corresponding year. This is consistent with previous descriptions of the beginning of annual cambial activity in olea europaea39,40. In addition, there seems to be a cessation of growth during the end of the year until new growth is restarted in the following April. This is especially noticeable in 1963 and 1964, where if growth were continuous, we would expect to see a gradual decrease in radiocarbon levels, following the highest point (which also happens to be the latest in the year) of both peaks. Instead, there is a noticeable break in autumn (around September) until the following year begins.
Identification of annual growth using CT scans of fresh and charred wood
As rings were originally identified in the olive branch found in Santorini41, the olive wood sections from segments II and III were scanned by micro-CT in order to observe changes in wood density. As shown in Fig. 3, the identifiable rings in the image generated by the micro-CT are easier to distinguish than those in the raw image. The banding in the raw image is, in part, due to dark-colored phenols which diffuse through multiple rings but are invisible to the micro-CT. It should be noted that an attempt to identify annual rings based on elemental fluctuations17 was carried out using scanning electron microscopy coupled with energy-dispersive X-ray spectroscopy (SEM–EDS) but did not reveal any ring patterns (Figure S1).
With the data from radiocarbon and the δ13C pattern, we were able to identify the locations on the micro-CT image of transitions between years. It should be noted that ring boundaries are found at the point of an increase in density, observed as white streaks. Intra-annual density fluctuations (IADFs) are observed as narrow white streaks between the thicker areas of increased density which were identified as rings. The IADFs may be distinguished from changes of density, which do reflect a ring boundary, as a true ring boundary is thicker and more continuous, compared to the IADFs, which are thinner and, in some cases, discontinuous even across the 1 cm wide section analyzed (Fig. 4). We, therefore, show that annually deposited wood increments may generally be detected using micro-CT.
The olive branch (Fig. 1) was cut during 2013. Thus, the last ring in the section should be dated to this year. Indeed, the radiocarbon dating of cellulose closest to the bark was dated to 2009 (the latest date possible in the NH2 calibration curve30). However, in both the micro-CT image and the raw image, there are less than ten possible rings visible between the ring dated to 1971 and the outermost wood dated to 2005–2009. Thus, just within the last 1.5 cm of the section, there is a discrepancy of about 30 years between the number of rings identified by micro-CT and the years measured by radiocarbon (four bottom-most dates in Figs. 1 and 4). Under a stereomicroscope, 17 parenchyma bands were identified in the last 0.5 cm (black rectangle in Fig. 4B, enlarged in Fig. 4E, parenchyma bands marked by arrows). Parenchyma bands have previously been used as a marker of growth ring boundaries42. The first half of this section (Fig. 4E) was radiocarbon dated as bulk to between 1990–1995, and the second half was dated in the same manner to 2005–2009, corresponding roughly to the number of parenchyma bands identified. However, no parenchyma bands were detected in the preceding 1 cm (the area just above the black rectangle in Fig. 4A), dated to 1973–1975, or in fact, anywhere else on the radius. Thus, for this last region of 1.5 cm near the bark, we were not able to align radiocarbon years to physically identified rings in the olive wood.
We have furthermore found that the number of bands visible using micro-CT is not altered by charring, although the entire segment underwent non-homogenous shrinkage (Fig. 4D). It was not possible to align images of the charred and fresh segments by simply enlarging the image of the charred sample. Rather, different areas in the image of the charred segment required different enlargements (Fig. 4C) in order to correlate to the original, non-charred segment (Fig. 4A). The δ13C recurring annual pattern (Fig. 2B), which corresponds with the years determined by radiocarbon, was found to be relatively preserved in the charred segment (Fig. 4D), as the number of rings expected from the combination of radiocarbon and δ13C (Fig. 4C) is comparable to that identified by the δ13C pattern in the tangentially parallel segment (Fig. 4D). These results are illustrated in Figure S3, with the cellulose samples having a higher, more enriched average δ13C value of − 22.9‰, while the average δ13C value of the charred samples is − 24.0‰. The amplitude of δ13C fluctuation is generally higher in the cellulose samples, with an average standard deviation of 0.3‰, while the average standard deviation among the charred samples is 0.2‰.
Simulation of dating scenarios based on modern olive wood chronological anomalies
The chronological anomalies we observed in modern olive wood included one CT-visible ring which, through radiocarbon dating, was discovered to hold about 20 years. In addition, previous work43 has shown that in a modern living olive branch, the outer wood, closest to the bark, can be off by a number of decades from the expected date. Thus, the wood, which should represent the last year of growth, may, in fact, be decades old, as olive wood can cease growth in one area of the circumference of a branch while continuing growth in another.
