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Journal articles on the topic 'Tertiary Piedmont Basin'

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Published: 9 March 2023
Last updated: 10 March 2023

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1

Natalicchio, Marcello, Francesco Dela Pierre, Pierangelo Clari, Daniel Birgel, Simona Cavagna, Luca Martire, and Jörn Peckmann. "Hydrocarbon seepage during the Messinian salinity crisis in the Tertiary Piedmont Basin (NW Italy)." Palaeogeography, Palaeoclimatology, Palaeoecology 390 (November 2013): 68–80. http://dx.doi.org/10.1016/j.palaeo.2012.11.015.

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2

Capponi, Giovanni, Laura Crispini, Laura Federico, Michele Piazza, and Barbara Fabbri. "Late Alpine tectonics in the Ligurian Alps: constraints from the Tertiary Piedmont Basin conglomerates." Geological Journal 44, no. 2 (March 2009): 211–24. http://dx.doi.org/10.1002/gj.1140.

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3

Festa, Andrea, and Giulia Codegone. "Geological map of the External Ligurian Units in western Monferrato (Tertiary Piedmont Basin, NW Italy)." Journal of Maps 9, no. 1 (January 9, 2013): 84–97. http://dx.doi.org/10.1080/17445647.2012.757711.

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4

Bonci, Maria Cristina, Davide Dagnino, Andrea Mandarino, Aaron Mazzini, and Michele Piazza. "Revision of Ostrea (Gigantostrea) gigantica Solander var. oligoplana Sacco and Ostrea (Ostrea) isseli Rovereto (Oligocene, Tertiary Piedmont Basin, NW Italy)." Carnets de géologie (Notebooks on geology) 21, no. 3 (February 24, 2021): 55–66. http://dx.doi.org/10.2110/carnets.2021.2103.

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The aim of this paper is the revision and redocumentation of Ostrea (Gigantostrea) gigantica Solander var. oligoplana Sacco, 1897, Ostrea (Ostrea) isseli n. denom. Rovereto, 1897, and Ostrea (Ostrea) isseli n. denom. var. elongata Rovereto, 1897. These taxa are from the Oligocene strata of the Molare Formation (Tertiary Piedmont Basin, southern Piedmont - central Liguria, NW Italy). The syntypes of O. (G.) gigantica var. oligoplana are in the "Collezione Bellardi e Sacco", at the Museo Regionale di Scienze Naturali di Torino; the syntypes of O. (O.) isseli and O. (O.) isseli var. elongata are in the "Collezione BTP" (BTP Collection, at the Dipartimento di Scienze della Terra, dell'Ambiente e della Vita - DISTAV - of the Università di Genova). The var. oligoplana is here moved to the species rank and allocated to the genus Pycnodonte Fischer von Waldheim, 1835. O. (O.) isseli and O. (O.) isseli var. elongata are recognized as junior synonyms of the Sacco's taxon. Rovereto (1897) compared his new species with Ostrea subgigantea Raulin & Delbos, 1855, a poorly known taxon, that is here figured for the first time and shown to represent a species different from P. oligoplana (Sacco, 1897).
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5

Martire, Luca, Marcello Natalicchio, Catalin Costel Petrea, Simona Cavagna, Pierangelo Clari, and Francesco Dela Pierre. "Petrographic evidence of the past occurrence of gas hydrates in the Tertiary Piedmont Basin (NW Italy)." Geo-Marine Letters 30, no. 3-4 (February 25, 2010): 461–76. http://dx.doi.org/10.1007/s00367-010-0189-8.

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6

Carrapa, B., and D. Garcia-Castellanos. "Western Alpine back-thrusting as subsidence mechanism in the Tertiary Piedmont Basin (Western Po Plain, NW Italy)." Tectonophysics 406, no. 3-4 (September 2005): 197–212. http://dx.doi.org/10.1016/j.tecto.2005.05.021.

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7

Lozar, Francesca, Pierangelo Clari, Francesco Dela Pierre, Marcello Natalicchio, Elisa Bernardi, Donata Violanti, Emanuele Costa, and Marco Giardino. "Virtual Tour of Past Environmental and Climate Change: the Messinian Succession of the Tertiary Piedmont Basin (Italy)." Geoheritage 7, no. 1 (February 8, 2014): 47–56. http://dx.doi.org/10.1007/s12371-014-0098-8.

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8

Maino, Matteo, Alessandro Decarlis, Fabrizio Felletti, and Silvio Seno. "Tectono-sedimentary evolution of the Tertiary Piedmont Basin (NW Italy) within the Oligo-Miocene central Mediterranean geodynamics." Tectonics 32, no. 3 (June 2013): 593–619. http://dx.doi.org/10.1002/tect.20047.

