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REVIEW 3 major objections 5 minor 29 references

Noble gases in carbonate melts: constraints on the solubility and the surface tension by molecular dynamics simulation

T0 review · 3 major / 5 minor · reviewed 2026-08-14 · deepseek-v4-flash

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Pith's one-line read Carbonate melts dissolve noble gases no better than silicate melts at mantle pressures.

desk verdict First MD solubility data for noble gases in carbonate melts, with a pressure series to 6 GPa and surface tensions; the mantle-degassing takeaway is plausible but rests on an untested transferability assumption for the noble-gas force field. read the letter →

arxiv 1908.03745 v1 pith:DEPPXHGQ submitted 2019-08-10 physics.chem-ph physics.geo-ph

Elsa Desmaele , Nicolas Sator , Bertrand Guillot This is my paper · ORCID
classification physics.chem-phphysics.geo-ph
keywords noblegasescarbonatemeltssolubilitymoleculardynamicssimulationsurfacetensionmantlegeochemistrynatrocarbonatitemoltencarbonates
verification ladder T0 review T1 audit T2 compute T3 formal

The pith

A machine-rendered reading of the paper's core claim, the machinery that carries it, and where it could break.

The reading

With molecular dynamics simulations, this paper computes how much helium, neon, argon, and xenon dissolve in molten carbonates from 1 bar to 6 GPa. The central result is that at mantle pressures the solubilities remain in the same 1-10 mol% range as in molten silicates. The authors take this to mean that carbonatitic melts at depth are not preferential carriers of noble gases, a conclusion that matters because noble gas isotope ratios are the main tracers of mantle degassing. The paper also finds that the surface tension at the melt/noble-gas interface roughly doubles when pressure rises to 6 GPa, opposite to the behavior of hydrous silicate melts.

What carries the argument

The calculation rests on two complementary simulation routes. In the test-particle method, a ghost noble-gas atom is inserted many times into equilibrated melt configurations; the averaged Boltzmann factor of its insertion energy gives the excess chemical potential, and from it the Henry constant at low pressure. In the explicit interface method, a slab of melt is put in contact with a noble-gas reservoir and the saturated concentration is read off the density profile; this works at high pressure. Both methods rely on a force field whose key ingredient is a set of Lennard-Jones parameters for noble-gas interactions with cations and oxygens, transferred from earlier silicate-melt work under the assumption of melt-to-melt transferability, with noble-gas interactions with carbon atoms set to zero because carbon is screened by surrounding oxygens.

What would settle it

A diamond-anvil cell measurement of He or Ar solubility in a Ca-Mg carbonate melt at 3 to 6 GPa and 1600-1700 K would settle the claim: if the measured mol fractions deviate from the 1-10 mol% range, or if He keeps rising instead of passing through a maximum near 2 GPa, the transferred force field fails.

Watch

Extended reading notes

Core claim

Starting from a force field validated on carbonate melt thermodynamics and on noble-gas solubility in silicate melts, the study computes solubilities in K2CO3-CaCO3 mixtures at 1 bar and reproduces the measured values once the known helium-loss problem of the experiments is taken into account. Under pressure, the solubility in natrocarbonatite follows Henry's law only up to about 0.1 GPa; above one GPa it levels off, with helium passing through a maximum near 2 GPa and argon near 4 GPa. In molten dolomite the solubility is nearly independent of pressure between 3 and 6 GPa. The result is that all four gases dissolve in carbonate melts at mantle conditions at concentrations comparable to those in silicates, so carbonatitic melts are not enriched in noble gases relative to coexisting mantle melts. The surface tension between carbonate melt and noble-gas fluid increases by about a factor of two as pressure goes from 0 to 6 GPa, independent of melt and gas composition.

Load-bearing premise

Everything at high pressure depends on the idea that Lennard-Jones parameters fitted to noble-gas interactions with silicate melts describe noble-gas atoms in carbonate melts just as well, and that noble-gas/carbon interactions can be ignored; only a 1-bar comparison for K2CO3-CaCO3 mixtures checks that transfer.

