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USING RAPID ATMOSPHERIC 14C CHANGES IN THE 7TH CENTURY BC TO PRECISELY DATE THE FLOATING CHRONOLOGY FOR PINE WOOD FROM JÓZEFOWO (NORTHERN POLAND)

Published online by Cambridge University Press:  14 March 2024

Damian Wiktorowski Open the ORCID record for Damian Wiktorowski [Opens in a new window] ,
Marek Krąpiec Open the ORCID record for Marek Krąpiec [Opens in a new window] ,
Jacek Pawlyta Open the ORCID record for Jacek Pawlyta [Opens in a new window] ,
Joanna Barniak  and
Andrzej Rakowski Open the ORCID record for Andrzej Rakowski [Opens in a new window]
Damian Wiktorowski*
Affiliation:
AGH University of Science and Technology (AGH-UST), Mickiewicza Av. 30, 30-059 Krakow, Poland
Marek Krąpiec
Affiliation:
AGH University of Science and Technology (AGH-UST), Mickiewicza Av. 30, 30-059 Krakow, Poland
Jacek Pawlyta
Affiliation:
AGH University of Science and Technology (AGH-UST), Mickiewicza Av. 30, 30-059 Krakow, Poland
Joanna Barniak
Affiliation:
AGH University of Science and Technology (AGH-UST), Mickiewicza Av. 30, 30-059 Krakow, Poland
Andrzej Rakowski
Affiliation:
Silesian University of Technology, Konarskiego 22B str., 44-100 Gliwice, Poland
*
*Corresponding author. Email: wiktorowski@agh.edu.pl
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Abstract

The floating dendrochronological sequence of pine wood from Józefowo, N. Poland was expected to cover the ∼660 BC radiocarbon (14C) excursion. The sequence was radiocarbon dated using the OxCal wiggle matching procedure and the IntCal20 calibration curve. 14C concentrations were measured in one-year α-cellulose samples from around 660 BC. The published data on the ∼660 BC 14C excursion from Grabie, Poland were used to absolute date the Józefowo chronology with 1-year accuracy. The results confirm the occurrence of a rapid increase in Δ14C in 664/663 BC and its potential to be used as a fixing point for floating dendrochronological sequences.

Keywords

dendrochronologyMiyake eventradiocarbon AMS datingtree rings

Information

Type
Conference Paper
Information
Radiocarbon , Volume 66 , Issue 6: 24th Radiocarbon and 10th 14C & Archaeology, Zurich, Sept. 11–16, 2022 Proceedings Part 2 of 2 , December 2024 , pp. 2012 - 2021
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Copyright
© The Author(s), 2024. Published by Cambridge University Press on behalf of University of Arizona

