Results from simulation modeling of crater degradation by fluvial and eolian processes are compared with size-frequency and depth of infilling statistics for the heavily cratered Sinus Sabaeus quadrangle of Mars. The fractional degree of infilling of craters greater than 10 km in diameter in this region is bimodal, with a small population of post-Noachian craters with little infilling, whereas most Noachian craters are strongly infilled. This pattern is most consistent with fluvial erosion of craters, because modeling indicates that craters fill rapidly at first, but the rate of infilling diminishes through time as crater wall heights diminish and the area of deposition on the crater floor increases. Simulated rates of crater infilling by eolian processes are more constant, which would be expected to produce craters equally distributed in degree of infilling, which is not observed. The small slope of the size-frequency distribution in the 10–30 km size range is also consistent with the more rapid fluvial erosion of smaller craters. The analysis also suggests that rates of crater production and of crater degradation were in rough balance during the Noachian epoch in the 10–30 km size range.
 Since the first detailed pictures of the surface of Mars were returned by Mariner 4, the degraded nature of most Martian highland craters has been apparent. With the exception of relatively fresh post-Noachian craters, craters on the southern highlands generally demonstrate an absence of recognizable ejecta, low or missing crater rims, relatively flat crater floors, and much shallower depth than fresh craters of equivalent diameter. A variety of processes may have been involved in crater degradation, including superimposed impacts, weathering, mass wasting, fluvial incision and deposition, ice-related processes, lacustrine processes, lava infilling, eolian saltation, and airfall deposition from 1) dust storms, 2) ash from volcanic eruptions, or 3) regionally distributed ejecta from large impacts. Craters carry an important record of geomorphic processes acting on planetary surfaces because they are ubiquitous and, unless their rims are breached, their interiors represent a closed sedimentary system (an exception is eolian deflation of fine-grained sediments in a few impact craters [Malin and Edgett, 2000]).
 The processes and history of crater degradation in the Noachian is addressed in this paper by morphometric analysis of crater morphology in a portion of the cratered highlands coupled with simulation modeling of the two most widespread degradation processes, eolian (saltation and airfall) modification and fluvial erosion and deposition. We use as our study site the heavily cratered Sinus Sabaeus Quadrangle (0–30°S, 0–45°E) in which the dominant Noachian geomorphic processes were likely eolian modification (as broadly conceived to include both saltation and airfall) and fluvial erosion and deposition (including concomitant weathering and mass-wasting). At equatorial latitudes post-Noachian sedimentation and modification by ice-related processes [Soderblom et al., 1973; Mustard et al., 2001; Head et al., 2003; Kreslavsky and Head, 2003] has apparently been negligible.
 Previous studies have argued for the predominance of fluvial erosion in the degradation of craters during the Noachian on the basis of channeling of the inner and outer crater rims, maintenance of a steep interior crater wall during degradation, inward-sloping crater floors with gradients typical of fluvial fans, and preferential destruction of the raised crater rim [Craddock and Maxwell, 1993; Craddock et al., 1997; Craddock and Howard, 2002]. Further evidence for fluvial erosion is offered here on the basis of the frequency distribution of the amount of infilling of degraded craters and comparison with the results of simulation modeling.
 We first introduce the simulation models of eolian and fluvial crater degradation and investigate the temporal progression of relative crater degradation and the effect of initial crater size on the rate of infilling. We then present data on the frequency distribution of relative crater degradation in a representative area of the Martian highlands. On the basis of these data and comparison with the results of simulation modeling we conclude that the production of new craters and their erosional destruction by fluvial processes were roughly balanced during the Noachian, at least for craters smaller than 30 km in diameter.
2. Simulation Modeling of Crater Degradation
 A computer simulation program has been developed [Howard, 1994, 1997; Craddock and Howard, 2002] that simulates crater degradation by the processes of airfall deposition and by fluvial erosion and sedimentation. This simulation program is applied here to predict the temporal evolution of crater modification and the effects of crater size on modification rates. These predicted properties are then compared with measured properties of degraded craters in a portion of the Martian highlands.