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9

Dela Pierre, Francesco, Elisa Bernardi, Simona Cavagna, Pierangelo Clari, Rocco Gennari, Andrea Irace, Francesca Lozar, et al. "The record of the Messinian salinity crisis in the Tertiary Piedmont Basin (NW Italy): The Alba section revisited." Palaeogeography, Palaeoclimatology, Palaeoecology 310, no. 3-4 (October 2011): 238–55. http://dx.doi.org/10.1016/j.palaeo.2011.07.017.

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10

Tropeano, Domenico. "High flow events and sediment transport in small streams in the ‘tertiary basin’ area in piedmont (Northwest Italy)." Earth Surface Processes and Landforms 16, no. 4 (June 1991): 323–39. http://dx.doi.org/10.1002/esp.3290160406.

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11

Federico, Laura, Laura Crispini, Gian Mario Dabove, Michele Piazza, and Giovanni Capponi. "Stratigraphic vs structural contacts in a late orogenic basin: the case of the Tertiary Piedmont Basin in the Sassello area (Ligurian Alps, Italy)." Journal of Maps 12, no. 5 (October 19, 2015): 959–67. http://dx.doi.org/10.1080/17445647.2015.1100561.

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12

Briguglio, Antonino, Grazia Vannucci, Clarissa Bruzzone, and Michele Piazza. "Stratigraphic development of a Late Oligocene Reef Complex under strong fluviatile influence in the Tertiary Piedmont Basin (Liguria, NWItaly)." Micropaleontology 67, no. 4 (2021): 315–39. http://dx.doi.org/10.47894/mpal.67.4.01.

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The modern-day decline of coral reefs due to bleaching events has been recognized as one of the major consequences of man-driven climate change. However, also eutrophication has been highlighted as an equally great danger for coral reefs and as such for biodiversity hotspots. In the latest years this phenomenon has moved to the forefront in the scientific community. Fossil reefs play a key role in studying the emergence, development and faunal/floral diversity of reef environments under eutrophic conditions. Their importance as valuable data sources for studying long-term changes of coral reef environments and their resilience cannot be disputed, especially since they may record the complete life cycle of a reef complex. In this study, nine sections nearby the town of Dego (Savona Province, NW Italy) are presented and discussed with regards to their lithostratigraphic and paleontological contents. Due to the extensive amount of data, the original morphology of a fringing reef, consisting of core, flank and fore reef, under strong fluviatile influence could be reconstructed. This study emphasizes the importance of the coralline red algae association in such biocarbonatic build-ups as major constituent and as substrate stabilizers. The sections record the original colonization event of the local basement by the builder community, the emergence of the coral reef and finally the suffocation by the fluviatile sediments. The variation of the red algae association reflects a deepening trend and is possibly correlated to enhanced fluvial input, which tends to deteriorate ecological conditions and functions as a major trigger for initial reef suffocation.
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13

Basso, Daniela, Francesca Quaranta, Grazia Vannucci, and Michele Piazza. "Quantification of the coralline carbonate from a Serravallian rhodolith bed of the Tertiary Piedmont Basin (Stazzano, Alessandria, NW Italy)." Geodiversitas 34, no. 1 (March 2012): 137–49. http://dx.doi.org/10.5252/g2012n1a8.

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14

Felletti, Fabrizio. "Statistical modelling and validation of correlation in turbidites: an example from the Tertiary Piedmont Basin (Castagnola Fm., Northern Italy)." Marine and Petroleum Geology 21, no. 1 (January 2004): 23–39. http://dx.doi.org/10.1016/j.marpetgeo.2003.11.006.

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15

Carrapa, B., G. Bertotti, and W. Krijgsman. "Subsidence, stress regime and rotation(s) of a tectonically active sedimentary basin within the western Alpine Orogen: the Tertiary Piedmont Basin (Alpine domain, NW Italy)." Geological Society, London, Special Publications 208, no. 1 (2003): 205–27. http://dx.doi.org/10.1144/gsl.sp.2003.208.01.10.

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16

Felletti, Fabrizio. "Complex bedding geometries and facies associations of the turbiditic fill of a confined basin in a transpressive setting (Castagnola Fm., Tertiary Piedmont Basin, NW Italy)." Sedimentology 49, no. 4 (August 2002): 645–67. http://dx.doi.org/10.1046/j.1365-3091.2002.00467.x.

