Engineering topics
Publications and source records attributed to Woronow, A..
As a portion of the Martian surface becomes more densely cratered, the more the surface and subsurface materials become laterally redistributed and impact metamorphosed. Specimen redistribution is characterized as a function of both impact density and original specimen depth, and the impact histories of those specimens are also characterized.
Even relatively young surfaces on Mars have superposed craters and must carry a dusting of impact debris. For increasingly more ancient surfaces, deposits of ejecta generally increase in thickness, and the signatures of the geology beneath become more obscured. Although nothing can be done about this obscuration, these newer deposits can be described, temporally and spatially, and thereby avoid falsely interpreting the geology beneath. The task of temporal and spatial characterization was begun by considering the areal variability of ejecta cover with increasing exposure to meteorite bombardment. This study establishes a baseline for evaluating the quality and distribution of exposures of strata lying temporally beneath the ejecta. Of special interest is the distribution of ejecta overlying surfaces that have never sustained a direct impact by a large meteorite, for these retain the volcanic and sedimentary stratigraphy in its most pristine state.
Two techniques proposed for the recovery of the crater production functions on densely cratered surfaces were appraised. The first technique classifies craters according to their degree of rim preservation, then interprets the statistics of the freshest craters as closely mimicing the full population's production function. This method is misleading for densely cratered surfaces. The second technique measures and weighs each crater diameter by the fraction of the crater that remains unoverlapped by subsequent impacts. The method is theoretically sound even at saturation crater densities, though it too fails at high densities.
Computer models of cratered surfaces often use inputs of uncertain nature and importance. This work evaluates the sensitivity of the resulting crater-saturation estimates to the input parameters, principally applicable to the study of craters upward from 8km diameter. In order of decreasing importance, crater saturation simulations are found to be sensitive to: (1) the dynamic range of crater diameters used; (2) the effectiveness of ejecta-blanket obliteration assumed; and (3) the number of points taken to describe the crater rim. The size of the largest crater in proportion to the size of the simulated surface has no effect on the results when the edges of the simulated surface are correctly treated and craters are counted by the fraction of the crater within the simulated area. A similar procedure is recommended when gathering crater size-density data from images.
A Monte Carlo model of lunar megaregolith development is proposed. Minimum megaregolith depths are obtained in the preliminary model. The model impacts a gridded, initially flat surface area randomly, with points not constrained to grid intersections. Information is recorded at grid points on evolving topography, deepest depth impacted to, and number of hits at that location. Two types of lunar surfaces ar simulated, maria and highlands. Crater production functions are after run to densities that are multiples of observed lunar crater densities for craters of 8 km in diameter and larger. all craters are considered to have formed in a gravity scaled regime. Edge effect problems are corrected in this model by allowing craters forming outside the grid area or along its edges to effect the gridded area.
The use of a new Monte Carlo model to examine the development of the lunar megaregolith through impact cratering processes is discussed. The simulation incorporates some of the features and assumptions of the models of Short and Forman (1972), Gault et al. (1974), Quaide and Oberbeck (1968), Oberbeck et al. (1973, 1975), and Hoerz et al. (1976); and also greatly improves on some of these features. The problem of edge effects in computer modeling is resolved, and information on the geometry of craters and their ejecta blankets, as well as on crater production functions are included in the model. It is shown that this new model predicts greater megaregolith thicknesses than did the other models. The increase is due to the use of the observed lunar highlands crater size-frequency curve as the production function, to the retention of topographic information as cratering proceeds, and to the differences in the crater bowl and ejecta geometries.
Computer models of cratered surfaces often use inputs of uncertain nature and importance. This work evaluates the sensitivity of the resulting crater-saturation estimates to the input parameters, principally applicable to the study of craters upward from 8 km diameter. In order of decreasing importance, crater saturation simulations are found to be sensitive to: (1) the dynamic range of crater diameters used, (2) the effectiveness of ejecta-blanket obliteration assumed, and (3) the number of points taken to describe the crater rim. The size of the largest crater in proportion to the size of the simulated surface has no effect on the results when the edges of the simulated surface are correctly treated and craters are not counted simply by integers. Craters should be counted by their fractions lying within the simulated area. A similar procedure is recommended when gathering crater size-density data from images.
Two techniques proposed for the recovery of the crater-production functions on densely cratered surfaces have been appraised. The first technique classifies craters according to their degree of rim preservation, then interprets the statistics of the freshest craters as closely mimicking the full population's production function. Although commonly practiced, in fact, this method is demonstrably misleading for densely cratered surfaces. The second technique uses a weighting scheme to recover the production function. Each crater diameter measured is weighed by the fraction of the crater that remains unoverlapped by subsequent impacts. While this method is theoretically sound even at saturation crater densities, it too fails at high densities due to practical difficulties. For this technique to work effectively, one would have to be able to recognize and accurately measure the diameters of craters having less than 10 percent of their rims remaining, a feat beyond reasonable expectation.