Editorial extensions

If this is right

  • Carbonatitic melts at depth will not fractionate noble gases strongly from silicate melts, so noble gas abundances in such melts should track the coexisting silicate melt; the composition dependence, roughly a factor of three for argon, still requires case-by-case evaluation.
  • Low-pressure Henry's law cannot be extrapolated to mantle pressures: in natrocarbonatite the linear regime stops near 0.1 GPa, and extrapolating to several GPa would overestimate the helium and argon contents by a factor of several.
  • The pressure-driven doubling of surface tension at carbonate melt/noble-gas interfaces will affect bubble nucleation, growth, and coalescence in carbonatite magmas, in the opposite direction to hydrous silicate melts where water lowers surface tension.
  • Melt composition controls solubility as much as pressure: K-rich carbonate melts dissolve an order of magnitude more helium than pure CaCO3 at 1 bar, and natrocarbonatite holds more noble gas than dolomite at all studied pressures.

Reading between the lines

Editorial extensions of the paper, not claims the author makes directly.

  • If carbonate melts are not noble-gas carriers, then noble gas budgets of deep Earth carbon reservoirs may be carried by silicate melts or fluids instead, making carbonatites effectively invisible to helium and argon isotope tracers.
  • The predicted crossover at high pressure, where He and Ne converge and Xe approaches Ar, could serve as a barometer for the depth at which a carbonatite magma trapped its gas, if confirmed by experiment.
  • A targeted ab initio simulation of one noble gas in natrocarbonatite would test whether neglecting noble-gas/carbon interactions and electronic polarization shifts the mantle-pressure solubilities by more than the reported error bars.
  • The same interfacial method could be applied to CO2 in carbonate melts; since CO2 is the actual mantle volatile and is much more abundant than noble gases, its surface tension behavior would directly affect carbonatite degassing models.
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Editorial analysis

A structured set of objections, weighed in public.

Desk editor's note, referee report, and a circularity audit.

Referee Report

3 major / 5 minor

Summary. The manuscript reports molecular dynamics simulations of the solubility of He, Ne, Ar, and Xe in carbonate melts, using a force field previously developed for carbonate melts and Lennard-Jones parameters for noble-gas interactions that were fitted for silicate and CO2-bearing silicate melts. Solubilities are computed by the Test Particle Method at low pressure and by an Explicit Interface Method at high pressure, with a comparison to the only available experimental data (Burnard et al., 2010) for K2CO3-CaCO3 mixtures at 1 bar. The authors then extend the calculations to natrocarbonatite at 1600 K and dolomite at 1673 K up to 6 GPa, finding that noble-gas solubilities are of the same order of magnitude as in molten silicates at mantle pressures, which suggests that carbonatitic melts are not preferential carriers of noble gases. The paper also reports the pressure evolution of the melt/noble-gas surface tension, which increases with pressure for all compositions and gases.

Significance. If the results hold, this is the first quantitative simulation-based estimate of noble-gas solubilities in carbonate melts at mantle pressures, filling a gap where experimental data are sparse. The finding that carbonatitic melts do not strongly fractionate noble gases relative to silicates is geochemically relevant for interpreting noble-gas systematics in carbonatite-sourced magmas. The paper benefits from standard, well-established methods (TPM and EIM) with convergence checks (Fig. B.2) and explicit error bars, and it transparently states the transferability assumption. However, the validation against experiment is partial: helium data are lower limits, and no quantitative comparison is given for argon. The central mantle-pressure conclusion therefore rests on a force-field transferability that is only weakly constrained.