INTRODUCTION

The use of dendrochronology, one of the most precise methods of absolute dating allowing annual precision, is limited by the availability of standard chronologies for individual tree species. In Central Europe, the most common taxa are oak (Quercus robur L. and Quercus petraea L.— anatomically indistinguishable wood) and pine (Pinus sylvestris L.). For oak, a chronology covering thousands of years has been compiled (Leuschner and Delorme Reference Leuschner and Delorme1988; Becker Reference Becker1993; Krąpiec Reference Krąpiec2001; Leuschner et al. Reference Leuschner, Sass-Klassen, Jansma, Baillie and Spurk2002; Friedrich et al. Reference Friedrich, Remmele, Kromer, Hofmann, Spurk, Felix Kaiser and Küppers2004), while for pine the standard chronologies cover the last millennium (Heussner Reference Heussner1996; Zielski Reference Zielski1997; Szychowska-Krąpiec and Krąpiec Reference Szychowska-Krąpiec and Krąpiec2005; Szychowska-Krąpiec 2010). Their extension is often limited by the poor availability of wood in both archaeological and geological sites. A chance to compile older chronologies is provided by subfossil pine wood found in peat deposits excavated during peat mining. Based on subfossil pine wood, a number of floating chronologies have been compiled in Poland and neighbouring areas, the time placement of which was determined by radiocarbon dating and the wiggle-matching technique (Pukienè 2001; Barniak et al. Reference Barniak, Krąpiec and Jurys2014; Edvardsson et al. Reference Edvardsson, Corona, Mazeika, Pukienè and Stoffel2016a; Krąpiec et al. Reference Krąpiec, Margielewski, Korzeń, Szychowska-Krąpiec, Nalepka and Łajczak2016; Achterberg et al. Reference Achterberg, Eckstein, Birkholz, Bauerochse and Leuschner2018). In Central Europe, the lack of accumulation of pine trunks in peatlands in the last two millennia is characteristic, and it is probably climatically determined (Edvardsson et al. Reference Edvardsson, Stoffel, Corona, Bragazza, Leuschner, Charman and Helama2016b), making it impossible to dendrochronologically date older floating chronologies based on standards going up to the present day. A new opportunity to date such floating chronologies has been provided by the discovery of abrupt changes in radiocarbon concentrations ascending within a single year by Miyake et al. (Reference Miyake, Nagaya, Masuda and Nakamura2012, Reference Miyake, Masuda and Nakamura2013, Reference Miyake, Masuda, Hakozaki and Nakamura2014, Reference Miyake, Jull, Panyushkina, Wacker, Salzer, Baisan, Lange, Cruz, Masuda and Nakamura2017). Such events from 774–775 AD and 994–995 AD have been used to date with annual accuracy floating chronologies or to confirm dendrochronological dates from Switzerland (Wacker et al. Reference Wacker, Güttler, Goll, Hurni, Synal and Walti2014), Japan (Hakozaki et al. Reference Hakozaki, Miyake, Nakamura, Kimura, Masuda and Okuno2018), and Poland (Krąpiec et al. Reference Krąpiec, Rakowski, Pawlyta, Wiktorowski and Bolka2021).

Another rapid increase in radiocarbon concentration has been noted around 660 BC and confirmed by Park et al. (Reference Park, Southon, Fahrni, Creasman and Mewaldt2017), Rakowski et al. (Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019), Koldobskiy et al. (Reference Koldobskiy, Mekhaldi, Kovaltsov and Usoskin2023), and Sakurai et al. (Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020). Similarly, to events from 774–775 AD and 994–995 AD, an increase in the production rate of 10Be and 36Cl has been noted, confirming the solar origin of this event (O’Hare et al. Reference O’Hare, Mekhaldi, Adolphi, Reisbeck, Aldahan, Anderberg, Beer, Christl, Fahrni, Synal, Park, Possnert, Southon, Edouard, ASTER and Muscheler2019). The event occurring around 660 BC is characterized by a prolonged increase in the Δ14C values between 665 and 661 BC, with differences in radiocarbon concentrations (Δ14C) from 665 BC and 664 BC presented in the literature as 8.9 ± 0.4‰ (Park et al. Reference Park, Southon, Fahrni, Creasman and Mewaldt2017), 8.3 ± 2.9‰ (Rakowski et al. Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019), and 9.8 ± 2.2‰ (Sakurai et al. Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020).

The amplitude of the event observed between 665 BC and 661 BC was 9.3 ± 2.6‰ in the data of Park et al. (Reference Park, Southon, Fahrni, Creasman and Mewaldt2017), 19.3 ± 3.5‰ in the data of Rakowski et al. (Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019) and 16.3 ± 2.1‰ in the data of Sakurai et al. (Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020). For all datasets, the minimum occurred around 665 BC and the maximum around 661 BC.

In this publication, we show for the first time the successful use of the Miyake event from 664–663 BC to date floating pine chronologies, which will serve as a reference to build a long absolute pine chronology from northern Poland for the first millennium BC, which is an important period for archaeological research in the region (Rose et al. Reference Rose, Müller-Scheeßel, Meadows and Hamann2022).

MATERIALS AND METHODS

All the used wood samples are in the archives of the AGH Dendrochronology Laboratory in Kraków. The pine (Pinus sylvestris L.) wood samples were taken from a peat bog exploited by the peat mining company AGARIS Poland in Józefowo, located about 25 km east of Elbląg (N Poland, GPS: 54.135763 N, 19.818319 E) (Figure 1). In 2013–2021, more than 500 wood samples were taken from the trunks of subfossil pines in the form of round discs (wood slices) cut with a chainsaw. Annual tree rings were precisely measured (with an accuracy of 0.01 mm) using Dendrolab 1.0 equipment (Zielski and Krąpiec Reference Zielski and Krąpiec2004). The measured tree-ring sequences were processed using the TREE-RINGS software (Krawczyk and Krąpiec Reference Krawczyk and Krąpiec1995) and the TSAP computer program (Rinn Reference Rinn2005).