As these scenarios were observed in modern olive wood, it is possible similar effects may have occurred in the olive branch found buried in tephra at Santorini, resulting in shifted date ranges that could include the beginning of New Kingdom more easily. We modeled the following scenarios (Fig. 5), first as was modeled by the original authors: 1. assuming ring count is accurate13; 2. increasing ring count by 25% and gap uncertainty to 25% of the section count13; 3. considering measured segments only as a chronological sequence, with no regard to ring count7. Next, we simulated the possible scenarios we observed in modern olive wood: 4. The last ring visible by CT actually includes 20 years; 5. branch ceased growth in the area sampled for radiocarbon, but continued growth elsewhere along the circumference of the branch for 20 years more43, until the eruption (adding 20 years to scenario 1); 6. a combined effect of the last ring comprising 20 years in addition to growth cessation 20 years previously; 7. Age discrepancy of 40 years around the circumference of the branch43; 8. The combined effect of the last ring comprising 20 years in addition to 40 years age discrepancy around the branch circumference.
It should be noted that all dates within the range are not of equal probability. For example, the modeled and calibrated 2σ date range of scenario 3 (the only one in which the 1σ reaches a date range which can be settled with archaeological evidence-based chronology) using the recently published IntCal2014 is 1625–1567 BCE. It might then seem like the earliest possible date for the eruption at the beginning of the New Kingdom sometime after 1570 BCE could plausibly fit in this range. However, examining the probability distribution for this modeled date reveals a more complex picture (Fig. 6), due to the nature of the calibration curve, where not all dates in the date range are of equal probability.
Olive wood is frequently found as charred material in archaeological sites in the Mediterranean but is rarely exploited in dendrochronology due to the difficulty in objectively identifying annual rings. Here we utilized the “bomb peak” as an objective chronological reference for identifying annual rings in modern olive wood and unprecedentedly confirmed the annual fluctuating pattern of δ13C in fresh as well as charred wood. The intra-annual cyclicity of δ13C has been observed in many other tree species and is thus expected to be the result of a physiological mechanism, which can serve as a chronological tool independent of the “bomb peak”.
Based on the “bomb peak,” we have identified the growth season of olive wood, between April and September. It has been previously suggested that the olive would be out of sync with the northern hemisphere radiocarbon calibration curve, as it is harvested in autumn to winter10. However, as we have shown here, the growing season of the olive is springtime (during which olive pits form and harden19, making their time of harvest irrelevant), and therefore no shift from the regional calibration curve should be expected. This is indeed what we have observed – the contiguous radiocarbon measurements from olive wood match the “bomb peak” flawlessly.
The rings identified by micro-CT in this study were correlated with the rings confirmed by radiocarbon and the δ13C annual pattern. However, we have shown that nearly 30 years were masked in the last 1.5 cm of the wood radius. These were not detected by micro-CT or optical microscopy, but were evidenced by radiocarbon. Another example from a different olive tree growing nearby shows a similar problem of a deficit in the number of rings identified by micro-CT, compared with the number expected based on radiocarbon dating (Figure S2).
Considering it is possible for olive wood to contain a number of decades in the last CT-visible ring, as well as display an age discrepancy of a number of decades around the circumference of one living branch, these scenarios must be taken into account as possible explanations for the decades long unresolved disagreement between the radiocarbon-derived versus the archaeology-derived age of the Bronze Age eruption of Santorini. A crucial step forward was taken by Pearson et al.44, by publishing an annually resolved record of radiocarbon for the time period of 1700–1500 BCE. This work was combined in the updated IntCal20 standard radiocarbon calibration curve14. However, in most modeled scenarios, under a 1σ confidence level, the date range obtained from calibrating the last radiocarbon dated segment of the olive branch did not overlap with the date range of the beginning of the New Kingdom in Egypt.
Here, we modeled a number of scenarios based on the chronological anomalies we discovered in modern olive wood, and applied them to the olive branch radiocarbon results from Santorini. Calibrating the radiocarbon ages of the Santorini olive branch13 with the recently published annually resolved radiocarbon curve44 and IntCal 2014, and modeling the possible scenarios in which the measured date may not reflect the date of the eruption, results in date ranges which overlap with the date range suggested for the beginning of the New Kingdom in Egypt5.
