Coupling between surface winds and saltation is a fundamental factor governing geological activity and climate on Mars. Saltation of sand is crucial for both erosion of the surface and dust lifting into the atmosphere. Wind tunnel experiments along with measurements from surface meteorology stations and modelling of wind speeds suggest that winds should only rarely move sand on Mars. However, evidence for currently active dune migration has recently accumulated. Crucially, the frequency of sand-moving events and the implied threshold wind stresses for saltation have remained unknown. Here we present detailed measurements of Nili Patera dune field based on High Resolution Imaging Science Experiment images, demonstrating that sand motion occurs daily throughout much of the year and that the resulting sand flux is strongly seasonal. Analysis of the seasonal sand flux variation suggests an effective threshold for sand motion for application to large-scale model wind fields (1–100 km scale) of τs=0.01±0.0015 N m−2.
The current landscape and stratigraphic observations of Mars attest to the importance of aeolian processes in shaping the planet and building its sedimentary cover1,2. Aeolian processes are known to dominate the current Martian climate through the modulation of atmospheric thermal forcing by suspended dust3,4,5,6. However, the intensity of wind activity has been judged as significantly lower than on Earth, such that recent evidence for currently active dune migration7,8,9 and measurements of Martian sand fluxes comparable to terrestrial values10 came as a surprise. Prevailing expectations based on wind tunnel experiments, theory for initiation of saltation, atmospheric modelling and limited in situ wind measurements suggested that sand-moving winds should be very rare11,12,13,14,15,16. The apparent contradiction between rare implied saltation and reasonably common dust lifting17,18 remains unresolved but has variously been ascribed to the uncertainties in interparticle cohesion, the role of electrostatics, the role of gustiness and the vertical wind shear and suction in dust devils18,19. Indeed, a major dust storm occurred during the time period between the acquisitions of the two images analyzed in the preceding Nili Patera High Resolution Imaging Science Experiment (HiRISE) study10,20, allowing the possibility that anomalously high storm winds accounted for a significant fraction of the measured sand flux.
Quantitative interpretation of aeolian features and realistic dynamical modelling of the Martian dust cycle are impeded by the difficulty of transferring to Mars the semi-empirical laws of sand transport established for Earth and estimating the time-integrated effect of high-speed winds based on dynamical simulations. An extra uncertainty for dust emission is the question of whether saltation of sand is the dominant mechanism for dust lifting. Saltation appears to be required, given that sand-sized particles (~100 μm) are significantly easier to mobilize than dust (~1 μm) under most reasonable assumptions regarding the interparticle cohesion of dust (particles >100 μm are also progressively harder to mobilize)1,21. The key parameter for sand motion is the effective stress threshold for sustained saltation22. When applied to wind stress output from an atmospheric model, the threshold determines the fraction of the year over which sand transport is active, the seasonal variation of sand fluxes and hence the annual erosive potential, and the seasonal evolution and magnitude of saltation-induced dust lifting. The latter factor yields a feedback loop in the Martian climate system as the mass of dust lofted modifies the atmospheric and surface thermal forcing (due to absorption/emission and shading, respectively), which in turn significantly modifies the strength of surface wind stresses. The identification of a stress threshold appropriate for use in mesoscale and General Circulation Models (GCM), which have computational grid scales of order 1 to 100 km (O[1–100 km]), is thus a crucial factor in simulating and thus better understanding the ‘steady-state’ Martian dust cycle and the initiation and evolution of dust storms. The lack of viable constraints on the stress threshold in O[1–100 km] scale models creates a vast area of plausible domain space within which the dust cycle might be operating23,24, much of which ultimately will not be relevant to Mars.
We estimate an effective threshold from satellite-based observation of sand activity over an area of about 40 km2. Sustained sand flux is observed throughout a Mars Year (MY), with strong seasonal variability. Wind simulations applied to a set of sand transport laws provide a predicted sand flux, which is compared with the measured sand flux. We determine the effective shear stress threshold that allows the predicted sand flux to best reproduce the measured sand flux variations. The threshold, estimated at ~0.01±0.0015 N m−2, is an effective threshold relevant for mesoscale and general circulation modelling in the O[1–100 km] scale range for which the turbulent characteristic of the wind is not resolved (though in such models the amount of turbulence, and its impact on surface exchange of momentum and mixing within the boundary layer, are typically parametrized in some manner).
