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Дисертації з теми "Geology, Stratigraphic"

Автор: Grafiati

Опубліковано: 4 червня 2021

Оновлено: 1 серпня 2024

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1

Jutras, Pierre. "Tectonostratigraphie du carbonifère de la Gaspésie, Québec, Canada /." Thèse, Chicoutimi : Montréal : Université du Québec à Chicoutimi ;. Université du Québec à Montréal, 2001. http://theses.uqac.ca.

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Thèse (D.R.Min.) -- Université du Québec à Chicoutimi, programme extensionné à l'Université du Québec à Montréal, 2001.<br>Bibliogr.: f. 250-265. Document électronique également accessible en format PDF. CaQCU

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2

Udgata, Devi Bhagabati Prasad. "Glauconite as an indicator of sequence stratigraphic packages in a Lower Paleocene passive-margin shelf succession, Central Alabama." Auburn, Ala., 2007. http://repo.lib.auburn.edu/07M%20Theses/UDGATA_DEVI_55.pdf.

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3

Shoore, David Joseph. "Sequence stratigraphy of the Bridal Veil Falls Limestone, carboniferous, Oquirrh Group, on Cascade Mountain, Utah : a standard Morrowan cyclostratigraphy for the Oquirrh basin /." Diss., CLICK HERE for online access, 2004. http://contentdm.lib.byu.edu/ETD/image/etd775.pdf.

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4

Kertznus, Vanessa Raquel. "Stratigraphic development of delta-fed slope systems." Thesis, Available from the University of Aberdeen Library and Historic Collections Digital Resources. Restricted: no access until Jul. 3, 2013, 2009. http://digitool.abdn.ac.uk:80/webclient/DeliveryManager?application=DIGITOOL-3&owner=resourcediscovery&custom_att_2=simple_viewer&pid=56267.

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5

Elrick, Maya. "Development of cyclic ramp-to-basin carbonate deposits, lower Mississippian, Wyoming and Montana." Diss., This resource online, 1990. http://scholar.lib.vt.edu/theses/available/etd-09092008-063649/.

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6

Eifert, Tambra L. "The Cretaceous-Paleogene transition in the northern Mississippi Embayment, S.E. Missouri: palynology, micropaleontology, and evidence of a mega-tsunami deposit." Diss., Rolla, Mo. : Missouri University of Science and Technology, 2009. http://scholarsmine.mst.edu/thesis/pdf/Eifert_09007dcc80658622.pdf.

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Анотація:

Thesis (Ph. D.)--Missouri University of Science and Technology, 2009.<br>Vita. The entire thesis text is included in file. Title from title screen of thesis/dissertation PDF file (viewed May 4, 2009) Includes bibliographical references (p. 243-265).

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7

Jensen, Paul H. "Mapping and piecing together the Triassic/Jurassic stratigraphy along the south flank of the Uinta Mountains, Northeast Utah : a stratigraphic analysis of the Bell Springs Member of the Nugget Sandstone /." Diss., CLICK HERE for online access, 2005. http://contentdm.lib.byu.edu/ETD/image/etd983.pdf.

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8

Hogan, John Patrick. "Mineralogical, chemical and isotopic diversity in plutonic rock suites from the Coastal Maine Magmatic Province : the role of source region heterogeneity, tectonic setting and magmatic processes /." This resource online, 1990. http://scholar.lib.vt.edu/theses/available/etd-08082007-114045/.

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9

Morante, Richard. "Permian-Triassic stable isotope stratigraphy of Australia." Phd thesis, Australia : Macquarie University, 1996. http://hdl.handle.net/1959.14/47568.

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"September, 1995"<br>Thesis (Ph.D.) -- Macquarie University, School of Earth Sciences, 1996.<br>Bibliography: leaves 171-183.<br>Introduction -- Australian ð¹³Corg-isotope profiles about the Permian-Triassic (P/TR) boundary -- Strontium isotope seawater curve in the late Permian of Australia -- ð¹³Cco₃ AND ð¹⁸Oco₃ seawater profiles through the Permian-Triassic of Australasia -- Paleomagnetic stratigraphy about the Permian/Triassic boundary in Australia -- Synthesis.<br>The Permian-Triassic boundary mass extinction is the largest in the Phanerozoic and therefore is the major event in the Phanerozoic. The mass extinction cause is problematical but studying global geochemical and geophysical signatures about the Permian-Triassic boundary can provide insights into the cause of the mass extinction. Global events about the Permian-Triassic boundary are marked by changes in: ð¹³C values of carbon ; ⁸⁷Sr/⁸⁶Sr in unaltered marine calcite ; magnetic polarity. -- This study aims to identify these features in the sedimentary record and to test the ca libration of the Australian biostratigraphical schemes to the global geological timescale. The following features are found in the Permian-Triassic sediments of Australia: a ð¹³Corg in Total Organic Carbon excursion in 12 marine and nonmarine sections from Northwest to Eastern Australia ; a ⁸⁷Sr/⁸⁶Sr minimum in a composite section mainly from the Bowen Basin ; a magnetic polarity reversal in the Cooper Basin, central Australia. The Australian sections are thus time correlated, as follows: The negative ð¹³Corg excursion indicates the Permian-Triassic boundary and occurs: 1) in Eastern and Central Australia at the change from coal measures to barren measures with red beds at the beginning of the Early Triassic coal gap; 2) in Northwest Australia about the boundary between the Hyland Bay Formation and the Mount Goodwin Formation in the Bonaparte Basin and at the boundary between the Hardman Formation and the Blina Shale in the Canning Basin. The base of the negative ð¹³Corg excursion lies at or near the base of the Protohaploxypinus microcorpuspalynological zone. The ⁸⁷Sr/⁸⁶Sr minimum determined about the Guadalupian/Ochoan stage boundary in North America is found in the Bowen Basin about the boundary between the Ingelara and Peawaddy Formations. The ð¹³Corg excursion in the Cooper Basin is near a magnetic reversal within the Permo-Triassic mixed superchron. The implications of these findings include: confirmation of the traditional placement of the Permian-Triassic boundary at the coal measures/barren measures with redbeds boundary in Eastern Australia ; the linking of the the Permian-Triassic boundary to a mass extinction of plant species on land and the beginning of the Triassic coal gap indicated by the Falcisporites Superzone base that is coincident with the negative ð¹³Corg excursion ; a mass extinction causal model that links the ⁸⁷Sr/⁸⁶Sr minimum determined about the Guadalupian/Ochoan stage boundary to a fall in sealevel that led to changing global environmental conditions. The model invokes greenhouse warming as a contributing cause of the mass extinction.<br>Mode of access: World Wide Web.<br>xii, 183 leaves ill., maps

