INTRODUCTION
Environmental carbon-bearing materials are inherently complex mixtures of inorganic and organic matter, often embedded in a mineral matrix (Hedges et al. Reference Hedges, Eglinton, Hatcher, Kirchman, Arnosti, Derenne, Evershed, Kögel-Knabner, De Leeuw, Littke, Michaelis and Rullkötter2000). The chemical compositions and isotopic signatures of the complex organic mixtures provide important means to elucidate origin, reactivity and age of carbon in environmental, archeological and geochemical research. An array of methods are employed to investigate the carbon isotopic composition in natural samples. Sequential thermal analysis is a powerful technique to characterize carbon mixtures and to target pools with similar bonding characteristics. The instrumentation (cf. Figure 1A) developed for this purpose at the National Ocean Sciences Accelerator Mass Spectrometry (NOSAMS) facility is a sequential thermal procedure, referred to as the Ramped Pyrolysis and Oxidation (RPO) apparatus or informally the “dirt burner” (Rosenheim et al. Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008). It has been used extensively for understanding the organic carbon provenance in natural (Rosenheim et al. Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008; Plante et al. Reference Plante, Beaupré, Robert and Baisden2013; Zhang et al. Reference Zhang, Bianchi, Cui, Rosenheim, Ping, Hanna, Kanevskiy, Schreiner and Allison2017; Zigah et al. Reference Zigah, Minor, McNichol, Xu and Werne2017; Bao et al. Reference Bao, Strasser, McNichol, Haghipour, McIntyre, Wefer and Eglinton2018; Hemingway et al. Reference Hemingway, Hilton, Hovius, Eglinton, Haghipour, Wacker, Chen and Galy2018, Reference Hemingway, Rothman, Grant, Rosengard, Eglinton, Derry and Galy2019; Sanderman and Grandy Reference Sanderman and Grandy2020) and anthropogenic systems (Rogers et al. Reference Rogers, Bosman, Lardie-Gaylord, McNichol, Rosenheim, Montoya and Chanton2019). Several studies have investigated methodological aspects, instrumental performance, and sample pretreatment procedures (Fernandez et al. Reference Fernandez, Santos, Williams, Pendergraft, Vetter and Rosenheim2014; Hemingway et al. Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a, Reference Hemingway, Rothman, Rosengard and Galy2017b; Bao et al. Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019).
Figure 1 (A) Overview sketch of the NOSAMS RPO (aka “dirt burner”) which includes the combustion columns (B) within the oven (reactor); (B) Overview of different combustion columns used in this study, including pyrolysis-RPO, oxidation-RPO and the full oxidation (FOX) mode described here (right inset). Note that the sidearm was used in (a) to supply the O2 aside of the sample insert to oxidize thermally mobilized matter in the lower combustion section (800°C). In (b) it is available for switching between modes yet commonly is just flushed with premixed He + O2 and thus was waived for (c) the full oxidation mode. During operation the entire combustion column is enclosed by the resistance furnace and operated between ambient temperature (25°C) and 1000°C.
The analytical approach was originally developed to separate Holocene from more ancient organic carbon in order to improve chronologies in Antarctic sediments (Rosenheim et al. Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008). Figure 1 illustrates the apparatus and analytical procedure. In brief, a sample is sequentially heated while carrier gas strips the evolved gases from a sample oven to a combustion oven for oxidation, then through transfer lines into a flow-through cell equipped infrared-gas analyzer (IRGA), to glass coiled cryogenic sample collection traps for purification and isolation through a vacuum line for offline carbon isotope analyses.
In their initial work, Rosenheim et al. (Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008) chose a pyrolysis quartz column (about 42 cm height) with helium as inert carrier gas transporting thermally released volatile carbon species from the sample-containing upper section (Figure 1B (a) upper section) to an oxidation zone in the bottom section that contains a catalyst wire, to which about 2% oxygen is supplied through a separate inlet (Figure 1B). As the system evolved, this setup was extended for usage in oxidation mode by using a 8% oxygen in helium mixture supplied throughout the entire system, resulting in the ramped pyrolysis-oxidation system that is in operation today at NOSAMS. The advantage of oxidation compared to the pyrolysis mode includes the minimization of artifacts from potential charring of biomass in the sample container (Figure 1B (b) upper section), and reducing the incomplete oxidation of released gases (Figure 1B (b) lower section) due to lack of the reagent oxygen. For samples releasing negligible quantities of interfering volatile species (chiefly sulfur and chlorine), e.g., for analysis of non-acid treated samples, pyrolysis and oxidation modes yield similar results (Grant et al. Reference Grant, Galy, Chadwick and Derry2019; Hemingway et al. Reference Hemingway, Rothman, Grant, Rosengard, Eglinton, Derry and Galy2019). This system has proven versatile for a variety of applications and sample types, allowing for the isolation of CO2 sample splits typically between 100 and 1000°C. It is routinely operated in either slow ramp (5°C min–1) to collect CO2 fractions, or in fast ramp (20°C min–1) setting to define thermal behaviors. In the current user controlled setup, the CO2 sample split size typically varies between about 30 µg C to several 100 µg C for offline analysis of stable carbon and natural abundance radiocarbon (14C) isotope composition. To purify the evolved gas, the current instrumentation comprises a custom-made catalyst wire: a braid of nickel, platinum, copper custom wires (1:1:3), as well as two water traps (propanol-filled dewars chilled with dry ice), one before the IRGA and one on the vacuum line.
However, the thermal heating of some environmental samples can result in the release of a mixture of volatile carbon and non-carbon molecules including chlorine and sulfur species. Depending on the amount of these impurities, they can precipitate on surfaces and compromise the reduction step when the CO2 is graphitized for 14C measurements. Therefore, sample recombustion with copper oxide wires (CuO) and silver (Ag) prior to graphitization is currently necessary to successfully produce filamentous carbon for AMS analyses and enhance gas purity for isotope ratio mass spectrometry. Eliminating the sample recombustion step would be beneficial for several reasons: First it would ease quality assurance by reducing the exposure of purified sample splits to potential extraneous carbon-bearing reagents; second it would reduce processing time and improve sample throughput. Finally, it could facilitate novel interface developments including an online (semi-)continuous stable carbon isotope analysis with cavity ring-down spectroscopy, the purification and loading of sample splits on molecular sieve cartridges or other sample transfer techniques for direct CO2 14C measurement using a CO2 gas ion source AMS, such as a MICADAS.