Seasonal sand flux measurement
In this study, we examine a time series of HiRISE images25 of the Nili Patera dune field (8.8° N, 67.3° E) over the course of a MY to determine the seasonal distribution of sand transport. The barchanoid dune field sits in Nili Patera, a 55 km diameter, ~2 km deep caldera at the top of Syrtis Major, a 1,000 × 1,500 km wide shield volcano lying a maximum of ~6 km above the neighbouring Isidis Planitia basin (Isidis) to the east. The dune field covers an area of ~200 km2 and is located 500 km west of Isidis (Fig. 1). The HiRISE imager aboard the Mars Reconnaissance Orbiter acquired a time series of nine optical images (Supplementary Table 1) at 25 cm pixel scale during MY30 (2010–2011), which cover an area of ~43 km2 at the eastern (upwind) edge of the dune field. The resolution of the imagery allows observation of ripples that cover the dune surfaces. The sand ripple migration is measured with a precision of a few centimeters from the precise registration and cross-correlation of pairs of successive images using the Co-registration of Optically Sensed Images and Correlation (COSI-Corr) methodology26. For each pair of images, a ‘difference’ image is constructed that represents the magnitude of ripple migration during the analyzed time interval. We apply a principal component-based analysis which takes into account the uncertainties assigned to each local measurement, and which produces a time series of ripple migration images with non-correlated noise filtered out (see Methods). We then estimate the average sand flux over each time interval based on ripple migration6. The total sand flux, q, scales with the ripple migration sand flux, qr, as q~qr1.2 (ref. 27). Our results show a sustained sand flux throughout the year with a strong seasonal variation: during the southern summer period, which includes perihelion (time of closest approach to the Sun), the flux is about three times larger than during the northern summer (Fig. 2). The sand flux measured over a 3-month period in the northern winter of MY28 (2007) (ref. 10) is comparable, though about 30% lower, to the winter values obtained for MY30 in this study. We measure only the space- and time-averaged values within each period separating each data acquisition, although a glimpse of the stochasticity of sand-moving winds can be inferred, as follows. All the analyzed pairs show evidence of significant ripple migration, even two pairs of images taken only 17 or 16 days apart (corresponding to the periods with planetocentric solar longitude (Ls)=322–332° and Ls 332–340°, respectively). Over these two consecutive periods the average flux is different by a factor of 2, suggesting that while sand-moving wind events were probably numerous during both of these short-time periods, the variability in frequency, duration and/or strength of these winds must have been large. However, the south-westward direction of the flux, indicated by the migration direction of the sand ripples, is stable over the year (Supplementary Table 1), indicating a fairly constant direction of sand-moving winds.
Atmospheric models on various scales show that the circulation at Nili Patera is dominated by a combination of the tropical-mean overturning (‘Hadley’) circulation, thermal tides and slope flows associated with the dichotomy boundary and the Isidis basin28,29,30,31. Nili Patera is located roughly 9° N of the equator within the seasonally reversing Hadley circulation. During northern summer, the intertropical convergence zone (the location of mean upwelling in the Hadley circulation) is displaced northward of Nili Patera. The cross-equatorial surface expression of this cell (the ‘monsoonal’ circulation) curves due to planetary rotation, yielding mean north-eastward winds at the latitude of Nili Patera. This flow reverses in southern summer, generating south-westward winds. A significant thermal tide5 is superposed on the monsoonal flow, yielding major daily variations of wind speed and direction, with the latter rotating over a full cycle during the day. Finally, the daily solar heating of the surface in the presence of the dichotomy boundary and the Isidis impact basin yields strong daytime winds that blow up the rim of the basin and then flow radially outward for hundreds of kilometers, contributing west-south-westward winds to the circulation at Nili Patera (Fig. 1). By contrast, nighttime winds that flow down the Isidis rim do not significantly influence Nili Patera flows.
We observe that ripple migration occurs throughout the year, and remarkably keeps a south-westward direction, suggesting that sand-moving winds are most likely dominated by the daily flows running outward over the southern highlands from the Isidis basin rim. The peak speed of these winds varies over the year due to the variation of solar heating of the surface with season that is produced for Mars’s current orbital configuration (specifically its obliquity and eccentricity). In southern summer the background winds of the Hadley circulation also blow towards the south-west, reinforcing the Isidis basin topographic forcing. The lower sand flux in MY28 compared with MY30 at the same time of year (Fig. 2) additionally suggests that the global dust storm of MY28 may have inhibited sand transport. Observations from the Martian surface during the 1977a and b dust storms show that increased atmospheric opacity during storms reduces the solar heating of the surface. The MY28 storm is thus likely to have damped buoyancy-slope winds at Isidis in that year.