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10

Li, Yongxiang. "Paleomagnetism of late paleozoic to cenozoic rocks in Hong Kong, China /." Hong Kong : University of Hong Kong, 2000. http://sunzi.lib.hku.hk/hkuto/record.jsp?B21490107.

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11

Tang, Lai-kwan Denise. "Geology of Tuen Mun Area, NW Hong Kong an updated model /." Click to view the E-thesis via HKUTO, 2007. http://sunzi.lib.hku.hk/hkuto/record/B3829283X.

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12

Zumsteg, Cathy L. "Metamorphism of the Wales Group and Moria Group on Prince of Wales and Dall Islands, southeastern Alaska." Diss., Columbia, Mo. : University of Missouri-Columbia, 2007. http://hdl.handle.net/10355/5957.

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Thesis (Ph. D.)--University of Missouri-Columbia, 2007.<br>The entire dissertation/thesis text is included in the research.pdf file; the official abstract appears in the short.pdf file (which also appears in the research.pdf); a non-technical general description, or public abstract, appears in the public.pdf file. Title from title screen of research.pdf file (viewed on December 28, 2007) Includes bibliographical references.

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13

Liu, Junsuo. "Pétrogénèse des roches alcalines mafiques d'âge méso-cénozoique dans les provinces de Hunan et Guangxi, Chine septentrionale = petrogenesis of the mesosoic-cenozoic mafic alkaline subvolcanic rocks in Hunan-Guangxi provinces, southern China /." Thèse, Chicoutimi : Université du Québec à Chicoutimi, 1992. http://theses.uqac.ca.

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14

Roth, Frances Ann. "Implications of stratigraphic completeness analysis for magnetic polarity stratigraphic studies." Thesis, The University of Arizona, 1985. http://hdl.handle.net/10150/558017.

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15

Kahmann-Robinson, Julia A. Atchley Stacy C. "The sequence stratigraphic evolution of the Sturgeon Lake bank, central Alberta, Canada and its regional implications." Waco, Tex. : Baylor University, 2005. http://hdl.handle.net/2104/3016.

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16

Guj, P., and P. Guj. "The Damara mobile belt in the south-Western Kaokoveld." Doctoral thesis, University of Cape Town, 2016. http://hdl.handle.net/11427/23739.

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After the establishment of the N-S Andib-Ganamub trough, the ubiquitous Lower Nosib subarkose was succeeded in the west by the Upper Nosib greywacke which indicates that orthogeosynclinal subsidence was already active in pre-Damara times. A pulse of NNE folding (F₁N) concluded this sedinentary cycle and was accompanied by amphibolite-grade metamorphism (M₁), occasional migmatisation (A₁), and later feldspar blastesis. This episode was most intense in the west, so that the overlying Damara rocks paraconformable in the east, are unconformable there. Martin's (1965) separation of the succeeding Damara basin into a western eugeosyncline and an eastern miogeosyncline applies very well to this area, though the separating hinge-line appears to have been located farther to the west (±80 Km) of the Kamanjab inlier, along the western flank of a N-S geanticlinal belt. The Lower Bakos semipelite and lenticular carbonate, thinning out against the eastern flank of this positive element controlling the deposition, may, prior to deformation, have created a transition between the western eugeosynclinal greywacke and the eastern miogeosynclinal Lower Otari carbonates. The fractured hinge-zone provided channels for the ascent of syndepositional intrusions and volcanics. Regional erosion following upwarping in the east caused a large influx of detritus into the Khomas furrow prior to the disconformable deposition of the Tillite Substage, which is the only reliable chronostratigraphic link between the base of the Upper Otavi and that of the Upper Bakos Series, the latter partially intertongueing with the succeeding Khomas Series. Gravitational creeping of the miogeosynclinal carbonates down the western slope of the upwarped Kamanjab inlier towards the sinking basin, produced the first folding (F₂O) in the east. Almost contemporaneously, buoyant uplifting forces, related to anatexis (A₂) along the axis of the eugeosyncline, created slopes sufficient to convey nappes (F₂S) of scarcely metamorphosed Damara schists towards the eastern foreland, overriding the miogeosyncline along the N-S Sesfontein Thrust. Eastern foredeeps were rapidly filled by the Mulden molasse. Steep slip folding (F₂S and F₄) in the cores and roots, and the formation of scattered domes at depth, controlled the successive structural evolution of the nappes. Large-scale axial undulations were later produced by orthogonally superposed F₃ folds striking east. The Damaran metamorphism (M₂ ), which outlasted deformation, has a Barrovian character and grades in the Damara sediments from amphibolite (sillimanite) grade in the west to greenschist (sericite- chlorite) grade in the east. In the previously dehydrated, deformed and metamorphosed, polymetamorphic (M₁/M₂ ) Nosib terrains, retrograde parageneses and transition granulites developed to the east and to the west of the Damaran hornblende-oligoclase isograd respectively. The Damaran tectono-thermal episode culminated in advanced migmatisation of the Khomas greywacke (possibly equivalent to the Salem granite-gneiss) and final anatexis (A₂ ) in the late-kinematic Ganias -Uhima (possibly equivalent to the Donkerhoek) granite, followed by widespread feldspar blastesis. The drop in rheomorphism in the deformed mass at the margin of the migmatite zone induced intense shearing and produced belts of mylonite and cataclastic gneiss. At a later stage, the Sesfontein Thrust was buffered against the Otavi dolomite relief and its speed of advancement reduced to match that of the erosion of its frontal toe, which now separates two completely different structural-stratigraphic domains: i) an eastern miogeosynclinal, feebly metamorphosed and volcanic-free domain (Damara System, Outjo Facies) deformed into non-basement-involving tectonites, overridden by ii) a western domain of suprastructural nappes and metamorphosed eugeosynclinal sediments (Damara System, Swakop Facies) deformed in response to basementinvolving tectonic processes promoted by deeply seated anatexis along the axis of the former eugeosyncline. The present model involves many stratigraphic revisions, one of the most important being that no rocks older than the Nosib Formation outcrop in the area and possibly along most of the Damara mobile belt in the western Kaokoveld.

