A 600-kyr reconstruction of deep Arctic seawater &delta;18O from benthic foraminiferal &delta;18O and ostracode Mg/Ca paleothermometry

Farmer, Jesse R.; Keller, Katherine J.; Poirier, Robert K.; Dwyer, Gary S.; Schaller, Morgan F.; Coxall, Helen K.; O'Regan, Matthew; Cronin, Thomas M.

doi:https://doi.org/10.5194/egusphere-2022-1212

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https://doi.org/10.5194/egusphere-2022-1212

Preprints

07 Nov 2022

| 07 Nov 2022

A 600-kyr reconstruction of deep Arctic seawater δ¹⁸O from benthic foraminiferal δ¹⁸O and ostracode Mg/Ca paleothermometry

Jesse R. Farmer, Katherine J. Keller, Robert K. Poirier, Gary S. Dwyer, Morgan F. Schaller, Helen K. Coxall, Matthew O'Regan, and Thomas M. Cronin

Abstract. The oxygen isotopic composition of benthic foraminiferal tests (δ¹⁸O_b) is one of the preeminent tools for correlating marine sediments and interpreting past terrestrial ice volume and deep-ocean temperatures. Despite the prevalence of δ¹⁸O_b applications to marine sediment cores over the Quaternary, its use is limited in the Arctic Ocean because of low benthic foraminiferal abundances, challenges with constructing independent sediment core age models, and an apparent muted amplitude of Arctic δ¹⁸O_b variability compared to open ocean records. Here we evaluate the controls on Arctic δ¹⁸O_b by using ostracode Mg/Ca paleothermometry to generate a composite record of the δ¹⁸O of seawater (δ¹⁸O_sw) from fourteen sediment cores in the intermediate to deep Arctic Ocean (700–2700 m) covering the last 600 kyr. Results show that Arctic δ¹⁸O_b was generally higher than open ocean δ¹⁸O_b during interglacials but was generally equivalent to global reference records during glacial periods. The reduced glacial-interglacial Arctic δ¹⁸O_b range resulted in part from the opposing effect of temperature, with intermediate-to-deep Arctic warming during glacials counteracting the whole-ocean δ¹⁸O_sw increase from expanded terrestrial ice sheets. After removing the temperature effect from δ¹⁸O_b, we find that the intermediate-to-deep Arctic experienced large (≥ 1 ‰) variations in local δ¹⁸O_sw, with generally higher local δ¹⁸O_sw during interglacials and lower δ¹⁸O_sw during glacials. Both the magnitude and timing of low local δ¹⁸O_sw intervals are inconsistent with the recent proposal of freshwater intervals in the Arctic Ocean during past glaciations. Instead, we suggest that lower local δ¹⁸O_sw in the intermediate-to-deep Arctic Ocean during glaciations reflected weaker upper ocean stratification and more efficient transport of low-δ¹⁸O_sw Arctic surface waters to depth by mixing and/or brine rejection.

Received: 03 Nov 2022 – Discussion started: 07 Nov 2022

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14 Mar 2023

A 600 kyr reconstruction of deep Arctic seawater δ¹⁸O from benthic foraminiferal δ¹⁸O and ostracode Mg ∕ Ca paleothermometry

Jesse R. Farmer, Katherine J. Keller, Robert K. Poirier, Gary S. Dwyer, Morgan F. Schaller, Helen K. Coxall, Matt O'Regan, and Thomas M. Cronin

Clim. Past, 19, 555–578, https://doi.org/10.5194/cp-19-555-2023,https://doi.org/10.5194/cp-19-555-2023, 2023

Short summary

Jesse R. Farmer et al.

Interactive discussion

Status: closed

RC1:
'Comment on egusphere-2022-1212', Robert F. Spielhagen, 01 Dec 2022

Farmer et al. present a collection of benthic oxygen isotope data from Arctic deep-sea sediment cores, derived from benthic foraminifers. The data are partly new, but several data sets have been published in the last decades. The authors use these data to calculate past seawater d180, taking into account past changes in global ice volume and bottom water temperature. For the latter they use Mg/Ca data, which are a reliable paleothermometer. The major result is that glacial periods of the last 600 kyr often saw significantly lower values of d18O at the sea floor than interglacials. The authors then discuss possible explanations for this observation and rule out that the Arctic Ocean was filled with freshwater during recent glacials, as proposed by Geibert et al. (2021, Nature). Instead they suggest intensive brine formation during glacials as a process which could have led to a downslope transport of dense, low-d18O waters.

The manuscript is written in excellent English; it is well structured and the figures are illustrative. I suggest to add a table with details on core numbers, geographical coordinates and water depths. This table may be added as a supplement. The reader should not be forced to look up all the core details in various papers. There are some vertical differences in temperature even in the deeper Arctic Ocean and since these difference may affect the d18O in carbonates, water depths of individual cores (e.g., those used for Fig. 2) are critical information (even though there is a temperature correction from Mg/Ca data in the d18O data sets).

Overall, I find this manuscript already in a very mature condition. The Abstract is informative, as is the Introduction which gives various aspects of background information. One or two sentences on the research question(s) tackled in this manuscript would be helpful for the reader to better understand what the authors are aiming at. The work performed is nicely described in the last paragraph of the Introduction, but I guess the authors started with a research question before they performed the data acquisition and collection.

The second chapter gives further background information on the various factors controlling oxygen isotopes in seawater and on the modern oceanographic situation in the Arctic Ocean. All necessary details are presented.

The chapter on Materials and Methods supplies details on the measurements performed, on the core chronology, and on the calculation of d18O of paleo-seawater. The subchapters give all necessary details in a concise manner. In particular I like the subchapter on chronology which clearly states some of the current problems with assigning definite ages to interglacial sediments older than 200 ka. Although the U/Th-based age model put forward by Hillaire-Marcel et al. (2017) is at odds with the "conventional" age model of, e.g., Jakobsson et al., 2000, Spielhagen et al., 2004; O'Regan et al., 2008, 2020, it should still be mentioned.

