the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
A wind-driven snow redistribution module for Alpine3D v3.3.0: Adaptations designed for downscaling ice sheet surface mass balance
Nander Wever
Jan T. M. Lenaerts
Brooke Medley
Abstract. Ice sheets gain mass via snow accumulation at the ice sheet surface, which is the primary component of surface mass balance. On the Antarctic ice sheet, winds redistribute snow resulting in surface mass balance that is variable in both space and time. Representing wind-driven snow redistribution processes in models is critical for local assessments of surface mass balance, repeat altimetry studies, and interpretation of ice core accumulation records. To this end, we have adapted Alpine3D, an existing distributed snow modeling framework, to downscale Antarctic surface mass balance to horizontal resolutions up to 1 km. In particular, we have introduced a new two-dimensional advection-based wind-driven snow redistribution module that is driven by an offline coupling between WindNinja, a wind downscaling model, and Alpine3D. We then show that large accumulation variability can be at least partially explained by terrain-induced wind speed variations which subsequently redistribute snow around rolling topography. By comparing Alpine3D to airborne-derived snow accumulation measurements within a testing domain over Pine Island Glacier in West Antarctica, we demonstrate that our Alpine3D downscaling approach improves surface mass balance estimates when compared to MERRA-2, a global atmospheric reanalysis which we use as atmospheric forcing. In particular, when compared to MERRA-2, Alpine3D reduces simulated surface mass balance root mean squared error by 23.4 mm w.e. yr-1 (13 %) and increases variance explained by 24 %. Despite these improvements, Alpine3D still underestimates observed accumulation variability, thus providing an opportunity for future model improvement.
Eric Keenan et al.
Status: final response (author comments only)
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RC1: 'Comment on gmd-2022-28', Anonymous Referee #1, 10 May 2022
General comments:
The article "A wind-driven snow redistribution module for Alpine3D v3.3.0: Adaptations designed for downscaling ice sheet surface mass balance" presents a strategy for downscaling large scale surface mass balance (SMB) predictions using Alpine3D. Alpine3D is a 3-D model that computes the mass and energy balances of snow covered regions by solving the 1-D snow model SNOWPACK at each grid cell. In the proposed methodology, the meteorological conditions are extracted from MERRA-2 and downscaled to the Alpine3D grid. In addition, snow drift events are modeled with a new 2-D advection scheme that takes into account a parameterization for the mass flux in saltation previously implemented in SNOWPACK. In order to correctly estimate snow drift, high resolution wind fields are needed. They are computed offline with the software WindNinja, which takes into account the small scale topographic features through a digital elevation model (DEM). The proposed approach has the potential to improve our understanding of SMB variability at small scales and can easily be applied to other locations. Even though the snow drift model needs further improvement, the coupling of MERRA-2 outputs, WindNinja wind fields and a snow drift scheme with Alpine3D has significant scientific value. In addition, from the comparison between Alpine3D and the measured annual-averaged snow accumulation over a 130 km transect, the authors show the importance of wind redistribution of snow to the local SMB. However, I think the manuscript can be improved, both from a strategic and scientific points of view. Besides the scientific comments presented below I have one general comment:
1) The article risks promising more than it gives regarding the snow drift model. Emphasis is given to snow drift in the title, in the abstract and in the introduction. However, even though the treatment of erosion and deposition presented in section 2.4 can be considered new, it is highly dependent on the parameterizations for the fluid threshold friction velocity and the mass flux in saltation (eqs. 3 and 4). In particular, it is shown and stated by the authors that equation 4 is highly uncertain, as it relies on a poorly constrained parameter. These equations are standard in SNOWPACK and no improvement is suggested by the authors. In addition, it is not clearly stated why this snow drift model is better than the one previously implemented in Alpine3D (Lehning et al. 2006). In this way, I would suggest counter-balancing the focus on the snow drift model with an extended description of the peripheral developments that are of the utmost importance for a successful downscaling: the downscaling of MERRA-2 meteorological forcing to the Alpine3D grid, the use of WindNinja with the ICESat-2 DEM, and the coupling of WindNinja to Alpine3D. In my view, the technical details of these contributions are of interest to the users of Alpine3D or other models alike. In addition, it is aligned with the scope of the GMD journal.