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17

Tinterri, Roberto, and Andrea Civa. "Laterally accreted deposits in low efficiency turbidites associated with a structurally-induced topography (Oligocene Molare Group, Tertiary Piedmont Basin, NW Italy)." Journal of Sedimentary Research 91, no. 7 (July 19, 2021): 751–72. http://dx.doi.org/10.2110/jsr.2020.174.

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ABSTRACT The origin of laterally accreted deposits in ancient deep marine successions is often controversial. Indeed, not always do these features imply the occurrence of meanders or high-sinuosity turbidite channels, but they can be generated by other causes, such as sediment-gravity-flow dynamics controlled by the morphology of tectonically confined mini-basins. This work discusses laterally accreted deposits composed of sharp-based, normally graded beds in a very small tectonically controlled mini-basin. These beds, characterized by a well-defined asymmetrical cross-current facies tract, form well-developed lateral-accretion surfaces dipping in directions ranging between W and SW, and perpendicular to the paleocurrents directed towards the N. For this reason, these deposits have always been interpreted as point bars related to meandering channels. A new detailed stratigraphic framework and facies analysis have led to an alternative interpretation, namely that these deposits record lateral deflections of small volume, longitudinally segregated turbidite dense flows against a structurally controlled morphological high. This interpretation is also supported by a comparison to other tectonically controlled turbidite systems that are characterized by higher degrees of efficiency but show similar laterally accreted deposits and cross-current facies tracts.
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18

Dela Pierre, Francesco, Luca Martire, Marcello Natalicchio, Pierangelo Clari, and Catalin Petrea. "Authigenic carbonates in Upper Miocene sediments of the Tertiary Piedmont Basin (NW Italy): Vestiges of an ancient gas hydrate stability zone?" Geological Society of America Bulletin 122, no. 7-8 (March 29, 2010): 994–1010. http://dx.doi.org/10.1130/b30026.1.

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19

Cavagna, Simona, Pierangelo Clari, Francesco Dela Pierre, Luca Martire, and Marcello Natalicchio. "Sluggish and steady focussed flows through fine-grained sediments: The methane-derived cylindrical concretions of the Tertiary Piedmont Basin (NW Italy)." Marine and Petroleum Geology 66 (September 2015): 596–605. http://dx.doi.org/10.1016/j.marpetgeo.2015.04.013.

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20

Dela Pierre, Francesco, Pierangelo Clari, Elisa Bernardi, Marcello Natalicchio, Emanuele Costa, Simona Cavagna, Francesca Lozar, et al. "Messinian carbonate-rich beds of the Tertiary Piedmont Basin (NW Italy): Microbially-mediated products straddling the onset of the salinity crisis." Palaeogeography, Palaeoclimatology, Palaeoecology 344-345 (August 2012): 78–93. http://dx.doi.org/10.1016/j.palaeo.2012.05.022.

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21

Felletti, Fabrizio. "Depositional architecture of a confined, sand-rich submarine system: the Bric la Croce – Castelnuovo turbidite system (Tertiary Piedmont Basin, Oligocene, NW Italy)." Italian Journal of Geosciences 135, no. 3 (October 2016): 365–82. http://dx.doi.org/10.3301/ijg.2015.15.

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22

Grunert, Patrick, Mathias Harzhauser, Yair Rosenthal, and Giorgio Carnevale. "Estuarine Lago Mare fauna from the Tertiary Piedmont Basin indicates episodic Atlantic/Mediterranean exchange during the final stage of the Mediterranean Salinity Crisis." Palaeogeography, Palaeoclimatology, Palaeoecology 457 (September 2016): 70–79. http://dx.doi.org/10.1016/j.palaeo.2016.06.005.

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23

Felletti, Fabrizio. "Spatial variability of Hurst statistics in the Castagnola Formation, Tertiary Piedmont Basin, NW ITaly: discrimination of sub-environments in a confined turbidite system." Geological Society, London, Special Publications 222, no. 1 (2004): 285–305. http://dx.doi.org/10.1144/gsl.sp.2004.222.01.15.

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24

Rossi, Massimo, and Jonathan Craig. "A new perspective on sequence stratigraphy of syn-orogenic basins: insights from the Tertiary Piedmont Basin (Italy) and implications for play concepts and reservoir heterogeneity." Geological Society, London, Special Publications 436, no. 1 (2016): 93–133. http://dx.doi.org/10.1144/sp436.10.

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25

Natalicchio, Marcello, Daniel Birgel, Francesco Dela Pierre, Luca Martire, Pierangelo Clari, Christoph Spötl, and Jörn Peckmann. "Polyphasic carbonate precipitation in the shallow subsurface: Insights from microbially-formed authigenic carbonate beds in upper Miocene sediments of the Tertiary Piedmont Basin (NW Italy)." Palaeogeography, Palaeoclimatology, Palaeoecology 329-330 (April 2012): 158–72. http://dx.doi.org/10.1016/j.palaeo.2012.02.026.