In the Discussion the authors argue that uncertainties with the chronology (including possible hiatuses like in the LGM) make it problematic to discuss individual periods with d18O minima beyond MIS 6. In the following subchapters they almost entirely concentrate an possible explanations for low glacial d18O of seawater and how these explanations can or cannot be reconciled with the Geibert et al. (2021) hypothesis. While I find the arguments sound and the debate highly interesting, I think the authors miss a chance to comment also on paleoenvironments in previous glaciations. I fully acknowledge that the authors want to be cautious with age assignments beyond MIS 6, but still they should discuss to some greater extent than at present the time back to MIS 15 for which they have collected a nice data set shown in Fig. 4. If they do not do this, one may ask why data from MIS 7-15 are shown at all and why d18O differences between individual stages and substages are laid out in detail in subchapter 4.2.

The debate on a possible "fresh glacial Arctic" explanation for the low glacial d18O of seawater makes up most of the Discussion chapter. I find the arguments given highly plausible, but I have to admit that I am somewhat biased against the Geibert et al. (2021) hypothesis, as demonstrated in our comment on that paper (Spielhagen et al., 2022, Nature). Nevertheless, I think that Farmer et al. have done a good job in collecting various other data speaking against a "fresh glacial Arctic" and discussing these in depth so that their own explanation for low glacial d18O data is left as the most plausible hypothesis.

This explanation is described in the last subchapter of the Discussion (5.2). The authors propose a weakened glacial stratification in the glacial oceans as the most likely cause for low d180 of intermediate to deep waters. They explicitly mention "enhanced vertical mixing" and "the transport of low-δ18Osw brines to intermediate depths". While the latter seems sufficiently clear, considering the previous discussion of eNd values in subchapter 5.1, there is no statement on what may have caused "enhanced vertical mixing" and how and where this may have happened in an ice-covered ocean. This needs be be made clear - otherwise it will remain a "black box" for the readers. I also suggest to include a figure (cartoon) showing the proposed scenario for brine formation.

The Conclusion chapter nicely summarizes the major findings discussed in the previous chapter. It ends with some comments on the suitability of benthic d18O data and ostracode Mg/Ca paleothermometry for future paleoclimate research in the Arctic. In my (not necessarily correct) opinion, the latter point should have been tackled with some pros and cons already in chapter 5 and not just as the last sentences of the manuscript.

Specific comments by line numbers

93: Actually, the isotopic change during the transition from sea water to sea ice is only very minor (fractionation factor ~1.003; https://doi.org/10.3189/S0022143000042751) and can be neglected when isotopic changes on glacial-interglacial scales are discussed. However, the d18O/salinity relation in ocean waters can be strongly affected. This can lead to density changes and the sinking of low-d18O near-surface waters to greater depths. Considering these details, the statement in line 93 is too much simplified.

109: What is "AL"?

124: color bar

144: analysis. Analyses

185-186: Since the default R is 550 yr in Marine20 (and was 402 yr in Marine13), it might be worth mentioning the R used in this study.

186: Blaauw (to be corrected also in the list of references!)

192: Bulimina aculeata

200: Lomonosov Ridge

282: A temperature of -0.3°C may be correct for intermediate waters (AIW), but deeper waters are colder (-0.9°C; see line 106).

284: Temperatures are numbers and cannot be "warmer", only higher. Check for other usage of "cooler" and "warmer" BWTs throughout the manuscript!

289-291: I suggest to discuss the differences going from 50 ka to present and not vice versa.

346 (and 437): I would regard 7b and 13b as interstadials within MIS 7 and 13, comparable to MIS 5d and 5b within MIS 5. Please note that 5b (which was globally just a colder interval within MIS 5) saw one of the largest glaciations over northern Eurasia in the last 200 ky (Svendsen et al., 2004, QSR).

375: Since freshwater is buoyant, wouldn't it make more sense to say that the Arctic Ocean may have been filled with freshwater DOWN to 2500 m water depth? It certainly depends on the point of view, but I would understand "up to 2500 m" as the description of a bottom water mass.

451: Spielhagen

455: timescales???

470: Moreover, there were no large ice sheets on northern Eurasia during MIS 5c (Svendsen et al., 2004, QSR) to produce large amounts of brines.

519-521: This is correct. However, there is a recent paper (Rogge et al., 2022, https://doi.org/10.1038/s41561-022-01069-z) showing the formation of plumes which are sinking down to 1200 m even under modern conditions. During glaciations with (partly) ice-covered shelves and strong erosion, conditions allowing the formation of sediment-laden plumes may have occurred even more frequently than during interglacials. Since the Arctic deep-sea basins (>2500 m) are filled with fine-grained sediments (plumites, turbidites; see Goldstein, 1983, DOI: 10.1007/978-1-4613-3793-5_9; Svindland and Vorren, 2002, https://doi.org/10.1016/S0025-3227(02)00197-4), such plume formation may have been a major process for the vertical (and then horizontal) transport of both fines and low-d18O waters during glacials. Maybe the authors want to consider this possibility...

Figures: When figures consist of several "subfigures" (e.g., data panels), they are labeled A, B, C... In the text, they are referenced as a, b, c...

Citation: https://doi.org/10.5194/egusphere-2022-1212-RC1
- AC1: 'Reply on RC1', Jesse Farmer, 07 Feb 2023
  
  Please see responses to the Reviewer's comments in the attached PDF file. Note that the same PDF file includes responses both to RC1 and RC2, and the same file has been uploaded for the Reply to RC2.
  
  Citation: https://doi.org/10.5194/egusphere-2022-1212-AC1
CC1:
'Comment on egusphere-2022-1212', Claude Hillaire-Marcel, 05 Dec 2022

1) I see potential issues with the radiocarbon-based chronostratigraphy at sites with very low sedimentation rates (Lomonosov, Mendeleev, Alpha...) - see https://doi.org/10.1029/2022GL100446
2) The 600 ka-time frame used is similarly open to question; not only because of recent findings by Vernassen et al. (2021) mentioned in the text (see also https://doi.org/10.5194/gchron-2022-25.), but because several papers based on 230Th-excess data (e.g., https://doi.org/10.1002/2017GC007050 or https://doi.org/10.1038/s41586-021-03186-) invalidate it. An overview of these issues could be find in https://doi.org/10.1016/j.quascirev.2021.107239. Summer season insolation conditions were too low during MIS 11 for optimal conditions in the Arctic Ocean. The T. egelida peak (as well as the Bolivina aculeata interval) should both be reassigned to older isotopic stages than MIS 11 or MIS 5a, respectively..
Claude Hillaire-Marcel