Previous research investigated the impact of different acidification procedures on the isotopic signatures of environmental sample materials and introduced a second packed combustion column (held at ∼450°C) to enhance the gas purity, particularly for acid-fumigated samples (Bao et al. Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019). This served as a proof-of-concept that sequential thermal analyses with an additional oxidative combustion column yields comparable results. Nevertheless, these samples were recombusted with Ag and CuO and increased the length of transfer lines by at least 1.5 m. A combination of the original RPO setup with the enhanced purification capacity of a packed chemical column with metal oxidant catalysts could simplify the analytical setup with improved gas purity. In this study we investigate the suitability of this column for gas purity, and if the recombustion step could be eliminated. Further we introduce a set of 14Cdepleted and 14Cmodern sodium bicarbonate procedural standards for quality control. We present data for a suite of typical materials including acid fumigated and high concentration sulfur samples that have been measured with the RPO/oxidation, and now with the novel full oxidation (FOX) mode combustion column, for comparison.
MATERIALS AND METHODS
A suite of 7 samples including 2 pure chemicals, sodium bicarbonates (NaHCO3; CAS #: 144-55-8) as procedural standards, and 5 different environmental samples were used to test the full oxidation (FOX) column (Table 1). The actual matrix samples comprise a selection of different materials with varying carbon contents, spanning almost the entire range of natural abundance 14C signatures.
Table 1 Sample details on types, pretreatment, and bulk carbon isotopic contents measured in this study or previously reported in the literature.
a) this study;
b) Hanke et al. (Reference Hanke, Wacker, Haghipour, Schmidt, Eglinton and McIntyre2017);
c) NIST 1649a certificate of analyses;
d) Bao et al. (Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019);
e) Rosenheim et al. (Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008).
Note the number of replicate analysis and measurement uncertainty (δ13C) differs among the reported values from literature. Please refer to the original publications.
Briefly, the 5 samples include urban dust NIST SRM 1649a—a frequently studied environmental reference material (Currie et al. Reference Currie, Benner, Cachier, Cary, Chow, Urban, Eglinton, Gustafsson, Hartmann and Hedges2002)—collected in 1974 during the above-ground nuclear “bomb” testing period and thus perfectly suited to benchmark the new system. The Nantucket Mud Patch is an in-house NOSAMS ocean sediment standard material that is frequently used to test the performance of the RPO (Bao et al. Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019). The Gulf of Terror and Erebus Antarctic sediment (KC-5 24–25 cm) is the original sample material that was included in the first publication by Rosenheim et al. (Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008) and is representative of samples with depleted 14C and low carbon contents. The other two samples constitute materials that are typical candidates of failure for the conventional combustion column setup because they require the recombustion of sample splits with Ag and CuO. These samples are the original acid fumigated Sierra Leone Rise sediment (Bao et al. Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019) and Wild Harbor Falmouth (USA) salt marsh sediment sample (36–39 cm), with high sulfur content (3.4% dry weight of acid rinsed sample).
The two NaHCO3 materials differ in their 14C content. The 14C depleted material was off-the-shelf (Matheson Coleman and Bell; ≥ 99.7% purity; Fm = 0.0119 ± 0.0013; δ13C = –5.7 ± 0.4‰; n = 5) and the 14C modern material was produced at NOSAMS from the former by replacing the carbon signature with modern pure CO2 tank gas (Fm = 1.0398; Airgas Inc.). In brief, 7.0 g of lab-grade NaHCO3 was dissolved in 100 mL high purity MilliQ water, placed on a stirring plate with bar and bubbled with tank CO2 gas for 30 min, then equilibrated for 12 hr under a 1 atm continous flow CO2 gas stream and dried on a heating plate for 36 hr. The re-precipitated NaHCO3 was homogenized with mortar and pestle, transferred into a storage vial and dried at 105°C for 4 hr prior to storage in a desiccator to minimize absorbed water in the sample. The sample homogeneity was tested in repetitive (n = 6) bulk carbon isotope measurements yielding a Fm = 1.0354 ± 0.0021 and δ13C = –4.2 ± 0.1‰. The small variation of the 14C and stable carbon isotope compositions suggests that the newly produced NaHCO3 standard is homogenous.
Full Oxidation (FOX) Mode
The setup of the RPO (sequential thermal) instrumentation at NOSAMS was described for pyrolysis mode (pyrolysis-RPO) in Rosenheim et al. (Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008) and for the ramped pyrolysis oxidation mode (oxidation-RPO) in Hemingway et al. (Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a). The new column generation used in this study utilizes the same setup and specifications of the analytical protocol, but aims at enhancing the purification capacity and oxidation efficiency to yield high purity CO2. Therefore a custom-made column was acquired with a wider diameter bottom section (Figure 1B) than the pyrolysis column (widened from 1 to 7 mm ID) allowing to pack a granular combustion column with alternating layers of silver grains (99.99%; CAS: 7440-22-4; Alfa Aesar, manganese oxide powder (≥ 99%; CAS: 1313-13-9; Sigma-Aldrich) and CuO 4 × 0.5 mm wires (> 90%; CAS: 1317-38-0; Elemental Microanalysis).
In a first comparative experiment we interfaced the RPO with a residual gas analyzer (RGA) via open-split. In this experiment we aimed at tracing the purification capacity of oxidation-RPO and the novel FOX combustion column (see Appendix for details). Even though constraints on the experimental setup limited the information content, because the RGA compositional data are qualitative, the results indicated that the FOX column providing an enhanced CO2 purification capacity.
The full oxidation (FOX) combustion column can be used within the existing instrumentation and thus allows to switch modes between the original pyrolysis, the oxidation and the novel FOX columns. In addition to the new column generation, the RPO system at NOSAMS was recently updated with digital flowmeters (Alicat Scientific, Tucson; model MC-50SCCM) in place of lower precision manual flowmeters, effectively increasing the accuracy of He carrier gas and O2 supply to 0.01% of full scale reading. This allows better control of the carrier gas flow rate and ensures a constant proportion of 10% oxygen (instead of 8% used in earlier studies). The sidearm of the pyrolysis column used to supply oxygen in the original setting can be deactivated as it is superfluous in the oxidation mode, but poses a risk for memory effects between sample runs. Therefore, the sidearm was eliminated for the FOX mode column.
