INTRODUCTION
Ice cores, marine and lake sediments provide important insights into past climate changes, and much of our knowledge concerning Quaternary climate history, as well as mechanisms and forcing of climate change, comes from those archives (Bradley Reference Bradley1999). Loess-paleosol sequences (LPS) are valuable terrestrial archives, which are important in order to refine climate reconstructions regionally and to understand environmental consequences of climate change, both in the geologic past and the future (Field and Van Aalst Reference Field and Van Aalst2014). LPS form due to eolian transport and deposition of mineral dust and record more or less favorable conditions for pedogenesis in the past (Pécsi Reference Pécsi1990). It has, for example, long been recognized that the more than 200-m-thick LPS on the Chinese Loess Plateau reflects the alternation of cold and dry glacials with warm and more humid interglacials during the Quaternary (Kukla Reference Kukla1987; Derbyshire et al. Reference Derbyshire, Kemp and Meng1997). Extensive LPS also occur in Europe and Siberia (Haase et al. Reference Haase, Fink, Haase, Ruske, Pecsi, Richter, Altermann and Jäger2007; Zykina and Zykin Reference Zykina and Zykin2008; Haesaerts et al. Reference Haesaerts, Borziac, Chekha, Chirica, Drozdov, Koulakovska, Orlova, van der Plicht and Damblon2010; Marković et al. Reference Marković, Hambach, Stevens, Kukla, Heller, McCoy, Oches, Buggle and Zöller2011). Typically, LPS studies focus on malacology, grain size analyses, magnetic susceptibility, paleopedology and geochemistry, but there is also great potential for developing and applying novel biomarker and compound-specific isotope proxies (Liu and Huang Reference Liu and Huang2005; Zech et al. Reference Zech, Zech, Buggle and Zöller2011b; Gao et al. Reference Gao, Nie, Clemens, Liu, Sun, Zech and Huang2012; Zech et al. Reference Zech, Tuthorn, Detsch, Rozanski, Zech, Zöller, Zech and Glaser2013a, Reference Zech, Zech, Marković, Hambach and Huang2013b; Lu et al. Reference Lu, Liu, Wang and Wang2016). Attempts are increasingly made to establish high-resolution records from LPS and to correlate these with ice core records (Antoine et al. Reference Antoine, Rousseau, Moine, Kunesch, Hatte, Lang, Tissoux and Zöller2009; Kadereit et al. Reference Kadereit, Kind and Wagner2013; Heiri et al. Reference Heiri, Koinig, Spötl, Barrett, Brauer, Drescher-Schneider, Gaar, Ivy-Ochs, Kerschner and Luetscher2014). Key to such attempts and for paleoenvironmental reconstructions in general is robust age control.
Chronologies for LPS are typically established by analyzing the stratigraphy, luminescence dating the loess and radiocarbon (14C) analyses on charcoal, macrofossils, and soil organic carbon from the paleosols (Lang et al. Reference Lang, Hatté, Rousseau, Antoine, Fontugne, Zöller and Hambach2003; Frechen et al. Reference Frechen, Zander, Zykina and Boenigk2005; Haesaerts et al. Reference Haesaerts, Borziac, Chekha, Chirica, Drozdov, Koulakovska, Orlova, van der Plicht and Damblon2010; Stevens et al. Reference Stevens, Marković, Zech, Hambach and Sümegi2011). However, uncertainties of luminescence dating are on the order of ~10% for the last glacial cycle, and organic material suitable for 14C dating is often scarce. This limits the possibility to fully exploit the potential of LPS for paleoclimate and environmental studies, and has motivated research to find alternative ways to date LPS.
Various chemical treatments, such as acid-base-acid (ABA) or acid-base wet oxidation (ABOX), have been suggested to extract soil organic matter fractions that are more reliable for 14C dating (Hatté et al. Reference Hatté, Pessenda, Lang and Paterne2001a, Reference Hatté, Morvan, Noury and Paterne2001b). Yet the exact molecular composition of these chemical fractions remains unclear, and in many cases is likely to be heterogeneous in source and age. Roots, microorganisms, and dissolved organic matter might contribute too-young carbon (Matsumoto et al. Reference Matsumoto, Kawamura, Uchida and Shibata2007; Gocke et al. Reference Gocke, Peth and Wiesenberg2014b), whereas more recalcitrant compounds (humins e.g., pyrogenic carbon residues) might be reworked and redeposited, and therefore too old.
