The tectonic evolution of northern Ellesmere Island is dominated by the accretion of the Pearya Terrane and the progressive reworking of materials from the Pearya Terrane and the northern Caledonides. Geochronology from a suite of seven Succession I orthogneiss samples defines a range of earliest Neoproterozoic ages from 962 ± 6 Ma to 974 ± 8 Ma. Geochemistry of both zircon and whole rock samples reveal a complex magmatic history tapping multiple sources. The rocks include both I and S type granitoids, with silica contents ranging from 62% to 73%. Trace element geochemistry reveals LILE enrichment decoupled from low to depleted HFSE values, suggestive of an origin above a subduction zone. Isotope geochemistry supports input from juvenile and evolved materials, with εNd(i) values between -1 and -4.6, and a similar range for εHf from zircon. The northern elements of the Caledonian Orogen preserve a record of magmatism in the c. 985 Ma to 920 Ma range. These ages are also observed in orthogneiss units of the south central Brooks Range and Farewell terrane, Alaska. The Pearya Terrane orthogneiss units and those currently dispersed in Alaska are interpreted to have originated near or on the eastern margin of Greenland and record post-Rodinia assembly subduction outboard of the supercontinent. Succession II (Trettin, 1987) of the Pearya Terrane represents variably metamorphosed metasedimentary rocks of Proterozoic to early Paleozoic age. These units are structurally juxtaposed with Succession I orthogneiss and Paleozoic sedimentary units of the Pearya Terrane. Detrital zircon age spectra from seven samples of Neoproterozoic meta-sedimentary rocks reveal three groups defined by observed dominant age peaks and youngest observed age populations. Group I includes three quartzite samples and contains numerous c. 1100 Ma to 1800 Ma peaks, with the youngest population at c. 1050 Ma. Two samples of immature meta-sandstone form Group II, defined by a dominant c. 970 Ma age peak. Two samples from the diamictite unit below the Deutchers Glacier thrusts form Group III, with a similar pattern of c. 1000 Ma to 1800 Ma age peaks to Group I; however, this group includes a small population of c. 600 Ma to 700 Ma grains as well. The ubiquitous Mesoproterozoic ages reflect a Grenvillian-Sveconorwegian provenance. These data are consistent with detrital zircon datasets from other North Atlantic-Arctic Caledonide terranes, reinforcing stratigraphic links between the Pearya Terrane and the northern Caledonides. The utility of the Pearya Terrane dataset is multiplied by probable links to Circum-Arctic and Cordilleran terranes, many of which contain similar populations of Mesoproterozic-aged detrital zircon. U/Pb ages and Hf isotopic data from detrital zircon suites sampled from Ordovician to Carboniferous sedimentary rock of the Pearya Terrane and northern Ellesmere Island record define the background for terranes translating along the northeastern Laurentian margin in the Paleozoic. Ordovician to Silurian clastic sediments deposited on the Pearya Terrane record pre terrane accretion provenance dominated by recycling of the metaigneous and metasedimentary Proterozoic basement as well as an Ordovician arc source. The provenance of Late Devonian sediments deposited during the Ellesmerian Orogen is dominated by similar recycled materials, with new sources derived from Paleoproterozoic domains of the Canadian-Greenland shield and documented late Devonian granitoids emplaced the Canadian Arctic Islands and Arctic Alaska. The basal Sverdrup Basin records increasing proportions of Paleoprtoerozoic and Archean aged grains relative to Mesoproterozoic ages, suggestive of increased contributions from the Laurentian craton and no little detritus exotic to Laurentia. Detrital zircon age spectra from Devonian to Carboniferous sediments in the northern Cordilleran clastic wedge and western Canadian Arctic Islands contain abundant exotic zircon likely derived from the Caledonian and Timanian Orogens. This variance of sediment provenance indicates that the eastern Canadian Arctic Island were isolated from non-Laurentian or Caledonian detritus, and that sources of the exotic Timanian zircon reconstruct farther west along the margin.