Specific comments:
l.13-14: Taking into account the focus that is given in the Conclusions regarding the effect of the parameter L, I suggest moving the focus in this sentence from the underestimation of SMB variability to the sensitivity of the snow accumulation patterns to the saltation model employed.
l.19-21: The terms drifting and blowing snow are used both to define the processes of aeolion snow transport and the particles aloft. This paragraph focuses on processes (precipitation, sublimation, etc). Hence, I suggest rephrasing so that drifting and blowing snow are presented as processes. An example is provided to clarify the comment made: "Additionally, local SMB is influenced by wind redistribution of snow. This process is generally defined as drifitng snow (when the snow particles are transported by the wind in the first 2 m above the snow surface) or blowing snow (when the snow particles are transported by the wind at greater heights - above 2 m height). We refer to deposition when drifting and blowing snow lead to net mass gain and to erosion when they lead to mass loss."
l.34-35: More recent works can be cited describing the effect of interparticle cohesion not only on the fluid threshold but in the whole saltation dynamics (e.g. Comola et al. 2019, Melo et al. 2022).
l.39: I suggest citing also the early work of Schmidt (1980) on the impact of interparticle ice bonds on the fluid threshold.
l.42: The work of Amory et al. (2021) can also be cited here - a parameterization for drifting snow compaction is also proposed in their work.
l.85-86: Is this a standard assumption? Maybe the authors can clarify its validity.
l.121: Even though Φ has units of mass flux (kg/m2/s), it can only be considered a mass flux if the mass rate of saltating particles per unit width, Q (kg/m/s), is assumed to be deposited along a fetch of L meters long. From my point of view, only in this way it makes sense to describe Φ as the mass rate of particles "crossing" the section Ly times Lx, where Ly is the width and Lx is the fetch length L. Is this the meaning of L? Even though this parameter is not well constrained, I think an effort should be made to better define it.
l.124 (eq.4): The numerator of this equation corresponds to the expression proposed by Sørensen (1991) for the transport rate (see page 75 of the article, eq. 3.22). This expression is in units of g/cm/s (this is stated at the end of page 72 of the article, below equation 3.9). This poses a problem because the coefficients 0.0014 and 205 are not dimensionless values - 205 has velocity units (cm/s) and 0.0014 has units of s2/cm. If we want to express Q in units of kg/m/s, these factors should change to 2.05 and 0.14, respectively. The dimensionally correct expression predicts much higher values of Q and its validity to model snow saltation is still to be assessed. This issue with the Sørensen's expression was previously pointed out in the PhD thesis of Vionnet (2012), page 103, Fig. 5.3 (french only). In the mentioned PhD thesis as well as in Vionnet et al. (2014), the use of the latest expression of Sørensen (2004) is proposed. This can be a good option for Alpine3D as it does not deviate significantly from the dimensionally wrong Sørensen equation (see Fig.5.3 in the PhD thesis). Independently of the approach chosen by the authors, I believe it is advisable to present Q - the numerator of eq.4 - in a separate equation and cite the respective article.
l.131-132 (point 1): The wind field at multiple vertical levels cannot be computed with WindNinja?
l.133-134 (point 3): This is not advisable at high wind speeds because the aeolian transport of snow stops being governed by the wind field close to the ground alone. In addition, the saltaion velocity considered in eq.7 would have to be revised (it describes saltation only as suspended particles are expected to have velocities comparable to the wind speed).