Citation: https://doi.org/10.5194/egusphere-2022-1212-CC1
- AC3: 'Reply on CC1', Jesse Farmer, 07 Feb 2023
  
  We thank Claude Hillaire-Marcel for his Community Comment that raised deficiences with our age model presentation. Our responses to his two points are below:
  1) Radiocarbon-based chronostratigraphy issues. The ¹⁴C-based age models for the western Arctic cores have been independently verified by new nitrogen isotope measurements (δ¹⁵N) on N. pachyderma-bound organic matter on these same cores (Farmer et al., 2023). The δ¹⁵N results are not compatible with the results or interpretation of Hillaire-Marcel et al. (2022), for two reasons:
  a. MIS 2 foraminifera cannot be mixing between Holocene and MIS 3 populations. Hillaire-Marcel et al. (2022) argue that MIS 2 dates on N. pachyderma in their studied cores from the Lomonosov Ridge are artifacts of benthic mixing between MIS 3- and Holocene-aged populations. However, Farmer et al. (2023) showed that, in the western Arctic cores used in both their and this current study, N. pachyderma-bound δ¹⁵N data from MIS 2 are isotopically distinct (~5‰ vs. air) compared to N. pachyderma-bound d15N data from the Holocene (~8‰) or MIS 3 (~9‰). It is not possible to obtrain such low MIS 2 δ¹⁵N values by mixing MIS 3 and Holocene populations. Therefore, ¹⁴C ages on these same foraminifera cannot also be mixed.
  b. Old (>35 ¹⁴C kyr) ages appear reliable, and not diagenetic artifacts. Hillaire-Marcel et al. (2022) question whether ¹⁴C ages > 35 ¹⁴C kyr BP are reliable given observations of diagnetic alteration of foraminiferal calcite by Broecker et al. (2006) in opal-rich sediments. We note that this observation is of questionable relevance to the Arctic basin, where sediments are opal-poor (e.g., Schubert and Stein, 1996). However, Farmer et al. (2023) found a large N. pachyderma-bound δ¹⁵N decline at ~36 ka in three separate western Arctic cores; the date of this decline was contemporaneous within uncertainty of the ¹⁴C-based age models for these cores. This shows that older ¹⁴C dates do provide consistent and useful chronostratigraphic constraints and cannot simply be discounted.
  2) Questions concerning the 600 kyr time frame and the assigned ages to biostratigraphic datums. This is a fair point. Age models derived from ²³⁰Th excess extinction have certainly challenged the chronostratigraphic framework for Pleistocene sediments in the Arctic. However, they have not invalidated them. There remains significant disparities between these Th-based age models and those generated using known extinction and evolutionary appearances of calcareous nannofossils (Jakobsson et al., 2001; O'Regan et al., 2020), and MIS 5 age assignments derived from OSL dating of quartz grains (Jakobsson et al., 2003; West et al., 2021). We will further discuss the age models in Section 3.3.2, including incorporating the alternative ages for the biostratigraphic datums based on ²³⁰Th excess extinction. We will also update the abstract to note that the 600 kyr assignment is based on biostratigraphy and orbitally tuned age models.
  References:
  Broecker, W. et al., 2006, https://doi.org/10.1029/2005PA001212
  Farmer, J. et al., 2023, https://doi.org/10.1073/pnas.2206742119
  Hillaire-Marcel, C. et al., 2022, https://doi.org/10.1029/2022GL100446
  Jakobsson, M. et al., 2001, https://doi.org/10.1016/S0921-8181(01)00110-2
  Jakobsson, M. et al., 2003, https://doi.org/10.1029/2002GC000423
  O'Regan, M. et al., 2020, https://doi.org/10.1130/G47479.1
  Schubert, C.J., & Stein, R., 1996, https://doi.org/10.1016/0146-6380(96)00042-3.
  West, G., et al., 2021, https://doi.org/10.1016/j.quascirev.2021.107082.
  
  Citation: https://doi.org/10.5194/egusphere-2022-1212-AC3
RC2:
'Comment on egusphere-2022-1212', Kaustubh Thirumalai, 08 Dec 2022
Kaustubh Thirumalai, University of Arizona

I found this manuscript by Farmer and colleagues to be highly interesting. The authors attempt to reconstruct bottom water δ¹â¸Osw values in the Arctic using a combination of benthic foraminiferal δ¹â¸O measurements paired with ostracode Mg/Ca paleothermometry. Using Site 1123 (SW Pacific Ocean) bottom water δ¹â¸Osw as a reference record, they find that local Arctic δ¹â¸Osw (corrected for the influence of ice-volume-related changes in global oceanic δ¹â¸O) is lower than the modern difference between these records during glacial periods over the past 600 kyr. A major portion of the discussion in this manuscript focuses on refuting the “fresh glacial Arctic” hypothesis (Geibert et al. 2021) to explain the anomalously lower δ¹â¸Osw values in the glacial - which is compelling. The authors instead prefer a mechanism that involves “stratification breakdown” wherein relatively lower-δ¹â¸O upper ocean waters sink to the bottom due to relatively higher densities (via salinity) modulated by brine formation.

Overall this work is compelling, of interest to the broader community, and I feel that the manuscript will be eventually suitable for publication in Climate of the Past pending some revision. My major concerns regarding this version are two-fold: one centers around the discussion and proposed mechanism of brine-formation to explain relatively lower-δ¹â¸O in Arctic bottom-waters, and the other is a request to assist readers by providing more information on some of the details related to Mg/Ca paleothermometry and background information. I detail my major and minor suggestions to improve this work below:

Mechanisms and “low-δ¹â¸O” of brine versus “lower δ¹â¸O” of surface waters:

The authors refer to “low-δ¹â¸O” brines (Line 93), but the briny waters themselves are not anomalously lower in their δ¹â¸Osw values due to relatively low ice-water δ¹â¸O fractionation (see e.g. Yamamoto et al. 2001, 2002). Thus, I suggest expanding the text in the introduction to discuss how brine potentially affects bottom water δ¹â¸Osw by advecting relatively lower upper-ocean δ¹â¸Osw (Line 93 and thereafter).