major comments (3)
  1. [Section II.A and Section III.A, Fig. 2] The a posteriori justification of force-field transferability is weaker than presented. The paper states in Section II.A that the NG-melt interactions are assumed transferable and 'justified a posteriori' by agreement with Burnard et al. However, as acknowledged in Section III.A, the experimental helium data are lower limits because of gas loss during quenching; agreement with these data only establishes that the simulated He solubility is greater than or equal to the measured values, not that the force field is accurate. For argon, no numerical comparison is tabulated, only a qualitative statement of better agreement. Since the high-pressure predictions in Section III.B and the conclusion about non-preferential noble-gas transport rest entirely on this transferability, the validation is insufficient. I recommend adding a quantitative comparison for Ar (and, where possible, Ne and Xe if experimental data exist) and performing a sensitivity test in which the NG-O and NG-cation Lennard-Jones parameters are scaled by a plausible factor (e.g., ±10% in epsilon or sigma) to show that the mantle-pressure conclusion (order-of-magnitude similarity to silicates) is robust.
  2. [Section III.B vs. Table C.1 and Table C.2] There is a temperature inconsistency for the dolomite melt. The main text (Section III.B) and the caption of Fig. 3 state 1673 K for dolomite, but the appendix tables (Table C.1 and Table C.2) report dolomite at 1623 K. This discrepancy must be resolved because the reported solubility and surface-tension values depend on the actual thermodynamic state. Please correct the inconsistency and state clearly which temperature was used in the simulations.
  3. [Section II.A and Table A.3] The neglect of NG-carbon interactions, justified by the screening of carbon by oxygen, is plausible for large noble gases but is not tested for helium. Helium is small enough to approach the central carbon atom of the carbonate ion, and the experimental He data are lower limits, so they cannot validate this choice for He. The paper's prediction of a helium solubility maximum near 2 GPa in natrocarbonatite (Fig. 3) could be sensitive to this approximation. A concrete test would be to compute He solubility with a non-zero NG-C interaction (or a repulsive potential) and quantify the change in the predicted solubility and its pressure dependence.
minor comments (5)
  1. [Section III.A] The text says 'K2CO3–Na2CO3 mixtures' but the studied system and Fig. 2 caption refer to K2CO3–CaCO3 mixtures; this appears to be a typo and should be corrected.
  2. [Table B.1] For xK2CO3 = 0, the reported Xe solubility parameter is 0.059 ± 0.05, with an uncertainty nearly equal to the value itself. Please check this entry; it may be a typographical error or an indication that the TPM calculation is poorly converged for Xe in pure CaCO3.
  3. [Fig. 2] The axis label 'X (10□4 mol%)' is unclear because of the missing superscript and ambiguous multiplier. Please specify the units explicitly, e.g., 'molar fraction (10^-4 mol%)' or use mole fraction directly, to avoid confusion.
  4. [Section IV] The abstract and conclusion state that the surface tension increases 'by a factor ~2' from 0 to 6 GPa. From Fig. 4 and Table C.2, the increase is closer to a factor of about 1.5 to 1.8 for most gas/melt pairs (e.g., 206 to 363 mN/m for He in natrocarbonatite). Please adjust the wording to reflect the actual range.
  5. [Conclusion] The connection between the calculated solubility ratio and the 4He/40Ar ratio measured at Ol Doinyo Lengai (Fischer et al., 2009) is stated without quantitative elaboration. A brief explanation of how the solubility results translate into a predicted He/Ar fractionation would make the geochemical argument more transparent.

Circularity Check

0 steps flagged · score 0.0 of 10

No significant circularity: prior force-field parameters are independent inputs, and the low-pressure benchmark is external.

full rationale

The derivation chain is force field -> MD simulation -> solubility/surface tension -> geochemical conclusion. The NG-melt Lennard-Jones parameters are taken from prior papers by the same group (Guillot and Sator 2012; Aubry et al. 2013), where they were calibrated for silicate and CO2-bearing silicate systems; they are not fitted to the carbonate solubility data reported here. The solubility is computed via the standard Widom test-particle method, Eqs. (1)-(4), without any parameter adjustment to the target results. The only in-paper empirical check is the comparison with Burnard et al.'s 1-bar K2CO3-CaCO3 measurements, which is an independent external dataset. The paper explicitly states that the transferability of the potentials is an assumption justified a posteriori, and it acknowledges that the He data are lower limits. That makes the high-pressure predictions dependent on an unverified assumption, but it is a modeling limitation rather than a circular reduction of output to input. The conclusion that carbonate and silicate solubilities are of the same order of magnitude is a computed outcome of the simulation, not an identity forced by the choice of parameters. No equation is defined in terms of the result, no fitted parameter is renamed as a prediction, and no uniqueness theorem is imported from the authors' prior work. Therefore no significant circularity is present.

Assumptions & free parameters 4 free parameters · 4 assumptions · 0 invented entities

The central claim rests on an empirical force field with parameters fitted to other systems in prior publications. No new parameters are fitted in this paper. The transferability assumption is explicitly stated and only partially validated. The invented_entities list is empty because no new physical entities are postulated.

