Relevant bibliographies by topics / Piggyback Basin

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  1. Journal articles
  2. Dissertations / Theses
  3. Book chapters
  4. Conference papers

Academic literature on the topic 'Piggyback Basin'

Author: Grafiati
Published: 4 June 2021
Last updated: 1 February 2022

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Journal articles on the topic "Piggyback Basin"

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Salazar, Migdalys, Lorena Moscardelli, William Fisher, and Maria Antonieta Lorente. "Tectonostratigraphic evolution of the Morichito piggyback basin, Eastern Venezuelan Basin." Marine and Petroleum Geology 28, no. 1 (2011): 109–25. http://dx.doi.org/10.1016/j.marpetgeo.2009.07.004.

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Zoetemeijer, R., S. Cloetingh, W. Sassi, and F. Roure. "Modelling of piggyback-basin stratigraphy: Record of tectonic evolution." Tectonophysics 226, no. 1-4 (1993): 253–69. http://dx.doi.org/10.1016/0040-1951(93)90121-y.

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Cook, Frederick A., and Elizabeth A. Clark. "Middle Proterozoic piggyback basin in the subsurface of northwestern Canada." Geology 18, no. 7 (1990): 662. http://dx.doi.org/10.1130/0091-7613(1990)018<0662:mppbit>2.3.co;2.

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Ferrière, Jacky, Jean-Yves Reynaud, Andreas Pavlopoulos, et al. "Geologic evolution and geodynamic controls of the Tertiary intramontane piggyback Meso-Hellenic basin, Greece." Bulletin de la Société Géologique de France 175, no. 4 (2004): 361–81. http://dx.doi.org/10.2113/175.4.361.

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Abstract The Meso-Hellenic Basin (MHB) is a large, narrow and elongated basin containing up to c. 5 km of Cenozoic sediments, which partially covers the tectonic boundary between the external, western zones (Pindos) and the internal, eastern zones (Pelagonian) of the Hellenide fold-and-thrust belt. New results, based on micropaleontologic, sedimentologic and tectonic field data from the southern half of the MHB, suggest that the MHB originated as a forearc basin during the first stages of a subduction (Pindos basin), and evolved into a true piggyback basin as a result of the collision of thicker crustal units (Gavrovo-Tripolitsa). The late Eocene forearc stage is marked by sharply transgressive, deep sea turbiditic deposition on the subsiding active margin. At this stage, large scale structures of the Pelagonian basement (i.e. the newly defined “Pelagonian Indentor”) control deposition and location of two main subsiding sub-basins located on both sides of the MHB. The Eocene-Oligocene boundary corresponds to a brief tectonic inversion of the basin, at the onset of collision (main compressive event). The true piggyback stage (Oligo-Miocene) is recorded by slope deposition and dominated by gravity processes (from slumped, fine grained turbidites to conglomeratic fan- or Gilbert-deltas). The new elongated geometry of the MHB is controlled by the underthrusted, NNW-SSE trending, thick external zones. During this stage, the locus of subsidence migrates in the same direction (eastward) as underthrusting. This subsidence, favoured by thick dense ophiolitic basement, is attributed to basal tectonic erosion of the upper Pelagonian unit while the tectonic structures of this upper unit control the stepped migration of subsidence. Growing duplexes in the Gavrovo underthrusted unit, which formed local uplifts, were mainly situated on the eastern side of the subsiding areas and associated with normal faulting (late Oligocene–early Miocene). They constituted new loads that could also have been responsible for minor but widespread lithospheric subsidence. The development of the local and regional uplifts explains the basin evolution toward shallow, dominantly conglomeratic deposits and its final emergence at the end of the middle Miocene. This trend toward emersion is emphasized by the late Miocene global sea-level fall. The MHB was subsequently overprinted by neotectonic deformation associated with the development of a continental basin (Ptolemais) and uplift attributed to the evolution of the Olympos structure that developed further east as the underthrusting moved in this direction. These results demonstrate that the Meso-Hellenic Basin evolves as a large scale piggyback Basin and that its sedimentary infill is largely controled by tectonic activity rather than only eustatic sea-level variations.
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Philip, G., N. S. Virdi, and N. Suresh. "Morphotectonic evolution of Parduni Basin: An intradun piggyback basin in western Doon valley, NW Outer Himalaya." Journal of the Geological Society of India 74, no. 2 (2009): 189–99. http://dx.doi.org/10.1007/s12594-009-0121-x.