Advances in Planetary Geology is a new series intended to serve the planetary geology community with a form for quick and thorough communications. There are no set lists of acceptable topics or formats, and submitted manuscripts will not undergo a formal review. All submissions should be in a camera ready form, preferably spaced, and submitted to the editor.
A first analysis is presented of what the Galilean satellites' crater production function is, along with some interpretations of the conclusion. The basic premise is that the larger crater population of the lunar highlands is not at saturation density. The saturation issue is addressed, showing why the concept of saturation of lunar highlands can no longer be regarded as the best hypothesis, at least for large craters. The cratering records of Mars, Mercury, and the moon are reviewed and synthesized, and crater characteristics and statistics for Callisto and Ganymede are discussed and interpreted. It is shown that even the very densely cratered lunar highlands still retain considerable information about their production function; that remarkable similarities exist among the cratering histories of all of the terrestrial planets, both in terms of their production functions and of their total crater densities; and that the Gallilean satellites seem to have experienced quite a different impact history from that of the terrestrial planets.
Three dissertations are provided covering (1) the stochastic evolution of asteroidal regoliths and the origin of brecciated and gas-rich meteorites; (2) ridge systems on Mars; and (3) the morphology and evolution of Ganymede and Callisto.
Voyager 1 observations reveal heavily cratered surfaces on Ganymede and Callisto which suggest that a period of heavy bombardment occurred in the outer solar system. The overall crater density on Ganymede indicates that the oldest regions began recording the observed crater population at a later time than Callisto. A diameter-dependent loss of craters from 10-40 km occurs on Ganymede and may be due to ice formation or the formation of arcuate troughs. Evidence is given which suggests that the population of bodies responsible for the period of late heavy bombardment in the inner solar system is very different from that responsible for the late heavy bombardment in the outer solar system. In addition, it is postulated that Ganymede and Callisto may principally record a population of bodies that never penetrated the inner solar system in numbers great enough to leave a recognizable signature.
By comparing results of Monte Carlo simulations of the crater population on Callisto with the observed surface, it is demonstrated that the relative dearth of large craters on Ganymede and Callisto, compared with the terrestrial planets, can not be totally ascribed either to craters relaxing or to craters piercing a thin icy crust. Consequently, the population of objects responsible for the heavy bombardment of the Jovian system differed markedly from that responsible for the late heavy bombardment of the terrestrial planets.
This second issue in a new series intended to serve the planetary geology community with a form for quick and thorough communications includes (1) a catalog of terrestrial craterform structures for northern Europe; (2) abstracts of results of the Planetary Geology Program, and (3) a list of the photographic holdings of regional planetary image facilities.
Measurements of extents of rampart ejecta deposits as a function of the size of the parent craters support models which, for craters larger than about 6 km diameter, constrain ejecta blankets to all have a similar maximum thickness regardless of the crater size. These volatile-rich ejecta blankets may have failed under their own weights, then flowed radially outward. Assuming this to be so, some of the physicomechanical properties of the ejecta deposits at the time of their emplacement can then be determined. Finite-element studies of the stress magnitudes, distributions, and directions in hypothetical Martian rampart ejecta blankets reveal that the material most likely failed when the shear stresses were less than 500 kPa and the angle of internal friction was between 26 and 36 deg. These figures imply that the ejecta has a water content between 16 and 72%. Whether the upper limit or the lower limit is more appropriate depends on the mode of failure which one presumes: namely, viscous flow of plastic deformation.
Studies using different measurement resolutions on a single morphologic feature may yield vastly different measured values for the perimeter. Apparent internal inconsistencies such as these have greatly impeded the numerical taxonomy, description, and modeling of landforms. Fortunately, the underlying internal consistency of measurements can often be reestablished by introducing the Hausdorff-Besicovich dimension into the analysis. This is demonstrated here by the example of perimeter-area ratio measurements made on some of the complicated ejecta deposits that surround many Martian meteorite-impact craters.
Research reports concerning the planetary geology of Mars are presented. Topics covered include the geomorphology of Martian valleys and various aspects of Martian volcanology.
A study of the Martian rampart and pedestal craters in the Coprates quadrangle is presented. Relationships between crater size and ejecta-blanket areal extents imply a maximum ejecta-blanket thickness or maximum rim height for Martian rampart craters; the limiting thickness is encountered only for craters exceeding 6 km diameter. The larger craters have an additional component of internal flow of the ejecta caused by the greater weight of their thicker ejecta deposits, although smaller rampart craters have ejecta which appears to have undergone flow during emplacement; pedestal craters most likely result from impacts into less volatile-rich substrates which produce a less fluidized ejecta and no flow lobes.