This study shows that charred olive wood fragments, which are frequently found in archaeological sites around the Mediterranean, have the potential to reveal annual identifiable deposits. The δ13C pattern was relatively conserved through charring, as was found previously for almond45. In short sequences, the identification of a close estimate for ring count will enable carrying out “wiggle matching”15 for precise radiocarbon dating. Climatic information might also be extracted in longer sequences, either directly from the δ13C record or possibly from changes in cell structural properties46.
Correlation between δ13C and climate has been shown for many different species, but we have not been able to find a significant correlation between the δ13C values of the olive wood to climate data, such as the sum of annual precipitation or the average of maximum temperatures recorded for the area between the years 1957–1971 (Figure S4). In addition, we did not find a correlation between annual precipitation and widths of the corresponding growth rings during this period in the sampling location (Havat Hanania) in the olive or in the pine, a species often used in dendrochronology for this purpose (Figure S5). However, as a climate signal was not evident from the few pine trees sampled, the lack of correlation of olive tree rings in one branch to climate conditions should not be surprising, and should not discourage this direction of investigation.
In order to use the intra-annual δ13C fluctuation as an indication of the number of rings in olive wood, a more efficient method for high-resolution δ13C analysis of many continuous samples would be required, such as laser ablation-combustion-gas chromatography-isotope ratio mass spectroscopy (LA-C-GC-IRMS)47. In addition to the identification of olive wood growth season (spring through late summer), we have also noted a non-homogenous effect of charring on ring width size, which may have serious implications for dendrochronological studies of charred wood or paleoclimatic reconstructions based on ring width measurements carried out on other tree species. To our knowledge, the effect of charring on differential width change of tree rings has never been addressed.
In conclusion, by identifying annual and even seasonal growth in olive wood using high-resolution radiocarbon dating based on the “bomb peak”, we were able to provide plausible scenarios in which the radiocarbon dating of the olive branch found buried alive under the tephra of the Bronze Age volcanic eruption of Santorini can be reconciled with the archaeological evidence.
Our aim in this study was to find a method which may allow the detection of growth rings in olive wood, which would be confirmed as annual with radiocarbon dating. The highly resolved dating of a modern olive branch, besides serving as a reference for any potential annual ring detection method, also revealed some chronological anomalies. We then simulated these anomalies as possible scenarios for the olive branch found in Santorini, one of the most valuable remains for dating the Bronze Age eruption.
Study area and sampling procedure
Olive (Olea europeae) and pine (Pinus halepensis) trees were sampled from Havat Hanania (N32°56.153′, E035°25.296′, 415 m) in northern Israel. The pine was cored at about 1.5 m above ground using a 5.15 mm increment borer. A branch of olive wood was cut transversally, into slices ~ 10 cm thick. Both pine and olive wood were polished to 1000 grit grade. The olive transverse wood section required a belt sander (Makita #9404) with five grades of grit (24, 40, 80, 150, 320) followed by polishing with a random orbit sander (Makita #BO5041) with four grades of grit (400, 600, 800 and 1000), while the pine required only the latter sander, beginning at 80 grit grade. A radial section of 10 × 650 × 5 mm sampled from the branch of one olive tree, which was cut down as part of landscaping work, as well as one pine core were cut into thin sections of 30 µm using a WSL-Lab Microtome48.
Precipitation and temperature information for Havat Hanania was retrieved from the Israeli Meteorological Service database. Precipitation data was obtained from weather stations 212,500 and 212,499 in Havat Hanania, with a few missing data points filled by using data from nearby stations 212,720 and 212,850. Daily temperature data was retrieved from the nearest weather station 4640, with missing data points taken from weather station 5360.
Between 20–40 mg of thin sections of wood were placed in 16 × 125 mm borosilicate glass test tubes. The tops of the tubes were stuffed with meshed glass wool. Acid–base-acid (ABA) pretreatment was carried out based on Southon and Magana (2010):samples were treated with aliquots of 5 ml 1 N HCl for 1 h, washed with DDW, followed by 5 ml of 0.1 N NaOH for 1 h, again washed with DDW and finally treated for 1 h with 5 ml 1 N HCl in a water bath at 70 °C to remove any carbon that may have adhered during the alkaline treatment. Immediately following the ABA pretreatment, hollocellulose was extracted using a modification to a variation of the Jayme-Wise method suggested by Southon and Magana (2010): 2.5 ml of 1 N HCl and 2.5 ml of 1 M NaClO2 were added to the samples which were then transferred to a water bath at 70 °C and left overnight. After bleaching, the samples were washed with DDW. The samples were treated with 6 ml of 5 N NaOH for 1 h, followed by washing with DDW and subsequently treated for 1 h with 5 ml of 1 N HCl in a water bath at 70 °C. The samples were then washed with DDW until reaching a neutral pH, and dried in an oven at 100 °C.