l.144 (eq.6): I believe the variable us should be defined in a more clear way: does it represent the particles speed or the wind speed in the saltation layer? Pomeroy and Gray (1990) proposed 2.8u*th as the average particle speed inside the saltation layer. However, if eq.6 is a mass conservation equation, where the quantity Ms is being advected by the flow, us should represent the wind speed. The wind speed in the saltation layer must be higher than the particles speed so that the particles are continuously accelerated. Do the authors consider these two quantities to be equal so that the mass in saltation is considered a passive scalar?
l.175-176: It is not clear if Alpine3D is ran for some time before the time period of interest in order to improve the initial state of the firn column. I suggest making it clear in the text.
l.191: Please specify over what years was the annual average performed.
l.190-195: Can the authors say something about the uncertainty/accuracy of the snow accumulation predictions derived from the firn thickness?
Fig.4 and 5: The observations signal (red line) seems the same in Figures 4c and 5c. However, the simulations correspond to different time periods (2015 only vs 2015-2020). Is the observation signal indeed the same? If yes, to what time period does it correspond?
l.225: The authors assume R-squared to be a proxy of the variance explained. As this is not accurate for all distributions, I suggest the authors to justify this assumption.
l.245: Is the discrepancy between the Alpine3D and the MERRA-2 transect results completely explained by snow being drifted from the analysis domain to the 15km border? It is not clear why the comparison between Alpine3D and MERRA-2 along the whole analysis domain is directly related to the comparison between these two models along the transect.
l.255-256: In the manuscript, surface mass balance variability is completely attributed to snow redistribution. Even though it is well known that snow redistribution plays an important role, it would be interesting to compare the outputs of the Alpine3D downscaling with and without the snow drift model. This would isolate the effect of snow redistribution from the effect of spatially varying heat fluxes.
l.265: It would be interesting if the authors could present how the process of wind-driven compaction is modeled in Alpine3D. For example, are the properties of deposited snow prescribed? Or do they depend on the properties of the previously eroded snow?
l.317: The definition of SMB is not very clear in the Conclusions. The definition presented in the Introduction is more accurate. Please consider rephrasing.
Technical corrections:
l.44: The word "recent" is doubled.
l.64-67: I suggest referring to the respective sections as in lines 60-64.
l.69: I suggest revising the need for section 2.1. The content of this section is mainly an introductory paragraph of section 2. Hence, it can be included below the title "Methods" without the need for a new subsection.
Figure 1: It would be interesting to add the remaining applications to the scheme (e.g. MeteoIO, WindNinja, ICESat-2, MERRA-2).
l.91: Consider replacing "off" by "on".
l.100: Consider replacing "cheaper" by "computationally lighter".
l.120: Consider replacing "layers" by "snow layers".
l. 135: Taking into account that Alpine3D is more than a wind redistribution module, this title might mislead the reader. Consider removing "Alpine3D:".
l.165: I suggest considering the option of moving subsections 2.5-2.7 to a new section. It can be called "Case Study", for example.
l.184: Even though the meaning of "efficiency" is clear in the text, please keep in mind that it has a specific meaning in high performance computing (see parallel efficiency).
l.184: I suggest writing all numbers in a consistent way: either delete the comma in number 27126 (l.182) or add it in number 1130 (1,130).
l.185 and 187: Taking into account that Alpine3D includes SNOWPACK, I believe it is not vary precise to talk about "SNOWPACK and Alpine3D" in this context. Consider replacing by Alpine3D only.
l.187: Considering replacing "cheaper". What about "computationally less expensive"?
l.232: The word "decreasing" is misspelled.
l.243: It is not very clear what is the "2015-2020 period" and the "long term average". Please consider rephrasing.
l.268: Is it R or R-squared?
l.339: Consider adding "that" after "shown".
l.347-348: Did the authors consider adding the model to the gitlab of Alpine3D?
