Catálogo de publicaciones - revistas

<jats:title>ABSTRACT</jats:title> <jats:p>Vertical bed scale heterogeneity in six massive sandstone beds is investigated using digital image analysis to determine flow processes. Images parallel to the bedding plane and perpendicular to the apparent grain long-axis orientation were acquired to minimize the uncertainty in the grain-size and fabric, and increase the statistical significance of the data. Hypothesis testing was used to reduce the subjectivity in assigning vertical trends within each bed. Results show that a significant part of the deposit contains statistically significant vertical variation in grain-size and fabric (ρ-values &amp;lt; 0.01). At the bed scale, grain-size can be normally graded or non-graded. However, at shorter length scales, complex grading patterns emerge in the different percentiles of the grain-size distribution, including “oscillating,” “diverging,” and “converging” trends involving the fine- and coarse-tail percentile. Grain fabrics in the bedding-parallel sections show a consistently flow-oblique trend with an average azimuthal deviation of 48°, but becoming increasingly flow aligned at the tops of most beds. The majority of the bedding-perpendicular sections show imbrication angles &amp;gt; 15°, with an average imbrication angle of 78°. Both up- and down-current imbrication polarities are observed in equal abundance. These textural trends are interpreted as a product of active near-bed sedimentation processes that operate in high concentration near-bed layers, which develop at the base of concentrated, turbulent flows, and active fluidization processes that operate during sediment deposition. The short length-scale grain-size trends are likely a reflection of fluctuations in the sediment concentration in these near-bed layers and elutriation, which led to differential grain segregation processes influencing the different grain-size percentiles. The high shear stresses and frequent grain interaction in the near-bed layers, with concomitant fluidization, also generate the oblique bedding-parallel fabric and very high imbrication angles.</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>In southern New Mexico and West Texas, USA, the Late Cambrian–Early Ordovician Bliss Formation is a relatively thin and dominantly siliciclastic succession that was deposited on the Proterozoic basement during a major global transgression. The Bliss Formation can be divided into two members: 1) a lower, coarser-grained member composed mostly of sandstone (quartz arenite and subarkose) that lacks glauconite and calcite cement, and 2) an upper, finer-grained member that includes glauconitic sandstone, arkosic sandstone, and mixed siliciclastic–carbonate siltstone to fine-grained sandstone, intercalated with thin carbonate beds of grainstone, packstone, and rudstone. Iron oolite and oolitic sandstone are locally exposed at the base of the upper member. Sandstone of the lower member represents upper-shoreface to foreshore deposits, whereas sedimentary structures in the upper member indicate deposition in a middle- to lower-shoreface setting, and locally in a tidal-flat environment. Intercalated carbonate beds are storm layers (tempestites). Glauconite grains are abundant in the upper member as mostly rounded to well-rounded, spheroidal to ovoidal pellets. Two types of glauconite grains are present: homogeneous, dark green grains with high K2O contents (&amp;gt; 8 wt.%; stage 4) and mottled pellets composed of a mixture of glauconite and apatite. Glauconite of the Bliss Formation is not autochthonous as proposed by earlier workers, but of allochthonous (parautochthonous) origin. Thus, the glauconite grains were reworked from deeper shelf environments in northern Mexico to the south and were transported and deposited under regressive–transgressive conditions. Mottled glauconite grains formed by the reworking of phosphatized and glauconitized micritic sediments during regression and were transported and deposited by storm-induced currents, particularly in storm layers during transgressive events. Homogeneous, mature glauconite grains probably were derived from the reworking of glauconitized fecal pellets or completely glauconitized micritic sediments during regressive–transgressive cycles. The world-wide occurrence of glauconite in Cambrian–Early Ordovician sediments indicates that glauconite formation during that period can be considered as a “global event.”