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Lash, Gary G. "The Shochary Ridge sequence, southeastern Pennsylvania—a possible Ordovician piggyback basin fill." Sedimentary Geology 68, no. 1-2 (1990): 39–53. http://dx.doi.org/10.1016/0037-0738(90)90118-d.

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Nijman, Wouter. "Cyclicity and basin axis shift in a piggyback basin: towards modelling of the Eocene Tremp-Ager Basin, South Pyrenees, Spain." Geological Society, London, Special Publications 134, no. 1 (1998): 135–62. http://dx.doi.org/10.1144/gsl.sp.1998.134.01.07.

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Wagreich, Michael. "A 400-km-long piggyback basin (Upper Aptian-Lower Cenomanian) in the Eastern Alps." Terra Nova 13, no. 6 (2001): 401–6. http://dx.doi.org/10.1046/j.1365-3121.2001.00362.x.

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Hippolyte, J. C., J. Angelier, F. Roure, and P. Casero. "Piggyback basin development and thrust belt evolution: structural and palaeostress analyses of Plio-Quaternary basins in the Southern Apennines." Journal of Structural Geology 16, no. 2 (1994): 159–73. http://dx.doi.org/10.1016/0191-8141(94)90102-3.

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Lawton, Timothy F., and James H. Trexler, Jr. "Piggyback basin in the Sevier orogenic belt, Utah: Implications for development of the thrust wedge." Geology 19, no. 8 (1991): 827. http://dx.doi.org/10.1130/0091-7613(1991)019<0827:pbitso>2.3.co;2.

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Dissertations / Theses on the topic "Piggyback Basin"

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Chanvry, Emmanuelle. "Caractérisation et facteurs de contrôle des distributions minéralogiques du Bassin Piggyback de Graus-Tremp-Ainsa (Espagne), à l’Eocène Inférieur." Thesis, Lyon, 2016. http://www.theses.fr/2016LYSEM034/document.