2.1. Fresh Crater Morphology
 The initial conditions for the simulations are a single crater of specified diameter superimposed on an otherwise flat surface. Craters are generated by a routine that simulates the gross geometric properties of Martian craters on the basis of published statistics on crater depth, rim height, and interior wall gradient [Garvin et al., 2002, 2003]. The program uses power functions of elevation versus distance from the crater center or rim to simulate the crater shape. A certain level of random noise is superimposed on this geometric form, with the amount of noise going from zero at the crater center to a maximum at the rim, and declining beyond the rim. The program does not simulate central peaks, multiring basins, or wall terracing. Simulated craters ranged from 1 km to 100 km in diameter, with the corresponding cell size for the rectangular DEM ranging from 8 m to 800 m, so that the crater diameter was about half the dimensions of the 256 × 256 simulation domain. The top and bottom boundaries are periodic, as are the left and right boundaries. Figure 1a shows an example 50 km simulated crater, and Figure 2 shows example scaled profiles through craters of varying diameter.
2.2. Eolian Modification
 Airfall and eolian degradation are modeled by a heuristic set of rules that model deposition and erosion as a function of the degree of exposure of a given location. Locations on or near ridges or isolated peaks (e.g., crater rims) are either eroded by eolian stripping and abrasion or receive diminished rates of sedimentation compared to relatively sheltered locations, such as crater floors and lower walls, which undergo net aggradation. The degree of deposition or erosion at any location within or outside of a crater is a function of an “exposure index”, Ie, which is based on a weighted sum of the gradients, Si, between the local elevation, E, and that of surrounding locations, Ei:
where Δxi is the distance to the nearby point. The exposure index, Iek, for points lying along a transect, k, extending from the given location is given by
where the parameter η governs the relative importance of nearby versus distant points in determining the exposure. In computing equation (2) for a given location, transects near the crater rim include locations both within and outside of the rim. Points that are not visible from the location (lying behind a closer high point) are not included. For computational efficiency exposure indices are calculated only along the eight cardinal and diagonal directions from a given point and the net exposure index, Ie, is the average of the eight Iek. The rate of eolian erosion or deposition, ∂z/∂t∣e is a function of the exposure index (z is the vertical dimension). The functional dependence of the erosion rate utilized here is shown in Figure 3.
2.3. Fluvial Erosion and Deposition
 The modeling of fluvial erosion of impact craters is based on the model of Howard [1994, 1997] with components modeling physical or chemical weathering of rocks to form transportable colluvium, mass wasting by nonlinear creep, fluvial detachment, and fluvial transport and deposition. Parameters used for these simulations are based on terrestrial values in semi-arid or arid landscapes except for correcting for the difference in gravity between Mars and Earth.
 It is assumed that the materials below the surface (lava, sediments, ejecta, etc., collectively termed “bedrock”) may be indurated, but can be weathered at a finite rate by physical or chemical processes to form colluvium. The rate of bedrock weathering, ∂zb/∂t, is assume to decrease exponentially with the thickness, H, of overlying colluvium:
where Kb is the intrinsic maximum weathering rate (a joint function of rock properties and climate), and c governs the rate of decay of weathering rate with colluvium thickness In accord with terrestrial observations [Heimsath et al., 1997, 1999, 2000] in semi-arid landscapes c is set to 0.02 m−1, while Kb is a variable parameter in the range of 0.02 to 0.0002 m/yr (Table 1). Conversion of bedrock to colluvium is assumed to be isovolumetric. Note that ∂zb/∂t is the rate of lowering of the colluvial-bedrock contact, and when weathering is isovolumetric it does not change the land surface elevation.
Ratio of colluvium erodibility to that of bedrock.
