Early Eocene carbon isotope excursions in a lignite bearing succession at the southern edge of the proto-North Sea (Sch&ouml;ningen, Germany)

Lenz, Olaf K.; Montag, Mara; Wilde, Volker; Methner, Katharina; Riegel, Walter; Mulch, Andreas

doi:https://doi.org/10.5194/cp-2021-81

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https://doi.org/10.5194/cp-2021-81

Preprints

23 Jul 2021

Status: a revised version of this preprint was accepted for the journal CP and is expected to appear here in due course.

Early Eocene carbon isotope excursions in a lignite bearing succession at the southern edge of the proto-North Sea (Schöningen, Germany)

Olaf K. Lenz^1,2, Mara Montag², Volker Wilde¹, Katharina Methner^3,5, Walter Riegel¹, and Andreas Mulch^3,4 Olaf K. Lenz et al.

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¹Senckenberg Research Institute and Natural History Museum Frankfurt, 60325 Frankfurt am Main, Germany
²Institute of Applied Geosciences, Technical University Darmstadt, 64287 Darmstadt, Germany
³Senckenberg Biodiversity and Climate Research Centre (SBiK-F), Senckenberganlage 25, 60325 Frankfurt am Main, Germany
⁴Institute of Geosciences, Goethe University Frankfurt, 60438 Frankfurt am Main, Germany
⁵Department of Earth System Science, Department of Geological Sciences, Stanford University, USA

Received: 30 Jun 2021 – Discussion started: 23 Jul 2021

Abstract. Situated at the southern edge of the proto-North Sea the lower Eocene Schöningen Formation of the Helmstedt Lignite Mining District, Lower Saxony, Germany is characterized by several lignite seams alternating with estuarine to brackish interbeds. Here, we present carbon isotope data of bulk organic matter (δ¹³C_TOC), organic carbon content (%TOC), and palynomorphs from a 98 m thick sequence of the Schöningen Formation embedded into a new robust age model. This is based on eustatic sea-level changes, biostratigraphy, and a correlation to existing radiometric ages. Based on the δ¹³C_TOC data we observe six negative carbon isotope excursions (CIEs) reflecting massive short-term carbon cycle perturbations. A strong CIE of −2.6 ‰ in δ¹³C_TOC values in the Main Seam and the succeeding marine interbed can be related to the Paleocene–Eocene Thermal Maximum (PETM). The subsequent CIE of −1.7 ‰ in δ¹³C_TOC values may be correlated with the Eocene Thermal Maximum 2 (ETM2) or slightly older events preceding the ETM2. High-amplitude climate fluctuations including at least 4 minor CIEs with a maximum negative shift of −1.3 ‰ in δ¹³C_TOC in the upper part of the studied section are characteristic for the EECO. Palynological analysis across the Main Seam proved that shifts in δ¹³C_TOC values are correlated with changes in the peat forming wetland vegetation, specifically the change from a mixed angiosperm and gymnosperm flora to an angiosperm dominated vegetation at the onset of the PETM. The PETM-related CIE shows a distinct rebound to higher δ¹³C_TOC values shortly after the onset of the CIE, which is here recognized as a common feature of terrestrial and marginal marine PETM-records worldwide and may be related to changes in the vegetation including different carbon isotope budgets of gymnosperms and angiosperms.

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Olaf K. Lenz et al.

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RC1:
'Comment on cp-2021-81', Anonymous Referee #1, 11 Oct 2021

This paper presents carbon isotope data of bulk organic matter (δ¹³C_TOC), organic carbon content, and palynomorphs from an Early Eocene study site in Germany. The authors provide a new age model for the section and despite the variability in carbon isotope values, try to make educated interpretations to outline up to six potential negative carbon isotope excursions (CIEs). A full assessment of the intricacies of the lithological interpretations and stratigraphic framework is outside my area of expertise. That said, the paper appears to provide a lengthy description of observations.

One particular challenge is that there is a lot of variability in the δ¹³C_TOC values, which is a problem with relying on bulk organic matter to define carbon isotope excursion intervals. The authors do provide some context relative to other sections, especially with regards to the variability in the isotope values. I cannot help but wonder if others looking at the carbon isotope values would draw the same conclusions because of the variability.

It does seem like this paper is a helpful addition to constraining an additional study site of Early Eocene CIEs. This would be constructive for future work analyzing this area and for comparison to study sites in other regions to understand climate in the past. I think it’s important to better note the level uncertainty in the results and age correlations to avoid oversimplification though.