A recent study has shown that compound-specific 14C analyses of long-chain n-alkanes and n-alkanoic acids yield ages consistent with independent age control based on stratigraphy and luminescence dating (Häggi et al. Reference Häggi, Zech, McIntyre, Zech and Eglinton2014). Long-chain n-alkanes and n-alkanoic acids are leaf waxes produced predominantly by higher terrestrial plants, and due to their low water-solubility, chemical inertness and resistance against biodegradation, they are preserved as biomarkers, i.e. molecular fossils, in soils and sediments (Huang et al. Reference Huang, Li, Bryant, Bol and Eglinton1999; Eglinton and Eglinton Reference Eglinton and Eglinton2008).
Within the last 2 decades, compound-specific 14C analysis has become feasible (Eglinton et al. Reference Eglinton, Aluwihare, Bauer, Druffel and McNichol1996) and is now more routine. This is technically possible through the development of the mini carbon-dating system MICADAS, an accelerator mass spectrometer (AMS) system that enables on-line coupling of CO2-producing devices (e.g., an elemental analyzer, EA) to gas-accepting ion sources that allow automated measurement of samples containing less than 100 µg carbon (C) (Synal et al. Reference Synal, Stocker and Suter2007; Ruff et al. Reference Ruff, Fahrni, Gäggeler, Hajdas, Suter, Synal, Szidat and Wacker2010; Wacker et al. Reference Wacker, Fahrni, Hajdas, Molnar, Synal, Szidat and Zhang2013). A major disadvantage of compound-specific 14C analyses, however, is the need for a preparative gas chromatography system (Prep-GC) and the very time-consuming laboratory and instrumental procedures to isolate specific compounds in sufficient quantity for AMS analysis. In addition, recoveries are also often very low, which further limits respective applications to samples with sufficiently high concentrations of target analytes.
Due to various practical constraints, we performed this study to empirically test the potential of dating n-alkanes as a whole compound class. This approach was previously shown to have promise for 14C dating of soils (Huang et al Reference Huang, Li, Bryant, Bol and Eglinton1999) but had not been applied to LPS. We selected 13 samples from the key LPS Kurtak in central Siberia, spanning from the MIS 3 paleosol through the last glacial loess to the Holocene, and compared the 14C ages of the extracted and purified n-alkanes with independent published age control based on luminescence and 14C analyses on charcoal and macrofossils.
MATERIAL AND METHODS
Geographical Setting and Sampling
Extensive loess deposits occur in tectonic depressions of the central Siberian platform and on the piedmont plains north of the Altai and Sayan Mountains (Figure 1A, Chlachula Reference Chlachula2001; Zykina and Zykin Reference Zykina and Zykin2008). During cold Pleistocene periods, the region became a prominent periglacial sedimentation area for loess derived from the glacier forefields and river floodplains. The investigated LPS is exposed along the northwestern shore of the Yenisei water reservoir in the Minusinsk Basin near the village of Kurtak (Figure 1B, 55°8'47.472''N, 91°33'25.3074''E).
Figure 1 (A) Location of the LPS Kurtak. (B) Picture of the LPS Kurtak. Arrow indicates sampling site. (C) Upper part of LPS Kurtak. (D) Close-up view of the lowermost MIS3 humic-rich layer with cryoturbation structures.