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Cette thèse propose une méthodologie pour caractériser et intégrer les distributions minéralogiques des dépôts de l’Eocène Inférieur du Bassin de Graus-Tremp-Ainsa dans un cadre séquentiel reconstruit à haute résolution. Le couplage des approches stratigraphiques et géochimiques/minéralogiques permet d’évaluer la part des forçages tectoniques, climatiques, eustatiques et diagénétiques sur l’enregistrement sédimentaire et minéralogique du bassin. La caractérisation de la minéralogie repose sur un calcul automatisé utilisant la géochimie multi-élémentaire et calibré ponctuellement par les outils d’analyse minéralogique conventionnels (pétrographie, DRX, Qemscan, microsonde). Elle a l’avantage de permettre de traiter les évolutions minéralogiques à l’échelle du bassin et sur l’ensemble des lithologies rencontrées. Après avoir évalué les effets de la diagenèse, du tri hydrodynamique et reconstitué la composition minéralogique primaire des sédiments, nous caractérisons les différentes sources.Nous précisons l’évolution de la tectonique (avec un pas de temps de l’ordre du million d’années) et ses effets sur l’architecture sédimentaire et la minéralogie des dépôts. Ceux-ci montrent un contrôle spatial de la diagenèse et des changements spatio-temporels des sources, liés à une compétition entre la tectonique intrabassinale (activité des chevauchements locaux) et régionale (surrection de l’orogène et subsidence flexurale). Nous montrons également que l’impact de la tectonique est modulé par des anomalies climatiques ponctuelles de l’ordre de la centaine de milliers d’années (PETM, ELMO, X-Event), que nous avons reconnues par un changement marqué des environnements de dépôt et des cortèges argileux.Deux grands épisodes régionaux caractérisent l’évolution du Bassin piggyback de Graus-Tremp-Ainsa. Le stade précoce, d’âge Ilerdien-Cuisien Inférieur, est marqué par le passage d’une rampe carbonatée mixte à des systèmes deltaïques alimentés depuis l’orogène pyrénéen par des contributions plutoniques. Cet ensemble passe ensuite à un vaste système fluvio-deltaïque au Cuisien Inférieur / Moyen, montrant l’apport de lithiques carbonatés et silicoclastiques qui coïncide avec l’émergence des nappes sédimentaires. La fin de cet épisode est marquée par la propagation du chevauchement du Montsec et de ses rampes latérales, provoquant un partitionnement du bassin, induisant la surrection du Bassin de Graus-Tremp et une forte subsidence du Bassin d’Ainsa. Ce contraste de subsidence est souligné par un partitionnement de la diagenèse, avec une kaolinisation des formations supérieures du Bassin de Graus-Tremp, liée à la percolation d’eaux météoriques, et, dans le Bassin d’Ainsa, une albitisation des grès couplée à une illitisation des smectites dans les lutites, liée à une diagenèse d’enfouissement plus marquée<br>We develop here a methodology to integrate the mineralogical record into a high resolution sequence stratigraphic framework realized in the Early Eocene Graus-Tremp-Ainsa Basin. Coupling stratigraphic with geochemical and mineralogical approaches allows us to unravel the effects of tectonics, climate, eustasy and diagenesis on basin architecture and mineralogy. An automated computed mineralogy is derived from whole-rock geochemical data, and calibrated against direct mineral quantifications (petrography, DRX, Qemscan, microprobe). It provides a basinscale view of mineral distribution, irrespective of the lithology. Diagenetic overprint and hydrodynamic sorting effects are evaluated first, then primary mineral distributions are reconstructed and ascribed to different types of sediment sources.We show that, at the million-year timescale, tectonics shape the architecture and the mineralogy of the deposits. Spatially distributed diagenesis and temporal and spatial changes in sediment sources reflect the competing effects of intrabasinal tectonics (local thrust displacements) versus basinscale flexural subsidence linked to the orogen uplift and loading. Tectonically-driven changes are also sensitive to higher frequency (100 ky) anomalic climatic events (PETM, ELMO, X-EVENT) leaving a mineralogical signal in clay fractions and environment deposits succession.The basinscale evolution displays two contrasting stages. During the Ilerdian to the lower Cuisian, a mixed carbonate ramp evolves to a set of deltaic fans of Northern (Pyrenean orogen) provenance delivering plutonic-dominated materials. Then, during the lower/mid Cuisian, they are overprinted by a large fluvial and deltaic system bringing recycled carbonates and siliciclastics sourced in the emerging eastern to southern sedimentary thrust sheets. Later on, the propagation of the Montsec thrust and its lateral ramp decouples the uplifted Graus-Tremp basin from the strongly subsiding Ainsa basin. These different subsidizing schemes are underlined diagenetic overprints diverge, with an extensive kaolinisation of the uppermost units in the Graus-Tremp Basin driven by meteoric fluid circulations, and a severe albitisation of sandstones in the Ainsa basin, coupled with the illitisation of smectites in the lutites and caused by deep basinal fluids
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Kao, Stephen Chung-Yen, and 高仲彥. "Development of Pliocene-Holocene piggyback basins in Western Taiwan Foreland Basin System：Examples from Taichung and Kao-ping basins." Thesis, 2012. http://ndltd.ncl.edu.tw/handle/40186809466872417426.