 Erosion by mass wasting, ∂zm/∂t, is proportional to the spatial divergence of colluvial mass flux, qm:
Colluvial flux is given by a nonlinear relationship:
where ∣S∣ is the absolute value of local slope, s is the unit vector in the downslope direction, g is gravitational acceleration, St is a threshold gradient at which the rate of mass wasting becomes infinite (i.e., landsliding) (assumed to be 0.8), and Ks is creep diffusivity, which is assumed to be 0.0005 m2/yr, characteristic of arid environments [e.g., Carson and Kirkby, 1972; Martin, 2000]. The influence of gravity on Ks is uncertain, but its influence should affect diffusivity by a maximum of a factor of 2.6. The exponent, a, is assumed to be 3.0, and Kf takes a value (0.5) that provides for a smooth but rapid approach to threshold slopes for rapid erosion rates. Erosion of bare bedrock slopes (exposed when erosion rates are greater than the maximum weathering rate given by equation (3)) follows equation (5), but with Ks set to zero and a critical gradient, St, of 2.7.
where Kf is a variable parameter taking values from 0.02 to 0.0002 m2 yr kg−1 (Table 1) when the reference shear stress is that which corresponds to the mean annual flood. This range encompasses measured terrestrial erosion rates in rocks ranging from shale to moderately strong sedimentary or metamorphic rocks (A. D. Howard, manuscript in preparation, 2004). Flow of water is assumed to be channelized and originating from runoff. Shear stress can be related to channel gradient and drainage area using equations of hydraulic geometry and steady, uniform flow as discussed by Howard :
where R is hydraulic radius, S is channel gradient, V is mean velocity, N is Manning's resistance coefficient, P is a specific runoff yield (depth per unit area per unit time), Q is an effective discharge, W is channel width, A is drainage area, and Kn, Kp, Ka, Kw are coefficients. These coefficients and exponents are assumed temporally and spatially invariant. The following parameter values are assumed: N = 0.03, Kn = 0.3 (for metric units); P = 3.0 × 10−5 m1.6/s, e = 0.7, b = 0.5, and Kw = 5.0 s0.5 m−0.5. Weathered bedrock (colluvium) is assumed to be a factor Kr more erodible than bedrock. The erodibility factor, Kr, is a parameter of the model with assumed values of 1.0 (equal erodibility) and 10.0 (Table 1).
 When the flux of sediment transported as bed and suspended load reaches or exceeds the transporting capacity of the flow (an alluvial channel as opposed to a bedrock channel), the erosion or deposition rate, ∂za/∂t, is proportional to the spatial divergence of transport flux qs (volume per unit time per unit width):
 Sediment transport flux is estimated using a bedload transport formula that expressed as the relationship between a dimensionless transport rate, Φ, and a dimensionless shear stress, τ* [e.g., Yalin, 1977]:
In these equations τc* is the value of τ* at the threshold of motion, qsb is bed sediment transport rate in bulk volume of sediment per unit time per unit channel width, Ss is the specific gravity of the sediment, g is gravitational acceleration, ρf is the fluid density, d is the sediment grain size, and μ is alluvium porosity. A dominant bed grain size of 0.02 m is assumed, with Ke = 8.0, p = 1.5, τc* = 0.05, and Ss = 2.65. The shear stress is estimated from equations (7)–(11), with the dominant discharge for sediment transport assumed to be 0.6 of the mean annual flood, flowing 2% of the year. The bed sediment load is assumed to constitute 20% of sediment eroded from slopes.
 In bedrock channels the overall erosion rate, ∂z/∂t, is a weighted function of the rates of mass wasting and fluvial erosion, as discussed by Howard [1994, 1997]. Where channel gradients are low enough that channels transport a capacity bedload, erosion and deposition rates are governed by equation (12). For the simulations reported here, the climate was assumed to be sufficiently arid that no standing water was present for appreciable periods of time within the crater, and that runoff characteristics are typical of terrestrial deserts or periglacial environments.
 Making different assumptions about the values of most of the simulation parameters will affect absolute erosion rates and details of crater morphology, but will have little effect on the issues most relevant to this study, that is, relative infilling rates of craters of different sizes and the temporal changes in infilling rates through time. The model parameters that most affect these properties are the relative rates of rock weathering (Kb), rock fluvial erodibility (Kf), and relative colluvium erodibility (Kr). A series of simulations were conducted for fluvial and mass wasting erosion on craters of different sizes with several combinations of these parameters (Table 1). For more information on model details and scaling, see Howard .