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17

Queen, Sandra June. "Petrologic characterization and differentiation of Neogene and Pleistocene sediments in the Verdi-Reno Truckee River corridor." abstract and full text PDF (UNR users only), 2008. http://0-gateway.proquest.com.innopac.library.unr.edu/openurl?url_ver=Z39.88-2004&rft_val_fmt=info:ofi/fmt:kev:mtx:dissertation&res_dat=xri:pqdiss&rft_dat=xri:pqdiss:1460773.

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18

Bouroullec, Renaud. "Synsedimentary fault kinematics and stratigraphic response." Thesis, Imperial College London, 2002. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.268915.

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19

Warrior, Shalina. "A paleomagnetic investigation of the Mojave-Sonora Megashear hypothesis in north-central and northeastern Mexico." To access this resource online via ProQuest Dissertations and Theses @ UTEP, 2008. http://0-proquest.umi.com.lib.utep.edu/login?COPT=REJTPTU0YmImSU5UPTAmVkVSPTI=&clientId=2515.

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20

Pak, Ŭn-ju. "Cenozoic geohistory of the southwestern margin of the Ulleung basin, East Sea." [S.l. : s.n.], 1986. http://catalog.hathitrust.org/api/volumes/oclc/53229626.html.

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21

Bullock, Michelle. "Holocene sediments and geological history, Woolley Lake, near Beachport, South Australia /." Adelaide : Thesis (B. Sc.(Hons)) -- University of Adelaide, Dept. of Geology and Geophysics, 1994. http://web4.library.adelaide.edu.au/theses/09SB/09sbb938.pdf.

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22

Anderson, Bryan James. "Evolution of coarse-grained, upper slope channel fairway deposits, Paleocene El Rosario Formation, San Carlos, Baja California, Mexico." Thesis, Montana State University, 2009. http://etd.lib.montana.edu/etd/2009/anderson/AndersonB1209.pdf.

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23

Lee, Jin-Hyung. "Stratigraphy and sedimentology of the Lower Triassic Montney Formation, Peace River Arch area /." *McMaster only, 1999.

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24

Williford, Kenneth Hart. "Biogeochemistry of the Triassic-Jurassic boundary /." Thesis, Connect to this title online; UW restricted, 2007. http://hdl.handle.net/1773/6708.

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25

Gollop, Alison. "Structural controls on the seismic sequence stratigraphy of the Ben Nevis, Avalon, and Eastern Shoals formations, Terra Nova field, Jeanne D'Arc Basin, offshore Newfoundland /." Internet access available to MUN users only, 2003. http://collections.mun.ca/u?/theses,76559.

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26

Cleveland, David M. Atchley Stacy C. Nordt Lee C. "Fluvial sequence stratigraphy and paleoclimate of the Upper Triassic (Norian-Rhaetian) Chinle Strata, northern New Mexico." Waco, Tex. : Baylor University, 2007. http://hdl.handle.net/2104/5118.

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Thesis (Ph.D.)--Baylor University, 2007.<br>In the abstract "[delta]13C" the "13" and "[delta]18O" the "18" are superscript; "pCO2" the "2" is subscript. Includes bibliographical references (p. 107-118).

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27

Cunderla, Brent Joseph. "Stratigraphic and petrologic analysis of trends within the Spencer Formation sandstones : from Corvallis, Benton County, to Henry Hagg Lake, Yamhill and Washington counties, Oregon." PDXScholar, 1986. https://pdxscholar.library.pdx.edu/open_access_etds/3588.

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Within the thesis study area Spencer Formation arkosic/arkosic lithic sandstone lithofacies of Narizian age crop out in a sinuous north-northwesterly band from the Corvallis area into the Henry Hagg Lake vicinity ten kilometers southwest of Forest Grove, Oregon.

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28

Shaw, Neil B. "Biostratigraphy of the Cowlitz Formation in the upper Nehalem River Basin, northwest Oregon." PDXScholar, 1986. https://pdxscholar.library.pdx.edu/open_access_etds/3654.