Orientador: George Luiz Luvizotto / Resumo: O Gráben Ribeirão das Lajes (GRL) foi mapeado no limite entre as escarpas da Serra do Mar e o Gráben da Guanabara, no estado do Rio de Janeiro, Brasil. O presente estudo buscou caracterizar a configuração e evolução tectônica cenozoica do GRL a partir de métodos que integram procedimentos em laboratório e trabalhos de campo, envolvendo Geologia Estrutural e Geomorfologia Tectônica. Esta bacia tipo gráben encontra-se encaixada na estrutura pretérita NE-SW do embasamento pré-cambriano, composto de gnaisse bandado milonítico da Unidade Arcádia-Areal, juntamente com ortognaisses e granitoides do Arco Magmático Rio Negro. Essas rochas estão intrudidas por diques de diabásio cretáceos de direção NE-SW. O registro sedimentar está associado, principalmente, aos depósitos aluvionares e coluvionares, que se estendem por 20 km de comprimento por 9 km de largura, expostos de maneira irregular e separados por altos intrabacinais. As características da rede de drenagem e do relevo da área, somados aos inúmeros e persistentes lineamentos, mostram, em conjunto com os dados levantados em campo, que os traços principais se associam às fraturas. O GRL é uma estrutura alongada e estreita delimitada por falhas NE-SW, em ambas as bordas, e compartimentada fundamentalmente por fraturas de direção NW-SE e E-W. O primeiro evento de formação do GRL se relaciona com as falhas normais NE-SW do embasamento, equivalente ao processo de geração das bacias do Sistema de Riftes Cenozoicos do Sudeste do Brasil... (Resumo completo, clicar acesso eletrônico abaixo) / Abstract: Ribeirão das Lajes Graben (RLG) was mapped at the boundary between Serra do Mar escarpments and Guanabara Graben, in the state of Rio de Janeiro, Brazil. The present study aimed to characterize the Cenozoic tectonic evolution and shape of RLG from methods which incorporate procedures in laboratory and field work, involving structural geology and tectonics geomorphology. This basin was developed on thrust-sheared precambrian NE-SW substrate, consisting of banded milonytic gneisses from the Arcadia-Areal Unit, along with orthognaisses and granitoids from the Rio Negro Magmatic Arc. These rocks are intruded by cretaceous diabase dikes with NE-SW direction. The sedimentary record is mainly associated with alluvial and colluvial deposits, extending 20 km long and 9 km wide, irregularly exposed and separated by intrabacinal highs. The drainage network and relief characteristics, added to the numerous and persistent lineaments, even along with the data collected in the field, demonstrate that the main features are associated to fractures. This elongated and narrow graben is delimited by NE-SW faults at both edges, in addition to NW-SE and E-W fractures which compartmentalize it. The RLG was formed due to recognized NE-SW normal faults, event related to Cenozoic Rift System of Southeastern Brazil generation process. NE-SW structures are expressive in the fluvial system, morphotectonic pattern and preferential erosion and sedimentation zones. In a local scale, field-recognized high-an... (Complete abstract click electronic access below) / Mestre

京都大学 / 0048 / 新制・課程博士 / 博士(理学) / 甲第22266号 / 理博第4580号 / 新制||理||1658(附属図書館) / 京都大学大学院理学研究科地球惑星科学専攻 / (主査)教授 田上 高広, 教授 山路 敦, 教授 生形 貴男 / 学位規則第4条第1項該当 / Doctor of Science / Kyoto University / DGAM

Three-dimensional mechanical simulations of the San Andreas fault (SAF) within the Coachella Valley in California produce deformation that match geologic observations and demonstrate the impact of fault geometry on uplift patterns. Most models that include the Coachella Valley segment of the SAF have assumed a vertical orientation, but recent studies suggest that this segment dips 60-70° northeast. We compare models with varied fault geometry and evaluate how well they reproduce observed uplift patterns. Our model with a dipping SAF matches geologic observations, while models containing a vertical fault do not. This suggests that the active Coachella Valley segment of the SAF dips 60-70° northeast. Since ~1.5 Ma, the SAF in this region has undergone a major reorganization that entailed initiation of the San Jacinto fault and termination of slip on the West Salton detachment fault. The trace of the SAF itself has also evolved, with several shifts in activity through the San Gorgonio Pass. Despite a rich geologic record of these changes, the mechanisms that controlled abandonment of faults, initiation of new strands, and shifting loci of uplift are poorly understood. We model snapshots in time through the evolution of the fault system, and assess the mechanical viability of our snapshots by comparison with uplift patterns inferred from the stratigraphic record. Model results are compared with vertical axis rotation. We examine incipient faulting using maps of strain energy density, and explore changes to the mechanical efficiency of the system to better understand the evolution of this fault system.