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26

Dela Pierre, F., A. Festa, and A. Irace. "Interaction of tectonic, sedimentary, and diapiric processes in the origin of chaotic sediments: An example from the Messinian of Torino Hill (Tertiary Piedmont Basin, northwestern Italy)." Geological Society of America Bulletin 119, no. 9-10 (September 1, 2007): 1107–19. http://dx.doi.org/10.1130/b26072.1.

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27

Briguglio, Antonino, Simone Crobu, Eleni Lutaj, and Michele Piazza. "Integrated stratigraphy from a transgressive upper Oligocene section in NW Italy." Stratigraphy 18, no. 2 (June 15, 2021): 123–37. http://dx.doi.org/10.29041/strat.18.2.03.

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ABSTRACT: The Oligo-Miocene Transition (OMT) is one of the most important climatic transitions of the last 30 million years. This short period of climate warming coincides with a few biotic turnovers, which are well known in deeper marine settings where stratigraphic successions yield a detailed record; in shallowmarine environments they have been proved difficult to recognize as the occurrence and absence of certain taxa due to ecological preferences hamper the study. This study focuses on the Case Cné section in the late Oligocene of the Tertiary Piedmont Basin (TPB) as it represents a gradual transgressive event, which shows the drowning of a locally developed reef complex and development of a deeper marine sedimentary setting influenced by gravity flow mechanics. Larger foraminifera biostratigraphy was used to date the section to the late Oligocene (SBZ23); preliminary strontium isotope data confirms this result. Using sedimentological, semi-quantitative microfacies and geochemical analysis the sedimentary history of the section was reconstructed and divided into four major phases: the drowning of the reef complex, a short prograding phase of the fluvial system, the onset of gravity flow mechanics and a final transgressive phase with an initial turbiditic influence which continues regionally into the Miocene.
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28

Hupalo, О. О., S. О. Afanasiev, О. М. Lietytska, А. М. Roman, І. І. Abramiuk, N. V. Tymoshenko, and O. O. Holub. "ПОРІВНЯЛЬНА ХАРАКТЕРИСТИКА ІХТІОФАУНИ РІЧКИ СТРИЙ ТА ДІЛЯНКИ ВЕРХНЬОГО І СЕРЕДНЬОГО ДНІСТРА." Scientific Issue Ternopil Volodymyr Hnatiuk National Pedagogical University. Series: Biology 82, no. 1-2 (September 6, 2022): 51–56. http://dx.doi.org/10.25128/2078-2357.22.1-2.8.

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The qualitative analysis of fish fauna of the Stryi River and the upper and middle sections of the Dniester River is conducted, and the taxonomy and faunistic structure are analyzed. The fish assemblage investigation was carried out during 2017–2020 in different seasons of the year. Fish sampling was performed by gill nets and sweep nets. Totally 15 locations were investigated and 465 specimens were caught. It has been established that the ichthyofauna includes 24 species in the studied section of the Upper Dniester and 22 species in the section of the Stryi River. The share of rare species is rather high: for the Dniester section, 33.3 % of the species listed in the Bern Convention and 12.5 % listed in the Red Book of Ukraine, and for the Stryi River, 40.9 % and 22.7 % respectively. The similarity of the Upper Dniester and the Stryi River ichthyofauna according to Shorigin was 53.9 %. The similarity of communities according to Jaccard was 0.59. Weinstein's index of biocenological similarity of ichthyocenoses in the studied rivers was low: 0.32. The low values of similarity indices are explained by the specificity of faunal structure in the studied rivers. Ichthyofauna of the Stryi and the Upper Dniester includes six ichthyocomplexes (boreal piedmont, boreal plain, tertiary plain freshwater, Pontocaspian freshwater, Pontocaspian marine, Chinese plain). The main similarities in the ichthyofauna of these rivers are formed due to the representatives of Pontocaspian freshwater, boreal plain and Chinese plain complexes: up to 72.7 % of total ichthyofauna. There has recently been an intensive advance of alien and invasive fish species into the piedmont of the Dniester River basin, which use transformed sections of the river with the silted bottom as refuges where they settle, increase in number and spread upstream. The share of alien species was rather high and amounted to 29.2 % in the Upper Dniester and 22.7 % in the Stryi River.
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29

Bernet, Matthias, and Pierre Tricart. "The Oligocene orogenic pulse in the southern Penninic arc (western Alps): structural, sedimentary and thermochronological constraints." Bulletin de la Société Géologique de France 182, no. 1 (January 1, 2011): 25–36. http://dx.doi.org/10.2113/gssgfbull.182.1.25.