Between 2–4 mg of α-cellulose were weighed into pre-baked (1 h at 900 °C) quartz tubes containing 200 mg CuO and oxidized to CO2 in a vacuum line at 900 °C for 3 h. CO2 pressure known to eventually result in ~ 1 mg carbon was transferred from each sample into tubes containing 1 mg of activated Co for graphitization. 14C content determination on the resulting graphite was carried out at the DANGOOR Research Accelerator Mass Spectrometry Laboratory at the Weizmann Institute49. All calculated 14C ages were corrected for isotopic fractionation based on the AMS stable carbon isotope ratio (δ13C value). Calibrated ages in calendar years were obtained from the IntCal20 (for pre-bomb) or Bomb 13 NH2 (for post-bomb) calibration curves14,30 using OxCal v 4.231 or CALIBomb30,50.
Stable isotope analysis
Cellulose samples of 0.3–0.55 mg were weighed into tin foil capsules (Elemental Microanalysis Ltd. 5 × 3.5 mm #D1015). Sample δl3C values were determined with an elemental analyzer (Carlo Erba 1108) linked to a continuous flow isotope ratio mass spectrometer (Optima, Micromass, UK).
X-ray computed tomography
Tree-ring visualization in olive wood was performed with a micro-CT scanner (CT-imaging, Germany). The protocol was performed with the following parameters:tubes voltage, 40 kV; tube current, 450 μA; exposure time, 90 ms.; effective voxel size, 0.080 mm. The charred segment was scanned with a micro-CT (Xradia Micro XCT-400) at an effective voxel size of 0.026 mm, where the parameters were:tubes voltage, 20 kV; tube current, 100 μA; exposure time, 20 s. The CT scans were performed at the In Vivo Imaging Center at the Weizmann Institute of Science. All images were viewed and analyzed with Avizo v. 9.2.
Scanning electron microscopy
The sample was mounted on an aluminium stub with carbon tape, and carbon coated using an evaporator (Auto 306 Turbo, Edwards, United Kingdom). Samples were imaged with a Supra 55 FEG SEM (Zeiss) using a secondary electron detector (2–5 kV), in combination with an EDS detector (Oxford) for elemental analysis. These experiments were carried out at the Electron Microscopy Unit of the Weizmann Institute of Science.
Sigurdsson, H. et al. Marine Investigations of Greece’s Santorini Volcanic Field. EOS Trans. Am. Geophys. Union 87, 337–348 (2006).
Druitt, T. H., McCoy, F. W. & Vougioukalakis, G. E. The late bronze age eruption of Santorini volcano and its impact on the ancient Mediterranean world. Elements 15, 185–190 (2019).
Huber, H. & Bichler, M. Geochemical correlation of archaeological sites using tephra from the Minoan eruption. Czechoslov. J. Phys. 53, A439–A453 (2003).
Höflmayer, F. The date of the Minoan Santorini eruption: quantifying the “offset”. Radiocarbon 54, 435–448 (2012).
Bronk Ramsey, C. et al. Radiocarbon-based chronology for dynastic Egypt. Science 328, 1554–1557 (2010).
Manning, S. W. et al. Dating the Thera (Santorini) eruption: archaeological and scientific evidence supporting a high chronology. Antiquity 88, 1164–1179 (2014).
Friedrich, W. L. et al. The olive branch chronology stands irrespective of tree-ring counting. Antiquity 88, 274–277 (2015).
Cherubini, P., Humbel, T., Beeckman, H., Tognetti, R. & Lev-Yadun, S. Bronze age catastrophe and modern controversy: dating the Santorini the olive-branch dating of the Santorini eruption. Antiquity 88, 267–274 (2013).
Kutschera, W. On the enigma of dating the Minoan eruption of Santorini. Proc. Natl. Acad. Sci. USA 117, 8677–8679 (2020).
Manning, S. W. et al. Mediterranean radiocarbon offsets and calendar dates for prehistory. Sci. Adv. 6, eaaz1096 (2020).
van der Plicht, J., Bronk Ramsey, C., Heaton, T. J., Scott, E. M. & Talamo, S. Recent developments in calibration for archaeological and environmental samples. Radiocarbon 62, 1–23 (2020).