</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>This study investigates the impacts of sample preparation procedures on grain-size measurements to determine comparability of data collected using differing methodologies. Grain-size distributions of marine and terrestrial sediments contain important information about the depositional environment. For example, the “sortable-silt index” (or mean grain size between 10 and 63 μm in marine sediments, is used as an indicator of flow speed and has been applied to the reconstruction of ocean current strength before the instrumental period. Similarly, the mean grain size of a sediment is used to classify it (e.g., silt versus sand). Accurate measurements of grain-size distributions often require chemical pre-treatments in order to remove sedimentary components of biogenic origin (e.g., shells), and multiple ways to perform these pre-treatments exist. This study tests whether the choice of pre-treatment introduces variability into grain-size distributions. We simulate multiple commonly used pre-treatments on a well-characterized internal standard (“Sillikers”) and compare the resulting mean size and sortable-silt index in each treatment group to untreated samples using ANOVA. Two instruments, a Coulter Counter Multisizer III and a Coulter LS 230 Laser Diffraction Analyzer are used. Results from the Multisizer III suggest that the choice of pre-treatment method does not significantly impact the final grain-size distributions but underlines the importance of replicates. Results from the laser sizer suggest that oven-drying leads to a small but statistically significant difference of ∼ 0.3 μm in the sortable-silt index, and drying samples via hot plate leads to another small but statistically significant difference of ∼ 0.29 μm. While it is unclear what causes these differences in the laser sizer data, they are smaller than the observed variations in sortable-silt index used to infer changes in current speed in a typical paleoclimate study. In conclusion, grain-size measurements are a robust tool for sediment analysis and are resistant to changes from differing pre-treatment methods tested here.</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>Deep-water channel and levee deposits are common depositional elements on modern and ancient continental slopes. Unlike their channel counterparts, the spatial and temporal evolution of levee stratigraphy is much less well understood, in part because of the typically more recessive nature of levee deposits in the ancient sedimentary record, and sparse, widely spaced core control or seismic images of insufficient resolution in the modern. Moreover, it is generally inferred that levee development, at least in part, precedes the main phase of channel filling, the reasons for which remain largely unknown. In the Isaac Formation of the Windermere Supergroup (Neoproterozoic) of east-central British Columbia, Canada, well-exposed levee deposits are divided vertically into packages, each consisting of a sand-rich lower part overlain sharply by a mud-rich upper part. The lower part (3–10 m thick) consists mostly of medium- to thick-bedded, upper medium- to coarse-grained, lower-division turbidites intercalated with thin-bedded, fine-grained, upper-division turbidites. Along depositional strike away from channel-fill margins, the thickness of lower-division turbidites exhibit a distinctive thickening and then thinning over a few hundreds of meters that results in a similar thickening and thinning of the entire lower part of a package. The upper part (3–16 m thick) consists mostly of thin-bedded, fine-grained, upper-division turbidites intercalated with uncommon medium- to thick-bedded, medium-grained, lower-division turbidites. Significantly, the thickness of very thin- and thin-bedded turbidites in the upper part generally decreases stratigraphically upward whereas the thickness of intercalated medium- and thick-bedded turbidites changes little. The lateral and vertical changes in these deposits suggest that channelized flows were initially coarse grained and moderately well-sorted, causing them to exhibit negligible density stratification, and therefore high flow efficiency. We interpret that the velocity maximum occurred above the height of the incipient channel margins, thereby allowing the lower, coarse-grained, dense part of flows to easily overspill and deposit thick-bedded, coarse-grained turbidites in the lower part of each package. The sharp contact with the upper part of each package marks the point when relief from channel floor to levee crest exceeded the height of the velocity maximum in average throughgoing turbidity currents. Above this height, density of the flow decreased abruptly and consisted of significantly finer-grained sediment that overspilled to form the upper, finer-grained part of each package. Later the makeup of the sediment supply changed to a more polydispersed grain-size distribution, which caused the throughgoing currents to be more density stratified. This enhanced near-bed stratification and concentration effects, which in addition to intense interfacial mixing, resulted in rapid kinetic energy loss, and promoted deposition in the channel.