Has any attempt been made to do compound-specific isotopes to help define the carbon isotope excursions? I think it would be worth mentioning this in the paper. For example, Ln 423 refers to work from the Bighorn Basin, where more recent work by Baczynski and others have provided evidence for how bulk organic matter carbon isotopes values can be distorted indicators of CIEs (as a function of a combination of organic matter sources, reworking of organic matter, and degradation). See for example, Baczynski et al. 2016 https://doi.org/10.1130/B31389.1

More specific comments:

Ln 99. The frequent changes between terrestrial and marine conditions and thus changes in TOC input type can be a challenge for sourcing. Mixed inputs would affect the δ¹³C of the bulk organic matter.

Ln 165. The figure number of the diagram needs to be specified.

Ln 276-281. How does the variability compare to other well-constrained CIEs and other sections with similar lithology changes as this section? In Ln 279, “comparatively high standard deviation” – what are the authors comparing to? What is causing the high variability, the “great range of δ¹³C_TOC”?

Ln 280. “significant decrease”. On what statistical basis was this determined to be significant?

Ln 333. “values increase significantly” As above, are there statistics to attest to the significance?

Ln 342 “a weak CIE”. Weak is a qualitative term, information on the magnitude of the excursion/time or depth interval/number of samples could help clarify the identification of this CIE.

Ln 389. I think the authors meant 1,000 years (1 kyr), not 1.000 years.

Ln 422. Can you provide and clarify the evidence that rules out reworking of organic matter? This is again stated in the conclusions, Ln 489, reworking is almost excluded within our seam. As far as I can tell, the logic may be that the rebound structure is consistent with the pollen and spore record…but that doesn’t mean reworking couldn’t also be a factor?

Table and Figure comments:

Table 1. What do the parentheses indicate vs. non-parentheses for the references? Also check for consistent spacing in the table between words.

Table 2. It would be useful to specify what stratigraphic positions (meter levels) were used for each of the identified excursions.

Figure 1. It looks like there is an extra space in the “Seam 7” label.

Figure 3. Is there any meaning between the different number of dots in the lines in the legend for global sea level curves?

Figure 6. I realize the authors may be citing the units used in the other publications, but it’s unclear to the reader whether there is any meaningful difference between the types of organic matter. For example, δ¹³C_org “organic matter” versus δ¹³C_TOC “bulk organic matter”.

Figure 7. Clarify is the carbon isotope data here from bulk organic matter?

Figure 8. TOC for the carbon isotope record should be subscipt.

Citation: https://doi.org/10.5194/cp-2021-81-RC1
- AC2: 'Reply on RC1', Olaf Lenz, 18 Aug 2022
  
  The comment was uploaded in the form of a supplement: https://cp.copernicus.org/preprints/cp-2021-81/cp-2021-81-AC2-supplement.pdf
  
  Citation: https://doi.org/10.5194/cp-2021-81-AC2
RC2:
'Comment on cp-2021-81', Anonymous Referee #2, 28 Jun 2022

The study by Lenz and colleagues provides a high-resolution terrestrial organic carbon isotope curve covering the Late Paleocene – Early Eocene. The new d13Corg curve is embedded into a detailed stratigraphic framework based on new dinoflagellate biostratigraphy coupled with sequence-stratigraphic considerations. The new age constraints enable comparison (and tentative correlation) of pronounced carbon isotope anomalies (CIE 1 to 6) observed the lignite-bearing record with marine carbon isotope trends and associated hyperthermals including the PETM, ETM2 (questionable) and EECO. The core of the study is a high-resolution d13Corg curve based on >320 measurements, part of which (~120 data points) has already been published by Methner et al. (2019) in Climate of the Past.

The manuscript represents a well written scientific study of very good quality, presenting new and important findings. The data-set is well presented in a number of high-quality figures and diagrams. Stratigraphically well constrained land-sea correlations during times of exceptional global warmth are of paramount importance to better understand the coupled response of the marine and continental biosphere during such hyperthermal events. In this respect, the study is clearly well suited for publication in Climate of the Past. However, some aspects remain critical and need revision, as outlined below.