Sample and Carbon Isotope Analysis
The analytical procedure in brief: the sample is weighed to target approximately 1 mg total C, transferred and packed between quartz wool in a quartz insert tube that is inset into the quartz reactor and sealed with ultratorr compression fittings. The system is purged with helium carrier gas and 10% O2 at 35 mL min–1 until CO2 is stabilized at background values of 0 ± 5 ppm, as measured using a CO2 analyzer (Sable Systems International CA-10A). Only then the combustion oven was heated to 800°C and subsequently the sample oven was heated from room temperature to 100°C at 5°C min–1 to start the sample heating. The isolation and purification of individual sample splits began at different time points and was continued until CO2 evolution ceased and stabilized at less than 50 ppm. Note that thermograms, and thus total duration of analysis, including start and end temperature, vary with carbon composition and mineralogy of a respective sample.
The measurements were carried out in late March 2020. Glassware was freshly combusted 48 hr prior to use (reactor inserts at 800°C and sample storage tubes at 450°C both for 4 hr). The reactor was pre-baked at 800°C as well, then the custom column was packed and conditioned during two heating cycles (blank fast ramps) to minimize the impact of extraneous carbon from reagents before the start of the sample heating sequence. Twenty-seven samples were analyzed using the same FOX combustion column. Decisions on the isolation of individual sample splits were informed by online thermogram CO2 evolution profiles aiming at (a) capturing periods of drastic variations, such as rise or depression of oxidized carbon, (b) plateaus that suggest similar material composition, or (c) sample mass to yield similar split sizes in a sample. In contrast to the previous protocol, in this study the samples were processed without the additional combustion of the CO2 splits with Ag and CuO, which previously was needed to purify the sample CO2. Instead, sample gas was directly expanded on the NOSAMS small sample line (SSL) vacuum system of which 96% of the gas was reduced to filamentous carbon (graphite) and 4% was used for IRMS 13C measurements on a VG Prism-II or Optima system. Graphite targets were measured on the NOSAMS CFAMS system with a typical instrumental precision better than 3‰ and the CO2 split for stable isotope composition on Prism/Optima with a typical IRMS precision of better than 0.2‰ (Xu et al. Reference Xu, Roberts, Elders, Kurz, McNichol, Reddy, Ward and Hanke2021).
Data Processing
Information on the quantitative thermal evolution of CO2 and on the respective combustion temperature for the samples were recorded in LabVIEW software through an infrared CO2 analyser (IRGA; Sable Systems International CA-10A) and are illustrated in Figures 2 and 3. Regarding the isotope measurements, individual sample splits were stored in flame-sealed pyrex tubes for about four weeks before further analyses. Blank corrections of 14C AMS data were carried out using the 96% mass yield through isotope mass balance calculations following the model of constant contamination published elsewhere (Hanke et al. Reference Hanke, Wacker, Haghipour, Schmidt, Eglinton and McIntyre2017; Roberts et al. Reference Roberts, Elder, Jenkins, Gagnon, Xu, Hlavenka and Longworth2019). To explore whether this blank procedure can be implemented in routine application for a sequence of samples, we carried out single measurements for both bicarbonates and corrected the observed Fm to the accepted bulk value. Thereby we obtained two blank masses for 14C depleted and modern contamination. Due to the lack of enough data to statistically derive the uncertainty, we assigned a 20% uncertainty to both mass and Fm and used this value to correct the individual splits of all five environmental samples.
Figure 2 Comparison of CO2 evolution profiles (thermograms) for NIST SRM1649a analyzed with the conventional RPO setup and the novel FOX combustion setup (in duplicate) at almost identical sample weight. Results support the similarity between RPO and FOX combustion reactors over the entire temperature range and highlight the slightly refined profile for FOX.
Figure 3 Sample thermograms showing CO2 profiles (lines; ppm; left y-axis) for each sample with fraction yields (bar plots; µg C; right y-axis) over the identical temperature range. Sodium bicarbonate plot contains results for both materials, type 1 14Cdepleted (light green line and light gray bars) and type 2 14Cmodern (dark green line and dark gray bars).
For the first time, we used a set of NaHCO3 procedural standards with 14Cmodern and 14Cdepleted signatures to determine a sequence-specific procedural blank value. The accurate blank determination in the sequential thermal decomposition of particulate carbon is inherently complex due to the steady temperature ramp from 100 to 1000°C at 5°C min–1. Here we test an indirect approach of a pure inorganic carbon material (sodium bicarbonate). Note that the “direct” and “indirect” blank determinations differ from one another. Whereas the “direct” method measures the carbon produced during a blank run without sample (using manometry), the “indirect” approach records the blank through the analysis of a well-characterized material, allowing assessment of the full procedural blank from calculation of the deviation from the accepted 14C value (Xu et al. Reference Xu, Roberts, Elders, Kurz, McNichol, Reddy, Ward and Hanke2021). A previous study used CO2 tank gas and found no indication of a shifting blank value or substantial isotopic fractionation during the ramping process (Hemingway et al. Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a). With reference to this observation, the isolated splits for NaHCO3 peak 1 (110–200°C) and peak 2 (650–850°C) were combined and compared to their bulk accepted Fm values. The resulting procedural blank was divided by the total duration of the collected fractions for sodium bicarbonates (290°C) to yield the total blank value per minute of fraction collection. Since almost all splits vary in the duration of fraction collection, this allows determination of the correct proportional blank per sample split and subsequently for the precise calculation of the actual blank-corrected sample 14C values. Furthermore it comprises a procedural blank including loading of sample on the system, the sequential thermal analysis, the purification and isolation of CO2, the blank of quartz tubes, and the SSL vacuum system blank with the additional uncertainty for the reproducibility in the AMS. To account for kinetic fractionation, the stable carbon isotope data were corrected following the procedure of Hemingway et al. (Reference Hemingway, Rothman, Rosengard and Galy2017b).
RESULTS AND DISCUSSION
A comparison between the novel FOX reactor and oxidation-RPO “dirt burner” analysis with NIST SRM1649a is shown in Figure 2. The temporal CO2 evolution profiles for subsequently isotopically resolved samples are illustrated in Figure 3. The 14C contents of individual and mass balance recombined NaHCO3 procedural standards are shown in Figure 4 and the 14C and δ13C data for the five typical environmental matrices are shown in Figure 5. Table 2 lists the temperature windows for all sample splits, with size, along with measured and corrected 14C data, including the results of the full error propagation versus AMS uncertainties.