</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>Compound clinoforms contain both shoreline and subaqueous clinoforms, both with a topset–foreset–bottomset morphology, but with a wide subaqueous platform (30–150 km) in between. Recent datasets suggest that compound clinoforms are common in tide-dominated deltas, but there are only a few good examples from ancient deposits. The limited vertical expression of the shoreline clinoform and the lateral extent of the subaqueous clinoform hamper the identification of compound clinoforms in the rock record. The modern Colorado River Delta, in Baja California, Mexico, is tide-dominated and exhibits a compound clinoform; we use this delta as an analog to guide our interpretation of the ancient (Pliocene) Colorado delta in Southern California. The outcrops of the Deguynos Fm. are a representative section of the Pliocene Colorado delta. Four stratigraphic sections were measured from the outcrops, seven facies associations are recognized, and three depositional environments are interpreted using the nearby modern Colorado delta as an analog system. The Deguynos Fm. exhibits at least 22 parasequences organized in 4 stratigraphic parasequence sets; the parasequences (∼ 12 ky each) are likely autogenic stratigraphic responses, while the parasequence sets (∼ 62 ky each) are interpreted as a combination of eustatic changes and tectonic response to the creation of accommodation space along the West Salton Detachment Fault. The comparison between the Pliocene and modern Colorado deltas provides an excellent opportunity to better understand ancient compound clinoform deposits and to aid recognition of this morphology in other locations.</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>Carbonate contourite drifts formed by bottom currents are common on modern sea floors but are rarely defined in the rock record. Regional subsurface well-log mapping in the northern Delaware Basin in southeast New Mexico, USA, reveals early Permian carbonate-dominated elongate, mounded accumulations along the slope of the western margin of the basin. Thickness maps also show possible moats oriented oblique to depositional dip. The thickness variations and moat geometries are hard to explain by deposition from gravity flows but are consistent with deposition from bottom currents with a counterclockwise deflection in the basin. The contourite drift system consists of three large elongate carbonate drifts that form in relation to significant bathymetric irregularities which may alter currents, resulting in localized drift accumulations along the slopes.</jats:p> <jats:p>These findings highlight the significant role bottom currents play in shaping carbonate margin and slope architecture, rivaling the impact of gravity flows. Furthermore, full-scale assessment of the basin geometry and deposits provide insight into paleo-oceanographic circulation that is inherently difficult to assess. Identification of these large sedimentary bodies requires extensive basin-wide data sets, which were acquired by decades of work in the Permian Basin, as well as comparison with drifts in modern carbonate settings. These new interpretations in one of the most data-rich geologic regions in the world indicate that drift systems may be easily overlooked and are likely more common in the ancient rock record than currently recognized.</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>Reconstructing the paleohydraulics of ancient fluvial systems has important implications when determining channel-body dimensions in the subsurface as well as aiding source-to-sink studies and quantitatively determining the impact of changing climatic conditions. We undertake a paleohydraulic analysis of the Upper Jurassic Salt Wash distributive fluvial system (DFS) of the Morrison Formation, SW USA, to determine if downstream trends such as decreasing channel size and discharge, inferred in studies of DFS, are present. Channel depth was estimated using cross-set height values and preserved bar thickness. Nine localities across the exposed part of the Salt Wash system were studied. In total, 49 bars were measured, full bar thickness was determined from 12 complete bars, and average cross-set height was calculated for 37 bars. Estimates of maximum bankfull channel depth were derived from measured bar thicknesses. Bar height was then obtained and converted to mean bankfull channel depth using a shape adjustment factor of 0.65. The bar-derived mean bankfull channel depths were then used to derive a factor for which dune cross-set heights could be converted to mean bankfull channel depth (4.6) and maximum bankfull channel depth (7.1). These factors were then applied to localities where only cross-set height data were available, thus allowing consistent comparison and extrapolation of mean bankfull channel depth over the preserved DFS area. The use of measured bar thicknesses to calibrate estimates of mean channel depth from reconstructed dune heights is considered a useful approach, with the factor of 4.6 estimated here being lower than that (6 to 10) commonly used in comparable studies.