Several studies have focused on the LPS Kurtak in the past, including stratigraphical, paleopedological, archeological, and paleontological research, as well as dating campaigns using luminescence and 14C analyses (Damblon et al. Reference Damblon, Haesaerts and van der Plicht1996; Chlachula Reference Chlachula2001; Zander et al. Reference Zander, Frechen, Zykina and Boenigk2003; Frechen et al. Reference Frechen, Zander, Zykina and Boenigk2005; Haesaerts et al. Reference Haesaerts, Chekha, Damblon, Drozdov, Orlova and van der Plicht2005). The Holocene soil is a degraded Chernozem typical for the forest-steppe zone in the area, which is intensively used for agriculture. The sampling site was likely used for mowing in the recent past, while birch and pine forests are found nearby, like in many places in the Minusinsk Basin. The topsoil is a ~20 cm Ah-horizon, followed by a ~20 cm thick carbonate free AB-horizon and then a carbonate-rich C-horizon (see Figure 2 left, for a schematic sketch, and Frechen et al. (Reference Frechen, Zander, Zykina and Boenigk2005) for a detailed paleopedological description). Modern roots were observed to a depth of ~1 m. The loess, loam and loess-like sediments beneath the Holocene soil (down to ~9 m depth) have accumulated in a tundra and cold steppe environment during the last glaciation, also known as Sartan glaciation, correlating with marine isotope stage (MIS) 2 (Arkhipov Reference Arkhipov1998; Zykina Reference Zykina1999). From 9 m to 11.9 m the “Kurtak Paleosol” documents forest steppe environment during the last interstadial, the Karginian interstadial (MIS 3). It is composed of chernozem-like paleosols and several humic-rich layers containing pieces of charcoal, as well as reworked loess in between. The Kurtak Paleosol has been severely affected by cryoturbation (Figure 1D). Below 12 m depth, loess and loess-like sediments document the tundra and cold steppe environment of the MIS 4 glacial period, or Ermakovo Glaciation in the north Siberian stratigraphy (Zykina Reference Zykina1999).
Figure 2 n-Alkane age model for the LPS Kurtak (black data points) in correlation and comparison to the luminescence chronology from Zander et al. (Reference Zander, Frechen, Zykina and Boenigk2003) and Frechen et al. (Reference Frechen, Zander, Zykina and Boenigk2005) (gray data points). The depths of the luminescence samples were adjusted (linearly stretched) to our profile, using the lower and upper boundary of the Kurtak paleosol as tie points.
Fieldwork and sampling was performed in summer 2014. A 1-m-wide and 12-m-high profile was prepared by removing several decimeters from the surface of the steep outcrop (Figure 1C). Samples of 100–150 g each were collected for 14C dating, one from 20 cm depth (Kurt1), five from the MIS 2 loess unit (Kurt2 to Kurt6), and seven from the MIS 3 Kurtak Paleosol (Kurt7 to Kurt13).
Sample Preparation and Analyses
The samples were air-dried and homogenized. Aliquots of ~40 g were extracted with dichloromethane and methanol (DCM:MeOH 9:1, all solvents were HPLC grade from Fischer Scientific) using the Dionex ASE 200 accelerated solvent extractor (1000 psi and 100°C, three 15-min cycles) at the Geographical Institute of the University of Bern. Resulting total lipid extracts were separated over aminopropyl columns, with the apolar fractions, containing n-alkanes, eluted using n-hexane. A gas chromatograph (Agilent 7890) mass spectrometer (Agilent 5975), equipped with an Agilent HP5MS column (30 m×250 µm×0.25 µm film thickness), was used for n-alkane quantification and identification. 5α-Androstane was used as internal standard and a nC21-40 alkane mixture as external standard. For further purification, samples were passed over AgNO3 and zeolite (Geokleen 5A, GHGeochemical Services) pipette columns with n-hexane. Zeolite is a molecular sieve that traps n-alkyl (straight-chain) compounds in its pores. The n-alkanes were recovered after drying in an oven (12 hr, 40°C) and dissolving the zeolite in hydrofluoric acid (40%), using liquid-liquid extraction with n-hexane. The AgNO3-zeolite n-alkane cleanup recoveries were ~80–90%. After again checking the n-alkanes for purity by GC-MS, aliquots were transferred with DCM into tin capsules (sample vessels from Elementar, Art. Nr. 05001727, 3.5×5.5×0.1 mm), and the DCM was evaporated on a hotplate at 35°C.