Figure 4 Details on individual 14C results (Fm) from sodium bicarbonate splits (100–190°C and 650–850°C) with AMS uncertainty, mass-balance reconstructed bulk Fmmeasured (only for sequence blank analysis illustrated in black squares) and bulk Fmcorrected after mass balance corrections with bulk Fm of accepted values (dashed lines). Independent blank analysis replicate 2 (open circles) and replicate 3 (open triangles) support the reproducibility of blank determinations using FOX combustion column with this set of sodium bicarbonates.
Figure 5 Results from carbon isotope analyes for samples showing Fmcorrected (black squares; left y-axis) and δ 13C (gray circles; right y-axis). Note that dots mark mid-temperature of each split with horizontal lines indicating temperature range of each split. Vertical error bars show analytical uncertainties, but are generally smaller than the symbols, except for the Wild Harbor sample because of the similar isotopic signatures. Note that reported uncertainties are unusually small for these measurements—we determined a low-level blank mass and measured large sample masses.
Table 2 Sample splits and temperature range with mass, Fmmeasured and Fmcorrected to illustrate the impact of mass balance blank correction for each sample as well as to show uncertainties from the AMS vs blank correction.
* 14C split mass = total split–split for δ13C measurements. Mass was quantified on the NOSAMS small sample line.
In preparation to deconvolve the isotopic signatures of the five environmental samples with the novel FOX reactor, we compare the records on the thermal CO2 evolution with that of the conventional RPO. We selected the well-studied NIST SRM1649a Urban Dust for these analyses (Figure 2). To further evaluate the reproducibility of the analyses we measured duplicates for the FOX. The profiles show an overall similar thermal degradation pattern for both generations of combustion reactor. Despite the slightly earlier start of oxidation in the RPO (at about 125°C) and the slightly more pronounced CO2 maximum for the FOX analysis at about 320°C, the thermograms for both combustion generations evolve identically. The results provide confidence for the similarity of results for oxidation-RPO and FOX combustion reactors and set the stage for subsequent analyses.
Temporal CO2 Evolution Profiles
The main results (Figure 3) reveal different decomposition patterns for all sample types beginning around 100°C and effectively exhausted between 600 and 850°C. Only the inorganic procedural standards NaHCO3 show a baseline separation between peak 1 (100–190°C) and peak 2 (650–850°C). Measured CO2 maximum values range from 840 ppm in the Antarctic sediment (Gulf of Terror and Erebus; KC-5 24–25 cm) to 3350 ppm in the Sierra Leone Rise sediment. All five environmental samples yielded distinct thermograms, indicating that they differ in their organic carbon composition and/or bonding characteristics. The bimodal to multimodal thermograms provide some insight into the heterogenous nature of the organic matter, with thermochemically reactive fractions released at lower temperature.
The two distinct peaks at low and high temperatures for the bicarbonates in this study are almost identical to those reported by Rosenheim et al. (Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008), in the premier publication on the RPO sequential thermal analysis in pyrolysis mode at NOSAMS. The good agreement between the two NaHCO3 thermograms (in light and dark green in Figure 3) demonstrates analytical reproducibility for the new column setup. The two different bicarbonates differ only in the magnitude of the CO2, which may be due to higher carbonate purity in the off-the-shelf 14Cdepleted material compared to the custom made 14Cmodern standard. We suspect a higher amount of residual water in the latter standard, i.e., an incomplete drying process at 105°C for four hours prior to the analyses. However, the congruency of the two distinct peaks and the good agreement between the two thermograms suggests the absence of other impurities that could have caused the unequal yields using the same material mass.
The NIST urban dust 1649a sample reveals a broad thermogram with a wide maximum between 450 and 500°C preceeded by a local maxima at lower temperatures, indicating a more refractory nature for the majority of carbon. This thermogram resembles the results of an evolved gas analyses (EGA) from the same standard reference material (Peralta et al. Reference Peralta, Baumgardner and Raga2007) yet with visually more refined fluctuations in CO2 evolution resulting in a higher resolution thermogram. The apparent congruency between the thermogram of the RPO-FOX analytical setup and an EGA for the same material demonstrates the potential for the classification and comparison of known to unknown samples.
The NOSAMS in-house sediment standard Nantucket Mud Patch has a clear bimodal thermogram with a maximum at low temperature (300°C) which is indicative of a higher proportion of relatively thermochemically reactive carbon, and a distinct maximum at around 500°C. This sample has been analyzed to control the performance of the RPO instrument at NOSAMS and, for instance, was published by Bao et al. (Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019) in a comparison of acidification pretreatment procedures. Our results indicate no substantial differences from their results using the oxidation-RPO combustion column.
In this study, the original Gulf of Terror and Erebus sediment sample (KC-5 34–35 cm) shows the most structure between 200 and 740°C with four maxima and a small shoulder at about 650°C. Even though seemingly in higher resolution, the thermogram with FOX here and pyrolysis mode (Rosenheim et al. Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008) show the same CO2 evolution with temperature increase. The first low temperature peak (around 325°C) is apparent in both studies, which will be discussed in the isotope section below. We also find a sharp maximum at 435°C followed by a second at 480°C and another distinct peak at around 615°C. This indicates a diversity of substrate labilties and the presence of different organic matter types and perhaps differences in the provenance of organic carbon. This thermogram highlights the success of the original research to thermally deconvolve organic matter and thereby targeting individual fractions for discrete isotope analyses. It thereby unambigously shows the abundant resolution with the full oxidation mode setup and suggests the absence of systematic differences between pyrolysis and FOX modes.
The Sierra Leone Rise sediment mineralizes between 220°C and 680°C with a distinct maximum at 500°C. This thermogram shows a small shoulder at 425°C and a minor second peak at 550°C following the maximum yet overall mimics a unimodal left-skewed distribution. With the apparent higher starting temperature this sample is composed of less volatile carbon compared to the others. A comparison of this thermogram with that reported by Bao et al. (Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019) for the oxidation-RPO column shows some differences, for instance the location of the first shoulder differs by almost 100°C, and the absence of a second peak after the maximum. However, the starting and ending temperatures, and the location of the maximum at about 480°C, are identical and support the comparability of the two analytical procedures.