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博士<br>國立臺灣海洋大學<br>應用地球科學研究所<br>101<br>The Taichung and Kao-ping basins, two small scale piggyback basins of the Taiwan foreland basin, have developed since Pliocene. Both basins were formed and filled while being carried on moving thrust sheets. The stratigraphic architecture and the lithofacies of both basins were studied in details. This paper has recognized sixteen lithofacies, which are grouped into ten facies associations and interpreted in ten distinct depositional environments. Based on analysis of evolution of depositional environments in both basins, associated with biostratigraphy and westwards propagation of thrust faults, we reconstruct the development in the Taichung and Kao-ping basins. Around 2.78 Ma, the Taichung basin was characterized by offshore environment during an underfilled stage. Later, the Shuangtung Fault located to the east of the Western Foothills began to thrust westwards and uplifted strata east of the Shunangtung Fault. The uplifted strata became sediment sources for the underfilled Taichung basin. The basin between the Shuangtung and Chelungpu faults has been filled with sediments, resulting upward coarsening sequence from offshore to fluvial during filling up stage. Then, the Chelungpu Fault thrust westwards and formed uplifted ramps to shed sediment filling the basin east of the Tachia Fault during filled to overfilled stages. After 0.46 Ma, the Tachia Fault began to thrust westwards and the sediments located immediately to the east of the Tachia Fault were uplifted to form ramps with about 300 m relief, producing the Houli and Tatushan tablelands respectively, thrust sheets east of tableland carries sediments of filling piggyback basins in the front of the Chelungpu Fault. Orogenic sediments mainly are transported westwards by Da-an, Tachia and Dadu streams to fill the Chingshui Coastal Plain. After 4.46 Ka, the basin in the coastal plain was dominated by fluvial environment during the overfilled stage. About 3.6 Ma, the Kao-ping basin was characterized by offshore environment during an underfilled stage. Later, the basin to the west of the Chaochou Fault has been filled with sediment, resulting upward coarsening sequence from offshore to tidal flat. Around 0.78 Ma, the Kao-ping basin was characterized by lagoon/barrier island complex during filled stage. Thereafter, this basin was dominated by gravel-braided stream environment during overfilled stage. Then, the Chishan Fault thrust westwards to uplift middle Pliocene to Pleistocene sediments to form ramps with about 400 m relief. The thrust sheet east of the Chishan Fault moves westwards and carry the filling piggyback basin in the front of the Chaochou Fault. The Taichung basin is bounded by Tachia and Shunangtung faults with the Chelungpu Fault in the middle part. Faults sequentially westwards thrusting, the Chelungpu Fault uplifted late Pliocene to Pleistocene sediments to the west of the Shunangtung Fault to become part of the Western Foothills. The present piggyback basin is bounded by Tachia and Chelungpu faults and currently is experiencing syn-deformational deposition. The Kao-ping basin is bounded by Chishan and Chaochou faults. The current piggyback basin is formed by westwards thrusting of the Chishan Fault associated with carried on thrust sheets. Coarsening upwards sequences with westwards thrusting sheets in the piggyback basins of Taichung and Kao-ping basins can be analogous to those in the piggyback basins of the Po and Ebro basins in Europe.
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Bens, Ashley Elizabeth. "Architecture of deposits formed in a tectonically generated tidal strait, upper Baronia Fm., Ager Basin, South Central Pyrenees, Spain." Thesis, 2011. http://hdl.handle.net/2152/ETD-UT-2011-05-3429.