Wind shear stress threshold constrain
We use the observed seasonal evolution of the sand flux to estimate an effective wind stress threshold. To do so, we simulate the seasonal evolution of sand flux using a numerical atmospheric model, and adjust the stress threshold used in the sand flux equation such that the predicted seasonal flux variation matches the observed one. The physical validity of the model wind fields are tested to some degree via the demand that—for some choice of threshold—they fit the evolution of the sand flux throughout the year.
Our numerical modelling of the wind field uses the MarsWeather Research and Forecast (WRF) system30,32, a multiscale, nonhydrostatic Mars atmospheric model based on the NCAR WRF system33. The model was sampled in seasonal windows over the annual cycle, with near-surface winds, densities and wind stresses output every Martian minute (1/1440th of a Martian day or sol; also see Methods) on a grid spacing scale of 120 km (O[120 km]). We also ran a mesoscale model on a scale of O[1.5 km], not continuously through the year because of the massive computing time that would involve, but for periods of ~5–10 continuous days, every 30° Ls. We find that the two models yield similar output (Supplementary Fig. 1), which suggests that the winds captured by the O[120 km] simulation dominate even in the presence of more local flows. We therefore infer that—whereas the seasonal variation of sand flux predicted by the model is very sensitive to the choice of wind stress threshold—the stress threshold for scales O[1–100 km] should be consistent with the one defined from the O[120 km] scale; we assume so for the rest of the study.
A variety of sand transport laws have been proposed which relate the sand flux to the wind stress, τ, in excess of some threshold wind stress, τs, which is the minimal threshold shear stress required to sustain transport, once initiated. Most agree that sand flux scales between the square and the cube of the frictional velocity . To investigate the sensitivity of our analysis to the chosen law, we predict the sand flux, q, using six different equations (see Methods).
Figure 3 shows the seasonal evolution of sand flux predicted at O[120 km] for the 6 sand flux formulations, and for 5 of the 25 values of the stress threshold examined in this study. The most noticeable aspects of these results are the similarity of the predicted sediment fluxes between the six transport laws tested, and that a strong seasonal variation is predicted in all cases. However, the observed ratio of the summer to winter sand flux is globally reproduced in the predictions for only a limited range of threshold stresses. If the threshold is >0.015 N m−2, the predicted summer flux drops to nearly zero and the predicted ratio of winter to summer sand flux is significantly too large. Conversely, if the stress threshold is <0.05 N m−2, the predicted ratio of winter to summer sand flux is too small, less than half the ratio observed. The correlation is generally good, with the exception of the two shortest periods (Ls 322–355° and Ls 355–105°), possibly due to uncertainties in the measurements or to the stochastic nature of the sand-moving winds as discussed above. The effective shear stress threshold for sustained sand motion is thus estimated to be ~τs=0.01±0.0015 N m−2 for simulation at a grid scale of O[1–100 km] (Fig. 4).
We note that the effective threshold value is in between the impact thresholds determined from simulations, 0.003 N m−2 (ref. 21) and 0.02 N m−2 (ref. 34), and much below the fluid threshold estimated at about 0.08 N m−2 (ref. 35). However, the significance of this similarity is unclear as the impact thresholds are defined from high resolution turbulence-resolving models, whereas the effective threshold in this study is defined from non-resolving turbulence large-scale simulations. The value of stress threshold inferred should be interpreted as the effective threshold, which is a unique threshold for initiation and sustenance of sand flux, for the instantaneous mean wind over scales from kilometers to a few degrees. This threshold is much lower than would be expected for turbulence-resolving models, wind tunnel experiments or lander-based local in situ observations1,20. Large-scale models do not resolve boundary layer turbulence (on scales O[1–1,000 m]) and hence do not simulate gust distributions superposed upon the area–mean winds. However, the estimation of the area average of the unresolved eddy wind stresses (the coherent net effect of ‘gustiness’) is a critical component of the surface layer parameterization included within global and mesoscale models, as realistic surface sources and sinks of angular momentum are needed to generate the observed large-scale circulation. Since turbulent gusts represent a distribution about the mean wind speed, there is a monotonic relationship between the area–mean wind stress threshold and the local instantaneous value. Further, the consistency over the Nili dune field over an area O[100 km2] and the barchanoid nature of the dunes suggest that the dunes form under strong mean winds and that the dune field is not dominated by the structure of the O[1–1,000 m] wind field. As such, the stress threshold estimated from the Nili observations is inherently the O[1–100 km] threshold that would result in a distribution of wind stresses such that some fraction of this distribution is above the local stress threshold for grain motion. This study does not address the nature of the mapping from O[1–100 km] scales to the local scale (O[1–1,000 m]), and it should be noted that this mapping may vary spatially with factors such as the interparticle cohesion, grain size or surface roughness. However, the estimation of the O[1–100 km] threshold stresses estimated here is relevant to estimate dust lifting, sand motion, dune formation and aeolian erosion-based global and mesoscale models.