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Examination of stream and roadcut exposures of the Cowlitz Formation allows the selection of measured representative sections, and collection of fossils, from an area roughly defined by the intersection of the boundaries of Clatsop, Columbia, Tillamook and Washington counties in Oregon. The study defines the features of the local environment of deposition, correlates sections to derive a composite columnar section, and develops a checklist of species for both microfossils and megafossils of the Cowlitz Formation.

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29

Byrnes, Mark Edward. "Provenance study of late Eocene arkosic sandstones in southwest and central Washington." PDXScholar, 1985. https://pdxscholar.library.pdx.edu/open_access_etds/3405.

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The purpose of this study is to compare the sandstone composition and trace element geochemistry between samples representing the Summit Creek sandstone, Naches, Chumstick, and Carbonado Formations in order to determine if these sediments were all derived from the same provenance, and to determine the composition of the source rocks in hopes to identify the present day location of the source areas.

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30

Strauss, Toby Anthony Lavery. "The geology of the Proterozoic Haveri Au-Cu deposit, Southern Finland." Thesis, Rhodes University, 2004. http://hdl.handle.net/10962/d1015978.

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The Haveri Au-Cu deposit is located in southern Finland about 175 km north of Helsinki. It occurs on the northern edge of the continental island arc-type, volcano-sedimentary Tampere Schist Belt (TSB) within the Palaeoproterozoic Svecofennian Domain (2.0 – 1.75 Ga) of the Fennoscandian Shield. The 1.99 Ga Haveri Formation forms the base of the supracrustal stratigraphy consisting of metavolcanic pillow lavas and breccias passing upwards into intercalated metatuffs and metatuffites. There is a continuous gradation upwards from the predominantly volcaniclastic Haveri Formation into the overlying epiclastic meta-greywackes of the Osara Formation. The Haveri deposit is hosted in this contact zone. This supracrustal sequence has been intruded concordantly by quartz-feldspar porphyries. Approximately 1.89 Ga ago, high crustal heat flow led to the generation and emplacement of voluminous synkinematic, I-type, magnetite-series granitoids of the Central Finland Granitoid Complex (CFGC), resulting in coeval high-T/low-P metamorphism (hornfelsic textures), and D₁ deformation. During the crystallisation and cooling of the granitoids, a magmatic-dominated hydrothermal system caused extensive hydrothermal alteration and Cu-Au mineralisation through the late-D₁ to early-D₂ deformation. Initially, a pre-ore Na-Ca alteration phase caused albitisation of the host rock. This was closely followed by strong Ca-Fe alteration, responsible for widespread amphibolitisation and quartz veining and associated with abundant pyrrhotite, magnetite, chalcopyrite and gold mineralisation. More localised calcic-skarn alteration is also present as zoned garnetpyroxene- epidote skarn assemblages with associated pyrrhotite and minor sphalerite, centred on quartzcalcite± scapolite veinlets. Post-ore alteration includes an evolution to more K-rich alteration (biotitisation). Late D₂-retrograde chlorite began to replace the earlier high-T assemblage. Late emanations (post-D₂ and pre-D₃) from the cooling granitoids, under lower temperatures and oxidising conditions, are represented by carbonate-barite veins and epidote veinlets. Later, narrow dolerite dykes were emplaced followed by a weak D₃ deformation, resulting in shearing and structural reactivation along the carbonate-barite bands. This phase was accompanied by pyrite deposition. Both sulphides and oxides are common at Haveri, with ore types varying from massive sulphide and/or magnetite, to networks of veinlets and disseminations of oxides and/or sulphides. Cataclastites, consisting of deformed, brecciated bands of sulphide, with rounded and angular clasts of quartz vein material and altered host-rock are an economically important ore type. Ore minerals are principally pyrrhotite, magnetite and chalcopyrite with lesser amounts of pyrite, molybdenite and sphalerite. There is a general progression from early magnetite, through pyrrhotite to pyrite indicating increasing sulphidation with time. Gold is typically found as free gold within quartz veins and within intense zones of amphibolitisation. Considerable gold is also found in the cataclastite ore type either as invisible gold within the sulphides and/or as free gold within the breccia fragments. The unaltered amphibolites of the Haveri Formation can be classified as medium-K basalts of the tholeiitic trend. Trace and REE support an interpretation of formation in a back-arc basin setting. The unaltered porphyritic rocks are calc-alkaline dacites, and are interpreted, along with the granitoids as having an arc-type origin. This is consistent with the evolution from an initial back-arc basin, through a period of passive margin and/or fore-arc deposition represented by the Osara Formation greywackes and the basal stratigraphy of the TSB, prior to the onset of arc-related volcanic activity characteristic of the TSB and the Svecofennian proper. Using a combination of petrogenetic grids, mineral compositions (garnet-biotite and hornblendeplagioclase thermometers) and oxygen isotope thermometry, peak metamorphism can be constrained to a maximum of approximately 600 °C and 1.5 kbars pressure. Furthermore, the petrogenetic grids indicate that the REDOX conditions can be constrained at 600°C to log f(O₂) values of approximately - 21.0 to -26.0 and -14.5 to -17.5 for the metasedimentary rocks and mafic metavolcanic rocks respectively, thus indicating the presence of a significant REDOX boundary. Amphibole compositions from the Ca-Fe alteration phase (amphibolitisation) indicate iron enrichment with increasing alteration corresponding to higher temperatures of formation. Oxygen isotope studies combined with limited fluid inclusion studies indicate that the Ca-Fe alteration and associated quartz veins formed at high temperatures (530 – 610°C) from low CO₂, low- to moderately saline (<10 eq. wt% NaCl), magmatic-dominated fluids. Fluid inclusion decrepitation textures in the quartz veins suggest isobaric decompression. This is compatible with formation in high-T/low-P environments such as contact aureoles and island arcs. The calcic-skarn assemblage, combined with phase equilibria and sphalerite geothermometry, are indicative of formation at high temperatures (500 – 600 °C) from fluids with higher CO₂ contents and more saline compositions than those responsible for the Fe-Ca alteration. Limited fluid inclusion studies have identified hypersaline inclusions in secondary inclusion trails within quartz. The presence of calcite and scapolite also support formation from CO₂-rich saline fluids. It is suggested that the calcic-skarn alteration and the amphibolitisation evolved from the same fluids, and that P-T changes led to fluid unmixing resulting in two fluid types responsible for the observed alteration variations. Chlorite geothermometry on retrograde chlorite indicates temperatures of 309 – 368 °C. As chlorite represents the latest hydrothermal event, this can be taken as a lower temperature limit for hydrothermal alteration and mineralisation at Haveri.The gold mineralisation at Haveri is related primarily to the Ca-Fe alteration. Under such P-T-X conditions gold was transported as chloride complexes. Ore was localised by a combination of structural controls (shears and folds) and REDOX reactions along the boundary between the oxidised metavolcanics and the reduced metasediments. In addition, fluid unmixing caused an increase in pH, and thus further augmented the precipitation of Cu and Au. During the late D₂-event, temperatures fell below 400 °C, and fluids may have remobilised Au and Cu as bisulphide complexes into the shearcontrolled cataclastites and massive sulphides. The Haveri deposit has many similarities with ore deposit models that include orogenic lode-gold deposits, certain Au-skarn deposits and Fe-oxide Cu-Au deposits. However, many characteristics of the Haveri deposit, including tectonic setting, host lithologies, alteration types, proximity to I-type granitoids and P-T-X conditions of formation, compare favourably with other Early Proterozoic deposits within the TSB and Fennoscandia, as well as many of the deposits in the Cloncurry district of Australia. Consequently, the Haveri deposit can be seen to represent a high-T, Ca-rich member of the recently recognised Fe-oxide Cu-Au group of deposits.