14C measurements were performed on a MICADAS AMS coupled online to an EA unit (Vario MICRO cube from Elementar, Synal et al. Reference Synal, Stocker and Suter2007; Ruff et al. Reference Ruff, Fahrni, Gäggeler, Hajdas, Suter, Synal, Szidat and Wacker2010; Wacker et al. Reference Wacker, Fahrni, Hajdas, Molnar, Synal, Szidat and Zhang2013; Salazar et al. Reference Salazar, Zhang, Agrios and Szidat2015) at the LARA AMS Laboratory, University of Bern (Szidat et al. Reference Szidat, Salazar, Vogel, Battaglia, Wacker, Synal and Türler2014). Results are reported as fraction modern (F14C), normalized using the reference material Oxalic Acid II (National Institute of Standards and Technology) after subtracting the background signal (Wacker et al. Reference Wacker, Christl and Synal2010). Sodium acetate (n=6) with a F14C of 0.013±0.001 was used as fossil standard in order to estimate the background signal.
All 14C measurements were corrected using the contamination drift model presented by Salazar et al. (Reference Salazar, Zhang, Agrios and Szidat2015). It assumes a combination of constant blank contamination (mass m c and 14C/12C ratio R c ) and cross contamination. In order to quantify and correct for constant contamination, we repeatedly measured 10 combined tin capsules. A single capsule yielded on average 0.43±0.11 µg C for mc with a F14C of 0.76±0.18. For error propagation, we assumed constant contamination and uncertainties of 15% and 20% for blank mass and F14C, respectively (Salazar et al. Reference Salazar, Zhang, Agrios and Szidat2015). A cross contamination of 0.2±0.1 % from the previous sample was determined for the EA-AMS system and was also corrected for following Salazar et al. (Reference Salazar, Zhang, Agrios and Szidat2015), including full error propagation.
Calibrated 14C ages were calculated using OxCal (Bronk Ramsey 2009) and the IntCal13 calibration curve (Reimer et al. Reference Reimer, Bard, Bayliss, Beck, Blackwell, Bronk Ramsey, Buck, Cheng, Edwards, Friedrich, Grootes, Guilderson, Haflidason, Hajdas, Hatté, Heaton, Hoffmann, Hogg, Hughen, Kaiser, Kromer, Manning, Niu, Reimer, Richards, Scott, Southon, Staff, Turney and van der Plicht2013). The calendar ages in this study are reported as calibrated ages before present (cal BP) and as age intervals in the 2σ probability range (95.4%).
RESULTS
Long-chain n-alkane concentrations (ΣC25-C35) in our samples range from 0.6 to 7.6 µg/g dry sediment. These homologues are the most abundant ones, typify vascular plant leaf cuticular wax n-alkanes, and we herein refer to them as “leaf wax” n-alkanes. Leaf wax n-alkane concentrations are lowest in the MIS 2 loess (0.6–1.2 µg/g), whereas the Holocene sample Kurt1 has a concentration of 1.9 µg/g, and concentrations are as high as 7.6 µg/g in the Kurtak paleosol.
Carbon amounts analyzed for purified n-alkane fractions on the EA-AMS ranged from 17.3 to 113.8 µg C (Table 1). F14C for n-alkanes from sample Kurt1 at 20 cm depth is 0.865±0.032 and yields a calibrated 14C age interval of 0.6–1.7 ka cal BP. Samples from the underlying loess (Kurt2 to Kurt6) have F14C values from 0.170 to 0.102 and calibrated ages range from 16.7 to 22.9 ka cal BP. Within uncertainties, they seem stratigraphically consistent and document rapid loess accumulation during MIS 2 at ~22 ka BP. The samples Kurt7 to Kurt13 from the Kurtak Paleosol have F14C values from 0.072 to 0.026 and ages from 24.5 to 35.3 ka cal BP. They are all older than the samples from the overlying loess, but not stratigraphically consistent when compared to each other. This may reflect the fact that the Kurtak Paleosol is strongly cryoturbated, but this interpretation requires further assessment.
Table 1 14C analysis of n-alkane fractions in stratigraphic order.
a Quantity of combusted and injected carbon, measured by the EA unit.