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Abstract The Oligocene evolution of the southern branch of the western Alpine arc, more precisely the stack of metamorphic Briançonnais and Piedmont nappes composing the southern Penninic arc (SPA), are the focus of this study. We review published structural, sedimentological and thermochronological data in order to discuss exhumation of the SPA. At first, we compare bedrock zircon and apatite fission-track (FT) data from the SPA with detrital thermochronologic data (zircon FT, white mica 40Ar/39Ar) from Oligocene molasse deposits. Using improved stratigraphic ages for the Barrême basin, samples from the uppermost Rupelian “Conglomérat de Clumanc” and the Chattian “Molasse Rouge” provided zircon FT lag times of ~3.5 and 8 m.y., indicating source exhumation rates on the order of ~1.5 and ~0.75 km/m.y. respectively. These short lag times are consistent with lag times of 40Ar-39Ar ages of detrital white mica from the same formations in the same basin, and also from Oligocene molasse sediments in the Tertiary Piedmont basin. The sediment source for these grains as for the associated clasts of blueschist, is identified as the HP-LT metamorphic units of the SPA. The source cannot be the Ubaye-Embrunais nappes as classically considered, because these nappes do not bear the required metamorphic imprint. This interpretation is consistent with fast Oligocene cooling of the SPA, as attested by in situ zircon and apatite FT analyses. Such fast and relatively old cooling is a peculiarity of the southern branch of the western Alpine arc, when considering the entire arc. A second range of data concerns the structural building of the SPA. The initial stacking of metamorphic nappes in a poorly elevated accretionnary wedge was completed before the end of the Eocene. During the Early Oligocene collision, this wedge was severely refolded, acquiring its fan structure, as visible in cross section, and its curvature in map view. In such a context, we propose that fast exhumation and cooling of the SPA during the Oligocene resulted from active erosion of rapidly raised high topography. This is consistent with the sudden arrival of metamorphic Penninic clasts in the molasse basins along both flanks of the belt. Moreover, detrital and in situ thermochronological ages, suggest a strong slowing down of cooling and exhumation from the Miocene onwards, coinciding with brittle extension that dominates in the SPA during this long period. The brief Early Oligocene rise of a SPA cordillera, contrasts with the preceding and subsequent period of poor relief of the SPA. The mountainous character of the SPA today is not directly inherited from the Oligocene orogenic climax, as modern high relief and elevation are most likely related to rejuvenation under climatic control during the Quaternary.
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30

Dela Pierre, Francesco, Pierangelo Clari, Marcello Natalicchio, Simona Ferrando, Roberto Giustetto, Francesca Lozar, Stefano Lugli, Vinicio Manzi, Marco Roveri, and Donata Violanti. "Flocculent layers and bacterial mats in the mudstone interbeds of the Primary Lower Gypsum unit (Tertiary Piedmont basin, NW Italy): Archives of palaeoenvironmental changes during the Messinian salinity crisis." Marine Geology 355 (September 2014): 71–87. http://dx.doi.org/10.1016/j.margeo.2014.05.010.

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31

Bertotti, Giovanni, Pietro Mosca, Joaquim Juez, Riccardo Polino, and Tibor Dunai. "Oligocene to Present kilometres scale subsidence and exhumation of the Ligurian Alps and the Tertiary Piedmont Basin (NW Italy) revealed by apatite (U-Th)/He thermochronology: correlation with regional tectonics." Terra Nova 18, no. 1 (February 2006): 18–25. http://dx.doi.org/10.1111/j.1365-3121.2005.00655.x.

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32

Thiry, Médard, Régine Simon-Coinçon, Florence Quesnel, and Robert Wyns. "Bauxitic palaeoweathering related to the Clay-with-Jurassic cherts Formation in the southeastern Paris Basin." Bulletin de la Société Géologique de France 176, no. 2 (March 1, 2005): 199–214. http://dx.doi.org/10.2113/176.2.199.