All images were provided by the US Geological Survey (USGS) in a radiometrically calibrated format named ‘balance cube’ (‘balance cube’ are pre-processed Exposure Data Recognizer (EDR) images which can be obtained from HiRISE PIs; alternatively, users can generate ‘balance cube’ equivalent from EDR images using ISIS). Each image came in the form of 9–10 stripes corresponding to each of the charge-coupled device (CCD) array in the broadband ‘red’ channel. The stripes were processed using the USGS recommended procedure with ISIS. The process stitches back the CCD stripes while accounting for any geometric distortions to provide a reconstructed, distortion-free, full image. Camera and orbital geometries were extracted from the SPICE kernels and imported into COSI-Corr along with the images. In addition to the nine images, a stereoscopic pair was acquired at the beginning of the time series to extract a 1 m post-spacing Digital Elevation Model (DEM) of the dune field. The second image of the stereoscopic pair is the first image of the time series. The topography was extracted using BAE SOCET-SET software. Using COSI-Corr, all the images were registered to the first image of the time series, which warrants a perfect registration of the first image to the DEM by construction. Approximately 25 tie-points were selected between the first image and each image of the time series. The tie-points were the same for all images, except where footprint differences prevented it, in which case the tie-points were relocated inside the overlap of the two images. All the tie-points were located on the bedrock, away from the dunes. The tie-points accuracy was optimized with COSI-Corr using a 256 × 256 pixels window size. The average mis-registration at the tie-point locations of the resulting registered pair of images are on the order of a few millimeters, with a s.d. of ~25 cm (Supplementary Table 1). Most of the registration residual comes from unrecorded jitter of Mars Reconnaissance Orbiter during image acquisition and residual in the CCD arrays relative orientations. Images were then orthorectified with COSI-Corr on the same 25 cm resolution grid, using the optimized set of tie-points, the DEM and the ancillary data. Pairs of time-adjacent images were correlated with COSI-Corr using a sliding window of 70 × 70 pixels (17.5 × 17.5 m) and a step of 16 pixels (4 m).
Bias in ripple migration maps due to DEM error
DEM extraction using a stereoscopic pair of images relies on feature tracking and measurement of feature shift due to the parallax. An underlying assumption to reconstruct a DEM is the stability of the scene between the images’ acquisitions. Indeed, to recover an accurate topography model, parallax is ideally due to topography only, and not to the topography augmented with a physical shift of the terrain. In this study, the DEM extraction on dunes tracks the ripples features to estimate the dune height. Ripples migration between the acquisitions, if any, will therefore bias the overall dune height. To estimate the bias on the ultimate ripple migration maps due to a potentially biased DEM, we estimated the error in elevation, assuming a ripple migration based on the first measurement map. Using this estimated DEM error, we estimated its contribution on all the migration maps by taking into account the stereoscopic angle between each image pairs of the time series. Ripple migration linearly scales with the elevation of the dune10, such that the error in elevation will linearly scale with the dune elevation. We estimate the maximum, average and s.d. of the dune elevation error to be 77 cm, 26 cm and 14 cm, respectively. The DEM error contribution to the subsequent ripple migration maps is listed in Supplementary Table 1, but overall the error is small, about few centimeters, with a maximum of ~20 cm in the worst case (pair 21652 and 22364 with a stereoscopic angle of 17°).
Bias in ripple migration maps due to the use of a unique DEM
The DEM was generated at the beginning of the time series. The first image is actually part of the stereo pair that was used to extract the topography. The last image of the time series was acquired 700 days later. In the meantime, dunes migrate, such that using a unique DEM may cause a misalignment of dunes with the images. In Bridges et al.10, dune migration speed was estimated to ~1 m per year for the fastest dunes. According to the DEM, the slopes of the dunes’ stoss slopes in the ‘axial’ direction are 4–8°. Assuming a dune displacement of 2 m (in 700 days) and a static morphology and height over this time scale, an error of around 28 cm in elevation would be introduced, which would contribute to a maximum of around 8 cm in ripple migration estimation in the worst case (pair 21,652–22,364 with a stereoscopic angle of 17°).
Overall, geometric errors due to (1) stability of the ripple between the stereo-pair acquisition and (2) stability of the dunes during the time series time span, can be neglected in view of the measured ripple displacements which are of the order of few meters.