Migmatites are a common rock type in the Adirondack Mountains, NY. We analyzed a single sample of biotite-garnet-sillimanite paragneiss with foliation parallel leucosome along Route 22 south of Whitehall, NY in order to determine the timing of melting using both in-situ monazite and zircon U/Pb geochronology from the restite and leucosome layers of the same rock. Monazite was analyzed via in-situ EMPA on the Ultrachron microprobe at the University of Massachusetts. Zircon was analyzed via LA-ICP-MS (in-situ and mounted mineral separates) at the LaserChron Center. Monazite analyses from the restite yielded six compositionally distinct populations with dates of 1178 ± 16, 1139 ± 4, 1064 ± 6, 1049 ± 4, 1030 ± 5, and 1004 ± 10 Ma. Yttrium and heavy REEs decrease in monazite in two steps: one dramatic drop from ca. 1150 to 1065 Ma and another between ca. 1065 and 1050, interpreted to reflect two periods of garnet growth and melting. Analyses from the restite zircon separate yielded a significant single peak near 1050 Ma. These zircon grains exhibit fir-tree sector zoning texture which is interpreted to indicate crystallization from melt. Monazite from leucosome yielded a unimodal population at ca. 1050 Ma, however, backscatter images document alteration of monazite to apatite on the edges of the grains, and abundant uranothorite inclusions. Leucosome zircon analyses yielded a ca. 1150 Ma population from cores and a 1050 Ma population from rims. Cathodoluminescence imaging reveals that the zircon rims have textures indicative of fluid alteration. The data are consistent with these rocks undergoing two periods of melting. The first event at ca. 1150 Ma may have involved a non-garnet producing melting reaction, such as muscovite dehydration-melting. The second event at 1065 Ma involved significant garnet growth, interpreted to represent biotite dehydration-melting. Subsequently, the rocks underwent hydrothermal alteration at 1050 Ma. Monazite grains with dates at 1030 ± 5 and 1004 ± 10 Ma have higher yttrium concentrations suggesting garnet breakdown and monazite growth during decompression and retrograde metamorphism. A combination of monazite and zircon dating techniques from each compositional layer is necessary to constrain leucosome-restite relationships and to accurately interpret the timing of melting from migmatites that have experienced multiple phases of melting.

Integrating field observation with petrochronology is critical for understanding the tectonometamorphic evolution of the North American Grenville Province. Despite methodological advances in geothermobarometry and geochronology, incorporating these data into larger models of the Adirondack Mountains remains particularly challenging due to the presence of multiple generations of deformation, primarily related to the ca. 1190 – 1140 Ma Shawinigan and ca. 1090 – 1020 Ma Ottawan Orogenies (McLelland et al.,2013). The Rock and Bear Ponds area is a dome of tight-to-isoclinally folded metapelites in structural contact with orthogneiss. Fold generations are orthogonal and partitioned such that the northern area is dominated by an earlier episode of D2 deformation and an E-W S2 fabric and the southern by D3 deformation and a N-S S3 fabric. Observed assemblages include Qtz + Pl + Kfs + Bt + Sil + Grt + Gr ± Py ± Mnz ± Zr in metapelite and Hbl + Pl + Grt + Qtz + CPx ± Ilm in metagabbro. Metapelitic garnet is anhedral and overgrows a strongly transposed S1 fabric. A population of small high-Y monazite cores are associated with S1 and yield a mean weighted date of 1174 ± 5 Ma. Monazite observed in S2-defining phases and matrix have very high-Y & HREE cores that yield dates of 1068 ± 7 Ma and are surrounded by low-Y & HREE mantles (1048 ± 4 Ma) with irregular high-Y rims (1023 ± 6 Ma). These data suggest garnet growth followed the transposition of a strong Shawinigan S1 fabric during D2 and D3 folding events, ca. 1090 – 1070 Ma. The timing of this shortening is interpreted to coincide with the early Ottawan Orogeny, ca. 1090 – 1050 Ma. Geothermobarometric calculations of S2-associated phases constrains peak metamorphic conditions to 700 – 750 ± 50 °C and 6.5-7.5 ± 1 kbar; these data are well in agreement with those reported in multiple studies, thereby suggesting that regional PT calculations reflect Ottawan tectonometamorphic conditions (Bohlen et al., 1985; Spear & Markussen, 1997; Storm & Spear, 2005). High-Y & HREE rims are also observed and interpreted to reflect garnet breakdown ca. 1050 – 990 Ma during decompression and orogenic collapse, which has become increasingly reported in the eastern Adirondack Mountains over the last decade (Wong et al., 2012; Chiarenzelli et al., 2017; Regan et al., 2019; Williams et al., 2019). The Mesoproterozoic metapelite of the Rock and Bear Ponds area record an intense polydeformational history and therefore provide a valuable window into episodic middle-to-lower crustal deformation and metamorphism. The integration of focused microstructural observation with geothermobarometric and timing constraints has provided much insight into the structural evolution of the Adirondack Mountains. Integrating field observation with petrochronology is critical for