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The upper Baronia Fm. of the Ager Basin, Spain, is composed of a hierarchy of prominently stacked sets of primarily unidirectional cross-strata in units up to 40m thick. These large sets of cross-strata are interpreted as deposits of migrating subaqueous tidal simple dunes, compound dunes, and compound dune complexes within an approximately 10km wide north-east to south-west oriented seaway with water depths of a calculated 60-90m. These interpretations are opposed to prior interpretations of the upper Baronia Fm. which suggests deposits were formed by tidal bars within a deltaic environment (Mutti et al., 1985). Dunes developed due to dominantly north-east directed tidal currents driven through the strait by tidal phase differences between the two bodies of water (Mediterranean and Atlantic basins) connected by the seaway. Evidence for syn-tectonic deposition further constrains timing of movement of the northern basin bounding Montsec thrust to the early Eocene. Indicators for movement on the Montsec thrust include the development of the Ager Basin elongate to the thrust front, and syn-tectonic signals in the fill of the basin such as local conglomerate wedges and emplacement of olistoliths. Individual cross-stratified successions are interpreted to have formed with variable flow velocity and orientation, resulting in a basin wide stacking of compound dune complexes. These compound dune complexes form cross stratified successions which are distributed throughout the basin according to the variable current speeds, dune size which impacts migration, and sediment availability during deposition. This results in the observed distributions of muddy and sandy sediments, where finer grained materials accumulate preferentially in the low energy troughs of the hierarchy of compound dunes.<br>text
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Book chapters on the topic "Piggyback Basin"

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Hogan, P. J., and D. W. Burbank. "Evolution of the Jaca piggyback basin and emergence of the External Sierra, southern Pyrenees." In Tertiary Basins of Spain. Cambridge University Press, 1996. http://dx.doi.org/10.1017/cbo9780511524851.023.

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Mascle, A., L. Endignoux, and T. Chennouf. "Frontal Accretion and Piggyback Basin Development at the Southern Edge of the Barbados Ridge Accretionary Complex." In Proceedings of the Ocean Drilling Program. Ocean Drilling Program, 1990. http://dx.doi.org/10.2973/odp.proc.sr.110.163.1990.

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Jurado, M. J., and O. Riba. "The Rioja Area (westernmost Ebro basin): a ramp valley with neighbouring piggybacks." In Tertiary Basins of Spain. Cambridge University Press, 1996. http://dx.doi.org/10.1017/cbo9780511524851.026.

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Huyghe, Pascale, Jean-louis Mugnier, Roger Griboulard, Yann Deniaud, Eliane Gonthier, and Jean-claude Faugeres. "Chapter 14 Review of the tectonic controls and sedimentary patterns in late neogene piggyback basins on the barbados ridge complex." In Sedimentary Basins of the World. Elsevier, 1999. http://dx.doi.org/10.1016/s1874-5997(99)80048-3.

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Coogan, James C. "Chapter 2: Structural evolution of piggyback basins in the Wyoming-Idaho-Utah thrust belt." In Geological Society of America Memoirs. Geological Society of America, 1992. http://dx.doi.org/10.1130/mem179-p55.

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Conference papers on the topic "Piggyback Basin"

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Haeussler, Peter J., Richard W. Saltus, Richard G. Stanley, et al. "THE PETERS HILLS BASIN, A NEOGENE PIGGYBACK BASIN ON THE BROAD PASS THRUST FAULT, SOUTH-CENTRAL ALASKA." In GSA Annual Meeting in Seattle, Washington, USA - 2017. Geological Society of America, 2017. http://dx.doi.org/10.1130/abs/2017am-307924.

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A. Castilla, R., N. Ellouz, and J. P. Brun. "Reflection Termination Patterns in Piggyback Basins of the Makran Accretionary Prism." In 69th EAGE Conference and Exhibition incorporating SPE EUROPEC 2007. European Association of Geoscientists & Engineers, 2007. http://dx.doi.org/10.3997/2214-4609.201401898.

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Ravet, Fabien, Atle Børnes, Carlos Borda, Even Tjåland, Halfdan Hilde, and Marc Niklès. "DEH Cable System Preventive Protection With Distributed Temperature and Strain Sensors." In 2012 9th International Pipeline Conference. American Society of Mechanical Engineers, 2012. http://dx.doi.org/10.1115/ipc2012-90274.

