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FIG. 3 in Stratigraphy and sedimentology of Neogene mammal bearing deposits in the Akkașdağı area, Turkey
FIG. 3. — Generalized stratigraphy of the Kaman-Keskin area. Names of the lithostratigraphic units are from previous studies mostly from Birgili et al. (1975).
FIG. 1 in Stratigraphy and sedimentology of Neogene mammal bearing deposits in the Akkașdağı area, Turkey
FIG. 1. — Primary geological elements of Central Anatolia and location of the study area; 1, Tertiary sedimentary basins; 2, Rodop- Pontid block; 3, Sakarya continent; 4, Galatian volcanic complex; 5, Ophiolitic melange; 6, KırSehir continent; 7, Taurus block (see text for details). A, Ankara; Ç, Çorum (map modified from Karadenizli 1999).
Text-fig. 4. Sedimentological log of the Main Cenoceras Bed and associated strata in the Quantocks Beds (Lyra Subzone) at Helwell Bay, Doniford (measured at NGR ST 0802 4314 and ST 0336 4305). BGS bed no. refers to bed numbers employed in Whittaker and Green (1983). in 'Cenoceras Islands' In The Blue Lias Formation (Lower Jurassic) Of West Somerset, Uk: Nautilid Dominance And Influence On Benthic Faunas
Text-fig. 4. Sedimentological log of the Main Cenoceras Bed and associated strata in the Quantocks Beds (Lyra Subzone) at Helwell Bay, Doniford (measured at NGR ST 0802 4314 and ST 0336 4305). BGS bed no. refers to bed numbers employed in Whittaker and Green (1983).
Magnetic and sedimentologic properties of siliciclastic cave sediments from the Muierilor Cave (Romania)
<p>Rock-magnetic and sedimentologic data of the siliciclastic sediments from the Muierii Cave (Southern Carpathians, Romania). These data were published by Mirea et al. (2021), Last deglaciation flooding events in the Southern Carpathians as revealed<br> by the study of cave deposits from Muierilor Cave, Romania, Palaeogeography, Palaeoclimatology, Palaeoecology, 562,110084 (https://doi.org/10.1016/j.palaeo.2020.110084).</p>
Magnetic and sedimentological properties of siliciclastic cave sediments from the Peștera cu Oase Cave
<p>Magnetic and sedimentological properties of siliciclastic cave sediments from the Peștera cu Oase Cave (South Carpathians, Romania: 45.030009° N, 21.835320° E, 617 m). Further details can be found in Panaiotu et al. (2013).</p>
A global review of subaqueous spreading and its morphological and sedimentological characteristics: A database for highlighting the current state of the art
<p>Subaqueous spreading, a type of extensional mass transport that is characterized by a ridge and trough<br> morphology, has been documented globally but is poorly understood. Subaqueous spreading is observed on<br> gently inclined surfaces (typically <3◦) when sediment bodies experience a sudden reduction of shear strength<br> along their basal plane during clay softening or liquefaction of sands or silty sand sediment. Historically,<br> spreading has been associated with very large landslides, but many unknown aspects of these mass movements<br> have yet to be clarified. Does spreading influences the large catastrophic failure? What are the sedimentological<br> and morphological aspects that contribute in initiating this process? These are some of the research questions<br> that spurred the present work. Here, we introduce a database that incorporates information from thirty-two case<br> studies, and use this to provide key insights into the sedimentary and morphological aspects of subaqueous<br> spreading that will assist in the identification of spreading elsewhere. We find that subaqueous spreading is most<br> common along passive glacial margins, but is also observed along active margins. The occurrence of contourites<br> interlayered with glaciogenic deposits is, in most cases, associated with landslides (or landslide complexes) with<br> spreading morphology. The database shows that seismic loading is commonly suggested to be the dominant<br> trigger mechanism, although more geotechnical observations and modelling analysis would be needed to support<br> this conclusion. We compare subaqueous spreading with terrestrial spreading, in particular to earthquake-related<br> lateral spreading and clay landslides. We find that subaqueous spreading shares the same driving processes and<br> potentially also some of the trigger mechanisms that are associated with the terrestrial spreading cases. Future<br> work will be required to address the association between spreading and its occurrence on some of the largest<br> landslides on Earth, its development mechanism, and its potential hazard implications.</p>
Fig. 1 Simplified geological map 1 in Oligocene - Lower Miocene Biostratigraphy And Sedimentology Of The Borşa Formation (N Romania, Maramureş Region)
Fig. 1 Simplified geological map 1:200.000 after Gherasi et al., 1967 and Patrulius et al., 1968.