understanding the tectonometamorphic evolution of the North American Grenville Province. Despite methodological advances in geothermobarometry and geochronology, incorporating these data into larger models of the Adirondack Mountains remains particularly challenging due to the presence of multiple generations of deformation, primarily related to the ca. 1190 – 1140 Ma Shawinigan and ca. 1090 – 1020 Ma Ottawan Orogenies (McLelland et al.,2013). The Rock and Bear Ponds area is a dome of tight-to-isoclinally folded metapelites in structural contact with orthogneiss. Fold generations are orthogonal and partitioned such that the northern area is dominated by an earlier episode of D2 deformation and an E-W S2 fabric and the southern by D3 deformation and a N-S S3 fabric. Observed assemblages include Qtz + Pl + Kfs + Bt + Sil + Grt + Gr ± Py ± Mnz ± Zr in metapelite and Hbl + Pl + Grt + Qtz + CPx ± Ilm in metagabbro. Metapelitic garnet is anhedral and overgrows a strongly transposed S1 fabric. A population of small high-Y monazite cores are associated with S1 and yield a mean weighted date of 1174 ± 5 Ma. Monazite observed in S2-defining phases and matrix have very high-Y & HREE cores that yield dates of 1068 ± 7 Ma and are surrounded by low-Y & HREE mantles (1048 ± 4 Ma) with irregular high-Y rims (1023 ± 6 Ma). These data suggest garnet growth followed the transposition of a strong Shawinigan S1 fabric during D2 and D3 folding events, ca. 1090 – 1070 Ma. The timing of this shortening is interpreted to coincide with the early Ottawan Orogeny, ca. 1090 – 1050 Ma. Geothermobarometric calculations of S2-associated phases constrains peak metamorphic conditions to 700 – 750 ± 50 °C and 6.5-7.5 ± 1 kbar; these data are well in agreement with those reported in multiple studies, thereby suggesting that regional PT calculations reflect Ottawan tectonometamorphic conditions (Bohlen et al., 1985; Spear & Markussen, 1997; Storm & Spear, 2005). High-Y & HREE rims are also observed and interpreted to reflect garnet breakdown ca. 1050 – 990 Ma during decompression and orogenic collapse, which has become increasingly reported in the eastern Adirondack Mountains over the last decade (Wong et al., 2012; Chiarenzelli et al., 2017; Regan et al., 2019; Williams et al., 2019). The Mesoproterozoic metapelite of the Rock and Bear Ponds area record an intense polydeformational history and therefore provide a valuable window into episodic middle-to-lower crustal deformation and metamorphism. The integration of focused microstructural observation with geothermobarometric and timing constraints has provided much insight into the structural evolution of the Adirondack Mountains.

Marine electromagnetic (EM) geophysics is an up-and-coming branch of the geosciences that is allowing for the advancement in our understanding of key properties of the oceanic lithosphere and subduction dynamics, particularly in how deformation manifests geophysically and how it evolves through time and under various conditions. This dissertation focuses on two unique marine EM data sets collected at the Hikurangi subduction zone, New Zealand, and on 33 Ma Pacific lithosphere. Analysis of the former, which constitutes the bulk of this dissertation, offers the first kilometer-scale characterization of offshore, margin-wide electrical resistivity variations at a subduction zone and provides an electrical framework for discussing the potential causes of along-strike differences in megathrust slip at the Hikurangi Margin. The latter data set is used to constrain electrical anisotropy of the shallow lithosphere, which enables an interpretation of the deformation history of normal oceanic lithosphere. Chapter 2 of this dissertation gives a brief overview of the physical underpinnings of EM methods with attention given to the marine magnetotelluric (MT) and controlled-source electromagnetic (CSEM) methods. Maxwell's equations are reviewed and the relevant derivations leading to the temporal and spatial behavior of EM waves for the frequencies used in this dissertation (~0.001--0.1 Hz) are presented. Chapter 3 focuses on the tectonic background of the Hikurangi Margin and on processing of the MT and CSEM data. Interest in the Hikurangi Margin has arisen both because of its proximity to the inhabitants of New Zealand and due to the recognition of several properties that vary along the strike of the margin. The most intriguing of those variations, and most concerning from a natural hazard perspective, are the along-strike change in interseismic coupling and slow slip event (SSE) occurrence, with stronger coupling and deeper, infrequent SSEs realized in the southern Hikurangi Margin and weaker coupling and shallower, more frequent SSEs in the north. Several proposed causes of these variations are cited, including differences in sediment thickness and roughness of the incoming plate, changes in the plate interface geometry, and the effect of geological terranes in the forearc on pore pressure. But the degree to which any or all of these factors affect interseismic coupling remains an open question. The remainder of Chapter 3 is devoted to detailing the steps involved in processing the marine MT and CSEM data. A workflow