Jitter and CCD-induced mis-registration
Unrecorded spacecraft jitter during image acquisition causes distortions in the imagery that are not corrected during the orthorectification. These geometric distortions are recovered in the subsequent correlation maps as erroneous ‘displacements’. As seen in Supplementary Figs 2–3, geometric distortions (most visible on the bedrock area) can be observed in the cross and along-track directions. The cross-track undulations are a direct effect of the jitter and the along-track stripes are caused by the effect of the jitter on the staggered CCD arrays. Collectively, these jitter and CCD artifact (jitter/CCD artifacts) account for up to 1–2 pixels (25–50 cm), and are the largest source of error in the ripple migration estimation. This source of error is accounted for during the weighted linear regression between predicted and measured fluxes (See Methods—Shear stress threshold estimation).
Principal component analysis
A principal component analysis (PCA) was applied to the time series to filter out measurement noise and to extract the main signal from the data. In practice, we used a weighted low rank approximation of the covariance matrix to account for the missing values (decorrelated pixels), and different noise amplitude between the maps. Noise amplitude between maps can vary due to the irregular time sampling of the acquisitions, which leads to different shadowing effects and temporal changes. We used an adapted version of PCAIM36, giving each map a weight inversely proportional to the number of decorrelated points in the data set. The assumption is that a map containing a large number of decorrelated points is a noisier measurement map. Prior to computing the PCA, all displacement maps were time normalized, to account for the unequal time span between pairs. The χ2 measurement indicates that the first two components of the PCA accounts for 84 and 82% of the time series variance, of the east/west and north/south displacement maps, respectively.
Estimates of ripple height
The DEM cannot distinguish ripple topography, so we had to assume a standard ripple height. We used the ripple height of 40 cm defined in Bridges et al.10 In this study, the ripple height was estimated from the HiRISE images, using two approaches:(1) From the ripple wavelength (directly measured on the image) and using the 1:10 ripple height to ripple wavelength ratio commonly found on Earth. (2) From the trace of the ripple footprint on the bedrock (for the ripple on the edges of the dunes) in association with the dune slope (measured from the DEM). Visual observation of the ripple shape shows a stable ripple wavelength in time and space (except at the very base of the dune where ripples nucleate and grow to stable state). This wavelength stability suggests a stable ripple height over time and space as well. Therefore, because ripple height is stationary, and because we are interested in the relative variation of the flux only, the ripple height actual value does not play a role during the linear regression between predicted and measured sand flux. Ripple height would play a definite role if we were to estimate the absolute sand flux quantity however.
Sand flux estimation
The ripple displacement maps were reconstructed (Supplementary Figs 4–11) using the first two components of the PCA (Supplementary Figs 2–3). The migration azimuth of the ripple is quite stable throughout the year (Supplementary Table 1), and is ~115° from north counterclockwise. This azimuth corresponds also to the azimuth found in Bridges et al.10 The scattered azimuth distribution for pairs 23,564–23,920 is due to strong un-modelled satellite jitter. To limit the jitter bias in the estimation of the sand flux, the ripple displacements are projected onto the main migration direction, and the average sand flux was estimated for each map using the method described in Bridges et al.10 Because the displacement maps are co-registered, and because we used the reconstructed maps, the exact same pixels, in location and amount, were used to compute the average reptation sand flux of each displacement map of the time series. Note that the sand flux estimated on every point on the dune scales linearly with the height of the dune10, that is, for a given dune, sand flux will vary from approximately no sand flux (base) to a maximum (crest). The average flux computed in this study differs from the traditional ways of quantifying sand flux, for example, at the crest, area based, but is relevant for the temporal evolution analysis.
GCM and mesoscale simulations
The MarsWRF model30,32 was run at 2° global grid spacing, with four levels of interactive nests used to increase the resolution over the Nili Patera region. Each embedded domain contained 120 × 120 grid points, and had a factor of 3 refinement of the grid (that is, produced a threefold increase in resolution), resulting in a grid spacing of ~1.5 km in the innermost nest, centred on the Nili Patera caldera.
MarsWRF, as run for this study, used surface boundary conditions from the 1/64th degree MOLA topographic map, 1/2 degree MOLA roughness map and albedo and thermal inertia maps30 derived from the Mars Global Surveyor Thermal Emission Spectrometer (MGS-TES). The simulation used the two-stream k-distribution radiative transfer model, treating CO2 and dust radiative heating37 and the MRFPBL boundary layer scheme. The dust distribution was defined using the Mars Climate Database ‘MGS’ dust scenario. The model includes a full carbon dioxide cycle that produces roughly 30% variation of atmospheric mass over a MY. The cycle is calibrated with respect to the multi-year Viking lander pressure data sets30.