Major points

My main criticism is the absence of an in-depth discussion on the controls of the carbon isotopic composition of the mire-derived OM, which is interpreted here to record a global atmospheric carbon isotope signal. In my view, several aspects should be considered in order to better distinguish between potential global and local carbon isotope signatures. Firstly, the overall composition of the predominantly land plant-derived OM is rather negative ( -25.5 to -28.5 ‰) which deserves some discussion. Gröcke (2002) gives an average of -23 to -27 for C3 land plant-derived OM. Comparison with time-equivalent plant derived carbon isotope values would help to get an idea of the background level expected during the Late Paleocene – Early Eocene. In addition, data from other near-shore mire deposits would provide a range for the carbon isotope composition variability in such environments.

In chapter 4.3, the authors refer to the general difference in the d13C composition of land- and marine-derived OM. In consequence, mixing of marine and terrestrial organic carbon is used to explain certain variations in the Schöningen stratigraphic record (line 321 ff.). However, when comparing the d13C signature of isolated marine particles (dinoflagellate cysts) analyzed from before and throughout the PETM (Sluijs et al. 2017, Geology), it becomes clear that the dinoflagellate-derived d13C composition covers a similar range compared to the OM from the Schöningen record. During the Early Paleogene, the d13Corg composition of marine OM is not depleted compared to the values obtained from Schöningen, which hampers any source assignment of the OM based on the d13C signature. To better distinguish between different sources, RockEval pyrolysis and/or palynofacies data would certainly help.

At the beginning of chapter 4.3 (line 309-310), the authors state that when comparing the new CIEs with known CIEs, a differentiation between shifts at lithological boundaries and shifts occurring within the same lithology is necessary. This statement seems to indicate that CIEs associated with lithological boundaries are more prone to be caused by local changes (e.g. OM composition) compared to within-facies shifts, which are - in consequence - interpreted as super-regional (global) phenomena. The authors do not refer to potential processes, which may cause the high-amplitude shifts in d13Corg within individual coal seams. Their data shows that pronounced changes do occur within many of the studied coal seams, which may be controlled by various environmental processes and not necessarily reflect changes in the global d13C signature. Mires do evolve with time and mire-producing plant successions change with mire growth, which is expected to cause stratigraphic changes in the bulk d13C signature of the peat/lignite. Interestingly, the detailed pollen record from the main seam (Fig. 7) does show pronounced changes in the pollen assemblage, which does occur time-equivalent to a major shift in the d13C record (e.g. pronounced increase of Myricaceae associated with a strong negative CIE). This negative CIE is considered to represent the onset of the PETM negative CIE and therefore, the co-occurrence of negative CIE and vegetation shift needs to be explained in more detail. In lines 411 ff. the authors refer to this coincidence as intra-PETM fluctuations, but a more in-depth discussion is lacking. The authors need to explain, on which basis local environmental drivers (incl. vegetation and/or humidity changes) can be excluded to explain the onset of the negative CIE 1. In general, potential environmental processes affecting the d13C composition of the OM need to be considered in more depth and need to be included in the interpretation of the stratigraphic trend obtained from Schöningen.

Chapter 4.4.1 deals with the CIE associated with the PETM. The authors provide compelling evidence for a correlation of the Schöningen CIE1 with the globally recognized PETM CIE. What is less clear is the basis for the base and top boundaries show in Fig. 6, which constrain the PETM CIE. Why is the basal boundary placed at the data point showing the least negative value in this part of the curve (and not slightly higher at the data point just before the negative shift)? This has implications for the total amplitude of the anomaly (see table 2). Similarly, the positioning of the upper limit (red line in Fig. 6) of the CIE is hard to follow given that another interval with comparatively negative values is following above. A more plausible termination of the CIE would be at the transition towards less negative values (~23 m height). Are there any stratigraphic constraints for the positioning of those boundaries?

Line 351 – here, the authors refer to the previous study by Methner et al. (2019, CP), which – according to the authors - already did suggest a position of both, the PETM and the P/E boundary below seam 1. However, when reading the study by Methner et al. (2019), one does get another impression. In this previous work, a pronounced negative anomaly (the interval entitled CIE2 in the submitted paper) is suggested to tentatively correspond to the PETM negative anomaly and comparison and correlation with PETM-equivalent anomalies (Cobham lignite, Vasterival) is given. This view is now significantly revised and the part considered to correspond to the PETM by Methner et al. (2019) is now placed in the post-PETM part of the Schöningen record. This is not in itself problematic since new stratigraphic data does results in a re-interpretation of the previous data set. But this re-interpretation needs to be made clear and the statement above (line 351) should be rephrased to better represent the suggestions of Methner et al. (2019).

Minor points

Line 22: The abbreviation EECO is not explained in the abstract.