free parameters (4)
  • NG-cation Lennard-Jones parameters (epsilon, sigma) for Mg, Ca, Na, K = Table A.3 (e.g. He-Mg epsilon=1.554 kJ/mol, sigma=2.076 A)
    Taken from Guillot and Sator (2012) fits to noble gas solubility in silicate melts. Central claim depends on transferability of these values to carbonate melts.
  • NG-oxygen Lennard-Jones parameters (epsilon, sigma) = Table A.3 (He-O epsilon=0.525 kJ/mol, sigma=2.81 A)
    From Aubry et al. (2013), fitted for silicate+CO2+NG systems. Applied here to carbonate oxygens.
  • Carbonate melt force field (Buckingham A, rho, C, partial charges) = Table A.2 (e.g. Mg-O A=243000 kJ/mol, rho=0.24335 A, C=1439 A^6/mol, qMg=+1.64202 e)
    Fitted in Desmaele et al. (2019) to reproduce thermodynamics and transport of carbonate melts. The solubility calculation depends on the melt structure it produces.
  • NG-NG Buckingham parameters = Table A.1 (He A=132917 kJ/mol, rho=0.2051 A, C=109.84 A^6/mol)
    Adjusted to Tang-Toennies ab initio potentials by Guillot and Sator (2012). Used to model the noble gas vapor phase.
assumptions (4)
  • domain assumption The NG-melt interaction potentials from silicate and CO2-bearing silicate systems are transferable to carbonate melts.
    Stated in Section II A, justified a posteriori by agreement with Burnard et al. data.
  • domain assumption The carbon atom in carbonate is fully screened by its surrounding oxygens, so NG-carbon interactions can be set to zero.
    Section II A states the carbon is 'deeply embedded into the oxygen electronic clouds'.
  • domain assumption Classical molecular dynamics with empirical pairwise potentials accurately captures solubility thermodynamics at mantle pressures.
    The entire method relies on this; no quantum or polarizable corrections are considered.
  • domain assumption NVE production runs of 10 ns with the stated equilibration are sufficient to converge solubility and surface tension averages.
    Convergence is shown for TPM in Fig. B.2 and for surface tension in Fig. C.1.

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Cite this review

Pith. "Pith review of Noble gases in carbonate melts: constraints on the solubility and the surface tension by molecular dynamics simulation." pith.science (2026). https://pith.science/paper/DEPPXHGQ

@misc{pith2026190803745,
  author       = {Pith},
  title        = {Pith review of: Noble gases in carbonate melts: constraints on the solubility and the surface tension by molecular dynamics simulation},
  year         = {2026},
  howpublished = {\url{https://pith.science/paper/DEPPXHGQ}},
  note         = {Machine review of arXiv:1908.03745}
}
read the original abstract

Although they are rare elements in the Earth's mantle, noble gases (NG) owe to their strongly varying masses contrasting physical behaviors making them important geochemical tracers. When partial melting occurs at depth, the partitioning of NGs between phases is controlled by a distribution coefficient that can be determined from the solubility of the NGs in each phase. Here we report quantitative calculations of the solubility of He, Ne, Ar and Xe in carbonate melts based on molecular dynamics simulations. The NG solubilities are first calculated in K2CO3-CaCO3 mixtures at 1 bar and favorably compared to the only experimental data available to date. Then we investigate the effect of pressure (up to 6 GPa), focusing on two melt compositions: a dolomitic one and a natrocarbonatitic one (modeling the lava of Ol Doinyo Lengai). The solubility decreases with the amount of alkaline-earth cation in the melt and with the size of the noble gas. In the natrocarbonatitic melt, Henry's law is fulfilled at low pressures (up to ~ 0.1 GPa). At higher pressures the solubility levels off or even starts to diminish smoothly. In contrast, in molten dolomite the effect of pressure is negligible on the studied P range (3-6 GPa). At the pressures of the Earth's mantle, the solubilities of noble gases in carbonate melts are still of the same order of magnitude as the ones in molten silicates (~ 1-10 mol%). This suggests that carbonatitic melts at depth are not preferential carriers of noble gases, even if the dependence with the melt composition is not negligible and has to be evaluated on a case-by-case basis. Finally we evaluate the surface tension at the interface between carbonate melts and noble gases and its evolution with pressure. Whatever the composition of the melt and of the NG phase, the surface tension increases when P increases from 0 to 6 GPa.

Figures

Figures reproduced from arXiv: 1908.03745 by the authors.

Figure 1
Figure 1. FIG. 1. Determination of the solubility of a noble gas (e.g. [PITH_FULL_IMAGE:figures/full_fig_p002_1.png] view at source ↗
Figure 3
Figure 3. FIG. 3. Solubity of He, Ne, Ar and Xe (in molar fraction) [PITH_FULL_IMAGE:figures/full_fig_p004_3.png] view at source ↗
Figure 4
Figure 4. FIG. 4. Pressure evolution of the surface tension between a [PITH_FULL_IMAGE:figures/full_fig_p005_4.png] view at source ↗

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