The GCM 2° output used in this study was taken from the last year of a multi-year run. The output (drag velocity, air density and vector winds near the surface) was sampled every Martian minute (1/1440th of a Mars day or Sol) over the whole year. Mesoscale simulations were not run for the whole year, but were sampled every minute for ~10 Sols over intervals starting at Ls=0° and every 30° of Ls thereafter. Each mesoscale simulation was initialized using output at the required Ls from the global 2° run, and the first three sols were discarded to avoid ‘spin-up’ effects (Supplementary Fig. 1).
Shear stress threshold estimation
The objective is to adjust the sand shear stress threshold used with the prediction of atmospheric simulations and a transport law, such that the predicted sand flux matches the observed sand flux (from the imagery).
Using the GCM prediction of the wind shear, we tested a total of six transport laws to estimate the shear stress threshold for sustained transport, once initiated. Because we are matching the seasonal variation of flux (that is, the relative flux, rather than the absolute magnitude of flux at a given time) the constants at the start of the equations are factored out:
where is the threshold velocity calculated from the atmospheric density, ρ, and stress threshold . Note that while the threshold is often stated in terms of the frictional velocity, as the latter is easier to measure, it is the shear stress that is of primary physical importance for the initiation of grain motion.
We estimated the optimal shear stress threshold from the χ2-analysis of the best fit (linear regression) between predicted and measured fluxes for a range of threshold values. Two main elements taken into account in the weighted linear regression are detailed below:
The measured ripple-induced sand flux represents only the reptation sand flux. However, the total sand flux is composed of the reptation and saltation sand fluxes. Andreotti27 proposed that the reptation flux scales with u*2, and that the total flux scales with , which is a relation also proposed by Werner39. We therefore assume the repton flux qr to scale with the total flux q as q~qr1.2 for u* above the threshold. This relation was accounted for during the estimation of the shear threshold, as the predicted sand flux from the simulations represents the total sand flux.
The larger source of flux measurement error is the jitter/CCD artifact (Methods—Jitter and CCD-induced mis-registration), which we accounted for in the linear regression as follows. For each pair, the error from the jitter/CCD artifact on the estimated sand flux is quantified: the east/west and north/south displacement maps of the bedrock only (that is, no dunes) are projected on the main migration direction (115°). The average and variance of the ‘equivalent’ sand flux is computed. In an artifact free setup, the average and variance of the resulting ‘equivalent’ sand flux should be null. As expected, the average is close to zero as the satellite ancillary parameters are optimized such that the overall co-registration of the ~25 tie-points located on the bedrock is optimal. The variance however is not null (Supplementary Table 1). Although the CCD/Jitter error is not uniformly distributed on the field area, the bedrock and dunes are sufficiently interlaced to consider the sand flux error estimated from the bedrock to correctly represent the sand flux error on the dunes. This error variance was used as a confidence weight on the measurement during the linear regression. Note: the jitter/CCD artifact does not depend on the time span between acquisitions. However, the resulting ‘equivalent’ sand flux does, and the larger the time span, the smaller the error on the measured sand flux.
The reduced χ2-curves have a minimum ~10, which indicates that some error sources, whether they originate from the measurement, the simulation or the transport law, are not properly accounted for. One source of error is the stochastic nature of wind events that cannot be captured in the simulations, but observed in the measurements with low time span. To account for the error sources that are not captured, we increased the error on the measurement such that the resultant-reduced χ2 falls to unity. The resulting probability density function gives us a conservative confidence level on the shear stress and are represented in Fig. 4.
List of software used
SOCET-Set. Commercial software provided by BAE Systems ( www.baesystems.com) used for the DEM generation from stereogrammetry. We followed the procedure recommended by the USGS ( http://webgis.wr.usgs.gov/pigwad/tutorials/socet-set/SocetSet4HiRISE.htm). Along with the DEM, the two orthorectified images from the stereopairs were generated, and one of them was used as the reference to register the time series to the topography.
ISIS. Free, open source image processing software developed and provided by the USGS ( http://isis.astrogeology.usgs.gov/). This software was used to pre-process the raw HiRISE imagery into a format that can be handled by COSI-Corr. The ISIS processing also extract the metadata of the images (telemetry, camera geometry and satellite jitter) from the NASA SPICE kernels, and store them into an ascii file that can be read by COSI-Corr.