The Wild Harbor marsh sediment shows a narrow thermogram starting at about 160°C and decreases back to the instrumental background between 450 and 600°C (about 200 to <50 ppm). It appears with an almost unimodal thermogram distribution illustrated by a distinct peak at 350°C with a shoulder at about 280°C. Whereas this thermogram shape is typical for a marsh sediment, it showed an almost identical profile on the oxidation-RPO column (not shown, but similar to NIST SRM 1649a in Figure 2). This sample was used because of its high sulfur content (3.4%), which represents an extreme sample type that typically would necessitate an additional cleaning of CO2 yields prior to isotope analyses.
Indirect Blank Determination with NaHCO3 Procedural Standards
The total indirect 14C blank was determined using a set of bicarbonates (NaHCO3), the results of which are illustrated in Figure 4 including measured (split 1 and split 2), recombined and fitted (Fm-corrected) 14C values for the 14Cmodern and 14Cdepleted end-members. These data comprise the upper and lower natural abundance 14C signatures in typical environmental samples. While these procedural standards differ in their 14C contents, both mineralize at the same temperature window and thus record the same experimental conditions. The carbon isotope content, however, is likely affected by partial release of CO2 from the crystal lattice leaving behind sodium carbonate (Rosenheim et al. Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008). To reduce the complexity of this kinetic process, we mass-balance-corrected both peaks to yield a reconstructed bulk value that records the 14Cmodern and 14Cdepleted blank (Figure 4; solid squares) over a total duration of 290°C which is equal to a duration of 58 minutes. The difference of the reconstructed to the accepted values account for 3 per mil for the 14Cdepleted and 18 per mil in the 14Cmodern sample. The combination of both blank values result in a total blank of Fm = 0.268 ± 0.054 and a blank mass of 4.4 ± 0.9 µg C for the same time period and ∆T. Included in the total blank is the small sample line blank, which is 0.35 µg C, and is minor (within uncertainty), yielding a total sequence blank value of 0.069 µg C min–1 (13.8 ng C °C–1) during discrete sampling with the FOX column. This calculation of a universal blank is possible because of the absence of a systematic or sudden shift caused by isotope fractionation processes in the sequential thermal analyses (Hemingway et al. Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a).
This indirect blank assessment for the FOX column reveals a total blank of only about 34% compared to the first comprehensive blank assessment of the RPO (Fernandez et al. Reference Fernandez, Santos, Williams, Pendergraft, Vetter and Rosenheim2014). More recent assessments in that laboratory yielded lesser total blank levels of 2.8 and 3.7 µg C, respectively (Subt et al. Reference Subt, Yoon, Yoo, Lee, Leventer, Domack and Rosenheim2017; Venturelli et al. Reference Venturelli, Siegfried, Roush, Li, Burnett, Zook, Fricker, Priscu, Leventer and Rosenheim2020). Both studies utilized the oxidation-RPO. The results indicate that blank levels—via the indirect assessment using external standard materials—are similar for both combustion columns.
In comparison to blank data determined with the direct blank approach, toggling sample traps in the oxidation-RPO (Hemingway et al. Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a) at NOSAMS, the results of this study are higher (about 9.4 ng C °C–1). This difference between the direct and indirect assessment has been observed in other studies, for instance by Xu et al. (Reference Xu, Roberts, Elders, Kurz, McNichol, Reddy, Ward and Hanke2021), and is likely due to the fundamentally different experimental approaches. The direct system blank reflects specific aspects of the instrumental setup up to measurement of carbon abundances. The indirect blank determinations, with procedural standards, includes all sample processing steps, and thus are more representative of the actual analyses of environmental sample matrices. Nonetheless the good agreement of the systematic direct characterization by Hemingway et al. (Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a) with our results supports the indirect blank procedure using NaHCO3 as procedural standards and suggest that the “dirt burner” overall yields similar blanks for the oxidation-RPO and the FOX-RPO combustion column discussed here.
The use of external standards entails information about the 14C signature in addition to the total blank level and thus provides insights on the composition of blank (Santos et al. Reference Santos, Southon, Griffin, Beaupre and Druffel2007). Sources of blanks are presumed to originate from at least ambient air, potential impurities of gases and residuals of organic solvents used for cleaning the instrument. Seasonal outside conditions such as fossil fuel burning nearby as well as vegetation productivity can influence the 14C composition through lab air intakes and thus impact the ambient air 14C signature among geographic locations of laboratories. The use of dry ice can also potentially impact the 14C signature of lab air. Nonetheless procedural blanks may change over time due to evolving instrumental performance between maintenance intervals and individual operators.
In an effort to ensure that the sequence blank is robust, we carried out additional analyses on the bicarbonates, with a freshly packed FOX reactor. The results are plotted as open symbols (Figure 4) to show the overall similarity between the blank values used to correct the environmental samples in this study. The calculated blank mass for the three reconstructed bulk 14Cdepleted NaHCO3 analyses varied between 0.23 and 4.80 µg C and for 14Cmodern between 3.1 and 5.9 µg C. With reference to the two-endmember blank assessment, we observe a larger variability in 14Cdepleted bicarbonates (Figure 4 left panel) particularly in the high temperature split than we observe for the modern counterpart. The correction of thermally deconvolved biocarbonates with bulk Fm values, however, enable to correct for the overall blank level and its magnitude also serves as an indicator for the robustness of analytical setup during a sequence of sample analyses.
Based on correction of the bicarbonate measurements, shown in Figure 4, the blank level is about 1.4 µg C for the collection of a sample split over a temperature range of 100°C (heating rate: 5°C min–1). This blank mass is similar to other molecular-level 14C analyses (Santos et al. Reference Santos, Southon, Drenzek, Ziolkowski, Druffel, Xu, Zhang, Trumbore, Eglinton and Hughen2010; Hanke et al. Reference Hanke, Wacker, Haghipour, Schmidt, Eglinton and McIntyre2017; Haghipour et al. Reference Haghipour, Ausin, Usman, Ishikawa, Wacker, Welte, Ueda and Eglinton2019) and lower than bulk 14C-DOC analyses (Xu et al. Reference Xu, Roberts, Elders, Kurz, McNichol, Reddy, Ward and Hanke2021). Further, a normalization of our sample splits (Table 2) to a theoretical split size of 100°C for all samples in this study, shows split sizes of 68–912 µg C (the disparity is caused by the dynamic evolution of thermograms), which translates to blank mass contributions of only 0.17–2.05% per split. In other molecular-level 14C analyses, this relationship can exceed 10% (Hanke et al. Reference Hanke, Wacker, Haghipour, Schmidt, Eglinton and McIntyre2017), depending upon sample type and sample size. This relationship of blank and sample mass provides some indication for the overall precision of sample data after the mass-balance corrections illustrated in Table 2.