Pearson, C. et al. Annual variation in atmospheric 14 C between 1700 Bc and 1480 Bc. Radiocarbon 00, 1–14 (2020).
Friedrich, W. L. et al. Santorini Eruption Radiocarbon Dated to 1627–1600 B.C. Science 312, 548–548 (2006).
Reimer, P. J. et al. The IntCal20 northern hemisphere radiocarbon age calibration curve (0–55 cal kBP). Radiocarbon 62, 725–757 (2020).
BronkRamsey, C., van der Plicht, J. & Weninger, B. Wiggle matching’ radiocarbon dates. Radiocarbon 43, 381–389 (2001).
Speer, J. H. Fundamentals of Tree Ring Research (University of Arizona Press, Tucson, 2010).
Cherubini, P. et al. Olive tree-ring problematic dating: a comparative analysis on Santorini (Greece). PLoS ONE 8, e54730 (2013).
Cherubini, P. et al. Identification, measurement and interpretation of tree rings in woody species from mediterranean climates. Biol. Rev. Camb. Philos. Soc. 78, 119–148 (2003).
Lavee, S. Biology and physiology of the olive. World Olive Encycl. 154, 59–110 (1996).
Moriondo, M. et al. Olive trees as bio-indicators of climate evolution in the Mediterranean Basin. Glob. Ecol. Biogeogr. 22, 818–833 (2013).
Ehrlich, Y., Regev, L., Kerem, Z. & Boaretto, E. Radiocarbon dating of an olive tree cross-section: new insights on growth patterns and implications for age estimation of olive trees. Front. Plant Sci. 8, 1918 (2017).
Battipaglia, G. et al. Variations of vessel diameter and δ13C in false rings of Arbutus unedo L. reflect different environmental conditions. New Phytol. 188, 1099–1112 (2010).
de Micco, V. et al. Discrete versus continuous analysis of anatomical and δ13C variability in tree rings with intra-annual density fluctuations. Trees - Struct. Funct. 26, 513–524 (2012).
Helle, G. & Schleser, G. H. Beyond CO2-fixation by Rubisco—an interpretation of 13C/12C variations in tree rings from novel intra-seasonal studies on broad-leaf trees. Plant, Cell Environ. 27, 367–380 (2004).
Vaganov, E. A. et al. Intra-annual variability of anatomical structure and δ13C values within tree rings of spruce and pine in alpine, temperate and boreal Europe. Oecologia 161, 729–745 (2009).
Ohashi, S., Okada, N., Nobuchi, T., Siripatanadilok, S. & Veenin, T. Detecting invisible growth rings of trees in seasonally dry forests in Thailand: isotopic and wood anatomical approaches. Trees - Struct. Funct. 23, 813–822 (2009).
Loader, N. J. et al. High-resolution stable isotope analysis of tree rings: implications of ‘microdendroclimatology’ for palaeoenvironmental research. The Holocene 5, 457–460 (1995).
Fichtler, E., Helle, G. & Worbes, M. Stable-carbon isotope time series from tropical tree rings indicate a precipitation signal. Tree-Ring Res. 66, 35–49 (2010).
Li, Z. H., Leavitt, S. W., Mora, C. I. & Liu, R. M. Influence of earlywood-latewood size and isotope differences on long-term tree-ring δ13C trends. Chem. Geol. 216, 191–201 (2005).
Hua, Q., Barbetti, M. & Rakowski, A. Z. Atmospheric radiocarbon for the period 1950–2010. Radiocarbon 55, 2059–2072 (2013).
Bronk Ramsey, C. Bayesian analysis of radiocarbon dates. Radiocarbon 51, 337–360 (2009).
Lorentzen, B. E. Variability in Levantine Tree-Ring Records and Its Applications in Dendrochronological Dating, Provenancing, and Paleoenvironmental Reconstruction in the Southern Levant (Cornell University, New York, 2015).
Nydal, R. & Lövseth, K. Carbon-14 Measurements in Atmospheric CO2 from Northern and Southern Hemisphere Sites, 1962–1993. https://doi.org/10.2172/461185 (1996).
Muraki, Y. et al. The New Nagoya Radiocarbon Laboratory. Radiocarbon 40, 177–182 (1997).