Line 40: Please include “to 27 to 35°C in the earliest Eocene (Inglis et al. 2020)”

Line 49: The author refers to “kilo year to millennial scale”. To me (and maybe to other readers) the difference between the 2 time intervals is not clear? Please explain or rephrase.

Line 76 ff. There is a new published terrestrial d13Corg record and associated palynology across the PETM published by Xie et al. (2022, Paleo3) entitled “Abrupt collapse of a swamp ecosystem in northeast China during the Paleocene–Eocene Thermal Maximum” which should be referred to.

Line 272: The heading refers to the “basal Schöningen Formation” but the interval studied does represent more then half of the Schöningen Formation. Hence, the phrase “lower” might be better suited here…

Line 421: Change to “observed in the terrestrial records”.

Citation: https://doi.org/10.5194/cp-2021-81-RC2
- AC1: 'Reply on RC2', Olaf Lenz, 18 Aug 2022
  
  The comment was uploaded in the form of a supplement: https://cp.copernicus.org/preprints/cp-2021-81/cp-2021-81-AC1-supplement.pdf
  
  Citation: https://doi.org/10.5194/cp-2021-81-AC1
- AC3: 'Reply on RC2', Olaf Lenz, 18 Aug 2022
  
  The comment was uploaded in the form of a supplement: https://cp.copernicus.org/preprints/cp-2021-81/cp-2021-81-AC3-supplement.pdf
  
  Citation: https://doi.org/10.5194/cp-2021-81-AC3

Status: closed

RC1:
'Comment on cp-2021-81', Anonymous Referee #1, 11 Oct 2021

This paper presents carbon isotope data of bulk organic matter (δ¹³C_TOC), organic carbon content, and palynomorphs from an Early Eocene study site in Germany. The authors provide a new age model for the section and despite the variability in carbon isotope values, try to make educated interpretations to outline up to six potential negative carbon isotope excursions (CIEs). A full assessment of the intricacies of the lithological interpretations and stratigraphic framework is outside my area of expertise. That said, the paper appears to provide a lengthy description of observations.

One particular challenge is that there is a lot of variability in the δ¹³C_TOC values, which is a problem with relying on bulk organic matter to define carbon isotope excursion intervals. The authors do provide some context relative to other sections, especially with regards to the variability in the isotope values. I cannot help but wonder if others looking at the carbon isotope values would draw the same conclusions because of the variability.

It does seem like this paper is a helpful addition to constraining an additional study site of Early Eocene CIEs. This would be constructive for future work analyzing this area and for comparison to study sites in other regions to understand climate in the past. I think it’s important to better note the level uncertainty in the results and age correlations to avoid oversimplification though.

Has any attempt been made to do compound-specific isotopes to help define the carbon isotope excursions? I think it would be worth mentioning this in the paper. For example, Ln 423 refers to work from the Bighorn Basin, where more recent work by Baczynski and others have provided evidence for how bulk organic matter carbon isotopes values can be distorted indicators of CIEs (as a function of a combination of organic matter sources, reworking of organic matter, and degradation). See for example, Baczynski et al. 2016 https://doi.org/10.1130/B31389.1

More specific comments:

Ln 99. The frequent changes between terrestrial and marine conditions and thus changes in TOC input type can be a challenge for sourcing. Mixed inputs would affect the δ¹³C of the bulk organic matter.

Ln 165. The figure number of the diagram needs to be specified.

Ln 276-281. How does the variability compare to other well-constrained CIEs and other sections with similar lithology changes as this section? In Ln 279, “comparatively high standard deviation” – what are the authors comparing to? What is causing the high variability, the “great range of δ¹³C_TOC”?

Ln 280. “significant decrease”. On what statistical basis was this determined to be significant?

Ln 333. “values increase significantly” As above, are there statistics to attest to the significance?

Ln 342 “a weak CIE”. Weak is a qualitative term, information on the magnitude of the excursion/time or depth interval/number of samples could help clarify the identification of this CIE.

Ln 389. I think the authors meant 1,000 years (1 kyr), not 1.000 years.

Ln 422. Can you provide and clarify the evidence that rules out reworking of organic matter? This is again stated in the conclusions, Ln 489, reworking is almost excluded within our seam. As far as I can tell, the logic may be that the rebound structure is consistent with the pollen and spore record…but that doesn’t mean reworking couldn’t also be a factor?

Table and Figure comments:

Table 1. What do the parentheses indicate vs. non-parentheses for the references? Also check for consistent spacing in the table between words.