I ask the authors to explore/discuss the work of Rasmussen and Thomsen (2009) who suggest that the initial thermohaline origin of brine formation can modulate their density and stable oxygen isotope composition. I recognize that the viewpoint from these authors on brine formation as a paleoceanographic driver has been updated since that paper (e.g. Rasmussen and Thomsen, 2014). However, their benthic δ¹â¸O values in a region of active brine formation in the Barents Sea appear similar (Figs. 2–3 in 2009 paper) to the relatively lower glacial values observed in this manuscript (e.g. Fig. 3A). Perhaps this can be used as support for brine-formation as a potential cause of the underlying data?

The authors also discount the possibility of reduced Atlantic water input during glacial stages. Although the records do not overlap entirely with the one presented in this manuscript, Ford and Raymo (2019) show that δ¹â¸Osw (not corrected for ice-volume) from ~400–600 ka at Sites 607 and 1208 in the North Atlantic and Pacific respectively are relatively similar to that at Site 1123 (Fig. 3 in their paper). Thus, perhaps the authors can use these records across the interval of overlap to more robustly assert that changes in inflow did not cause the anomalously low glacial δ¹â¸Osw in the Arctic Ocean (e.g. via a mixing model or relative differences between sites)? I recognize that their data points are fewer in this interval and that overlap is not complete, yet, I feel that this exercise would solidify their argument.

What is the driver of the stratification breakdown in the Arctic Ocean under glacial conditions? Presumably there was more perennial sea-ice coverage during glacial times, which could perhaps result in more year-round brine formation, but what would cause more mixing given that this would also likely reduce the impact of winds? Given that perennial Arctic sea-ice under pre-industrial conditions also covered a large extent of the basin, what changes during glacial times that cause radically different oceanic structure?

On this note, I wonder whether the “hyperpycnal flows” hypothesis of Stanford et al. (2011) might have a role to play here? Could intensified hyperpycnal flows related to runoff/melt in spring/summer coupled with more brine formation in the fall/winters be a viable way to reduce year-round δ¹â¸Osw in the water column? Stanford et al. (2011) also reject brine formation as a likely mechanism in the North Atlantic as there are different predictions for planktic versus benthic δ¹â¸O values. Considering this, I suggest the authors to expand their discussion section to include the implications of (not-yet-generated) planktic foraminiferal derived/surface-ocean δ¹â¸Osw in the Arctic and how it may help falsify/strengthen their hypothesis.

Discussion surrounding Mg/Ca and its uncertainty

The authors ought to provide more background information on ostracode Mg/Ca analysis and their underlying uncertainties. Although it is mentioned that a ‘Fisons Instrument Spectraspan atomic emissions spectrometer’ instrument was used (Lines 157–158), no details are provided about instrument precision, matrix/standard effects, external standard replicability, numbers of valves analyzed, what instaars were utilized, inter-sample variance etc. Although the authors cite previous studies that go more into detail on some of these aspects, I think that these details need to be in this manuscript, where the Mg/Ca data are front and central to the assertions. Accordingly, it is not clear how the “1sd” propagated error in Fig. 3A was constructed - was this propagated through a Monte Carlo procedure? It doesn’t seem like a constant “calibration” error of ±1°C (Line 164–165; Farmer et al. 2012) was employed. Thus, a clearer discussion of the procedures employed to propagate Mg/Ca uncertainties into the resultant BWT and δ¹â¸Osw records is needed.

Relatedly, there is no discussion about other trace metal values such as Mn/Ca, Fe/Ca, or Al/Ca in these measurements, which were presumably also measured alongside Mg/Ca for investigating clay contamination. To what extent are these parameters correlated or uncorrelated with the Mg/Ca data and what are the implications for sediment-based or post-depositional alteration?

Statistical robustness of Δδ¹â¸Osw reconstruction:

Although I am somewhat convinced looking at Fig. 4D that glacials generally have lower δ¹â¸Osw in the Arctic relative to Site 1123, I feel that this can be done in a more robust manner by compositing glacials and interglacials across the entire record - what is the average value (my apologies if I missed this in the text) of the difference in glacials versus interglacials? What is the impact of highly variable Δδ¹â¸Osw values in MIS 7, 11 and 13 interglacials on this average, as many of these anomalies appear to be equivalent or lower than the MIS 2–4 glacial values? Moreover, how robust is this average glacial-interglacial difference relative to the modern difference given the propagated uncertainty (see above point on Mg/Ca)? Although the 0.3–0.6 ‰ anomalies are likely significant, I wonder about smaller-magnitude anomalies…

Minor Points:

It would be helpful to label in the caption that Fig. 4C refers to δ¹â¸OL+IVC at both of the sites, right? If so, given that the record in Fig. 4D is constructed to be non-dependent on ice-volume/sea-level, I ask whether Fig. 4C is required at all? Moreover, this sub-plot is not cited/discussed explicitly in the text.

The authors provide information about the δ¹â¸O measurements - however, am I to understand correctly that this work only involved collating previously measured δ¹â¸O data? In that case, I would recommend adding “In these studies” before “Foraminifera were brush-picked,” on Line 140 and updating Line 148 to say “In these previous studies, all measurements were reported…” to clarify what has been done in this work versus previous studies.

Line 225: Although the average error and standard deviation was relatively low, I’d recommend providing an estimate of the overall ranges as well (Eqn. 3 estimates a of range from X to Y whereas Eqn. 4)

References:

Ford, H. L., & Raymo, M. E. (2019). Regional and global signals in seawater δ18O records across the mid-Pleistocene transition. Geology. https://doi.org/10.1130/g46546.1

Geibert, W., Matthiessen, J., Stimac, I., Wollenburg, J., & Stein, R. (2021). Glacial episodes of a freshwater Arctic Ocean covered by a thick ice shelf. Nature, 590(7844), 97–102. https://doi.org/10.1038/s41586–021–03186-y

Rasmussen, T. L., & Thomsen, E. (2009). Stable isotope signals from brines in the Barents Sea: Implications for brine formation during the last glaciation. Geology, 37(10), 903–906.

Rasmussen, T. L., & Thomsen, E. (2014). Brine formation in relation to climate changes and ice retreat during the last 15,000 years in Storfjorden, Svalbard, 76–78 N. Paleoceanography, 29(10), 911–929..