FIG. 6 in Stratigraphy and sedimentology of Neogene mammal bearing deposits in the Akkașdağı area, Turkey
FIG. 6. — Continued.
FIG. 6 in Stratigraphy and sedimentology of Neogene mammal bearing deposits in the Akkașdağı area, Turkey
FIG. 6. — Continued.
FIG. 5 in Stratigraphy and sedimentology of Neogene mammal bearing deposits in the Akkașdağı area, Turkey
FIG. 5. — Field appearance of the type section of the AkkaSdağı Fm.
FIG. 2 in Stratigraphy and sedimentology of Neogene mammal bearing deposits in the Akkașdağı area, Turkey
FIG. 2. — Geological map of the study area (from Seyitoğlu et al. 2005). See Figure 1 for location.
Dataset for modelling the apparent von Kármán parameter in thermally and sedimentologically stratified air flows
<p>The dataset is used to support the article titled as "Modelling the apparent von Kármán parameter in thermally and sedimentologically stratified air flows" by the same authors. There are two spreadsheets in the datasheet.xlsx file. The first one is the 5-min block averaged data derived from the measurements by a meterologoical tower. The second one is the sand transport and saltation sensor data derived from a number of 5-10 min measurements by sand trap stacks and a Sensit.</p> <p><strong>1. Description for Spreadsheet "Tower Data":</strong></p> <p> Date: Data collection date</p> <p>Run_number: the run number counting from the start of the experiment. Measurements were taken for 5 min for each run.</p> <p>UA1: resultant wind speed (m/s) measured by a 2D ultrasonic anemometer at 0.19 m above the bed</p> <p>UA2: resultant wind speed (m/s) measured by a 2D ultrasonic anemometer at 0.49 m above the bed</p> <p>UA3: resultant wind speed (m/s) measured by a 2D ultrasonic anemometer at 0.76 m above the bed</p> <p>UA: resultant wind speed (m/s) measured by a 3D ultrasonic anemometer at 1.49 m above the bed</p> <p>R_square: the R<sup>2</sup> value for log-linear curve fitting between wind speed measured by ultrasonic anemometers and elevation</p> <p>R_f: flux Richardson number R<sub>f</sub></p> <p>u_star: shear velocity u<sub>*</sub> (m/s)</p> <p>zeta: stability parameter ζ</p> <p>phi_m: dimensionless wind shear Φ<sub>m</sub></p> <p>kappa_a: apparent von Kármán parameter κ<sub>a</sub></p> <p>KE: KE values measured by Sensit</p> <p>Q: Calculated sediment transport rate Q ( g m<sup>-1</sup> s<sup>-1</sup>) using KE-Q relationship described in spreadsheet "Trap data"</p> <p> </p> <p><strong>2. Description for Spreadsheet "Trap Data":</strong></p> <p>KE: KE values measured by Sensit</p> <p>Q: sediment transport rate Q ( g m<sup>-1</sup> s<sup>-1</sup>) measured by sand traps</p> <p>The figure with regression equation describes the relationship between KE and Q.</p>
Supplementary Data for Provenance, Environments, and Tectonic Signatures of Tanjong-Sandakan Formations, Northeast Sabah, Malaysia: Implications for Sedimentology, Palynology, and Geochemistry
<p>This dataset includes supplementary sedimentary facies tables and geochemical analysis data used in the manuscript titled <strong>Provenance, Environments, and Tectonic Signatures of Tanjong-Sandakan Formations, Northeast Sabah, Malaysia: Implications for Sedimentology, Palynology, and Geochemistry</strong>.</p>
Fig. 5 in Oligocene - Lower Miocene Biostratigraphy And Sedimentology Of The Borşa Formation (N Romania, Maramureş Region)