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Abstract On the southeastern margin of the Paris Basin, Nivernais region, the marine deposits have been continuous all along the Jurassic period. The sea withdrew a first time during the Upper Tithonian. This regression coincided with erosion and weathering. Apparently, the sea invaded again the Nivernais region only during the Albian, to which are attributed a few relicts of glauconitic sandstone with quartz pebbles. The youngest marine occurrences are of Santonian-Campanian age, made of silicified urchins and microfauna preserved in flint flows. The Tertiary deposits are limited to small grabens and made of nodular lacustrine limestones with charophytes ascribed to the Middle Eocene. In this southeastern margin of the basin, palaeoweathering products of the Jurassic and Cretaceous, i.e. Clay-with-Jurassic cherts and Clay-with-Cretaceous flints, are widespread. Their study allow to reconstruct the long continental evolution of the area. A red silty clay formation, with scattered cherts and abundant ferruginous gravels, containing typically from 10 to 20% of gibbsite, has been identified at Beaumont-la-Ferrière. Besides the lack of granulometric sorting of the quartz grains and of the ferruginous nodules and gravels, the micromorphologic analysis of the thin sections shows well developed illuviation structures, pointing clearly out pedogenetic features. The red silty clay formation in Beaumont-la-Ferrière relates to an in situ bauxitic palaeoprofile developed above Callovo-Oxfordian limestones. Near Beaumont-la-Ferrière, at St-Benin-d’Azy and at Ste Colombe, outliers display several weathering formations with cherts and flints that total over 50 to 80 m thickness. At the base, there is in-situ Clay-with-cherts, in which occurs the siderolithic iron ore deposits and which locally contains also gibbsite. In places, this Clay-with-cherts is topped by rounded cherts, from 3 to 10 cm in diameter, and sand lenses containing quartz gravels. The Clay-with-flints of lustreous break, translucent, with branchy morphologies and porous cortex, typical of the Clay-with-flints known elsewhere, occurs at the top of the buttes. The reworked cherts, the sand and the Clay-with-flints Formation are often silicified by typical pedogenic silicification, with illuviation features and titania-rich matrix. The palaeoweathering formations occurring in the Nivernais region allow to specify at least three successive weathering stages in the southeastern Paris Basin. (1) Development during the early Cretaceous of a thick blanket of Clay-with-cherts by weathering of the Jurassic chert-bearing limestones after withdrawal of the sea at the end of the Tithonian. Locally this weathering lead to the development of true bauxitic profiles, with gibbsite, pisolites, nodules, wide illuviation structures, etc. The development of the siderolithic iron ores relates to this weathering stage. (2) A second weathering stage, after the withdrawal of the sea during the Campanian, lead to development of Clay-with-flints from leaching of the chalk deposits. (3) Silicification affected the Clay-with-cherts and the Clay-with-flints, as well as the reworked deposits that today armour the reliefs. These silicifications display the same micromorphologic and geochemic characters as the silcretes that developed during Middle/Upper Eocene in the central parts of the Paris Basin. This is the first time that in situ Cretaceous bauxitic profiles are described north of the Massif Central. It seems likely that these bauxitic formations have been initially much more widespread, but a number of profiles may probably have been resilicified, with alteration of the gibbsite into kaolinite along the silicification of the siderolithic piedmont during the Eocene. The old pisolithic iron ore workings of the nineteenth century are located in this Clay-with-cherts Formation. In this way, the siderolithic iron ore deposits, typical from the southern margins of the Paris Basin, are of early Cretaceous age and correlative to the bauxite deposits of southern France.
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33

Thiry, Médard, Florence Quesnel, Johan Yans, Robert Wyns, Anne Vergari, Hervé Theveniaut, Régine Simon-Coinçon, et al. "Continental France and Belgium during the early Cretaceous: paleoweatherings and paleolandforms." Bulletin de la Société Géologique de France 177, no. 3 (May 1, 2006): 155–75. http://dx.doi.org/10.2113/gssgfbull.177.3.155.