Stanford, J. D., Rohling, E. J., Bacon, S., Roberts, A. P., Grousset, F. E., & Bolshaw, M. (2011). A new concept for the paleoceanographic evolution of Heinrich event 1 in the North Atlantic. Quaternary Science Reviews, 30(9–10), 1047–1066.

Yamamoto, M., Tanaka, N., Tsunogai, S., 2001. The Okhotsk Sea intermediate water formation deduced from oxygen isotope systematics. Journal of Geophysical Research 106, 31075–31084.

Yamamoto, M., Watanabe, S., Tsunogai, S., & Wakatsuchi, M. (2002). Effects of sea ice formation and diapycnal mixing on the Okhotsk Sea intermediate water clarified with oxygen isotopes. Deep Sea Research Part I: Oceanographic Research Papers, 49(7), 1165–1174.
Citation: https://doi.org/10.5194/egusphere-2022-1212-RC2
- AC2: 'Reply on RC2', Jesse Farmer, 07 Feb 2023
  
  Please see responses to the Reviewer's comments in the attached PDF file. Note that the same PDF file includes responses both to RC1 and RC2, and the same file has been uploaded for the Reply to RC1.
  
  Citation: https://doi.org/10.5194/egusphere-2022-1212-AC2

Interactive discussion

Status: closed

RC1:
'Comment on egusphere-2022-1212', Robert F. Spielhagen, 01 Dec 2022

Farmer et al. present a collection of benthic oxygen isotope data from Arctic deep-sea sediment cores, derived from benthic foraminifers. The data are partly new, but several data sets have been published in the last decades. The authors use these data to calculate past seawater d180, taking into account past changes in global ice volume and bottom water temperature. For the latter they use Mg/Ca data, which are a reliable paleothermometer. The major result is that glacial periods of the last 600 kyr often saw significantly lower values of d18O at the sea floor than interglacials. The authors then discuss possible explanations for this observation and rule out that the Arctic Ocean was filled with freshwater during recent glacials, as proposed by Geibert et al. (2021, Nature). Instead they suggest intensive brine formation during glacials as a process which could have led to a downslope transport of dense, low-d18O waters.

The manuscript is written in excellent English; it is well structured and the figures are illustrative. I suggest to add a table with details on core numbers, geographical coordinates and water depths. This table may be added as a supplement. The reader should not be forced to look up all the core details in various papers. There are some vertical differences in temperature even in the deeper Arctic Ocean and since these difference may affect the d18O in carbonates, water depths of individual cores (e.g., those used for Fig. 2) are critical information (even though there is a temperature correction from Mg/Ca data in the d18O data sets).

Overall, I find this manuscript already in a very mature condition. The Abstract is informative, as is the Introduction which gives various aspects of background information. One or two sentences on the research question(s) tackled in this manuscript would be helpful for the reader to better understand what the authors are aiming at. The work performed is nicely described in the last paragraph of the Introduction, but I guess the authors started with a research question before they performed the data acquisition and collection.

The second chapter gives further background information on the various factors controlling oxygen isotopes in seawater and on the modern oceanographic situation in the Arctic Ocean. All necessary details are presented.

The chapter on Materials and Methods supplies details on the measurements performed, on the core chronology, and on the calculation of d18O of paleo-seawater. The subchapters give all necessary details in a concise manner. In particular I like the subchapter on chronology which clearly states some of the current problems with assigning definite ages to interglacial sediments older than 200 ka. Although the U/Th-based age model put forward by Hillaire-Marcel et al. (2017) is at odds with the "conventional" age model of, e.g., Jakobsson et al., 2000, Spielhagen et al., 2004; O'Regan et al., 2008, 2020, it should still be mentioned.

In the Discussion the authors argue that uncertainties with the chronology (including possible hiatuses like in the LGM) make it problematic to discuss individual periods with d18O minima beyond MIS 6. In the following subchapters they almost entirely concentrate an possible explanations for low glacial d18O of seawater and how these explanations can or cannot be reconciled with the Geibert et al. (2021) hypothesis. While I find the arguments sound and the debate highly interesting, I think the authors miss a chance to comment also on paleoenvironments in previous glaciations. I fully acknowledge that the authors want to be cautious with age assignments beyond MIS 6, but still they should discuss to some greater extent than at present the time back to MIS 15 for which they have collected a nice data set shown in Fig. 4. If they do not do this, one may ask why data from MIS 7-15 are shown at all and why d18O differences between individual stages and substages are laid out in detail in subchapter 4.2.

The debate on a possible "fresh glacial Arctic" explanation for the low glacial d18O of seawater makes up most of the Discussion chapter. I find the arguments given highly plausible, but I have to admit that I am somewhat biased against the Geibert et al. (2021) hypothesis, as demonstrated in our comment on that paper (Spielhagen et al., 2022, Nature). Nevertheless, I think that Farmer et al. have done a good job in collecting various other data speaking against a "fresh glacial Arctic" and discussing these in depth so that their own explanation for low glacial d18O data is left as the most plausible hypothesis.

This explanation is described in the last subchapter of the Discussion (5.2). The authors propose a weakened glacial stratification in the glacial oceans as the most likely cause for low d180 of intermediate to deep waters. They explicitly mention "enhanced vertical mixing" and "the transport of low-δ18Osw brines to intermediate depths". While the latter seems sufficiently clear, considering the previous discussion of eNd values in subchapter 5.1, there is no statement on what may have caused "enhanced vertical mixing" and how and where this may have happened in an ice-covered ocean. This needs be be made clear - otherwise it will remain a "black box" for the readers. I also suggest to include a figure (cartoon) showing the proposed scenario for brine formation.

The Conclusion chapter nicely summarizes the major findings discussed in the previous chapter. It ends with some comments on the suitability of benthic d18O data and ostracode Mg/Ca paleothermometry for future paleoclimate research in the Arctic. In my (not necessarily correct) opinion, the latter point should have been tackled with some pros and cons already in chapter 5 and not just as the last sentences of the manuscript.

Specific comments by line numbers

93: Actually, the isotopic change during the transition from sea water to sea ice is only very minor (fractionation factor ~1.003; https://doi.org/10.3189/S0022143000042751) and can be neglected when isotopic changes on glacial-interglacial scales are discussed. However, the d18O/salinity relation in ocean waters can be strongly affected. This can lead to density changes and the sinking of low-d18O near-surface waters to greater depths. Considering these details, the statement in line 93 is too much simplified.