Figure 1

Location of Józefowo village (54.135763 N, 19.818319 E) and Grabie village (50.0391 N, 19.992 E).

Crossdating of the sample was statistically validated using “t-coefficient” (Baillie and Pilcher Reference Baillie and Pilcher1973) and “Gl coefficient” (Gleichläufigkeit; Eckstein and Bauch Reference Eckstein and Bauch1969). The accuracy of the measurements and the quality of the series were verified by COFECHA software (Holmes Reference Holmes1999).

From the 78 individual best-correlated sequences, a local 2JOZ_SA3 chronology covering 292 years was constructed (Figure 2). For absolute dating, 10 tree rings were selected from two samples, 2JOZ228 and 2JOZ504. The dendrograms (annual increment width graphs) of these samples have a clear resemblance to the 2JOZ_SA3 chronology: 2JOZ228 between 1 and 168 relative years with t=12, Gl=70%***, and 2JOZ504 between 131-278 relative years, with t=9.5, Gl=73%***, where the t-value represents the significance of the correlation of two series in relation to their overlap (Baillie and Pilcher Reference Baillie and Pilcher1973). The Gleichläufigkeit (Gl) was developed by Eckstein and Bauch (Reference Eckstein and Bauch1969) as a special tool for crossdating of tree-ring series. The degree of similarity based on the positive or negative trend of each width is expressed as a percentage of the number of intervals.

Figure 2

Diagram of the temporal extent of growth sequences forming the 2JOZ_SA3 pine chronology from Józefowo.

The Green (Reference Green and Whistler1963) protocol was used to extract a-cellulose from wood. Additionally, this method was modified by using an ultrasonic bath (Pazdur et al. Reference Pazdur, Korput, Fogtman, Szczepanek, Hałas, Krąpiec and Szychowska-Krąpiec2005), with HCl instead of acetic acid to avoid any possible acetylation (Nemec et al. Reference Nemec, Wacker, Hajdas and Gäggeler2010).

After the pretreatment, around 4 mg of α-cellulose, extracted from each sample (one ring, one trunk) was combusted to CO2 and subsequently reduced to graphite (Krąpiec et al. Reference Krąpiec, Rakowski, Huels, Wiktorowski and Hamann2018; Wiktorowski et al. Reference Wiktorowski, Krąpiec, Rakowski and Cherkinsky2020). The resulting mixture of graphite and Fe powder was pressed into a target holder for AMS 14C measurements. All the prepared targets contained approximately 1 mg of carbon and were measured at the Center for Applied Isotope Studies at the University of Georgia, USA (laboratory code UGAMS; Cherkinsky et al. Reference Cherkinsky, Culp, Dvoracek and Noakes2010). The 14C concentrations are reported as Δ14C in per mil (‰) deviations from the standard sample, 0.7459 activity of NBS oxalic acid (SRM- 4990C). Vitrinite was used as a background sample. The background sample was subjected to standard acid-alkali-acid pretreatment. Age correction and isotopic composition correction were calculated following formulas presented elsewhere (Stuiver and Polach Reference Stuiver and Polach1977). The correction for isotopic composition was made based on δ¹³C, measured with an AMS system.

Preliminary matching of the floating chronology 2JOZ_SA3 to the absolute time scale was performed using the wiggle-matching method in the OxCal v4 program (Bronk Ramsey et al. Reference Bronk Ramsey, Dee, Lee, Nakagawa and Staff2010).

Subfossil oaks (Quercus robur L.) were recovered from a site in a gravel pit by the Vistula River in the village of Grabie near Kraków and were control series, of known calendar ages and known changes of radiocarbon concentrations around 660 BC (Rakowski et al. Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019).