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Abstract During the early Cretaceous, successive tectonic phases and several sea level falls resulted in the emersion of the main part of western Europe and the development of thick “lateritic” weathering. This long period of continental evolution ended with the Upper Cretaceous transgressions. During this period, the exposed lands displayed a mosaic of diverse morphologies and weathered landscapes. Bauxites are the most spectacular paleoweathering features, known for long in southern France. Recently, new residual outcrops have been identified, trapped in the karstic depressions of the Grands Causses. Other bauxitic formations, containing gibbsite, have also been recognised, occurring with the Clay-with-Jurassic-cherts in the southeastern border of the Paris Basin. These bauxitic formations overlay Jurassic limestone and are buried beneath Upper Cretaceous marine deposits. The recognition of bauxites up north into the southern Paris Basin significantly widens the extension of the Lower Cretaceous bauxitic paleolandscapes. On the Hercynian basements thick kaolinitic weathering mantles occur. They have been classically ascribed to the Tertiary. The first datings of these in situ paleosoils, by means of paleomagnetism and/or radiogenic isotopes, record especially early Cretaceous ages. This is the case for the “Siderolithic” formations on the edges of the French Massif Central, but also for the kaolinitic profiles in the Belgian Ardennes. In the Flanders, the Brabant basement is deeply kaolinised beneath the Upper Cretaceous cover. These paleosoils show polygenetic evolutions. The relief of these basement paleolandscapes may have been significant. There where probably high scarps (often of tectonic origin) reaching 200 m in elevation or beyond, as well as wide surfaces with inselbergs, as in the present day landscapes of tropical Africa and South America. On the Jurassic limestone platforms occur diverse kaolinitic and ferruginous weathering products. Around the Paris Basin they show various facies, ranging from kaolinitic saprolites to ferricretes. Due to the lack of sedimentary cover, the age of these ferruginous and kaolinitic weathering products has been debated for long, most often allocated to the Siderolithic sensu lato (Eocene-Oligocene). Recent datings by paleomagnetism have enabled to date them (Borne de Fer in eastern Paris Basin) back also to the early Cretaceous (130 ± 10 Ma). These wide limestone plateaus show karstified paleolandforms, such as vast closed and flat depressions broken by conical buttes, but also deep sinkholes in the higher areas of the plateaus and piedmonts. The depth of the karst hollows may be indicative of the range of relative paleoelevations. Dissolution holes display seldom contemporaneous karst fillings, thus implying that the karstland had not a thick weathering cover or that this cover had been stripped off before or by the late Cretaceous transgression. Nevertheless, some areas, especially above chert-bearing Jurassic limestone or marl, show weathering products trapped in the karst features or as a thick weathering mantle. In the Paris Basin, the Wealden gutter looked like a wide floodplain in which fluvio-deltaic sands and clays were deposited and on which paleosoils developed during times of non-deposition. The edges of the gutter were shaped as piedmonts linked up with the upstream basement areas. The rivers flowing down to the plain deposited lobes of coarse fluvial sands and conglomerates. The intensity of the weathering, the thickness of the profiles and their maturation are directly dependent on the duration of the emersion and the topographic location relative to the gutter. Near the axis of the gutter, where emersion was of limited duration, the paleoweathering features are restricted to rubefaction and argillization of the Lower Cretaceous marine formations. On the other hand, on the borders of the basin and on the Hercynian basement, where emersion was of longer duration, the weathering profiles are thicker and more intensively developed. The inventory of the Lower Cretaceous paleoweathering features shows the complexity of the continental history of this period. Moreover, the preserved weathering products are only a part of this long lasting period, all the aspects relative to erosion phases are still more difficult to prove and to quantify. In this domain, apatite fission tracks thermochronology (AFTT) can be helpful to estimate the order of magnitude of denudation. Residual testimonies and subsequent transgressions may enable to estimate relative elevations, but in return, we presently have no reliable tool to estimate absolute paleoelevations. In the work presented here, the inventory enabled to draw a continental paleogeographic map showing the nature of the weathering mantles and the paleolandscape features, just as paleoenvironments and paleobathymetry presently appear on marine paleogeographic maps. For the future, the challenge is to make progress in dating the paleoweathering profiles and especially in the resolution of these datings, in order to correlate precisely the continental records with the different events which trigger them (eustatism, climate, regional and global geodynamics). The final goal will be to build up a stratigraphic scale of the “continental geodynamic and climatic events” in parallel with “sequential stratigraphy” in the marine realm.
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34

"Climatic and tectonic control on the distributionof the Oligocene reefs of the Tertiary Piedmont Basin (NW Italy)." Italian Journal of Geosciences, no. 2 (June 2009): 587–91. http://dx.doi.org/10.3301/ijg.2009.128.2.587.

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35

Invernizzi, D., S. Reguzzi, and F. Felletti. "Petrographic data from the Oligocene-lower Langhian succession of the Arquata Scrivia area in the Tertiary Piedmont Basin (NW Italy)." Data in Brief, December 2022, 108810. http://dx.doi.org/10.1016/j.dib.2022.108810.

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36

Amadori, C., M. Maino, M. Marini, L. Casini, B. Carrapa, G. Jepson, R. G. Hayes, C. Nicola, S. Reguzzi, and A. Di Giulio. "The role of mantle upwelling on the thermal history of the Tertiary‐Piedmont Basin at the Alps‐Apennines tectonic boundary." Basin Research, January 6, 2023. http://dx.doi.org/10.1111/bre.12752.

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37

Piazza, Michele, Vannucci, Grazia, and Testa, Massimiliano. "Subterraniphyllum and free-living Neogoniolithon (coralline algae) from the Oligocene reef facies of Costa d’Ovada (Tertiary Piedmont Basin, Alessandria, NW Italy)." Italian Journal of Geosciences, no. 1 (2010). http://dx.doi.org/10.3301/ijg.2009.01.