</jats:p> <jats:p>The datasets for the Salt Wash DFS record systematic downstream trends in cross-set height, bar thickness, calculated channel depth, estimated channel width, and estimated Q, with variability and overlap between the proximal to medial, and medial to distal parts. The variability superimposed on the regional downstream trends is attributed to a combination of autocyclic processes such as variations in discharge, depth of scour, and avulsion as well as more regional-scale channel-belt switching together with allocyclic controls. The wide spatial distribution of the dataset in this study allows distinction between local autocyclic controls and regional downstream trends. Formative discharge shows no downstream trend across the entire Salt Wash DFS, with a wide range in coefficient of variation of preserved cross set thickness (CV(dst) values of 0.1 to 1.1) indicative of flashy (variable) discharge.</jats:p> <jats:p>The spatial distribution of the Salt Wash dataset allows extrapolation of trends upstream to the unexposed part of the system that allows insights into the characteristics of the channel system in the apex area (∼ 150 km to the southwest and removed by post depositional erosion). The fluvial system would have a mean depth of 9 m, and a bankfull-depth discharge of around 1450 m3/s with mean cross-set heights of between 50 and 70 cm. These estimates are in line with those from present-day DFSs in the Himalayan and Andean foreland basins that have a scale similar to that estimated for the Salt Wash system.</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>Recent studies have shown that distributive fluvial systems are the dominant fluvial forms in modern continental sedimentary basins, thus composing a large part of the stratigraphic record. This study provides a basin-scale architectural analysis of the Guará Formation, from the Upper Jurassic record of southwestern Gondwana, and attempts to compare the formation's depositional model to those developed for distributive fluvial system (DFS) successions. This time interval is significant because it was a period of intense tectonic activity related to the Paraná–Etendeka plume and the Gondwana breakup. Quantitative analyses were performed on stratigraphic sections at 17 locations (exposing a total of 720 m of stratigraphy) located in southern Brazil and northern Uruguay, from a larger dataset of 64 locations (comprising a total of 1070 m of stratigraphy). Four facies associations were identified: perennial fluvial channel fills, ephemeral fluvial channel fills, floodplain deposits, and aeolian deposits, indicating a dryland climate. Spatial trends were analyzed along a downstream-oriented transect (NNE–SSW) across the system. Grain size, channel-body thickness, number of stories, and bar thickness decrease downstream, indicating a reduction in channel depth, flow capacity, and channelization of the fluvial system, interpreted to be associated with downstream-increasing bifurcation, infiltration, and evapotranspiration. Based on spatial trends and distribution of facies associations, the deposits are interpreted to have been accumulated from a large DFS which can be divided into four zones, from proximal to distal: Zone 1, dominated by perennial fluvial channels; Zone 2, a mixture of perennial and ephemeral channels; Zones 3 and 4, deposits situated externally of the fluvial channel belts dominated by aeolian and floodplain deposits prevailing in each zone, respectively. The Guará Formation likely records the stratigraphic signature of the largest distributive fluvial systems reconstructed from both modern and ancient datasets, and one of the first where fluvio–aeolian interaction is quantified. The Guará Formation DFS model presented herein is key to understanding paleoenvironmental, paleoclimatic, and geotectonic changes related to Gondwanan fragmentation.</jats:p>

<jats:title>ABSTRACT</jats:title> <jats:p>The rarely witnessed process of river avulsion repositions channels across floodplains, which influences floodplain geomorphology and stratigraphic architecture. The way avulsions redirect water and sediment is typically generalized into one of two styles. Avulsions proceeding through rapid channel switching and producing little to no floodplain disturbance are annexational, while those that involve sequential phases of crevassing, flooding, and eventual development of a new channel are progradational. We test the validity of these avulsion style categories by mapping and characterizing 14 avulsion events in Andean, Himalayan, and New Guinean foreland basins. We use Landsat data to identify how avulsions proceed and interpret the possible products of these processes in terms of geomorphic features and stratigraphy. We show that during annexation the avulsion channel widens, changes its meander wavelength and amplitude, or increases channel thread count. During progradation, avulsion channels are constructed from evolving distributary