To precisely determine the calendar age of the studied trunk 2JOZ504 from Józefowo, the measured 14C concentration values expressed in pMC (Table 2) were converted into Δ14C while shifting the entire Józefowo sequence year by year. The resulting Δ14CJózefowo values were then compared to Δ14CG58 values for the G58 trunk (Rakowski et al. Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019). The G58 tree from Grabie was used for this purpose because it was taken from the absolutely dated dendrochronological sequence and is an excellent reference point for the period and region. For each shift (k), the sum of the squared difference of the Δ14C for Józefowo and G58 trunks was calculated. The sum of the squared differences was normalized (nSSD) by dividing it by the number of years (n) for which the difference could be calculated:

$$nSSD\left( k \right) = {{\mathop \sum \nolimits_{i = 1}^n {{\left( {{\Delta ^{14}}C_i^{J\acute ozefowo} - {\Delta ^{14}}C_i^{G58}} \right)}^2}} \over n}$$

The best fit of the Józefowo sequence to the G58 sequence is described by the minimum of nSSD(k).

RESULTS AND DISCUSSION

In the first stage, the measurements were made for ten single-ring, one-trunk (either JOZ228 or JOZ504 tree), α-cellulose samples, collected from the increments representing 12, 46, 86, 165, 170, 175, 180, 185, 190, and 195 relative years in chronology 2JOZ_SA3. The results of the 14C age determinations are presented in Table 1.

Table 1

List of radiocarbon dates for pine wood samples used for wiggle matching from the Józefowo site.

The age of the floating chronology was obtained using the wiggle-matching technique and the results are presented in Figure 3. The start of the Józefowo 2JOZ_SA3 sequence was determined by the wiggle-matching method to be between 845–825 cal BC (2 σ). The end of the sequence falls at 554–534 cal BC (2 σ).

Figure 3

14C wiggle matching of the floating pine chronology 2JOZ_SA3. Calibrated positions of the first and last rings of the pine chronology 2JOZ_SA3 (lower part of figure).

Table 2

Δ14C in the Józefowo samples calculated for the fitted period.

Dating results indicate that the increments between 170–180 relative years contained the diagnostic signal from 664/3 BC. In the two following sessions, 14C concentrations were measured in α-cellulose from rings corresponding to relative years 160–185 (Table 2).

The precise fixing of the Józefowo floating chronology was possible based on the data presented in Figure 4. The minimum value of the nSSD(k) is observed for the year 634 BC. However, the results for 635 and 634 BC do not differ significantly. Close inspection and visual comparison of the Józefowo dataset, the Sakurai et al. (Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020) dataset and new, interannual results for the Grabie trunk (Rakowski et al. Reference Rakowski, Pawlyta, Miyahara, Krąpiec, Molnar, Wiktorowski and Minami2023) presented in Figure 5 suggests that 634 BC is the correct fixing point. The data from Józefowo presented in Figure 5 show a similar pattern as well as Δ14C values to the G58 data sequence, the results of Sakurai et al. (Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020), the data of Park et al. (Reference Park, Southon, Fahrni, Creasman and Mewaldt2017) and new results for the Grabie trunk (Rakowski et al. Reference Rakowski, Pawlyta, Miyahara, Krąpiec, Molnar, Wiktorowski and Minami2023). In the Józefowo sequence, the increase in average Δ14C value between ranges 666–664 BC and 663–657 BC is 14.6 ± 5.8‰, which is consistent with the data presented in Sakurai et al. (Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020), Rakowski et al. (Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019), Rakowski et al. (Reference Rakowski, Pawlyta, Miyahara, Krąpiec, Molnar, Wiktorowski and Minami2023) and Park et al. (Reference Park, Southon, Fahrni, Creasman and Mewaldt2017). The rapid increase in Δ14C observed in Józefowo occurred in one or two years and is more abrupt than the one observed by Park et al. (Reference Park, Southon, Fahrni, Creasman and Mewaldt2017) but similar to the peak observed in Japan (Sakurai et al. Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020) and Poland (Rakowski et al. Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019, Reference Rakowski, Pawlyta, Miyahara, Krąpiec, Molnar, Wiktorowski and Minami2023).

Figure 4

Fitting of Józefowo Δ14C sequence to G58 sequence (Rakowski et al. Reference Rakowski, Krąpiec, Huels, Pawlyta, Hamann and Wiktorowski2019).