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38

Purkait, Barendra. "Hydrogeology of Brahmaputra Basin, India." Journal of Nepal Geological Society 28 (November 2, 2003). http://dx.doi.org/10.3126/jngs.v28i0.31729.

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The Ganga-Brahmaputra river system together forms one of the largest deltas in the world comprising some 59570 sq km. The waterpower resources of the Brahmaputra have been presumed to be the fourth biggest in the world being 19.83 x 103 m3s1. The entire lower portion of the Brahmaputra consists of a vast network of distributary channels, which are dry in the cold season but are inundated during monsoon. The catchment area of the entire river is about 580,000 sq km, out of which 195,000 sq km lies in India. The maximum discharge as measured at Pandu in 1962 was of the order of 72800 m3 s-1 while the minimum was 1750 m3 s-1 in 1968. The drainage pattern in the valley is of antecedent type while the yazoo drainage pattern is most significant over the composite flood plain to the south of the Brahmaputra. The Brahmaputra valley is covered by Recent alluvium throughout its stretch except a few isolated sedimentary hills in the upper Assam, inselbergs/bornhardt of gneissic hills in the Darrang, Kamrup and Goalpara districts and a few inlying patches of Older Alluvium in the Darrang and Goalpara districts. The basin is very unstable. The present configuration of the basin is the result of uplift and subsidence of the Precambrian crystalline landmasses. Four geotectonic provinces can be delineated in the N-E India through which the Brahmaputra flows. These are bounded by major tectonic lineaments such as the basement E-W trending Dauki fault, a NE-SW trending structural feature of imbricate thrusts known as 'belt of Schuppen' and the NW-SE trending Mishmi thrust. Hydrogeologically, the Brahmaputra basin can be divided into two distinct categories, viz(a) dissected alluvial plain and (b) the inselberg zone. The first category is rep resented in the flood plain extending from the south of Sub-Himalayan piedmont fan zone in the north to right upto the main rock promontory of Garo Hills and Shillong Plateau. The inselberg zone is characterized by fractured, jointed and weathered ancient crystalline rocks with interhill narrow valley plains, consisting of thin to occasionally thick piles of assorted sediments. From the subsurface lithological data, two broad groups of aquifers are identified. These are i) shallow water table and ii) deeper water table or confined ones, separated by a system of aquicludes. The shallow aquifer materials, in general, consist of white to greyish white, fine grained micaceous sand and the thickness ranges from 1.2 to 10.3 m. The sand and clay ratio varies from 1: 2.5 to 1:26. The bedrock occurs at depth ranges of 30.4 to 39.5 m. The materials of the deeper aquifers comprise grey to greyish white, fine to medium grained sand. The sand and clay ratio varies from 1:2 to 1:7. The effective size of the aquifer materials varies from 0.125 to 0.062 mm with uniformity co-efficient around 4.00, porosity 38 to 42%, co-efficient of permeability 304 to 390 galls per day/0.3m2. The ground water is mildly alkaline with pH value 6.5 to 8.5, chloride 10 to 40 ppm, bi-carbonate 50 to 350 ppm, iron content ranges from a fraction of a ppm to 50 ppm. Total dissolved solids are low, hardness as CaCo3 50 to 300 ppm, specific conductance at 25 °C 150 to 650 mhos/cm. The yield from shallow aquifers is 1440 litres to 33750 litres/hour and for deeper aquifers ~ 1700 litres/hour at a drawdown of 13.41 m, specific capacity 21 litres/minute. The temperatures of ground water are 23°-25° C during winter, 24°-26° C during pre-monsoon and 27°- 28° C during peak monsoon. The general hydraulic gradient in the north bank is 1:800 whereas in the south bank it is 1: 300-400 The Tertiary sediments yield a range of water from 200 to 300 l.p.m whereas the yield from the Older Alluvium is 500 to 700 1.p.m. The estimated transmissibility and co-efficient of storage is of the order of ~ 800 1.p.m/ m and 8.2 x 10-3 respectively. Depths to water levels range from 5.3 to 10m below land surface (b.l.s). In the Younger or Newer Alluvium, ground water occurs both under water table and confined conditions. Depths to water levels vary from ground level to 10 m b.l.s. Depth to water ranges from 6 m b.l.s. to 2 m above land surface. The yield of the deep tubewells ranges from 2 to 4 kl/minute for a drawdown of 3 m to 6 m. The transmissibility of the aquifers varies from 69 to 1600 l.p.m/m and the storage co-fficient is of the order of 3.52 x 10-2.
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