109: What is "AL"?

124: color bar

144: analysis. Analyses

185-186: Since the default R is 550 yr in Marine20 (and was 402 yr in Marine13), it might be worth mentioning the R used in this study.

186: Blaauw (to be corrected also in the list of references!)

192: Bulimina aculeata

200: Lomonosov Ridge

282: A temperature of -0.3°C may be correct for intermediate waters (AIW), but deeper waters are colder (-0.9°C; see line 106).

284: Temperatures are numbers and cannot be "warmer", only higher. Check for other usage of "cooler" and "warmer" BWTs throughout the manuscript!

289-291: I suggest to discuss the differences going from 50 ka to present and not vice versa.

346 (and 437): I would regard 7b and 13b as interstadials within MIS 7 and 13, comparable to MIS 5d and 5b within MIS 5. Please note that 5b (which was globally just a colder interval within MIS 5) saw one of the largest glaciations over northern Eurasia in the last 200 ky (Svendsen et al., 2004, QSR).

375: Since freshwater is buoyant, wouldn't it make more sense to say that the Arctic Ocean may have been filled with freshwater DOWN to 2500 m water depth? It certainly depends on the point of view, but I would understand "up to 2500 m" as the description of a bottom water mass.

451: Spielhagen

455: timescales???

470: Moreover, there were no large ice sheets on northern Eurasia during MIS 5c (Svendsen et al., 2004, QSR) to produce large amounts of brines.

519-521: This is correct. However, there is a recent paper (Rogge et al., 2022, https://doi.org/10.1038/s41561-022-01069-z) showing the formation of plumes which are sinking down to 1200 m even under modern conditions. During glaciations with (partly) ice-covered shelves and strong erosion, conditions allowing the formation of sediment-laden plumes may have occurred even more frequently than during interglacials. Since the Arctic deep-sea basins (>2500 m) are filled with fine-grained sediments (plumites, turbidites; see Goldstein, 1983, DOI: 10.1007/978-1-4613-3793-5_9; Svindland and Vorren, 2002, https://doi.org/10.1016/S0025-3227(02)00197-4), such plume formation may have been a major process for the vertical (and then horizontal) transport of both fines and low-d18O waters during glacials. Maybe the authors want to consider this possibility...

Figures: When figures consist of several "subfigures" (e.g., data panels), they are labeled A, B, C... In the text, they are referenced as a, b, c...

Citation: https://doi.org/10.5194/egusphere-2022-1212-RC1
- AC1: 'Reply on RC1', Jesse Farmer, 07 Feb 2023
  
  Please see responses to the Reviewer's comments in the attached PDF file. Note that the same PDF file includes responses both to RC1 and RC2, and the same file has been uploaded for the Reply to RC2.
  
  Citation: https://doi.org/10.5194/egusphere-2022-1212-AC1
CC1:
'Comment on egusphere-2022-1212', Claude Hillaire-Marcel, 05 Dec 2022

1) I see potential issues with the radiocarbon-based chronostratigraphy at sites with very low sedimentation rates (Lomonosov, Mendeleev, Alpha...) - see https://doi.org/10.1029/2022GL100446
2) The 600 ka-time frame used is similarly open to question; not only because of recent findings by Vernassen et al. (2021) mentioned in the text (see also https://doi.org/10.5194/gchron-2022-25.), but because several papers based on 230Th-excess data (e.g., https://doi.org/10.1002/2017GC007050 or https://doi.org/10.1038/s41586-021-03186-) invalidate it. An overview of these issues could be find in https://doi.org/10.1016/j.quascirev.2021.107239. Summer season insolation conditions were too low during MIS 11 for optimal conditions in the Arctic Ocean. The T. egelida peak (as well as the Bolivina aculeata interval) should both be reassigned to older isotopic stages than MIS 11 or MIS 5a, respectively..
Claude Hillaire-Marcel

Citation: https://doi.org/10.5194/egusphere-2022-1212-CC1
- AC3: 'Reply on CC1', Jesse Farmer, 07 Feb 2023
  
  We thank Claude Hillaire-Marcel for his Community Comment that raised deficiences with our age model presentation. Our responses to his two points are below:
  1) Radiocarbon-based chronostratigraphy issues. The ¹⁴C-based age models for the western Arctic cores have been independently verified by new nitrogen isotope measurements (δ¹⁵N) on N. pachyderma-bound organic matter on these same cores (Farmer et al., 2023). The δ¹⁵N results are not compatible with the results or interpretation of Hillaire-Marcel et al. (2022), for two reasons:
  a. MIS 2 foraminifera cannot be mixing between Holocene and MIS 3 populations. Hillaire-Marcel et al. (2022) argue that MIS 2 dates on N. pachyderma in their studied cores from the Lomonosov Ridge are artifacts of benthic mixing between MIS 3- and Holocene-aged populations. However, Farmer et al. (2023) showed that, in the western Arctic cores used in both their and this current study, N. pachyderma-bound δ¹⁵N data from MIS 2 are isotopically distinct (~5‰ vs. air) compared to N. pachyderma-bound d15N data from the Holocene (~8‰) or MIS 3 (~9‰). It is not possible to obtrain such low MIS 2 δ¹⁵N values by mixing MIS 3 and Holocene populations. Therefore, ¹⁴C ages on these same foraminifera cannot also be mixed.
  b. Old (>35 ¹⁴C kyr) ages appear reliable, and not diagenetic artifacts. Hillaire-Marcel et al. (2022) question whether ¹⁴C ages > 35 ¹⁴C kyr BP are reliable given observations of diagnetic alteration of foraminiferal calcite by Broecker et al. (2006) in opal-rich sediments. We note that this observation is of questionable relevance to the Arctic basin, where sediments are opal-poor (e.g., Schubert and Stein, 1996). However, Farmer et al. (2023) found a large N. pachyderma-bound δ¹⁵N decline at ~36 ka in three separate western Arctic cores; the date of this decline was contemporaneous within uncertainty of the ¹⁴C-based age models for these cores. This shows that older ¹⁴C dates do provide consistent and useful chronostratigraphic constraints and cannot simply be discounted.
  2) Questions concerning the 600 kyr time frame and the assigned ages to biostratigraphic datums. This is a fair point. Age models derived from ²³⁰Th excess extinction have certainly challenged the chronostratigraphic framework for Pleistocene sediments in the Arctic. However, they have not invalidated them. There remains significant disparities between these Th-based age models and those generated using known extinction and evolutionary appearances of calcareous nannofossils (Jakobsson et al., 2001; O'Regan et al., 2020), and MIS 5 age assignments derived from OSL dating of quartz grains (Jakobsson et al., 2003; West et al., 2021). We will further discuss the age models in Section 3.3.2, including incorporating the alternative ages for the biostratigraphic datums based on ²³⁰Th excess extinction. We will also update the abstract to note that the 600 kyr assignment is based on biostratigraphy and orbitally tuned age models.
  References:
  Broecker, W. et al., 2006, https://doi.org/10.1029/2005PA001212
  Farmer, J. et al., 2023, https://doi.org/10.1073/pnas.2206742119
  Hillaire-Marcel, C. et al., 2022, https://doi.org/10.1029/2022GL100446
  Jakobsson, M. et al., 2001, https://doi.org/10.1016/S0921-8181(01)00110-2
  Jakobsson, M. et al., 2003, https://doi.org/10.1029/2002GC000423
  O'Regan, M. et al., 2020, https://doi.org/10.1130/G47479.1
  Schubert, C.J., & Stein, R., 1996, https://doi.org/10.1016/0146-6380(96)00042-3.
  West, G., et al., 2021, https://doi.org/10.1016/j.quascirev.2021.107082.
  