COSI-Corr. Free, not open source software provided by Caltech ( http://tectonics.caltech.edu/slip_history/spot_coseis/), and used to orthorectify, register and correlate the image time series. The output of COSI-Corr is the ripple displacement maps. The methodology used to process and generate these images is the one described in the User Guide. The HiRISE capability of COSI-Corr, developed by the authors of this study, will be a part of the next COSI-Corr release.
PCAIM. Free and open source software provided by Caltech ( http://tectonics.caltech.edu/resources/pcaim/). This software was used to compute the PCA on the HiRISE time series.
MarsWRF. Free and open source atmospheric simulation software ( http://planetwrf.com/), developed and provided by Ashima Research ( http://ashimaresearch.com/). The GCM and mesoscale simulations of the wind regime at Nili Patera were computed using MarsWRF with the parameters that are described in Methods—GCM and mesoscale simulations.
How to cite this article: Ayoub, F. et al. Threshold for sand mobility on Mars calibrated from seasonal variations of sand flux. Nat. Commun. 5:5096 doi: 10.1038/ncomms6096 (2014).
Greeley, R. & Iversen, J. D. Wind as a Geological Process Cambridge University Press (1985).
Grotzinger, J. P. et al. Stratigraphy and sedimentology of a dry to wet eolian depositional system, Burns formation, Meridiani Planum, Mars. Earth Planet. Sci. Lett. 240, 11–72 (2005).
Strausberg, M. J., Wang, H. Q., Richardson, M. I., Ewald, S. P. & Toigo, A. D. Observations of the initiation and evolution of the 2001 Mars global dust storm. J. Geophys. Res. 110, E2 (2005).
Haberle, R. M., Leovy, C. B. & Pollack, J. B. Some effects of global dust storms on the atmospheric circulation of Mars. Icarus 50, 322–367 (1982).
Wilson, R. J. & Hamilton, K. Comprehensive model simulation of thermal tides in the Martian atmosphere. J. Atmos. Sci. 53, 1290–1326 (1996).
Moriyama, S. Effects of dust on radiation transfer in the Martian atmosphere III: numerical experiments of radiative-convective equilibrium of the Martian atmosphere including the radiative effects due to dust. J. Meteorol. Soc. Jpn. 54, 52–57 (1976).
Silvestro, S., Fenton, L. K., Vaz, D. A., Bridges, N. T. & Ori, G. G. Ripple migration and dune activity on Mars: Evidence for dynamic wind processes. Geophys. Res. Lett. 37, L20203 (2010).
Bridges, N. T. et al. Planet-wide sand motion on Mars. Geology 40, 31–34 (2012).
Hansen, C. J. et al. Seasonal erosion and restoration of mars’ northern polar dunes. Science 331, 575–578 (2011).
Bridges, N. T. et al. Earth-like sand fluxes on Mars. Nature 485, 339–342 (2012).
Haberle, R. A., Murphy, J. R. & Schaeffer, J. Orbital change experiments with a Mars general circulation model. Icarus 161, 66–89 (2003).
Chojnacki, M., Burr, D. M., Moersch, J. E. & Michaels, T. I. Orbital observations of contemporary dune activity in Endeavor crater, Meridiani Planum, Mars. J. Geophys. Res. 116, E00F19 (2011).
Sullivan, R. et al. Results of the imager for Mars Pathfinder windsock experiment. J. Geophys. Res. 105, 24547–24562 (2000).
Arvidson, R. E., Guinness, E. A., Moore, H. J., Tillman, J. & Wall, S. D. 3 Mars years—Viking lander imaging observations. Science 222, 463–468 (1983).
Pollack, J. B., Haberle, R., Greeley, R. & Iversen, J. Estimates of wind speeds required for particle motion on Mars. Icarus 29, 395–417 (1976).
Moore, H. J. The Martian dust storm of sol-1742. J. Geophys. Res. 90, D163–D174 (1985).
Szwast, M. A., Richardson, M. I. & Vasavada, A. R. Surface dust redistribution on Mars as observed by the Mars Global Surveyor and Viking orbiters. J. Geophys. Res. 111, E11 (2006).
Newman, C. E., Lewis, S. R., Read, P. L. & Forget, F. Modelling the Martian dust cycle—1. Representations of dust transport processes. J. Geophys. Res. 107, E12 (2002).
Kok, J. F. & Renno, N. O. Electrification of wind-blown sand on Mars and its implications for atmospheric chemistry. Geophys. Res. Lett. 36, L05202 (2009).
McCleese, D. J. et al. Structure and dynamics of the Martian lower and middle atmosphere as observed by the Mars Climate Sounder: Seasonal variations in zonal mean temperature, dust, and water ice aerosols. J. Geophys. Res. 115, E12016 (2010).