DISCUSSION
Comparison with Independent Age Control
The 14C ages of n-alkanes from the Kurtak LPS are in very good agreement with independent age control for the Kurtak LPS based on stratigraphy, luminescence, and 14C dating on charcoal and macrofossils. Zander et al. (Reference Zander, Frechen, Zykina and Boenigk2003) and Frechen et al. (Reference Frechen, Zander, Zykina and Boenigk2005) reported IRSL luminescence ages for the MIS 2 loess ranging from 17.9±2.1 to 26.3±2.8 ka (Figure 2). Within uncertainties, the luminescence ages are stratigraphically consistent and have been interpreted to document rapid loess accumulation at ~22 ky. Note that our Kurt1 sample from 20 cm depth is 0.6–1.7 ka cal BP and reflects recent pedogenesis, whereas our Kurt2 sample from 1 m depth is 16.7–17.9 ka cal BP and in good agreement with the IRSL age of 17.9±2.1 ka at ~70 cm depth.
For the Kurtak Paleosol, Zander et al. (Reference Zander, Frechen, Zykina and Boenigk2003) and Frechen et al. (Reference Frechen, Zander, Zykina and Boenigk2005) reported IRSL ages ranging from 28.8±2.7 to 36.0±3.2 ka. Damblon et al. (Reference Damblon, Haesaerts and van der Plicht1996) and Haesaerts et al. (Reference Haesaerts, Chekha, Damblon, Drozdov, Orlova and van der Plicht2005, Reference Haesaerts, Damblon, Drozdov, Checha and van der Plicht2014) reported dozens of 14C ages from charcoal and wood remains, which were deposited in a topographic depression in a nearby section. Uncalibrated ages range from 25.7±0.5 to 42.5±0.7 ka BP. Calibration yields ages from 29.7 to 47.4 ka cal BP, so within uncertainties our leaf wax n-alkane 14C ages for the Kurtak Paleosol (ranging from 24.5 to 35.3 ka cal BP) are in good agreement with reported luminescence and 14C ages. All findings corroborate that the Kurtak Paleosol formed during MIS 3. The underlying MIS 4 loess yields IRSL ages of ~60 ka (Figure 2, Zander et al. Reference Zander, Frechen, Zykina and Boenigk2003; Frechen et al. Reference Frechen, Zander, Zykina and Boenigk2005), which is beyond the reach of 14C dating.
Analytical Uncertainties
The assumed constant contamination, which we determined by combining 10 empty tin capsules and for which we corrected all our 14C measurements, was 0.43 µg C. This value is almost identical to the value of 0.4 µg C reported for tin capsules by Ruff et al. (Reference Ruff, Fahrni, Gäggeler, Hajdas, Suter, Synal, Szidat and Wacker2010), yet lower compared to a vacuum line blank of 0.91 µg C reported by Häggi et al. (Reference Häggi, Zech, McIntyre, Zech and Eglinton2014) and a full process blank of 1 µg C reported by Shah and Pearson (Reference Shah and Pearson2007). Our F14C value for the assumed constant contamination is 0.76, which is in agreement with 0.65 determined by Ruff et al. (Reference Ruff, Fahrni, Gäggeler, Hajdas, Suter, Synal, Szidat and Wacker2010), but higher than F14C values of 0.23 and 0.2 reported by Häggi et al. (Reference Häggi, Zech, McIntyre, Zech and Eglinton2014) and Shah and Pearson (Reference Shah and Pearson2007), respectively.
Future work should aim at searching for capsules with lower F14C and amount of carbon, in order to reduce uncertainties propagated to glacial and deglacial age samples. In this study, our corrections for constant contamination were between 0 and 0.01 F14C for all samples, with the Kurt5 subject to the largest correction (0.01 F14C), as it contained only 17.3 µg C. Corrections for cross contamination are negligible (<< 0.01 F14C) because samples with similar 14C were measured consecutively.
With regard to current analytical uncertainties, we note that (1) large sample sizes are essential to minimize uncertainties, especially for old samples (>20 ka BP) that contain low 14C abundances; (2) the 14C age scatter in the Kurtak Paleosol (MIS 3) exceeds the estimated analytical uncertainties and likely reflects the massive cryoturbation observed in the field; and (3) given sufficient sample availability, leaf waxes can be dated with reasonable uncertainties back to ~35–40 ka BP, corresponding to ~0.02 F14C.
Contributions from Fossil or Post-Sedimentary Lipids?