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31

Young, Jennifer Leigh. "The stratigraphy and structural history of the Mesozoic and Cenozoic of the central Nova Scotian Slope, Eastern Canada /." Internet access available to MUN users only, 2005. http://collections.mun.ca/u?/theses,111328.

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32

Burton, Renee. "Miocene to Recent stratigraphy, structural architecture and tectonic evolution of the Adana Basin, Southern Turkey /." Internet access available to MUN users only, 2002. http://collections.mun.ca/u?/theses,28504.

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33

Nakanishi, Takeshi. "Practical application of sequence stratigraphy and risk analysis for stratigraphic trap exploration." Title page, contents and abstract only, 2002. http://web4.library.adelaide.edu.au/theses/09PH/09phn1635.pdf.

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"September 2002" Includes bibliographical references (leaves 200-209) Outlines an evaluation procedure for stratigraphic trap exploration by employing sequence stratigraphy, 3D seismic data visualisation and quantitative risk analysis with case studies in an actual exploration basin.

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34

Bradway, Michael David. "Stratigraphy and structural geometry at the leading edge of the Montana Thrust Belt, east of Sun River Canyon, Lewis and Clark and Teton Counties, Montana." CONNECT TO THIS TITLE ONLINE, 2007. http://etd.lib.umt.edu/theses/available/etd-05072007-163806/.

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35

Tse, To-fun. "Stratigraphy of colluvial-alluvial fan deposits in Northwestern Hong Kong Island." Click to view the E-thesis via HKUTO, 2008. http://sunzi.lib.hku.hk/hkuto/record/B43783442.

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36

Hill, Joseph Christopher. "Structural geology and tectonics of the paleoproterozoic rocks of the Mount Rushmore Quadangle, Black Hills, Souh Dakota." Diss., Columbia, Mo. : University of Missouri-Columbia, 2006. http://hdl.handle.net/10355/4456.

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Thesis (Ph.D.)--University of Missouri-Columbia, 2006.<br>The entire dissertation/thesis text is included in the research.pdf file; the official abstract appears in the short.pdf file (which also appears in the research.pdf); a non-technical general description, or public abstract, appears in the public.pdf file. Title from title screen of research.pdf file viewed on (April 26, 2007) Vita. Includes bibliographical references.

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37

Luo, Hongjun. "Tectonostratigraphy of foreland basins the Upper Cretaceous in southwestern Wyoming /." Laramie, Wyo. : University of Wyoming, 2005. http://proquest.umi.com/pqdweb?did=990280521&sid=1&Fmt=2&clientId=18949&RQT=309&VName=PQD.

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38

Brightmore, Ian William. "Sedimentology and sequence stratigraphy of Brigantian Yoredale Strata in Northern England and Scotland, U.K." Thesis, University of Aberdeen, 2010. http://digitool.abdn.ac.uk:80/webclient/DeliveryManager?pid=165717.