2.4. Simulation Results
 Although attempts have been made to characterize absolute rates of Martian crater modification by eolian and fluvial processes [Barlow, 1995; Golombek and Bridges, 2000], the simulation results reported here are presented in relative terms, either as amounts of modification through time assuming constancy of process rates or the relative rates of degradation for craters of different size. Both eolian and fluvial processes may have been highly variable both in time and location due to effects of gradual climate deterioration during the Noachian, quasiperiodic climate change and, possibly, the effects of short-term increase of global temperatures and precipitation rates by large impactors [Segura et al., 2002].
2.4.1. Eolian Degradation
 The eolian model presented above is assumed to represent in a general way the long-term effects of crater modification by eolian processes, including airfall deposition of eolian dust, volcanic ash, or impact-produced debris transported over long distances. In addition, the long-term progression of crater filling by saltating sand is also assumed to be approximated by the model. However, the model does not attempt to represent the physics of eolian transport and deposition that modify craters, nor is the model mass-conserving. Nonetheless, the resulting pattern of crater infilling resembles images of many modified Martian craters. Figure 1 shows a crater with simulated eolian infilling, Figure 4 shows small Martian craters with obvious eolian deposition, and Figure 1d shows successive profiles of eolian blanketing during one simulation. A general characteristic of the simple eolian infilling is that the crater rims remain largely clear of deposits, whereas the crater center becomes filled with a deposit having a generally parabolic cross-section. Obviously the crater diameter remains unchanged during eolian modification. In the simulations reported here eolian crater rim erosion is assumed to be small (Figure 3).
2.4.2. Fluvial Degradation
 Simulated fluvial modification infills the crater bottom with alluvial fan deposits, whereas the crater rim gradually backwastes while maintaining a generally steep slope. Depending on the model parameters, the interior crater wall may be strongly gullied (Figure 5) or relatively smooth (Figure 6). Similar variations occur in Martian degraded craters (compare Figure 5 with Figure 7 and Figure 6 with Figure 8). Both the backwasting and the downcutting of the crater rim occur, so that in later stages of erosion the crater may become essentially rimless. Example craters degraded by fluvial erosion are shown in Figures 5 and 6. Successive profiles are shown in Figures 5d and 6d. Many strongly degraded Martian highland craters in the size range of 10–150 km exhibit both relatively steep inner walls, an inward-sloping crater floor, and fluvial gullying on the crater walls (e.g., Figure 7), suggesting fluvial erosion has been the dominant modifying process [Craddock and Maxwell, 1993; Craddock et al., 1997; Craddock and Howard, 2002].
2.4.3. Crater Infilling Rates and Their Diameter Dependency
 A series of simulations were conducted with both the fluvial and eolian degradation models to determine the temporal progression of crater modification and the dependency of initial crater diameter on infilling rates. In these simulations the intrinsic rate constants for the modification were assumed to be temporally constant and to be the same for initial craters of different size. The relative degree of crater modification was expressed as the ratio R,
where H is the initial fresh crater depth (measured from the average rim height to the lowest point of the crater floor) and h is the crater depth at any subsequent time. For a fresh crater this ratio is zero, and for a completely degraded crater the ratio approaches unity. Note that a reduction in crater depth can occur both by infilling and by rim erosion, although the magnitude of the former dominates for simulations of both fluvial and eolian degradation.
 For small craters the simulated eolian crater infilling was nearly linear with time, but for large craters the rate of infilling was slower near the beginning and end of the simulation, presumably due to the shallower relative depth (Figure 9). Simulations were conducted with model craters of 1, 2, 5, 10, 20, 50, and 100-km diameters whose initial geometry was given by the Garvin et al.  fresh crater scaling. The results were used to create multiple regression models, utilized to predict the actual simulation time, T, at various values of relative crater depth, R, and the corresponding crater diameter, D. The resulting equation for eolian infilling is
which explains 99% of the variation in simulation time (r2 = 0.99). The multiplicative constant is not reported because the absolute modification rates for Martian craters are uncertain and presumably varied with location and certainly through geologic time. Because of the initially slow infilling rate, which might be model dependent, an additional model was fit to the later stages of eolian infilling in which infilling was assumed to be linear with time. The resulting model is
where T0.1 is the simulation time at which the relative crater modification R equals 0.1 (R0.1). These results indicate a less than linear dependence of relative infilling on initial crater diameter. Initial models of crater infilling by eolian deposition [Hartmann, 1971; Opik, 1965, 1966] assumed a linear dependency of infilling time with crater diameter under the presumption that crater depth scaled linearly with diameter. Hartmann  and Hartmann et al.  later revised the predicted infilling times to reflect the less than linear increase of crater depth with diameter. The global fresh crater statistics collected from MOLA observations [Garvin et al., 2003] suggest H ∝ D0.8 for simple craters less than 7 km in diameter and H ∝ D0.5 for larger, complex craters. Thus equation (16) is reasonably consistent with the assumption that the eolian deposition rate in craters is independent of crater size.