The n-alkane homologue patterns of all investigated samples show a strong dominance of odd, long-chain (C25 to C35) n-alkanes (Figure 3). This is typical for epicuticular leaf waxes of higher terrestrial plants (Eglinton and Hamilton Reference Eglinton and Hamilton1967; Eglinton and Eglinton Reference Eglinton and Eglinton2008). C31 is the most abundant homologue for all samples with the exception of Kurt2 (Cmax=C29). This, as well as relatively long average chain lengths (abundance-weighted average of C25, C27, C29, C31, C33, and C35) from 30.2 to 31.2 for the samples Kurt3 to Kurt13, points to grasses and herbs as dominant sources for the leaf waxes (Schäfer et al. Reference Schäfer, Lanny, Franke, Eglinton, Zech, Vysloužilová and Zech2016 and references therein). Only the C29 dominance of Kurt2 and relatively short average chain lengths of 29.9 and 29.8 for Kurt1 and Kurt2, respectively, indicate some additional leaf wax input from deciduous trees and shrubs (Schäfer et al. Reference Schäfer, Lanny, Franke, Eglinton, Zech, Vysloužilová and Zech2016).
Figure 3 n-Alkane homologue pattern of sample Kurt4 before and after the AgNO3-Zeolite purification.
Odd-over-even chain length predominances (OEP), calculated as ratios of C27, C29, C31, and C33 over C26, C28, C30, and C32, following Hoefs et al. (Reference Hoefs, Rijpstra and Damsté2002) and Schäfer et al. (Reference Schäfer, Lanny, Franke, Eglinton, Zech, Vysloužilová and Zech2016), range from 6.2 to 20.6, indicating good preservation of the leaf waxes and little degradation. Low OEPs (~1) and occurrence of shorter chains (<C25) would point to possible input from reworked fossil n-alkanes and yield stratigraphically inconsistent and too old 14C ages (Lichtfouse et al. Reference Lichtfouse, Budzinski, Garrigues and Eglinton1997; Häggi et al. Reference Häggi, Zech, McIntyre, Zech and Eglinton2014).
We conclude that reworked leaf waxes, or fossil n-alkanes are unlikely to have contributed significantly to the sedimentary n-alkane signatures in the LPS Kurtak. Nevertheless, when compound-specific 14C dating is an option, we recommend determining 14C ages for odd and even n-alkanes separately, as discrepancies between these homologues could reveal fossil inputs (Häggi et al. Reference Häggi, Zech, McIntyre, Zech and Eglinton2014).
It is important to note that reworking associated with eolian processes may contribute not only fossil organic material, but also contemporary, non-local leaf waxes. Wind abrasion and sandblasting of leaf surfaces can produce airborne wax n-alkanes, which are transported and deposited in adjacent regions (Conte et al. Reference Conte, Weber, Carlson and Flanagan2003). Leaf wax homologue patterns and compound-specific stable isotope signals might thus be biased by the dust/leaf wax source region. Little is presently known concerning the relevance of such biases. More importantly, however, non-local leaf waxes will not influence the 14C signal of leaf waxes in LPS provided that they are produced and deposited contemporaneously. Eolian transport of leaf waxes does therefore not limit their potential for 14C dating LPS.