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This study provides a sequence stratigraphic framework within which to consider Brigantian Yoredale strata. The framework has been used to determine the relative effects of syn-depositional tectonics, eustasy and climate on Yoredale sequence stratigraphic architecture within the northern Britain study area. Seventeen high-frequency depositional sequences have been identified and correlated within Brigantian strata in northern England and the Midland Valley of Scotland. Examination of sequence thickness and lithofacies stacking patterns has allowed the spatial and temporal occurrence of syn-depositional tectonism to be constrained and the effects on sequence and lithofacies architecture defined. The overall effect of tectonics on Yoredale sedimentation and cyclicity are interpreted to have been minimal. The correlation of sequence boundaries between the two very different tectonic regimes of northern England and the Midland Valley of Scotland would suggest that tectonics was not the driving mechanism behind cyclicity as suggested by some workers. Correlation of sequences with coeval sequences in the Illinois Basin of mid-continent North America demonstrates a lack of correlation to a particular tectonic regime or depositional facies type. The close similarity of sequence architecture between the Illinois Basin and northern British basins is taken to indicate that the sequences were synchronous depositional events that resulted from high-frequency eustatic sea-level changes. Glacio-eustasy provides the most logical explanation for the observed sequence architecture and apparent synchronous development of sequences and sequence boundaries across the northern Britain study area and globally.

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39

Craigie, Neil William. "Chemostratigraphy of Middle Devonian lacustrine sediments in the Orcadian Basin, north-east Scotland." Thesis, University of Aberdeen, 1998. http://digitool.abdn.ac.uk:80/webclient/DeliveryManager?pid=88106.

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During Middle Devonian times, lacustrine deposition dominated much of NE Scotland including Caithness, Orkney, Shetland and the Inner Moray Firth. Donovan classified such deposits into five distinct facies associations:- the deep water facies association A and the progressively shallower water facies associations B, C, D and sandstones. Such facies associations occur in climatically induced cycles. Facies A sediments (known as "fish beds") are organic rich, comprising triplets of carbonate, clastic and organic laminae (each triplet is c. 1.5mm thick). In the present study the fish beds have been categorised on sedimentological grounds into four subtypes:- types I, II (a and b subtypes), III and IV fish beds. The former, which were deposited under the most reducing, deep water, quiescent conditions, comprise 1.3m+ thick laterally continuous beds containing abundant and well preserved, fully articulated fossil fish. Type II(a), and II(b) and III fish beds are less than 1.3 thick and deposited under increasingly more shallow water and more oxidising conditions. Type II(a) fish beds contain both articulated and dissarticulated fish carcass material while type II(b) fish beds, of similar thickness, contain scattered fish fragments. Type III fish beds occur in close vertical and lateral proximity to fluvial sandstones. Type IV fish beds are carbonate rich and are confined to the south Moray Firth coast. Type I fish beds have the greater source rock potential. It is possible to categorise the Middle Devonian facies, including the fish bed facies, on geochemical grounds. As far as major element geochemistry is concerned, SiO<sub>2</sub> is concentrated principally in detrital quartz, and for this reason is highest within sandstones, while K<sub>2</sub>O, Al<sub>2</sub>O<sub>3</sub> and Fe<sub>2</sub>O<sub>3</sub> are highest within the clay rich facies C and D. MnO is most concentrated within facies AIII and B, deposited closest to the thermocline. Trace elements were also analysed and are also useful in discriminating facies. Some elements, such as Zr and Nb are highly immobile, being concentrated in the dereital fraction of sandstones. By contrast, Rb, Ba and V are principally concentrated within clay and feldspars and, for this reason, are highly concentrated within the most clay rich deposits (facies D). The distributions of Mo, Cu, Ni, V and Cr are partly controlled by paleoredox and, consequently, may be used to discriminate relatively reducing from oxidising facies. U and Th are most highly concentrated within fish bone/scale material and it is possible to use the U/Th ratio to categorise the fish beds. This ratio is highest within the most reducing fish beds (type I) and in fish beds located close to fluvial sandstones (type III). Type II and IV fish beds have generally lower U/Th ratios. This ratio may be measured where spectral gamma ray logs have been run (e.g. Dounreay boreholes).

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40

Baar, Eric Edward. "Determining the regional-scale detrital zircon provenance of the middle-late Ordovician Kinnikinic (Eureka) Quartzite, east-central Idaho, U.S." Pullman, Wash. : Washington State University, 2009. http://www.dissertations.wsu.edu/Thesis/Spring2009/e_baar_050609.pdf.

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Thesis (M.S. in geology)--Washington State University, May 2009.<br>Title from PDF title page (viewed on July 15, 2009). "School of Earth and Environmental Sciences." Includes bibliographical references (p. 76-83).

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41

Dresbach, Russell Ivan. "Early ordovician conodonts and biostratigraphy of the Arbuckle group in Oklahoma /." free to MU campus, to others for purchase, 1998. http://wwwlib.umi.com/cr/mo/fullcit?p9901233.

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42

Chung, Yi-tak Teresa. "Quaternary stratigraphy of an offshore borehole from northern Lantau, Hong Kong." Click to view the E-thesis via HKUTO, 2009. http://sunzi.lib.hku.hk/hkuto/record/B42904730.

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43

Huang, Guangqing. "Holocene record of storms in sediments of the Pearl River Estuary and vicinity /." Hong Kong : University of Hong Kong, 2000. http://sunzi.lib.hku.hk/hkuto/record.jsp?B21687808.

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44

Dack, Ashley V. "Internal structure and geochronology of the Gerrei Unit in the Flumendosa area, Variscan External Nappe Zone, Sardinia, Italy." [Boise, Idaho] : Boise State University, 2009. http://scholarworks.boisestate.edu/td/56/.

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45

Isler, Ekrem Bursin. "Late quaternary stratigraphic and tectonic evolution of the northeastern Aegean Sea /." Internet access available to MUN users only, 2005. http://collections.mun.ca/u?/theses,147122.

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46

Ketrenos, Nancy Tompkins. "The stratigraphy of the Scappoose formation, the Astoria formation, and the Columbia River basalt group in northwestern Columbia County, Oregon." PDXScholar, 1986. https://pdxscholar.library.pdx.edu/open_access_etds/3632.