 For crater modification by fluvial erosion and deposition interpretation of relative infilling, R, is complicated by the increase of the crater diameter through time due to rapid erosion of the steep inner crater wall. For Martian degraded craters only the present diameter is known. Therefore using the present degraded crater diameter to predict the initial fresh crater depth will yield somewhat greater depths than the actual initial value if the degradation occurred by fluvial erosion. In the simulations of fluvial crater degradation the crater diameter enlarged by about 5% when R was in the range 0.4 to 0.5, but then increased rapidly to about 20% by R∼0.7 (e.g., Figure 5). Therefore two sets of regressions were run for temporal variation of crater infilling by fluvial processes, the first using (15) with H being the actual initial crater depth, and another regression for R′,
where H′ is the fresh crater depth predicted using the observed crater diameter at the given time during the simulation. The resulting regressions using R′ proved to be statistically indistinguishable from those using R, so we report only results using R.
 Several sets of process-related parameters were used with the simulation model, varying the parameters Kf, Kb, and Kr (Table 1). The temporal progression of R is shown for several simulations of erosion of a 50 km crater (Figure 10). Although there is considerable variability in the shape of the curves, they all differ from the eolian modification in that the infilling rate diminishes with time. This occurs primarily because the source region for the sediment filling the crater (the inner crater wall) diminishes in height during the simulation, and secondarily because erosion increases the crater diameter so that the area over which sediment is deposited increases. A set of simulations for various initial crater diameters were conducted for two sets of parameters (Cases 1 and 2 in Table 1). Regressions for the simulated time at given values of progressive infill yielded the following equations:
Although considerable variation in the exponents occurs for different sets of simulation parameters, the two cases presented are representative of two endpoints. For Case 1 the colluvium is as easily eroded as bedrock or the weathering rate keeps pace with fluvial erosion, so that slopes are colluvium-covered, whereas for Case 2 the bedrock is 10 times less erodible than colluvium, and the rate of weathering is sufficiently slow that steeper crater walls expose bedrock. The Case 1 results are very similar to a simplified model in which the rate of sediment delivery to the crater floor is assumed to be proportional to the exposed area of the interior crater wall.
3. Crater Morphology and Crater Counts
 The Sinus Sabaeus Quadrangle (0°S to 30°S and 0°E to 45°E) was selected as a representative highly cratered region to characterize the morphometry of all recognizable fresh and degraded craters greater than 10 km in diameter. Craters were identified and classified from Viking-based MDIM 5° × 5° quadrangle images supplemented by topographic contour maps of the same quadrangles made from MOLA observations. In this quadrangle 530 craters were analyzed for a range of morphometric parameters. Individual MOLA tracks were utilized rather than gridded data to avoid artifacts due to sparse data. An additional 320 craters were included in crater counts but were not morphometrically analyzed because of 1) poor MOLA coverage; 2) strong modification by later impacts, or 3) breaching of the crater wall by entering or exiting fluvial channels (not a closed depositional system). Each crater was visually assigned a degree of degradation using the standard classification system [Craddock and Maxwell, 1993; Craddock et al., 1997; Barlow et al., 2000], ranging from “A” for fresh to “E” for highly degraded craters. Qualitative characteristics were used in conjunction with the quantitative morphometric measurements to examine the properties of crater modification within the quadrangle as a function of crater diameter, location within the quadrangle and elevation. A variety of measurements and analyses were conducted [Forsberg, 2003], but we report here results related to determining the processes responsible for degradation.