References (only those not present in the manuscript):
Comola, F., Gaume, J., Kok, J. F., & Lehning, M. (2019). Cohesion-induced enhancement of aeolian saltation. Geophysical Research Letters, 46, 5566–5574. https://doi.org/10.1029/2019gl082195
Melo, D. B., Sharma, V., Comola, F., Sigmund, A., & Lehning, M. (2022). Modeling snow saltation: The effect of grain size and interparticle cohesion. Journal of Geophysical Research: Atmospheres, 127, e2021JD035260. https://doi.org/10.1029/2021JD035260
Schmidt, R. A. (1980). Threshold wind-speeds and elastic impact in snow transport. Journal of Glaciology, 26(94), 453–467. https://doi.org/10.1017/s0022143000010972
Sørensen, M. (1991). An analytic model of wind-blown sand transport. In O. E. Barndorff-Nielsen, & B. B. Willetts (Eds.), Aeolian grain transport 1 (pp. 67–81). Springer Vienna.
Sørensen, M. (2004). On the rate of aeolian sand transport. Geomorphology, 59(1), 53–62.
Vionnet, V. (2012). Etudes du transport de la neige par le vent en conditions alpines: observations et simulation à l’aide d’un modèle couplé atmosphère/manteau neigeux. Ph.D. thesis, Sciences et Techniques de l’Envitonnement, Université Paris-Est, France, http://tel.archives-ouvertes.fr/tel-00781279
Vionnet, V., Martin, E., Masson, V., Guyomarc’h, G., Naaim-Bouvet, F., Prokop, A., et al. (2014). Simulation of wind-induced snow transport and sublimation in alpine terrain using a fully coupled snowpack/atmosphere model. The Cryosphere, 8(2), 395–415. https://doi.org/10.5194/tc-8-395-2014
Citation: https://doi.org/10.5194/gmd-2022-28-RC1 -
RC2: 'Comment on gmd-2022-28', Charles Amory, 16 May 2022
General comments
This paper describes a new computational chain for downscaling the surface mass balance (SMB) over ice sheets, by combining the snowpack model SNOWPACK driven by MERRA2 reanalysis with an offline coupling between the wind downscaling model WindNinja and the wind redistribution model Alpine3D. This numerical design, while maintaining attractive computational costs, provides promising results by partially resolving the spatial variability in SMB due to wind redistribution of snow along a 130-km long transect in West Antarctica along which radar-derived SMB retrievals are available. Sensitivity to horizontal resolution and to a prescribed, yet influential parameter not constrained by observations, is explored. The proposed method is innovative and clearly fits with the scope of GMD, some limitations are addressed and the work is put in perspective of future developments. Furthermore, the study it concise and very pleasant to read. I think the paper deserves publication after the authors have addressed the following comments. I would particularly advise further discussion of the limitations of the modelling approach, notably regarding lacking suspension, atmospheric sublimation, feedbacks with the atmosphere and the attribution of the spatial variability in SMB to mostly saltation transport, in order to reach the level of rigour of the other discussion elements of the manuscript.
Specific comments
Abstract, L1: Snow accumulation is more the resultant of the SMB than a component of the SMB. The actual main components that lead to snow accumulation are snowfall, condensation/deposition and wind-driven snow deposition. Would you please reformulate a little to get this clearer?
L24-26: You should mention atmospheric sublimation as a source of surface mass loss when defining the SMB. Currently the definition in the first paragraph only describes wind redistribution.
L39-40: Would this assertion still be valid knowing that blowing snow layers can extend up to hundreds of meters above ground in Antarctica (Palm et al., 2017)? I find this assertion actually quite questionable, and one can expect the ratio of saltating to suspend snow mass to depend a lot on the area considered, and then to be very specific to the local snowpack, topographic and atmospheric conditions, or to the boundary conditions of the experiments. I did not find the materials in the referenced literature necessary to support such a statement. Gromke et al. (2014)’s results, which are based on wind tunnel experiments of limited dimensions, would not account for the well-developed bowing snow layers of hundreds of meters in depth, in which transport in suspension most likely dominate over saltation. Beside, these numbers are actually not demonstrated by Gromke et al. (2014), but just mentioned in the introduction and borrowed from Kind (1990), with no reason to consider it universally valid, especially when translated into an Antarctic environment. Moreover, contrary statements can be found in the literature. See for instance Bintanja (2000) p345: “Most of the snow transport occurs when snow is in suspension, with the saltation transport becoming rapidly less important as wind speeds increase (Pomeroy and Male, 1992; Mann, 1998).“. Please nuance and adapt your sentence accordingly.