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The study area is located in northwestern Columbia County, and covers an area of approximately 70 square kilometers. The purpose of the study was to investigate the possible correlation of the Scappoose and Astoria Formations and determine their stratigraphic relationship to the Columbia River Basalt Group through mapping, geochemistry and petrography.

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47

Heah, T. S. T. "Mesozoic ductile shear and paleogene extension along the eastern margin of the central Gneiss Complex, coast Belt, Shames River area, near Terrace, British Columbia." Thesis, University of British Columbia, 1991. http://hdl.handle.net/2429/29869.

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Near Terrace, British Columbia, the eastern margin of the Central Gneiss Complex (CGC) is a 3-4 km thick, gently northeast dipping, ductile-brittle shear zone with northeast movement of the upper plate. Along Shames River, deformed amphibolite-facies rocks to the west are juxtaposed against lower greenschist to amphibolite facies units to the east along the steep, east side down, brittle Shames River fault (SRF). Gentle to moderate northwest and northeast dips west of SRF contrast with steep southeast dips to the east. Lineations plunge gently northeast and southwest. West of SRF, the Shames River mylonite zone (SRMZ) separates granitoid rocks below from less deformed granitoid rocks, orthogneiss and metasedimentary rocks above. West of Exstew River, the moderately northeast dipping, ductile Exstew River fault, juxtaposes the SRMZ against metamorphic rocks and granitoids of the CGC. The SRMZ is cut by anastomosing brittle-ductile shear zones. Most kinematic indicators show northeast directed shear. Heterogeneous strain in SRMZ accommodates a minimum upper plate movement of 25 km to the east-northeast. Hornblende geobarometry indicates a structural omission of 13.4 km across SRMZ. East of SRF, amphibolite and greenschist facies supracrustal and plutonic rocks of Lower Permian and older Stikine Assemblage are thrust above greenschist facies volcanic strata correlated with Telkwa Formation of the Lower to Middle Jurassic Hazelton Group. Foliation in late synkinematic, 69 Ma granodiorite which intrudes this thrust package dips steeply southeast. Stikine Assemblage is comprised of lower greenstone, granitoid rocks, volcanic breccia and flows overlain by fusulinid-rich marble. A deformed intrusive rock in Stikine Assemblage has a minimum Pb-Pb date of 317 ± 3 Ma. Hazelton Group contains lower andesitic and upper dacitic to rhyolitic packages comprised of agglomerate, volcanic breccia, tuff, and plagioclase porphyry flows. The earliest recognised metamorphism and deformation in the SRMZ, at upper amphibolite grade, affects 188 ± 8 Ma orthogneiss, and occurred before intrusion of a garnet-biotite granite dated by Woodsworth et al. (1983) at 83.5 Ma. Early fabrics are overprinted by Campanian to Paleocene ductile deformation and a second metamorphism. The second deformation waned during intrusion of three granitic intrusions with concordant U-Pb zircon crystallization dates of 68.7 - 69 Ma. A late to post-kinematic granite dyke in the SRMZ has a U-Pb zircon crystallization date of 60 ± 6 Ma. The second phase of metamorphism began before, and outlasted ductile deformation. The SRF and other high angle normal faults cut 69 Ma granodiorite, but do not significantly offset Eocene (46.2-52.3 Ma) K-Ar biotite cooling isothermal surfaces. The 60 Ma granite is deformed by low angle semi-brittle faulting with upper plate movement to the northeast. A 48 ± 3 Ma synkinematic granite dyke in the footwall of SRMZ was intruded during this deformation, which ended before 46.2 - 46.5 ± 1.6 Ma, the K-Ar biotite cooling dates from SRMZ. The entire region is deformed by post-ductile open, upright, east-northeast plunging folds. K-Ar biotite dates for granitoid rocks range from 51.1 Ma in the upper plate to 46.2 Ma in SRMZ, indicating downward progression of cooling. North-northwest trending brittle faults and lamprophyre dykes cut the SRMZ, and are therefore younger than mid-Eocene. Thermobarometry of pelitic and granitoid rocks indicates increasing metamorphic grade with increasing structural depth. Al-j; in hornblende geobarometry indicates slightly lower pressure of crystallization for the interior than the margin of a granodiorite body east of SRF.In the upper plate of SRMZ, west of SRF, sillimanite-staurolite-garnet schist records ductile deformation and metamorphism at 3.8 ± 1.6 kbar and 570 ± 50°C. The schist is intruded by orthogneiss cut by 68.7 Ma granodiorite. The granodiorite crystallized at 3.4 ± 1 kbar, and was deformed at 2.2 ± 1 kbar at 68.7 Ma. In SRMZ, hornblende in pre-kinematic, 188 ± 8 Ma granodiorite crystallized at 5.5 ± 1 kbar. Deformation and synkinematic metamorphism occurred at 4.9 ± 1 kbar, between 83.5 and before 60 ± 6 Ma. East of SRF, greenschist conditions prevailed, except near the southern margin of the 69 Ma granodiorite body, where amphibolite facies was stable during ductile deformation. A metapelitic sample gives near-peak metamorphic conditions of 4.9 ± 1.6 kbar and 700 ± 50°C, and contact metamorphic conditions of 2.9 ± 1.6 kbar and 610 ± 50°C during intrusion of late synkinematic, 69 Ma granodiorite. P-T-time paths for the upper plate of SRMZ west of Shames River indicate initial rapid, near-isothermal decompression beginning before 69 Ma, continuing to 69 Ma, followed by rapid cooling to 0.9-1.1 kbar, at 51.1 Ma. Paleogene to middle Eocene deformation was probably extensional in nature. It occurred in a vigorous magmatic arc, in response to, and possibly coeval with, crustal thickening.<br>Science, Faculty of<br>Earth, Ocean and Atmospheric Sciences, Department of<br>Graduate

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48

Hesthammer, Jonny. "Stratigraphy and structural geology of Upper Triassic and Jurassic rocks in the central Graham Island area, Queen Charlotte Islands, British Columbia." Thesis, University of British Columbia, 1991. http://hdl.handle.net/2429/29872.