3.1. Observed Frequency of Relative Infilling
 The frequency distribution of the estimated degree of crater infilling, R, for craters in the 10–100 km diameter range within the Sinus Sabaeus Quadrangle is noteworthy in its bimodal character, with a peak near R = 0.05 (relatively fresh craters) and another, higher peak near R = 0.6 to R = 0.8 (Figure 11). The first peak (R = 0.5) is largely composed of craters visually classified as fresh or very slightly degraded (Classes A and B), whereas the higher peak is composed of visually moderately to highly degraded craters (Classes C, D, and E). The strong correspondence between the letter classification system based on visual characteristics of craters and the quantitative measurement of crater depth from MOLA topography indicates that the visual classification is a reliable indicator of degradation state. The lack of appreciable degradation and the size frequency distribution of craters in Classes A and B (Figure 12) are consistent with their constituting the population of post-Noachian craters within the region. The distribution of the remaining craters, presumably the Noachian population, thus displays strong negative skewing, indicating most of the craters are highly degraded. Also noteworthy is that the shape of this bimodal distribution does not appear to be a strong function of crater diameter within the range of 10–30 km diameter craters (Figure 13).
 A variety of Noachian temporal histories of crater production and degradation might have produced this distribution of crater degradation. Two end-members are explored here. The first is that this distribution resulted from degradation of a production (or, possibly saturation) population of fresh impact craters by a short-lived episode of modification late in the Noachian. This episodic model seems inconsistent with the lack of difference in the shape of the degradation frequency function, R, with crater diameter. Equations (19) and (20) above indicate that both eolian and fluvial modification act more swiftly on smaller craters. If the episodic model were appropriate, then the distribution of R values for smaller craters should be more negatively skewed than for larger craters.
 The other model to be explored is the steady state model, in which the rate of crater production and degradation were proportional to each other (although not necessarily temporally constant). Assuming that elapsed time, T, to a given degradation state, R, is a power function with exponent β (e.g., equations (16), (17), (19), and (20)), the frequency of craters in a given degradation state, f(R), should be proportional to ∂T/∂R,
Thus, for example, a simple model of a constant rate of crater floor buildup, such as was proposed by Opik [1965, 1966] and Hartmann  as representing eolian deposition (β = 1) would give a uniform frequency distribution of observed craters as a function of R (Figure 14). The simulation modeling of eolian crater infilling (16) suggests β = 0.77, giving a slightly positively skewed distribution (Figure 14). Fluvial infilling modeling, on the other hand, suggests β ≥ 1.4 (19 and 20), producing a negatively skewed distribution. The frequency distribution for Case 1 fluvial simulations is more similar to the observed distribution of R for degradation classes C through E in the range 0 < R< 0.8 than are the Case 2 simulations (compare Figures 11 and 14). The less strongly skewed distribution for Case 2 simulations occurs because erosion rates are limited by the rapidity of bedrock weathering. We conclude that, if the steady state model is reasonably accurate, fluvial degradation was primarily responsible for degradation of Noachian craters in the 10–100 km diameter range, and that the rate of crater degradation was not strongly limited by the rate of conversion of bedrock to colluvium. Clearly, however, eolian infilling becomes dominant in degradation of small craters during the post-Noachian (e.g., Figure 4), and in some locations, such as Arabia, appreciable thickness of sedimentary deposits have been emplaced and eroded [Moore, 1990; Malin and Edgett, 2000]. The origin of these deposits is controversial but may be eolian.
 The downturn of the frequency distribution of Sinus Sabaeus craters for degradation state beyond R = 0.8 (Figure 11) can be attributed to several factors: 1) highly degraded craters are hard to recognize in images; 2) older craters are more likely to have been eradicated by later impacts or so strongly modified that crater shape statistics could not be collected; and 3) older craters are more likely to have their rim breached by fluvial drainage either entering or leaving the crater; we excluded such craters from our morphometric sample. The simulations are not subject to these exclusions, so that the frequency-relative depth curves (Figure 14) do not show a leveling and downturn for R > 0.8.