Kok, J. F. Difference in the wind speeds required for initiation versus continuation of sand transport on Mars: implications for dunes and dust storms. Phys. Rev. Lett. 104, 7 (2010).
Kok, J. F., Parteli, E. J. R., Michaels, T. I. & Karam, D. B. The physics of wind-blown sand and dust. Rep. Prog. Phys. 75, 10 (2012).
Basu, S. & Richardson, M. I. Simulation of the Martian dust cycle with the GFDL mars GCME. J. Geophys. Res. 109, E11 (2004).
Kahre, M. A. & Haberle, R. M. Mars CO2 cycle: effects of airborne dust and polar cap ice emissivity. Icarus 207, 648–653 (2010).
McEwen, A. S. et al. The high resolution imaging science experiment (HiRISE) during MRO's primary science phase (PSP). Icarus 205, 2–37 (2010).
Leprince, S., Barbot, S., Ayoub, F. & Avouac, J. P. Automatic and precise orthorectification, coregistration, and subpixel correlation of satellite images, application to ground deformation measurements. IEEE Trans. Geosci. Remote Sens. 45, 1529–1558 (2007).
Andreotti, B. A two-species model of aeolian sand transport. J. Fluid. Mech. 510, 47–70 (2004).
Greeley, R., Skypeck, A. & Pollack, J. B. Martian aeolian features and deposits—comparisons with general-circulation model results. J. Geophys. Res. 98, 3183–3196 (1993).
Fenton, L. K. & Richardson, M. I. Martian surface winds: insensitivity to orbital changes and implications for aeolian processes. J. Geophys. Res. 106, 32885–32902 (2001).
Toigo, A. D., Lee, C., Newman, C. E. & Richardson, M. I. The impact of resolution on the dynamics of the martian global atmosphere: varying resolution studies with the MarsWRF GCM. Icarus 221, 276–288 (2012).
Rafkin, S. C. R., Michaels, T. I. & Haberle, R. M. Meteorological predictions for the Beagle 2 mission to Mars. Geophys. Res. Lett. 31, 1 (2004).
Richardson, M. I., Toigo, A. D. & Newman, C. E. PlanetWRF: a general purpose, local to global numerical model for planetary atmospheric and climate dynamics. J. Geophys. Res. 112, E9 (2007).
Skamarock, W. C. & Klemp, J. B. A time-split nonhydrostatic atmospheric model for weather research and forecasting applications. J. Comput. Phys. 227, 3465–3485 (2008).
Almeida, M. P., Parteli, E. J. R., Andrade, J. S. Jr & Herrmann, H. J. Giant saltation on Mars. Proc. Natl Acad. Sci. USA 105, 6222–6226 (2008).
Iversen, J. D. & White, B. R. Saltation threshold on Earth, Mars and Venus. Sedimentology 29, 111–119 (1982).
Kositsky, A. P. & Avouac, J. P. Inverting geodetic time series with a principal component analysis-based inversion method. J. Geophys. Res. 115, B03401 (2010).
Mischna, M. A., Lee, C. & Richardson, M. Development of a fast, accurate radiative transfer model for the Martian atmosphere, past and present. J. Geophys. Res. 117, E10009 (2012).
Lettau, K. & Lettau, H. H. Exploring the World's Driest Climate Vol. 101110–147University of Wisconsin-Madison, Institute for Environmental Studies (1978).
Werner, B. T. A steady-state model of wind-blown sand transport. J. Geol. 98, 1–17 (1990).
Durán, O., Claudin, P. & Andreotti, B. On aeolian transport: grain-scale interactions, dynamical mechanisms and scaling laws. Aeolian Res. 3, 243–270 (2011).
Sørensen, M. On the rate of aeolian sand transport. Geomorphology 59, 53–62 (2004).
White, B. R. Soil transport by winds on Mars. J. Geophys. Res. 84, 4643–4651 (1979).
This work was supported by the Keck Institute for Space Studies, the Mars Data Analysis Programme (MDAP# 11-MDAP11-0013), the Gordon and Betty Moore foundation and the Mars Fundamental Research Programme (grant NNX11AF59G). We thank Professor Oded Aharonson for granting us access to his BAE SOCET-SET workstation.
The authors declare no competing financial interests.
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Ayoub, F., Avouac, JP., Newman, C. et al. Threshold for sand mobility on Mars calibrated from seasonal variations of sand flux. Nat Commun 5, 5096 (2014). https://doi.org/10.1038/ncomms6096
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