Table 2. It would be useful to specify what stratigraphic positions (meter levels) were used for each of the identified excursions.

Figure 1. It looks like there is an extra space in the “Seam 7” label.

Figure 3. Is there any meaning between the different number of dots in the lines in the legend for global sea level curves?

Figure 6. I realize the authors may be citing the units used in the other publications, but it’s unclear to the reader whether there is any meaningful difference between the types of organic matter. For example, δ¹³C_org “organic matter” versus δ¹³C_TOC “bulk organic matter”.

Figure 7. Clarify is the carbon isotope data here from bulk organic matter?

Figure 8. TOC for the carbon isotope record should be subscipt.

Citation: https://doi.org/10.5194/cp-2021-81-RC1
- AC2: 'Reply on RC1', Olaf Lenz, 18 Aug 2022
  
  The comment was uploaded in the form of a supplement: https://cp.copernicus.org/preprints/cp-2021-81/cp-2021-81-AC2-supplement.pdf
  
  Citation: https://doi.org/10.5194/cp-2021-81-AC2
RC2:
'Comment on cp-2021-81', Anonymous Referee #2, 28 Jun 2022

The study by Lenz and colleagues provides a high-resolution terrestrial organic carbon isotope curve covering the Late Paleocene – Early Eocene. The new d13Corg curve is embedded into a detailed stratigraphic framework based on new dinoflagellate biostratigraphy coupled with sequence-stratigraphic considerations. The new age constraints enable comparison (and tentative correlation) of pronounced carbon isotope anomalies (CIE 1 to 6) observed the lignite-bearing record with marine carbon isotope trends and associated hyperthermals including the PETM, ETM2 (questionable) and EECO. The core of the study is a high-resolution d13Corg curve based on >320 measurements, part of which (~120 data points) has already been published by Methner et al. (2019) in Climate of the Past.

The manuscript represents a well written scientific study of very good quality, presenting new and important findings. The data-set is well presented in a number of high-quality figures and diagrams. Stratigraphically well constrained land-sea correlations during times of exceptional global warmth are of paramount importance to better understand the coupled response of the marine and continental biosphere during such hyperthermal events. In this respect, the study is clearly well suited for publication in Climate of the Past. However, some aspects remain critical and need revision, as outlined below.

Major points

My main criticism is the absence of an in-depth discussion on the controls of the carbon isotopic composition of the mire-derived OM, which is interpreted here to record a global atmospheric carbon isotope signal. In my view, several aspects should be considered in order to better distinguish between potential global and local carbon isotope signatures. Firstly, the overall composition of the predominantly land plant-derived OM is rather negative ( -25.5 to -28.5 ‰) which deserves some discussion. Gröcke (2002) gives an average of -23 to -27 for C3 land plant-derived OM. Comparison with time-equivalent plant derived carbon isotope values would help to get an idea of the background level expected during the Late Paleocene – Early Eocene. In addition, data from other near-shore mire deposits would provide a range for the carbon isotope composition variability in such environments.

In chapter 4.3, the authors refer to the general difference in the d13C composition of land- and marine-derived OM. In consequence, mixing of marine and terrestrial organic carbon is used to explain certain variations in the Schöningen stratigraphic record (line 321 ff.). However, when comparing the d13C signature of isolated marine particles (dinoflagellate cysts) analyzed from before and throughout the PETM (Sluijs et al. 2017, Geology), it becomes clear that the dinoflagellate-derived d13C composition covers a similar range compared to the OM from the Schöningen record. During the Early Paleogene, the d13Corg composition of marine OM is not depleted compared to the values obtained from Schöningen, which hampers any source assignment of the OM based on the d13C signature. To better distinguish between different sources, RockEval pyrolysis and/or palynofacies data would certainly help.