Fig. 5 Calcareous nannofossils from Moisei (X 2000). a, b Coccolithus formosus (Kamptner, 1963) Wise, 1973 (Sample 1) (a - NII, b – N+); c, d Coccolithus pelagicus (Wallich, 1871) Schiller, 1930 (Sample 3); e Coccolithus cf. pelagicus (Wallich, 1871) Schiller, 1930 (Sample 3); f-h Coccolithus subpertusus (Hay & Mohler, 1967) van Heck & Prins, 1987 (= Ericsonia subpertusa Hay & Mohler, 1967) (Sample 3) (f - NII, g – N+; h – N+); i, j Helicosphaera cf. compacta Bramlette & Wilcoxon, 1967 (Sample 3) (i – NII, j – N+); k, l Reticulofenestra bisecta (Hay et al, 1966) Bukry & Percival, 1971 (Sample 2) (k – NII, l – N+); m, n Reticulofenestra cf. bisecta (Hay et al, 1966) Bukry & Percival, 1971 (Sample 1) (m – NII, n – N+); o Discoaster cf. strictus Stradner, 1961 (Sample 3) (NII); p Reticulofenestra dictyoda (Deflandre in Deflandre & Fert, 1954) Stradner in Stradner & Edwards, 1968 & R. stavensis (Levin & Joerger, 1967) Varol, 1989 (Sample 3) (N+).
Fig. 3 in Oligocene - Lower Miocene Biostratigraphy And Sedimentology Of The Borşa Formation (N Romania, Maramureş Region)
Fig. 3 Frumuşeaua Valley section at Crasna Vişeului (column B is the continuation of A and C is the continuation of B).
Fig. 2 in Oligocene - Lower Miocene Biostratigraphy And Sedimentology Of The Borşa Formation (N Romania, Maramureş Region)
Fig. 2 Moisei section from Moisei (column B is the continuation of A and C is the continuation of B).
S2 - Supporting information 1 - sedimentological data - Yeha
<p>Detailed sedimentological data along with plots showing measurement results from ICP-OES and p-ED-XRF as well as XRD plots.</p>
Fig. 4 in Oligocene - Lower Miocene Biostratigraphy And Sedimentology Of The Borşa Formation (N Romania, Maramureş Region)
Fig. 4 Repedea section from Repedea (column B is the continuation of A).
Data from: A Tournaisian (earliest Carboniferous) conglomerate-preserved non-marine faunal assemblage and its environmental and sedimentological context
A conglomerate bed from the Tournaisian Ballagan Formation of Scotland preserves a rich array of vertebrate and other non-marine fossils providing an insight into the wider ecosystem and palaeoenvironment that existed during this pivotal stage of Earth history. It challenges hypotheses of a long-lasting post-extinction trough following the end-Devonian extinction event. The fauna recovered includes a wide size range of tetrapods, rhizodonts and dipnoans, from tiny juveniles or small-bodied taxa up to large adults, and more than one taxon of each group is likely. Some fauna, such as actinopterygians and chondrichthyans, are rare as macrofauna but are better represented in the microfossil assemblage. The fauna provides evidence of the largest Carboniferous lungfish ever found. The specimens are preserved in a localised, poorly-sorted conglomerate which was deposited in the deepest part of a river channel, the youngest of a group of channels. In addition to the fossils (micro- and macro-), the conglomerate includes locally-derived clasts of palaeosols and other distinctive elements of the surrounding floodplains. Charcoal fragments represent stem and possible trunk tissue from arborescent pteridosperms. Preservation of the fossils indicates some aerial exposure prior to transport, with abrasion from rolling. The findings presented here contrast with other published trends in vertebrate size that are used to interpret a reduction in maximum sizes during the Tournaisian. The richness of the fauna runs counter to the assumption of a depauperate non-marine fauna following the end-Devonian Hangenberg event, and charcoal content highlights the occurrence of fire, with the requisite levels of atmospheric oxygen during that stage.
Data from: A Tournaisian (earliest Carboniferous) conglomerate-preserved non-marine faunal assemblage and its environmental and sedimentological context
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