Post-sedimentary biogenic lipid contributions formed or introduced at depth would, on the other hand, result in too young 14C ages. It has been suggested that roots and rhizomicrobial activity are a significant source of long-chain n-alkyl lipids in the subsurface and may affect paleoenvironmental reconstructions based on leaf waxes in LPS. Root tissues tend to contain more C25 and C27 n-alkanes than longer-chain homologues (Gocke et al. Reference Gocke, Gulyás, Hambach, Jovanović, Kovács, Marković and Wiesenberg2014a) or are dominated by short-chain homologues (< C25) (Kirkels et al. Reference Kirkels, Jansen and Kalbitz2013). Litterbag studies document that microbial activity leads to post-sedimentary alteration of leaf wax patterns and corresponding isotopic compositions during early degradation (Nguyen Tu et al. Reference Nguyen Tu, Egasse, Zeller, Bardoux, Biron, Ponge, David and Derenne2011; Zech et al. Reference Zech, Pedentchouk, Buggle, Leiber, Kalbitz, Marković and Glaser2011a). Matsumoto et al. (Reference Matsumoto, Kawamura, Uchida and Shibata2007) performed compound-specific 14C dating on n-alkanoic acids in soils and suggested that the systematically younger ages for C24 and C26 compared to longer homologues can be explained with higher solubility and leaching, as well as with preferential microbial degradation and production. Häggi et al. (Reference Häggi, Zech, McIntyre, Zech and Eglinton2014) also found a tendency of younger ages for shorter-chain n-alkanoic acids and n-alkanes in four samples from the LPS Crvenka in Serbia, yet the overall good consistency of their 14C ages with the stratigraphy and independent age control based on luminescence led them to conclude that post-sedimentary lipid contributions at great depth were negligible. Likewise, we argue that the overall good agreement of our 14C ages with stratigraphy, luminescence and 14C dating, particularly in the MIS 2 loess, indicates that post-sedimentary contributions of long-chain n-alkanes are insignificant.
While we cannot fully exclude the possibility that post-sedimentary lipids, e.g. related to rhizomicrobial activity, were produced in the Kurtak Paleosol and cause slightly too-young and stratigraphically inconsistent ages (Kurt9 and 12, ~26 ka cal BP), we argue that these ages make perfect sense in view of the evidence for strong cryoturbation. Both these samples (Kurt9 and 12) are from reworked loess low in organic matter (see Figure 2), whereas the organic-rich samples (e.g. Kurt8, 10 and 11) are slightly older (~30–35 ka cal BP) and more consistent with the luminescence ages. We suggest that humus accumulation occurred before ~30 ka, i.e. during MIS 3, and that strong cryoturbation, solifluction and loess accumulation began with the transition into MIS 2. Thus, periglacial cover beds, dominated by organic-rich, reworked MIS 3 paleosols yield MIS 3 ages, whereas cover beds dominated by MIS 2 loess yield slightly younger MIS 2 ages.
CONCLUSIONS
14C dating of leaf wax n-alkane fractions in the LPS Kurtak resulted in good agreement (i.e., within methodological uncertainties) with independent, published ages of this sequence based on stratigraphy, luminescence, and 14C dating of charcoal and macrofossils. The uppermost Holocene sample reflects ongoing pedogenesis as well as humus accumulation. The samples from the underlying MIS 2 sediments document rapid loess accumulation at ~22 ka BP. The Kurtak Paleosol n-alkanes yielded 14C ages between 24.5 and 35.3 ka cal BP and are in good agreement with independent age control. The Kurtak Paleosol formed during MIS 3, but we suggest that strong cryoturbation and solifluction early during MIS 2 affected this paleosol and explains the observed age inversions and some apparently too-young 14C ages. Methodological artifacts, related to rhizomicrobial activity or analytical uncertainties, are probably much less relevant. The current analytical limits are estimated to be ~35–40 ka BP, corresponding to ~0.02 F14C.
Overall, our findings corroborate the stratigraphic integrity of leaf waxes in LPS and underline their potential as an innovative tool for 14C dating, particularly when charcoal and macrofossils are not available. Contributions from reworked n-alkanes (fossil hydrocarbons), which would result in too-old 14C ages, or from post-depositional processes (roots and rhizomicrobial activity), which would result in too-young ages, are negligible.
Separation and purification of long-chain n-alkanes over AgNO3 and zeolite pipette columns is relatively quick and easy, and recoveries are high, paving the way for rapid compound class-level 14C dating. The scope of this approach could be further extended by (1) extracting large sample amounts to minimize blank corrections, and (2) limiting sample batches to “very low 14C” samples in order to minimize cross contamination. 14C dating of leaf wax n-alkanes as a compound class represents a promising method for developing LPS chronologies. Future studies could be extended to long-chain n-alkanoic acids, or other leaf wax compound classes.
Acknowledgments
We would like to thank PD Dr. Michael Zech (University of Dresden) for his support during the concept development for this study, Imke Schäfer for her help in the field, and Lorenz Wüthrich for his support during sample preparation in the laboratory. We also thank the SNSF for funding (PP00P2 150590).