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Upper Triassic and Jurassic rocks in the central Graham Island area comprise shale, siltstone, sandstone, and conglomerate of the Kunga, Maude, and Yakoun Groups. Volcanic rocks are common in the Middle Jurassic Yakoun Group. The oldest unit exposed within the study area is the Lower Jurassic Sandilands Formation of the Kunga Group, a more than 250 metre thick sequence of interbedded organic-rich shale, tuff, siltstone, and sandstone. The Lower Jurassic Maude Group conformably overlies the Kunga Group and is divisible into four formations. The Ghost Creek Formation is an organic-rich black fissile shale, and is overlain by calcareous sandstone of the Fannin Formation. The Whiteaves Formation consists of fissile calcareous grey shale that grades upwards into fossil-rich medium- to coarse-grained, sandstone of the Phantom Creek Formation. The base of the Middle Jurassic Yakoun Group is marked by an angular unconformity. The unit is more than 1500 metres thick and is divided into four lithofacies. The lowermost shale and tuff lithofacies is a sequence of interbedded shale, tuff, siltstone, and sandstone, with shale dominating. The sandstone lithofacies overlies and partly interfingers with the shale and tuff lithofacies and comprises medium- to thickly-bedded lithic arenite interlayered with thinly-bedded shale. The conglomerate lithofacies exists within the sandstone lithofacies and consists mostly of thickly-bedded pebble and cobble conglomerate. The volcanic lithofacies interfingers with, and overlies the sedimentary rocks of the Yakoun Group, and includes lava flows, pyroclastic rock deposits, and lahars. The Kunga and Maude Groups record several relative changes in sea level. They formed in a progressively deepening basin. In Pliensbachian time, the basin shallowed and deposition, represented by the upper Fannin Formation of the Maude Group, was near-shore. Toarcian time is marked by an abrupt transgression. The upper part of the Whiteaves Formation and the Phantom Creek Formation of the Maude Group indicate a subsequent regression. The sedimentary rocks of the Yakoun Group were deposited in local shallow marine basins. Volcanic rocks are most abundant in the eastern parts of the map area, and indicate that an igneous source is located in that direction. All rock units in the map area are deformed by major northwest-trending faults and folds, reflecting at least four northeast-southwest oriented deformational events. The angular unconformity at the base of the Yakoun Group restricts one compressional phase to mid-Jurassic time. Abundant southwest-verging folds suggest development of northeast-dipping thrust faults during this compressional event. Northeast-trending normal faults cut through the thrust faults, postdating them and indicating a period of extension. Rocks of the Sandilands Formation are observed thrust on top of the Yakoun Group, thus indicating a second compressional event. Several small-scale strike-slip faults cut through all described rock units and overlying Tertiary sections, suggesting a late Tertiary deformational event. The Middle Jurassic compressional event may be a result of collision of Wrangellia with North America, or could have been caused by changes in relative plate motion between the North American and Pacific plates during the break-up of Pangaea. Lithologic similarities between the Jurassic and older units of Wrangellia on the Queen Charlotte Islands and coeval rocks of the Alexander terrane in southeastern Alaska suggest that there are no clear differences between the two, and that they were contiguous since Upper Paleozoic time.<br>Science, Faculty of<br>Earth, Ocean and Atmospheric Sciences, Department of<br>Graduate

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49

Malhame, Pierre. "Quartz arenites of the uppermost Cambrian-lowermost Ordovician Kamouraska Formation, Québec, Canada : gravity flow deposits of eolian sand in the deep sea." Thesis, McGill University, 2007. http://digitool.Library.McGill.CA:80/R/?func=dbin-jump-full&object_id=101868.

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The uppermost Cambrian-Lower Ordovician Kamouraska Formation in the external Humber Zone of the Quebec Appalachians consists of dominant thick massive to graded quartz arenite beds, subordinate pebble conglomerate and intercalated thin shale and siltstone beds. It was deposited by hyperconcentrated to concentrated density flows in a meandering submarine canyon on the continental slope bordering the Iapetus Ocean. Turbidity currents deposited beds with turbidite structure divisions. The sandstones consist of well sorted, well rounded quartz sand with frosted grains. Scanning electron microscopy reveals the presence of textures supporting eolian transport before redeposition in the deep sea. The Kamouraska quartz arenites are considered an ancient equivalent of Pleistocene eolian-sand turbidites on an abyssal plain off West Africa consisting of Sahara sand. Sand provenance is attributed to eolian equivalents of the Cairnside Formation of the Potsdam Group. The quartz arenites of the Kamouraska Formation provide a variant to tectonic sandstone provenance proposed in the scheme of Dickinson and Suczek (1979).

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50

Kerr, Dennis Rolland. "Sedimentology and stratigraphy of Pennsylvanian and lower Permian strata (Upper Amsden Formation and Tensleep Sandstone) in north-central Wyoming." 1989. http://catalog.hathitrust.org/api/volumes/oclc/22338168.html.

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Thesis (Ph. D.)--University of Wisconsin-Madison, 1989.<br>Typescript. Vita. Four plates on folded leaves in pocket. eContent provider-neutral record in process. Description based on print version record. Includes bibliographical references.

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