To correct sample data, the blank 14C signature is equally important to mass. We determined the 14C signature of the blank to be Fm = 0.268 ± 0.054. This agrees well with the average blank (Fm = 0.314) reported by Fernandez et al. (Reference Fernandez, Santos, Williams, Pendergraft, Vetter and Rosenheim2014). In contrast, Hemingway et al. (Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a) found a higher blank 14C signature (Fm = 0.555 ± 0.042), indicating a lesser contribution of 14Cdepleted sources such as petroleum-derived solvents. We showed that this set of 14Cmodern and 14Cdepleted NaHCO3 are suitable procedural standards to trace the blank level in sequential thermal 14C analyses, allowing each operator to control their own batch blank values. A careful blank procedure is particularly important as the combination of packing new columns, maintenance intervals, marginal differences in handling the instrument, and also storage of standard materials, can alter blank values. This should be taken into consideration for yielding good quality data, i.e., that allow for reproducible analysis and robust interpretation of data. An indirect blank assessment can provide sufficient data to assign an average blank value and to document robust differences in blanks for the different types of combustion columns. As an outlook towards online δ13C analysis it may become useful to supplement the set of bicarbonates standards for 14C with some mid-T-coals with largely differing 13C contents. As a counterpart to the inorganic materials this would be helpful for high precision analysis of pure materials that mineralize at intermediate temperatures.
Deconvoluted Sample Isotopic Signatures
Sequential thermal analyses provide the opportunity of resolving bulk materials into discrete fractions and are useful for identifying target fractions for 14C dating, determining autochthonous/allochthonous organic matter sources, tracing impact of anthropogenic carbons, or disentangling short versus long term carbon cycles. The focus here is primarily on the dynamic range of 14C in a sample, along with the natural abundance spectrum, to illustrate both potential and performance. The temperature range for each sample split with carbon yield is included in Figure 3 and the isotope data are illustrated in Figure 5.
The isotope data reveal a dynamic behaviour for both 14C and δ13C, with higher δ13C signatures associated with lesser 14C contents (Figure 5). For 14C, the samples span a large range of natural abundance 14C, from Fm = 0.109 in the Sierra Leone high temperature split to Fm = 0.979 in the mid-temperature Wild Harbor Marsh sediment sample. This implies that any distinct signature of the above-ground nuclear bomb testing is absent in these samples, or at least muted due to dilution with more 14C-depleted materials. The δ13C values vary from –30.0‰ intermediate temperature (split 2) Antarctic sediment to –12.4‰ in the high temperature (split 7) Sierra Leone Rise sediment, suggesting large differences in organic matter provenance. We observe smaller δ13C variability in the Nantucket Mud Patch, Antarctic sediment and Wild Harbor Marsh sediment (Figure 5; y-axis scales), which is consistent with the 14C values. In contrast we found the largest sample heterogeneity in the NIST 1649a Urban Dust sample with differences between fractions (∆Fm) of up to 0.635 Fm. The Urban Dust and Marsh sediment both reveal higher 14C contents in the second split compared to the first split, whereas the other three samples show decreasing 14C contents with increasing temperature. This indicates that low temperature (more thermochemically reactive) organic matter seems to consist of a larger portion of contemporary carbon and the portion of “older” (comparatively 14C-depleted) more refractory carbon increasingly dominates the higher temperature splits. These systematic trends support the potential of resolving the organic matter complexity via carbon isotope signatures through sequential thermal analyses.
NIST 1649a Urban Dust was sampled in four fractions revealing heterogeneous 14C distributions with Fm = 0.132 (split 4) to Fm = 0.768 (split 2) yet with a lesser dynamic range in δ13C (–23.5 to –27.7‰). The latter follows a clear trend of increasing 13C depletion with higher temperature whereas the 14C increases from split 1 to split 2 and stepwise shows quite depleted 14C values, pointing towards dominating 14Cdepleted carbon sources. As this reference material originates from an almost annual sampling of ambient air in a public parking garage (NIST. 2007), the impact of residues from incomplete combustion of engine fuels is assumed (Currie et al. Reference Currie, Benner, Cachier, Cary, Chow, Urban, Eglinton, Gustafsson, Hartmann and Hedges2002). A comparison to literature values for high temperature split 4 shows similarities between results of black carbon analyses, for instance for bulk chemical oxidation/residue of elemental carbon (Fm = 0.17) or targeted aromatic carbon (CuO oxidation after methylene chlorine extraction) analyses (Fm = 0.153). Both are included in a large interlaboratory comparison by Currie et al. (Reference Currie, Benner, Cachier, Cary, Chow, Urban, Eglinton, Gustafsson, Hartmann and Hedges2002). A molecular-level study, using the source-specific black carbon markers benzene polycarboxylic acids (BPCAs), yielded a 14C signature of Fm = 0.088 (Hanke et al. Reference Hanke, Wacker, Haghipour, Schmidt, Eglinton and McIntyre2017). Another study focused on the biogenic contribution to the solvent-extracted unresolved complex mixture (UCM), as well as to three fractions of n-alkanes (nC20-nC22; nC24-nC26; nC28-nC30), and found an almost fossil 14C signature (Fm = 0.007–0.029) (White et al. Reference White, Xu, Hartmann, Quinn and Reddy2013). Both specific molecular-level studies reported lesser 14C contents than split 4 (500–700°C; Fm = 0.132) in this study. The high-temperature split is more 14C depleted than the operationally defined bulk aromatic black carbon data (Currie et al. Reference Currie, Benner, Cachier, Cary, Chow, Urban, Eglinton, Gustafsson, Hartmann and Hedges2002). We infer that this high-temperature fraction records combustion and petroleum products of similar bonding energies. Apart from its predominance in fossil fuel residuals, the carbon isotope composition for this sample has not been previously characterized. Nevertheless, this material appears to be well suited to be used in benchmark analyses for similar instrumentation in future research.