Yamada, Y., Yasuike, K. & Komuran, K. Temporal variation of carbon-14 concentration in tree-ring cellulose for the recent 50 years. J. Nucl. Radiochem. Sci. 6, 135–138 (2005).
Park, J. et al. 14C level at Mt Chiak and Mt Kyeryong in Korea. Radiocarbon 44, 559–566 (2002).
Damon, P. E., Cheng, S. & Linick, T. W. Fine and hyperfine structure in the spectrum of secular variations of atmospheric 14C. Radiocarbon 31, 704–718 (1989).
Nakamura, T. et al. Variations in 14C concentrations of tree rings. Chikyu-Kagaku (Geochemistry) 21, 7–12 (1987).
Liphschitz, N. & Lev-Yadun, S. Cambial activity of evergreen and seasonal dimorphics around the Mediterranean. IAWA 7, 145–153 (1986).
Drossopoulos, J. B. & Niavis, C. A. Seasonal changes of the metabolites in the leaves, bark and xylem tissues of olive tree (Olea europaea L.) I. Nitrogenous compounds. Ann. Bot. 62, 321–327 (1988).
Friedrich, W. L. et al. Santorini eruption radiocarbon dated to 1627–1600 BC. Science 312, 548 (2006).
Gourlay, I. D. Growth ring characteristics of some African Acacia species. J. Trop. Ecol. 11, 121–140 (1995).
Ehrlich, Y., Regev, L. & Boaretto, E. Radiocarbon analysis of modern olive wood raises doubts concerning a crucial piece of evidence in dating the Santorini eruption. Sci. Rep. 8, 1–8 (2018).
Pearson, C. L. et al. Annual radiocarbon record indicates 16th century BCE date for the Thera eruption. Sci. Adv. 4, eaar8241 (2018).
Caracuta, V. et al. Charred wood remains in the natufian sequence of el-Wad terrace (Israel): New insights into the climatic, environmental and cultural changes at the end of the Pleistocene. Quat. Sci. Rev. 131, 20–32 (2016).
Björklund, J. et al. Cell size and wall dimensions drive distinct variability of earlywood and latewood density in Northern Hemisphere conifers. New Phytol. https://doi.org/10.1111/nph.14639 (2017).
Schulze, B. et al. Laser ablation-combustion-GC-IRMS—a new method for online analysis of intra-annual variation of δ13C in tree rings. Tree Physiol. 24, 1193–1201 (2004).
Gärtner, H. & Schweingruber, F. H. Microscopic preparation techniques for plant stem analysis. Tree-Ring Res. 70, 55–56 (2013).
Regev, L. et al. D-REAMS: A New Compact AMS System for Radiocarbon Measurements at the Weizmann Institute of Science, Rehovot, Israel. Radiocarbon 59, 775–784 (2017).
Reimer, P. J., Brown, T. A. & Reimer, R. W. Discussion: reporting and calibration of post-bomb 14C data. Radiocarbon 46, 1299–1304 (2004).
The researchers wish to thank Prof. Dan Yakir from the Department of Earth & Planetary Sciences at the Weizmann Institute for granting permission to use his elemental analyzer. We also wish to thank Dr. Brita Lorentzen for her help with coring and cross-dating pine trees, Dr. Adi Naali from the Israeli Olive Council for providing us the olive tree samples and Prof. Zohar Kerem and Dr. Yizhar Tugendhaft for finding the correct sample and assistance in retrieving it. Additional thanks to Dr. Vlad Brumfeld and Dr. Inbal Biton for their help in procuring the CT images, as well as Dr. Elena Kartvelishvily for her help in obtaining the SEM images. Finally, thanks to Eugenia Mintz for her help in graphitization and preparing the samples for AMS.
This research was funded by the Max Planck-Weizmann Center for Integrative Archaeology and Anthropology “Timing of Cultural Changes” and the Exilarch Foundation for the Dangoor Research Accelerator Mass Spectrometer (D-REAMS) Laboratory. We wish to thank the Kimmel Center for Archaeological Science and George Schwartzman Fund for the laboratory and funding support field work. E.B. is the incumbent of the Dangoor Professorial Chair of Archaeological Sciences at the Weizmann Institute of Science.
The authors declare no competing interests.
Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
About this article
Cite this article
Ehrlich, Y., Regev, L. & Boaretto, E. Discovery of annual growth in a modern olive branch based on carbon isotopes and implications for the Bronze Age volcanic eruption of Santorini. Sci Rep 11, 704 (2021). https://doi.org/10.1038/s41598-020-79024-4