  Citation: https://doi.org/10.5194/egusphere-2022-1212-AC3
RC2:
'Comment on egusphere-2022-1212', Kaustubh Thirumalai, 08 Dec 2022
Kaustubh Thirumalai, University of Arizona

I found this manuscript by Farmer and colleagues to be highly interesting. The authors attempt to reconstruct bottom water δ¹â¸Osw values in the Arctic using a combination of benthic foraminiferal δ¹â¸O measurements paired with ostracode Mg/Ca paleothermometry. Using Site 1123 (SW Pacific Ocean) bottom water δ¹â¸Osw as a reference record, they find that local Arctic δ¹â¸Osw (corrected for the influence of ice-volume-related changes in global oceanic δ¹â¸O) is lower than the modern difference between these records during glacial periods over the past 600 kyr. A major portion of the discussion in this manuscript focuses on refuting the “fresh glacial Arctic” hypothesis (Geibert et al. 2021) to explain the anomalously lower δ¹â¸Osw values in the glacial - which is compelling. The authors instead prefer a mechanism that involves “stratification breakdown” wherein relatively lower-δ¹â¸O upper ocean waters sink to the bottom due to relatively higher densities (via salinity) modulated by brine formation.

Overall this work is compelling, of interest to the broader community, and I feel that the manuscript will be eventually suitable for publication in Climate of the Past pending some revision. My major concerns regarding this version are two-fold: one centers around the discussion and proposed mechanism of brine-formation to explain relatively lower-δ¹â¸O in Arctic bottom-waters, and the other is a request to assist readers by providing more information on some of the details related to Mg/Ca paleothermometry and background information. I detail my major and minor suggestions to improve this work below:

Mechanisms and “low-δ¹â¸O” of brine versus “lower δ¹â¸O” of surface waters:

The authors refer to “low-δ¹â¸O” brines (Line 93), but the briny waters themselves are not anomalously lower in their δ¹â¸Osw values due to relatively low ice-water δ¹â¸O fractionation (see e.g. Yamamoto et al. 2001, 2002). Thus, I suggest expanding the text in the introduction to discuss how brine potentially affects bottom water δ¹â¸Osw by advecting relatively lower upper-ocean δ¹â¸Osw (Line 93 and thereafter).

I ask the authors to explore/discuss the work of Rasmussen and Thomsen (2009) who suggest that the initial thermohaline origin of brine formation can modulate their density and stable oxygen isotope composition. I recognize that the viewpoint from these authors on brine formation as a paleoceanographic driver has been updated since that paper (e.g. Rasmussen and Thomsen, 2014). However, their benthic δ¹â¸O values in a region of active brine formation in the Barents Sea appear similar (Figs. 2–3 in 2009 paper) to the relatively lower glacial values observed in this manuscript (e.g. Fig. 3A). Perhaps this can be used as support for brine-formation as a potential cause of the underlying data?

The authors also discount the possibility of reduced Atlantic water input during glacial stages. Although the records do not overlap entirely with the one presented in this manuscript, Ford and Raymo (2019) show that δ¹â¸Osw (not corrected for ice-volume) from ~400–600 ka at Sites 607 and 1208 in the North Atlantic and Pacific respectively are relatively similar to that at Site 1123 (Fig. 3 in their paper). Thus, perhaps the authors can use these records across the interval of overlap to more robustly assert that changes in inflow did not cause the anomalously low glacial δ¹â¸Osw in the Arctic Ocean (e.g. via a mixing model or relative differences between sites)? I recognize that their data points are fewer in this interval and that overlap is not complete, yet, I feel that this exercise would solidify their argument.

What is the driver of the stratification breakdown in the Arctic Ocean under glacial conditions? Presumably there was more perennial sea-ice coverage during glacial times, which could perhaps result in more year-round brine formation, but what would cause more mixing given that this would also likely reduce the impact of winds? Given that perennial Arctic sea-ice under pre-industrial conditions also covered a large extent of the basin, what changes during glacial times that cause radically different oceanic structure?

On this note, I wonder whether the “hyperpycnal flows” hypothesis of Stanford et al. (2011) might have a role to play here? Could intensified hyperpycnal flows related to runoff/melt in spring/summer coupled with more brine formation in the fall/winters be a viable way to reduce year-round δ¹â¸Osw in the water column? Stanford et al. (2011) also reject brine formation as a likely mechanism in the North Atlantic as there are different predictions for planktic versus benthic δ¹â¸O values. Considering this, I suggest the authors to expand their discussion section to include the implications of (not-yet-generated) planktic foraminiferal derived/surface-ocean δ¹â¸Osw in the Arctic and how it may help falsify/strengthen their hypothesis.