3.2. Size-Frequency Distribution of Craters
 The steady state model also has implications for the size-frequency distribution of craters in the Sinus Sabaeus area. If production and eradication of craters in a given size range are balanced, then the number of observed craters should be proportional to the average survival time, T, of craters of that size. If we estimate survival time by that duration required to reach an advanced state of degradation (say R = 0.8), then equations (16), (17), (19), and (20) can be used to predict the dependency of survival time on crater diameter. If the survival time is a power function of diameter with power μ,
and the cumulative production rate ∂N/∂t (number ≥ D per unit area per unit time) is a power function of diameter with exponent ϑ, then the observed cumulative number density, N', should also be a power function equal to the product of production rate and survival time [Hartmann, 1971, 1999]:
Hartmann and Neukum  suggest that ϑ = −1.8 for crater production in the range 1 < D < 32 km and ϑ = −2.2 for D > 32 km. Hartmann and Neukum  and Hartmann et al.  have generated a synthetic size-frequency curve for ancient cratered terrain on Mars (Figure 12) under the assumption that eolian infilling dominates crater degradation in the range of 1 to 50 km, with a slope N′ ∝ D−1.0, which is roughly consistent with our simulations of eolian sedimentation (17). Fluvial erosion should produce an even stronger reduction in the slope ϑ + μ to values approaching zero (using exponents for μ from equations (19) and (20)). The size-frequency curve for the Sinus Sabaeus region is strongly convex in the region from 10 km to 70 km with the slope decreasing from zero in the 12–26 km range through −1.1 in the 26–50 km range to about −2.6 in the 50–100 km range (Figure 12). We interpret this distribution to imply a gradual transition from a production or saturation distribution for craters >50 km to a steady state fluvial degradation distribution in the 10–25 km range.
 As a cautionary note to the above analysis, some studies suggest that the downturn of crater frequency at small diameters on heavily cratered terrains may only be partially due to degradation. Differences in the size-frequency distribution of the impacting populations may be at least partially responsible for the downturn in crater density at diameters <50 km since some size-frequency distribution analyses of fresh impact craters on Noachian-aged units also display this downturn [see Barlow, 1990]). Our analysis of fresh class A and B craters in the Sinus Sabaeus Quadrangle, however, shows a linear trend in the size-frequency distribution in the >10 km size range that is consistent with Hartmann's  production function (Figure 12).
 Degradation of craters by fluvial erosion and deposition in simulations results in rapid initial infilling but a slowing rate through time (Figure 5) likely due to the decreasing height of interior crater walls and the increasing area of deposition as the crater enlarges due to crater wall erosion. By contrast, simulated eolian infilling occurs at a nearly constant rate (Figure 1). If the rate of crater production and crater degradation were roughly balanced during the Noachian, a dominance of degradation by eolian infilling would imply roughly equal numbers of craters (for a given size range) in all stages of infilling. However, if fluvial erosion were dominant, only a few craters would be in initial stages of infilling and most craters would be at advanced stages of sedimentation, with low crater walls. This pattern of large numbers of strongly degraded craters is, in fact, what is observed in the Sinus Sabaeus region of the Martian highlands (Figure 11).
 For both eolian and fluvial crater degradation the length of time required to produce any specified fraction of crater infilling increases with crater diameter. As a result, as suggested by Hartmann [1971, 1999], the steepness of size-frequency crater curves should be reduced in those diameter ranges strongly affected by degradation. For the Sinus Sabaeus quadrangle the observed distribution of Noachian craters (Classes C, D, and E in Figure 12) is consistent with a gradual transition from a production or saturation distribution for craters >50 km to a steady state fluvial degradation distribution in the 10–25 km diameter range.
 In summary, our analysis of statistics of relative crater degradation and size-frequency distributions in the Sinus Sabaeus quadrangle confirms earlier conclusions that fluvial erosion was the dominant degradation process [Craddock and Maxwell, 1993; Craddock et al., 1997; Craddock and Howard, 2002] and also suggests that rates of crater production and of crater degradation were in rough balance during the Noachian epoch. If future studies find that Noachian craters were significantly modified by other processes, such as ice induced glacier-like flow or energetic mass wasting, then our conclusions would need to be revised.
 This research was supported by the NASA Planetary Geology and Geophysics Program and the Mars Data Analysis Program.