The Nantucket Mud Patch reveals decreasing 14C values with increasing temperature from split 1 to split 5 (Fm = 0.914 and Fm = 0.713, respectively). In contrast, the δ13C values rise (–21.9 to –17.4‰) between split 1 and split 4 and reveal a slightly lower δ13C = –18‰ for split 5. An interpretation of the latter is limited due to a potential isotope fractionation that might compromise interpretations of ∆δ13C ≤ 2‰ (Hemingway et al. Reference Hemingway, Galy, Gagnon, Grant, Rosengard, Soulet, Zigah and McNichol2017a; determined on the oxidation-RPO combustion column). This in-house sediment standard was also studied by Bao et al. (Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019) in a study to investigate the impact of acid pretreatment procedures for oxidation-RPO analysis. They isolated fractions of slightly different temperature windows, but the overall trends are consistent, with decreasing 14C signatures at increasing temperature. However, while the 14C contents are very similar in split 1 (∆Fm = 0.009), they differ in the high-temperature split with ∆Fm = 0.396. The latter quite likely is due to the longer duration of purification and different temperature windows of collection in the two studies. Indeed, considering the 14C depletion trend observed with increasing temperature and the lack of evidence for isotope homogeneity among individual temperature splits, it is not surprising that our high-temperature split (500–600°C) is less 14C depleted than reported by Bao and collaborators (558–900°C) because the latter integrates over a more refractory section of the reactivity continuum. We chose to stop the analyses when the online CO2 measurement decreased monotonously to less than 50 ppm CO2 due to constraints in the instrumental precision of the CO2 analyser (10% of reading plus drift) to ensure some robust signal-to-noise ratios. This limits the comparability of the results but also illustrates the potential for additional measures, such as online monitoring of stable isotope composition that could assist in the identification of changes in substrate composition. Nonetheless, in the comparison between the isotope values of oxidation-RPO-equipped chemical oven with that of FOX for this sample, we clearly see the same trends with temperature evolution, with different resolution.
The Antarctic sediment reveals a clear trend along four splits towards more depleted 14C signatures (Fm = 0.212–0.017) with an abrupt change between split 1 and split 2 (∆Fm = 0.152). In contrast, δ13C again show an opposing trend with –28.2 to –21.0‰ with an additional –1.8‰ depression in split 2. This sample was first described by Rosenheim et al. (Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008) when they reported the first NOSAMS carbon isotope data in pyrolysis mode. The aim of their study was to isolate autochthonous organic carbon that would facilitate 14C dating of Antarctic sub-ice shelf sediment. Focusing on sediments from two locations, their results from site K-49 demonstrated the successful application of this novel instrumentation. For the other site (Gulf of Terror and Erebus; KC-5 24–25 cm) in this study, they measured a low and high temperature split and observed more 14C-depleted carbon in the lower temperature split that were inconsistent with results on co-deposited foraminifera. In contrast, we obtained about 11200 14C years (split 1) which is approximately 5300 14C years younger than previously reported (Rosenheim et al. Reference Rosenheim, Day, Domack, Schrum, Benthien and Hayes2008) and, with reference to the foram-based sediment chronology, it likely reflects the correct age of sediment burial at this location. These results demonstrate an adequate analytical resolution that matches the initial pyrolysis-RPO and provide an analytical capacity to develop sediment chronologies even in extreme environments with minor autothonous inputs.
Among the two samples with high levels of chlorine and sulfur, we analyzed the acid-fumigated Sierra Leone Rise sediment in seven sample splits. Results show decreasing 14C contents (Fm = 0.248–0.100) between split 1 and split 7 with an initial drop between split 1 and split 2 (∆Fm = 0.096). In this sample set we detected the largest δ13C range, from δ13C = –26.3 to –12.4‰ with a 5.6‰ difference between split 1 and split 2. Thus the more refractory carbon contains a heavier isotope signature. We used the acid-fumed bulk δ13C value reported by Bao et al. (Reference Bao, McNichol, Hemingway, Lardie Gaylord and Eglinton2019) as a reference to correct the measured data and yielded a mass balance-corrected δ13C = –17.2‰, which differs only by 0.4‰ from the reported bulk value. In agreement with the other samples, the post-blank corrected values represent typical δ13C signatures for organic carbon in sediments and record a 13C depletion between thermochemically reactive and more refractory carbon.
The Wild Habor Marsh sediment (WH 36–39 cm) serves as a test sample with high sulfur content (3.4%). Results for three sample splits show a relatively homogenous compostion for both 14C (Fm = 0.979–0.971) and δ13C (–18.2 to –17.8‰). Similar to the other samples, we observe slightly higher 14C; the δ13C signature remains steady, but is lower in split 2 compared to the other splits. The differences are small (∆Fm = 8‰ and ∆δ13C = 0.4‰) and might reflect analytical uncertainties. Previous research determined the sediment acccumulation rate at this location at 0.35 cm yr–1, derived from constant initial concentration model with 210Pb and 137Cs yielding an age of deposition of about 105 years BP at this depth (White et al. Reference White, Xu, Lima, Eglinton and Reddy2005). Another study reported congruent down-core 14C contents for the microbial community (phospholipid fatty acids) and TOC at this location (Slater et al. Reference Slater, White, Eglinton and Reddy2005). It suggests that the microbial consumption of autochthonous sedimentary organic matter similarily affects the full organic matter spectrum (thermochemically reactive to refractory). Thus the absence of preferential degradation and decomposition in this sample that was buried by tidal and Marsh debris about 100 years ago can explain the minor isotopic variations in the three sample splits.
In summary, there was no indication of impurities within the CO2 fractions generated with the FOX combustion column during production of filamentous carbon or IRMS analyses in any of the samples. Using the RPO/FOX procedure all of the samples were successfully processed (n = 27) and analyzed for 14C and δ13C, including the two samples with high levels of chlorine and sulfur. This suggests the effective purification capacity of the FOX combustion column, and that the previously required recombustion with Ag and CuO is no longer necessary. Therefore, the procedure allows for faster sample throughput without additional chemicals that would add to the blank. It also facilitates direct sealed-tube graphitization or potentially online isotope monitoring, with lesser risk of secondary gases that can compromise instrumentation and might have corrosive effects in transfer lines and detectors.