L44: “recent” appears twice.
L80-84: How did you choose those lapse rates, particularly that of ILWR?
L164: Another limitation that you might also consider to discuss is the net domain-integrated erosion-deposition balance equal to zero, due to the absence of transport off the continental margins in this approach, which might be of some significance at the coastal grid points over steep continental margins. I also recommend to elaborate on the expected consequences of 1) assuming that the saltation mass flux accounts for both the contribution of suspension and saltation and 2) not taking into account atmospheric sublimation and its influence on surface sublimation, at least qualitatively, and more particularly for continental-scale simulations for which these processes are believed to be responsible for significant ablation at the surface. We can expect several other processes (vertical advection and sublimation of suspended particles, local turbulence and synoptic wind not related to local topography) to contribute to the net erosion/deposition balance and thus to the spatial variability in SMB. For instance, could they play a role in the discrepancy between modelled and observed SMB described in Sect. 3.2?
Section 2.4: Could you add to the text a recall on if and the, how, snow (microstructural) properties (sphericity, radius, bond radius, density, albedo) are altered by deposition of wind-driven snow?
L174-177: One could expect more info on the initialization procedure of SNOWPACK here, not provided in Sect. 2.3. How long is the spin-up before the period studied? Does the initialization procedure also account for the possible influence of erosion and deposition on the firn column? You could also refer to Keenan et al. (2021) and mention the reasonable agreement found with observed firn temperature and density profiles to strengthen your argumentation there.
Section 3.2: To evaluate the benefits of a newly-implemented parameterization, it is usually recommended to compare two simulations, one with and one without. By doing so with two Alpine3D downscalings, you could then quantitatively disentangle the contribution of erosion-deposition from that of SEB to the spatial variability in SMB, and attribute part of the enhanced variability and performance that is due to the modelled erosion-deposition process.
L307: “Simulations results” of what ? please specify.
L316: This sentence could be rewritten to present a more correct definition of SMB. You could for instance refer to as “Net snow accumulation” to describe mass gain, as SMB is not necessarily positive.
Conclusion: I think briefly recalling that atmospheric sublimation and suspension are both omitted in your calculation chain would make the conclusion more exhaustive.
References
Bintanja, R.: Snowdrift suspension and atmospheric turbulence. Part I : theoretical background and model description, Boundary-Layer Meteorol., 95, 343–368, 2000.
Gromke, C., Horender, S., Walter, B., and Lehning, M.: Snow particle characteristics in the saltation layer, Journal of Glaciology, 60, 431–439, https://doi.org/10.3189/2014JoG13J079, 2014.
Kind, R. J.: Mechanics of aeolian transport of snow and sand, J. Wind Eng. Ind. Aerodyn., 36(2), 855–866, doi: 10.1016/0167-6105(90)90426-D), 1990.
Palm, S. P., Kayetha, V., Yang, Y., and Pauly, R.: Blowing snow sublimation and transport over Antarctica from 11 years of CALIPSO observations, The Cryosphere, 11, 2555–2569, https://doi.org/10.5194/tc-11-2555-2017, 2017.
Citation: https://doi.org/10.5194/gmd-2022-28-RC2
Eric Keenan et al.
Model code and software
MeteoIO, SNOWPACK, and Alpine3D model source code SNOWPACK team https://doi.org/10.5281/zenodo.5914787
Eric Keenan et al.
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