At the beginning of chapter 4.3 (line 309-310), the authors state that when comparing the new CIEs with known CIEs, a differentiation between shifts at lithological boundaries and shifts occurring within the same lithology is necessary. This statement seems to indicate that CIEs associated with lithological boundaries are more prone to be caused by local changes (e.g. OM composition) compared to within-facies shifts, which are - in consequence - interpreted as super-regional (global) phenomena. The authors do not refer to potential processes, which may cause the high-amplitude shifts in d13Corg within individual coal seams. Their data shows that pronounced changes do occur within many of the studied coal seams, which may be controlled by various environmental processes and not necessarily reflect changes in the global d13C signature. Mires do evolve with time and mire-producing plant successions change with mire growth, which is expected to cause stratigraphic changes in the bulk d13C signature of the peat/lignite. Interestingly, the detailed pollen record from the main seam (Fig. 7) does show pronounced changes in the pollen assemblage, which does occur time-equivalent to a major shift in the d13C record (e.g. pronounced increase of Myricaceae associated with a strong negative CIE). This negative CIE is considered to represent the onset of the PETM negative CIE and therefore, the co-occurrence of negative CIE and vegetation shift needs to be explained in more detail. In lines 411 ff. the authors refer to this coincidence as intra-PETM fluctuations, but a more in-depth discussion is lacking. The authors need to explain, on which basis local environmental drivers (incl. vegetation and/or humidity changes) can be excluded to explain the onset of the negative CIE 1. In general, potential environmental processes affecting the d13C composition of the OM need to be considered in more depth and need to be included in the interpretation of the stratigraphic trend obtained from Schöningen.

Chapter 4.4.1 deals with the CIE associated with the PETM. The authors provide compelling evidence for a correlation of the Schöningen CIE1 with the globally recognized PETM CIE. What is less clear is the basis for the base and top boundaries show in Fig. 6, which constrain the PETM CIE. Why is the basal boundary placed at the data point showing the least negative value in this part of the curve (and not slightly higher at the data point just before the negative shift)? This has implications for the total amplitude of the anomaly (see table 2). Similarly, the positioning of the upper limit (red line in Fig. 6) of the CIE is hard to follow given that another interval with comparatively negative values is following above. A more plausible termination of the CIE would be at the transition towards less negative values (~23 m height). Are there any stratigraphic constraints for the positioning of those boundaries?

Line 351 – here, the authors refer to the previous study by Methner et al. (2019, CP), which – according to the authors - already did suggest a position of both, the PETM and the P/E boundary below seam 1. However, when reading the study by Methner et al. (2019), one does get another impression. In this previous work, a pronounced negative anomaly (the interval entitled CIE2 in the submitted paper) is suggested to tentatively correspond to the PETM negative anomaly and comparison and correlation with PETM-equivalent anomalies (Cobham lignite, Vasterival) is given. This view is now significantly revised and the part considered to correspond to the PETM by Methner et al. (2019) is now placed in the post-PETM part of the Schöningen record. This is not in itself problematic since new stratigraphic data does results in a re-interpretation of the previous data set. But this re-interpretation needs to be made clear and the statement above (line 351) should be rephrased to better represent the suggestions of Methner et al. (2019).

Minor points

Line 22: The abbreviation EECO is not explained in the abstract.

Line 40: Please include “to 27 to 35°C in the earliest Eocene (Inglis et al. 2020)”

Line 49: The author refers to “kilo year to millennial scale”. To me (and maybe to other readers) the difference between the 2 time intervals is not clear? Please explain or rephrase.

Line 76 ff. There is a new published terrestrial d13Corg record and associated palynology across the PETM published by Xie et al. (2022, Paleo3) entitled “Abrupt collapse of a swamp ecosystem in northeast China during the Paleocene–Eocene Thermal Maximum” which should be referred to.

Line 272: The heading refers to the “basal Schöningen Formation” but the interval studied does represent more then half of the Schöningen Formation. Hence, the phrase “lower” might be better suited here…

Line 421: Change to “observed in the terrestrial records”.

Citation: https://doi.org/10.5194/cp-2021-81-RC2
- AC1: 'Reply on RC2', Olaf Lenz, 18 Aug 2022
  
  The comment was uploaded in the form of a supplement: https://cp.copernicus.org/preprints/cp-2021-81/cp-2021-81-AC1-supplement.pdf
  
  Citation: https://doi.org/10.5194/cp-2021-81-AC1
- AC3: 'Reply on RC2', Olaf Lenz, 18 Aug 2022
  
  The comment was uploaded in the form of a supplement: https://cp.copernicus.org/preprints/cp-2021-81/cp-2021-81-AC3-supplement.pdf
  
  Citation: https://doi.org/10.5194/cp-2021-81-AC3

Olaf K. Lenz et al.

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Short summary

We describe different carbon isotope excursions (CIE) in a Paleocene to lower Eocene lignite succession (Schöningen, DE) . The combination with a new stratigraphic framework allows for an exact correlation of distinct CIEs to long- and short-term thermal events of the last natural greenhouse period on Earth. Furthermore, changes in the peat forming wetland vegetation are correlated with a CIE that can be can be related to the Paleocene–Eocene Thermal Maximum (PETM).


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