Impact of Blank Correction and Precision of Data
The results of 14C measured versus corrected data for the five environmental samples (splits: n = 23) are illustrated in Table 2 using the sequence blank (13.8 ± 2.8 ng C °C–1 and Fm = 0.268 ± 0.054). Note that the 14C contents of samples vary between Fm = 0.017 and 0.979 and thus span almost the full spectrum of natural 14C abundances. Because of the depleted blank 14C signature the impact of correction will be largest for modern samples compared to samples with lower 14C content with less effect on the precision. The magnitude of blank corrections ranges from –16.9‰ (split 3; Wild Harbor Marsh) to +6.1‰ (split 4; Antarctic Sediment). Even though minor, this is a substantial change of sample Fm if compared to the surprisingly small change in uncertainties (total uncertainties-AMS) up to 0.8‰. This very minor increase in the overall uncertainties of measurement after the error propagation demonstrates overall the robust approach for molecular-level 14C analyses. Considering the variabilities and potential inaccuracies that may be expected from multistep procedures, the correction of data appears mandatory even though the impact overall remains small for the comparatively large sample mass compared to isotope analysis of molecular markers (Santos et al. Reference Santos, Southon, Drenzek, Ziolkowski, Druffel, Xu, Zhang, Trumbore, Eglinton and Hughen2010).
Mass balance calculations of blank corrections impacted the splits among a sample more than between different samples. In this study the average duration of each split is 20 min or 100°C (between 30 and 200°C). With this variability in split duration, we determined an average split size of 207 ± 58 µg C (between 113 and 350 µg C). With respect to the dynamic nature of thermogram evolution for different sample types and the variability in 14C contents, this result may reflect a typical scattering in fraction size where individual split sizes sometimes even account for much less with only 50 µg C. The thermal heating gradient of a sample typically results in differing 14C signatures for the individual splits. Here the blank correction of data for split sizes and sampling duration allows determination of the actual isotopic composition of discrete fractions in a sample.
A correction of sample data with procedural standards is most precise if sample 14C falls within the modern and depleted 14C signatures. In this study we used a set of 14Cmodern (Fm = 1.0354 ± 0.0021; n = 6) and 14Cdepleted (Fm = 0.0119 ± 0.0013; n = 5) pure NaHCO3 procedural standards to access the magnitude of the blank including the associated uncertainty and to correct the data. Yet, a NaHCO3 standard with custom 14C contents spanning a larger 14C range could easily be produced at a similar high precision.
Potential of Full Oxidation Mode Columns for Interface Development
The successful installation of the RPO sequential thermal analysis instrumentation at NOSAMS over a decade ago has been extensively used to understand organic matter complexity. It has substantially improved our understanding of the global carbon cycle, including the identification of adequate autochthonous organic carbon for 14C dating, the fate of carbon across landscapes, and its powerful application in environmental forensics. To further advance the applicability and to expand the results with additional information, the incorporation of online δ13C monitoring as well as routine quality assurance procedures would result in improved precision and accuracy.
As discussed in this paper, the interpretation of distinct thermograms bear uncertainties for the identification of specific substrate types. A proof of concept study investigated the use of cavity ring-down spectroscopy to monitor discrete fractions of evolved CO2 yields (Cruz et al. Reference Cruz, Gagnon, McNichol, Burton, Elder, Lardie, Gospodinova, Hlavenka, Kurz, Longworth, Roberts, Trowbridge, Walther and Xu2017) during the sequential thermal analysis. The instrument failed to operate after the initial measurements, which may have been caused by corrosion of the detector by secondary gas species that were incompletely removed. Although this is not definitive, there are several lines of evidence that the custom-made wires used in the pyrolysis-RPO and oxidation-RPO setups incompletely purified the evolved CO2, resulting in the presence of oxidative nitrogen-, chlorine-, and sulfur-species. This eventually necessitated the sealed-tube combustion with CuO and Ag to successfully form filamentous carbon or measure the stable C isotopic composition on the IRMS. With the novel FOX combustion column, this extra step will no longer be necessary.
The good agreement between thermogram shape and isotope data between the pyrolysis/oxidation combustion columns and the novel FOX mode suggests no constraints for alternating use. With the FOX combustion column for the NOSAMS setup, we obtained successful analyses even for extreme types of organic mixtures in environmental samples without recombustion. The improved gas purification may now allow for online isotope monitoring with lesser risk to corrode the instrumentation. Further, it can also allow for sealed-tube zinc graphitization, a procedure that has recently been reported to return precise AMS data even for microscale sample amounts (Walker and Xu Reference Walker and Xu2019). This is a powerful sample processing procedure as it would allow to process splits (roughly 4–5 splits per sample) of two to three samples a day, graphitize overnight and have filamentous carbon ready for AMS analyses the next morning. Alternatively, the reduced carbon produced in sealed glass tubes can be stored for years without affecting the quality of the material. This largely increases sample throughput and accompanied by some procedural blanks it enables quality assessment for the operator while reducing labor costs for additional sample processing. Further developments in the future might also comprise the design of a sequential thermal analyses setup with multiple combustion columns that automatically transfer CO2 splits on molecular sieve traps that then could be measured with gas-accepting AMS instrumentation in series. This would also facilitate increasing the number of processing standards and enable larger data-series for 14C quality assurance.
The results from this study demonstrate the successful use for a diversity of complex environmental matrices and the improved purification capacity of the full oxidation column that makes the recombustion of gas sample splits unnnecessary. Further, the bicarbonate procedural standards now allow each operator to implement individual quality control measures.
SUPPLEMENTARY MATERIAL
To view supplementary material for this article, please visit https://doi.org/10.1017/RDC.2023.13
ACKNOWLEDGMENTS
The authors thank the NOSAMS staff for support of the analyses, Sean Sylva for critical discussions, Mark Roberts for help setting up the RGA interface, and Adam Subhas for support during the bicarbonate dissolution experiment. Reviews by Brad E Rosenheim and another anonymous reviewer provided valuable comments to improve the quality of this paper. We are grateful to Brad E Rosenheim and Bao Rui for sample materials, Josh Hvalenka for the technical sketch of the instrument, and Bob Nelson for helping with sampling the salt marsh sedimentary sequence in Wild Harbor, Falmouth, MA, USA. Author UMH acknowledges the NSF for funding his postdoctoral position at NOSAMS (OCE 1755125).