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Hydrate and wax formation in subsea flowlines is a major cause of production impairment. Among various approaches used to minimize the risk, Direct Electrical Heating (DEH) is being applied. DEH is based on passing a current through the pipe wall to mitigate heat losses from the fluid to the surroundings during events which require flow assurance measures. The Piggyback Cable, a high voltage cable attached to the DEH pipeline, is during operation exposed to thermal and mechanical loads which may be critical for the integrity of the DEH system. The overall safety requirement is that any potential Piggyback Cable fault is detected and disconnected from the power source before damage is caused to the pipeline. Conventional cable fault detection methods based on current measurements give adequate protection for the main part of the pipeline. However, for the far end of the Piggyback Cable complementary fault detection is required. A method based on fiber break monitoring has been qualified for this purpose. The new method is implemented in the North Sea on two DEH pipelines operated by Statoil, 43 and 21 km long respectively. The protection is facilitated by standard single-mode fibers integrated into the DEH cables. Although not basis for the design the integrated fibers open up possibilities for temperature and strain sensing using stimulated Brillouin scattering. Sensing has been performed on a 43 km DEH pipeline using the DITEST AIM (Distributed Temperature and Strain Asset Integrity Monitoring). Analysis of the sensing results reveal that distributed fiber optic sensing is capable of pin-pointing thermal events and strain induced loads for an object of this length.
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E. Padron de Carrillo, C., E. Deville, P. Huyghe, G. Mascle, and J. Schmitz. "Seismic Facies and Piggyback Basins Analysys between the Front of the Prism of Barbados and the Delta of Orinoco." In 69th EAGE Conference and Exhibition incorporating SPE EUROPEC 2007. European Association of Geoscientists & Engineers, 2007. http://dx.doi.org/10.3997/2214-4609.201401818.

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Ogata, Kun, Daisuke Shiramatsu, Yoshiyuki Ohmura, and Yasuo Kuniyoshi. "Analyzing the “knack” of human piggyback motion based on simultaneous measurement of tactile and movement data as a basis for humanoid control." In 2009 IEEE/RSJ International Conference on Intelligent Robots and Systems (IROS 2009). IEEE, 2009. http://dx.doi.org/10.1109/iros.2009.5354176.

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Manouchehri, Soheil. "Subsea Pipelines and Flowlines Decommissioning: What We Should Know for a Rational Approach." In ASME 2017 36th International Conference on Ocean, Offshore and Arctic Engineering. American Society of Mechanical Engineers, 2017. http://dx.doi.org/10.1115/omae2017-61239.

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Offshore and subsea decommissioning will increase in the next five years or so as many producing fields are matured and cease production while the oil price continues to remain low. This emphasizes the need for a thorough decommissioning plan to ensure a safe and technically feasible solution while it is economically viable and safeguards the environment. Offshore and subsea decommissioning is commonly considered on a case-by-case basis using the Comparative Assessment (CA) process in which the best decommissioning solution is obtained. Health, Safety and Environmental (HSE) considerations are always paramount in any decommissioning process. The aim is to significantly reduce the long term risks to other benefactors of the sea while the associated short term risks to those responsible for decommissioning operations are minimized. A major part of any decommissioning project is subsea pipelines decommissioning (by “pipelines”, it is meant to include flowlines, trunklines and flexible too). There are a number of techniques available for decommissioning of subsea pipelines ranging from preservation for potential future use to full recovery or leaving in-situ. However, each subsea pipeline decommissioning technique should be considered on its own merit. Selection of each decommissioning technique depends on many parameters, inter alia, size of pipeline, type of pipeline (e.g. single pipe, pipe-in-pipe, piggyback), type of conveying fluid, operational environment (location), production history, Inspection, Repair and Maintenance (IRM) records, HSE considerations, connection to other facilities, technical feasibility (including potential use of advanced technologies), regulatory authorities requirements and socio-economic considerations. This paper will look at specifics of subsea pipelines decommissioning. It will examine the procedures to be undertaken from desk top activities (e.g. planning and CA) up to operational activities (e.g. pigging, flushing, cleaning, removal or leaving in-situ). Different scenarios are discussed and potential advantages and disadvantages of each scenario are presented. In addition, a guide is proposed for future pipelines decommissioning projects to follow a rational approach.
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