Figure 5

Józefowo Δ14C sequence (red crosses) fitted to the G58 sequence (blue stars) and compared with data from Park et al. (Reference Park, Southon, Fahrni, Creasman and Mewaldt2017) (blue-green circles), new Grabie sequence (green stars) (Rakowski et al. Reference Rakowski, Pawlyta, Miyahara, Krąpiec, Molnar, Wiktorowski and Minami2023), Sakurai et al. (Reference Sakurai, Tokanai, Miyake, Horiuchi, Masuda, Miyahara, Ohyama, Sakamoto, Mitsurani and Moriya2020) sequence (black crosses) and IntCal20 data (grey shaded area) (Reimer et al. Reference Reimer, Austin, Bard, Bayliss, Blackwell, Ramsey, Butzin, Cheng, Edwards and Friedrich2020).

This match shows that the 164th tree-ring of the 2JOZ_SA3 chronology represents 665 BC. This allows us to determine that the chronology covers the period 828–537 BC. The value of chronology 2JOZ_SA3 for absolute dating is difficult to overestimate; it serves not only as a tool for precise dating, but also as a potential record to be used in dendroclimatic studies both in traditional terms, using tree ring width variability, as well as carbon and oxygen composition of stable isotopes. Similar method has been already successfully applied by Pearson et al. (Reference Pearson, Salzer, Wacker, Brewer, Sookdeo and Kuniholm2020).

It provides a repertoire that can enable the compilation of a long regional chronology for NE Poland for the first millennium BC, based on the available collections of subfossil pine samples from the surrounding peatlands covering more than 1900 samples.

CONCLUSIONS

The Δ14C rapid increase in the Józefowo sequence confirmed the presence of the radiocarbon excursion ∼660 BC. The excursion is more visible in the Józefowo and Grabie data than in the data published by Park et al. (Reference Park, Southon, Fahrni, Creasman and Mewaldt2017).

It has been demonstrated that the Δ14C increase of ∼660 BC can be used for dating a tree-ring sequence to an accuracy of 1 year. The floating tree-ring chronology from Józefowo was preliminarily fixed to the absolute time scale by radiocarbon dating using the wiggle-matching method. Later, the fixing was supported by Δ14C matching to the known abrupt 14C increase in the atmosphere of 664/3 BC. The refined fixing allowed for 1-year accuracy. The absolute time period covered by the floating chronology of the Józefowo 2JOZ_SA3 sequence is between 828 BC and 537 BC. The method can be used to fix other floating dendrochronologies from this period.

ACKNOWLEDGMENTS

This work was supported by the National Science Centre, Poland, grant UMO-2019/35/N/ST10/02696

Footnotes

Selected Papers from the 24th Radiocarbon and 10th Radiocarbon & Archaeology International Conferences, Zurich, Switzerland, 11–16 Sept. 2022

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Figure 0

Figure 1 Location of Józefowo village (54.135763 N, 19.818319 E) and Grabie village (50.0391 N, 19.992 E).

Figure 1

Figure 2 Diagram of the temporal extent of growth sequences forming the 2JOZ_SA3 pine chronology from Józefowo.

Figure 2

Table 1 List of radiocarbon dates for pine wood samples used for wiggle matching from the Józefowo site.14C wiggle matching of the floating pine chronology 2JOZ_SA3. Calibrated positions of the first and last rings of the pine chronology 2JOZ_SA3 (lower part of figure).

Figure 3

Figure 3 14C wiggle matching of the floating pine chronology 2JOZ_SA3. Calibrated positions of the first and last rings of the pine chronology 2JOZ_SA3 (lower part of figure).

Figure 4

Table 2 Δ14C in the Józefowo samples calculated for the fitted period.

Figure 5

Figure 4 Fitting of Józefowo Δ14C sequence to G58 sequence (Rakowski et al. 2019).

Figure 6

Figure 5 Józefowo Δ14C sequence (red crosses) fitted to the G58 sequence (blue stars) and compared with data from Park et al. (2017) (blue-green circles), new Grabie sequence (green stars) (Rakowski et al. 2023), Sakurai et al. (2020) sequence (black crosses) and IntCal20 data (grey shaded area) (Reimer et al. 2020).