Discussion surrounding Mg/Ca and its uncertainty

The authors ought to provide more background information on ostracode Mg/Ca analysis and their underlying uncertainties. Although it is mentioned that a ‘Fisons Instrument Spectraspan atomic emissions spectrometer’ instrument was used (Lines 157–158), no details are provided about instrument precision, matrix/standard effects, external standard replicability, numbers of valves analyzed, what instaars were utilized, inter-sample variance etc. Although the authors cite previous studies that go more into detail on some of these aspects, I think that these details need to be in this manuscript, where the Mg/Ca data are front and central to the assertions. Accordingly, it is not clear how the “1sd” propagated error in Fig. 3A was constructed - was this propagated through a Monte Carlo procedure? It doesn’t seem like a constant “calibration” error of ±1°C (Line 164–165; Farmer et al. 2012) was employed. Thus, a clearer discussion of the procedures employed to propagate Mg/Ca uncertainties into the resultant BWT and δ¹â¸Osw records is needed.

Relatedly, there is no discussion about other trace metal values such as Mn/Ca, Fe/Ca, or Al/Ca in these measurements, which were presumably also measured alongside Mg/Ca for investigating clay contamination. To what extent are these parameters correlated or uncorrelated with the Mg/Ca data and what are the implications for sediment-based or post-depositional alteration?

Statistical robustness of Δδ¹â¸Osw reconstruction:

Although I am somewhat convinced looking at Fig. 4D that glacials generally have lower δ¹â¸Osw in the Arctic relative to Site 1123, I feel that this can be done in a more robust manner by compositing glacials and interglacials across the entire record - what is the average value (my apologies if I missed this in the text) of the difference in glacials versus interglacials? What is the impact of highly variable Δδ¹â¸Osw values in MIS 7, 11 and 13 interglacials on this average, as many of these anomalies appear to be equivalent or lower than the MIS 2–4 glacial values? Moreover, how robust is this average glacial-interglacial difference relative to the modern difference given the propagated uncertainty (see above point on Mg/Ca)? Although the 0.3–0.6 ‰ anomalies are likely significant, I wonder about smaller-magnitude anomalies…

Minor Points:

It would be helpful to label in the caption that Fig. 4C refers to δ¹â¸OL+IVC at both of the sites, right? If so, given that the record in Fig. 4D is constructed to be non-dependent on ice-volume/sea-level, I ask whether Fig. 4C is required at all? Moreover, this sub-plot is not cited/discussed explicitly in the text.

The authors provide information about the δ¹â¸O measurements - however, am I to understand correctly that this work only involved collating previously measured δ¹â¸O data? In that case, I would recommend adding “In these studies” before “Foraminifera were brush-picked,” on Line 140 and updating Line 148 to say “In these previous studies, all measurements were reported…” to clarify what has been done in this work versus previous studies.

Line 225: Although the average error and standard deviation was relatively low, I’d recommend providing an estimate of the overall ranges as well (Eqn. 3 estimates a of range from X to Y whereas Eqn. 4)

References:

Ford, H. L., & Raymo, M. E. (2019). Regional and global signals in seawater δ18O records across the mid-Pleistocene transition. Geology. https://doi.org/10.1130/g46546.1

Geibert, W., Matthiessen, J., Stimac, I., Wollenburg, J., & Stein, R. (2021). Glacial episodes of a freshwater Arctic Ocean covered by a thick ice shelf. Nature, 590(7844), 97–102. https://doi.org/10.1038/s41586–021–03186-y

Rasmussen, T. L., & Thomsen, E. (2009). Stable isotope signals from brines in the Barents Sea: Implications for brine formation during the last glaciation. Geology, 37(10), 903–906.

Rasmussen, T. L., & Thomsen, E. (2014). Brine formation in relation to climate changes and ice retreat during the last 15,000 years in Storfjorden, Svalbard, 76–78 N. Paleoceanography, 29(10), 911–929..

Stanford, J. D., Rohling, E. J., Bacon, S., Roberts, A. P., Grousset, F. E., & Bolshaw, M. (2011). A new concept for the paleoceanographic evolution of Heinrich event 1 in the North Atlantic. Quaternary Science Reviews, 30(9–10), 1047–1066.

Yamamoto, M., Tanaka, N., Tsunogai, S., 2001. The Okhotsk Sea intermediate water formation deduced from oxygen isotope systematics. Journal of Geophysical Research 106, 31075–31084.

Yamamoto, M., Watanabe, S., Tsunogai, S., & Wakatsuchi, M. (2002). Effects of sea ice formation and diapycnal mixing on the Okhotsk Sea intermediate water clarified with oxygen isotopes. Deep Sea Research Part I: Oceanographic Research Papers, 49(7), 1165–1174.
Citation: https://doi.org/10.5194/egusphere-2022-1212-RC2
- AC2: 'Reply on RC2', Jesse Farmer, 07 Feb 2023
  
  Please see responses to the Reviewer's comments in the attached PDF file. Note that the same PDF file includes responses both to RC1 and RC2, and the same file has been uploaded for the Reply to RC1.
  
  Citation: https://doi.org/10.5194/egusphere-2022-1212-AC2

Peer review completion

AR: Author's response | RR: Referee report | ED: Editor decision | EF: Editorial file upload

ED: Publish as is (09 Feb 2023) by Gerald Ganssen

AR by Jesse Farmer on behalf of the Authors (18 Feb 2023) Author's response

Journal article(s) based on this preprint

14 Mar 2023

A 600 kyr reconstruction of deep Arctic seawater δ¹⁸O from benthic foraminiferal δ¹⁸O and ostracode Mg ∕ Ca paleothermometry

Jesse R. Farmer, Katherine J. Keller, Robert K. Poirier, Gary S. Dwyer, Morgan F. Schaller, Helen K. Coxall, Matt O'Regan, and Thomas M. Cronin

Clim. Past, 19, 555–578, https://doi.org/10.5194/cp-19-555-2023,https://doi.org/10.5194/cp-19-555-2023, 2023

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Jesse R. Farmer et al.

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Oxygen isotopes are used to date marine sediments via their similar large-scale ocean patterns over glacial cycles. However, the Arctic Ocean exhibits a different isotope pattern, creating uncertainty in the timing of past Arctic climate change. We find that the Arctic Ocean experienced large local oxygen isotope changes over glacial cycles. We attribute this to a breakdown of stratification during ice ages that allowed for a unique low isotope value to characterize the Arctic Ocean.


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