networks. Often beginning as crevasse splays, these networks migrate down the floodplain gradient and frequently create and fill ponds during the process. We also see evidence for a recently defined third avulsion style. Retrogradation involves overbank flow, like progradation, but is marked by an upstream-migrating abandonment and infilling of the parent channel. Avulsion belts in this study range from 5 to 60 km in length, and from 1 to 50 km in width. On average, these events demonstrate annexational style over 22.4% of their length. Eleven of 13 events either begin or end with annexation, and seven both begin and end with annexation. Only one event exhibited progradation over the entire avulsion-belt length. While there are many documented examples of purely annexational avulsions, we see little evidence for completely progradational or retrogradational avulsions, and instead suggest that a given avulsion is better envisioned as a series of spatiotemporal phases of annexation, progradation, and retrogradation. Such hybrid avulsions likely produce significantly greater stratigraphic variability than that predicted by the traditional end-member model. We suggest that a time-averaged, formation-scale consideration of avulsion products will yield more accurate characterizations of avulsion dynamics in ancient fluvial systems.</jats:p>

<jats:title>Abstract</jats:title> <jats:p>Deep-marine strata consisting of a sandy basal part overlain sharply by a muddier and mud-clast-rich upper part are increasingly being recognized in the deep-marine sedimentary record, and have been termed linked debrites, cogenetic debrite–turbidite beds, hybrid event beds, transitional-flow deposits, and bipartite beds. These composite strata are generally reported to develop downflow of clean (less muddy) sand, but the variable distance (hundreds of meters to tens of kilometers) over which this lithological change is reported to take place has resulted in a variety of physical depositional models. As such, the details about the origin and spatial evolution of these admixed sand–mud strata still remain poorly understood. Part of this uncertainty is that many earlier studies, with a few exceptions, have been based on macroscopic observations in drill core or discontinuous outcrops, and therefore interpreted bed continuity is based on similarity of textural or other sedimentological attributes. However, in slope to proximal basin-floor deposits of the Neoproterozoic Windermere Supergroup, and distal basin-floor deposits of the Ordovician Cloridorme Formation, exceptional outcrop exposure permitted individual two-part (bipartite) facies and their associated strata to be continuously traced and lithological changes to be documented along the strike of the outcrop.</jats:p> <jats:p>In both the Windermere and the Cloridorme, the bipartite facies consists of a lower sandy (25–60% matrix) part overlain sharply by a muddier (40–80% matrix), commonly mud-clast-rich upper part, and occurs downflow of muddy sandstone and upflow of sandy mudstone in a hundreds-of-meters long proximal to distal depositional continuum. These strata are then overlain everywhere by a thin- to very thin-bedded, traction-structured sandstone and/or silty mudstone cap. Notably, the interface separating the lower sand-rich part from the upper mud-rich part in the bipartite part of the depositional transect is always planar in the Windermere, but often alternates between planar and irregular in the Cloridorme. The continuum is interpreted to represent deposition downflow of an avulsion node that resulted in erosion of the local mud-rich seafloor and charged the flow with fine-grained sediment, resulting in increased effective fluid viscosity and significant changes in the characteristics, intensity, and transfer of fluid turbulence needed to maintain the particle suspension. Collapse of the suspension and development of overcapacity conditions resulted in rapid particle settling in the now rapidly depleting and negligibly sheared mud-enriched suspension that formed along the margins of the avulsion-wall jet in proximal-basin-floor and slope deposits (Windermere), or at the downflow terminus of the flow in more distal basin-floor deposits (Cloridorme). Additionally, when normalized to the total length of the continuum, the transition from muddy sandstone to bipartite facies and bipartite facies to sandy mudstone are equally proportioned in all examples, suggesting that, once formed, the depleting suspension evolved in a spatially systematic and dimensionally proportionate manner—a consistent depositional evolution difficult to reconcile with two mechanistically different parts to the flow. Moreover, differences in the morphology of the bipartite interface (i.e., planar vs. irregular) is not a primary depositional feature, but instead is interpreted to be a consequence of local postdepositional deformation of a previously continuous planar surface.</jats:p>