for optimizing MT response function estimation is presented and improvements to the marine CSEM processing scheme are described. In Chapter 4 of this dissertation, inversions of the data collected at the southern Hikurangi Margin are presented, and these resistivity models are compared with co-located seismic data. Individual inversions of the CSEM and MT data along with joint inversion of the two data sets highlights the distinct sensitivities and resolving capabilities of each data type. A thick (4--6 km) sediment package covers the Hikurangi Plateau of the incoming plate. The plateau itself is evident as a dipping resistor (>10 Ω-m) that approximately corresponds with the seismically interpreted depth of the Hikurangi Plateau. Resistors in the shallow forearc are interpreted as free gas or gas hydrate, which is prevalent at the Hikurangi Margin. A resistive anomaly beneath one of two main ridges appears to comprise the footwall of a thrust fault, which potentially implies a high permeability system that allows for preferential dewatering of the footwall. Using available P-wave velocity data for this region, equations relating resistivity to velocity are derived. The resistivity presented in Chapter 4 and Archie's law are used to derive porosity models of the southern Hikurangi profile in Chapter 5. Vertical compaction is shown to dominate trends in porosity. A reference compaction porosity model is approximated and removed from the resistivity-derived porosity model in order to identify porosity trends distinct from compaction. A deepening in the negative porosity anomaly of the shallow incoming plate sediments as they approach the trench suggests these sediments experience compression several kilometers seaward of the main frontal thrust. This could represent the early stages of protothrust zone development. An increasingly positive porosity anomaly observed in the sedimentary unit just above the Hikurangi Plateau as it nears the trench may indicate heightened fluid overpressures in an incipient décollement. In Chapter 6 of this dissertation, inversions of the central Hikurangi Margin are shown and discussed. Compared to resistivity in the southern Hikurangi Margin, the forearc and incoming plate of the central Hikurangi Margin are more complex in their resistivity structure, possibly due to the impact of rougher seafloor. Extensive evidence for free gas or gas hydrates is found as shallow resistive anomalies in these models. Other anomalous resistors may correspond to exhumed terranes in the forearc. Anomalous forearc conductors could indicate sediment underplating or damage zones associated with subducting topography. Chapter 7 shows the resistivity and porosity of the northern Hikurangi Margin and offers the first detailed electrical image of a seamount prior to and during subduction. The seamount on the incoming plate is shown to have a thin, resistive cap that traps a conductive matrix of porous volcaniclastics and altered material over a resistive core. Again applying Archie's law to estimate porosity from resistivity reveals that the seamount will allow ~3.2--4.7x more water than normal, unfaulted oceanic lithosphere to subduct with the seamount. In the forearc, a sharp, resistive peak on the slab is interpreted as the core of a subducting seamount. This cone of high resistivity lies directly beneath a prominent conductive anomaly in the upper plate. Burst-type repeating earthquakes and other seismicity from a recent SSE cluster in and around this conductive anomaly, which seems to implicate the subducting seamount in the generation of fluid-rich damage zones in the forearc. The interaction of the subducting topography with the upper plate will thus alter the effective normal stress at the plate interface by modulating fluid overpressure. The results in this chapter show that subducting topography can transport large volumes of water to the forearc and that such topography is able to severely modify the structure and physical conditions of the upper plate, which may influence the location and timing of SSEs. Finally, Chapter 8 provides a robust constraint on the electrical azimuthal anisotropy of oceanic lithosphere. The data for this chapter were collected in a region of oceanic lithosphere removed from the influence of plate boundaries and intraplate volcanism. The survey design was chosen to maximize azimuthal coverage so as to constrain the directional dependence of resistivity. Inversions of the data resulted in an anisotropic resistivity model wherein the crust is ~18-36x more conductive in the paleo mid-ocean ridge direction than the perpendicular paleo-spreading direction. In the uppermost mantle conductivity is ~29x higher in the paleo-spreading direction. The crustal anisotropy is interpreted to result from sub-vertical porosity created by ridge parallel normal faulting during extension of the young crust and thermal stress-driven cracking from cooling of mature crust. Anisotropy in the uppermost mantle implies that shearing of mantle olivine during plate formation generates a strong electrical signal that is preserved as the plate ages. Reanalysis of EM data collected offshore Nicaragua suggests that the Pacific Plate electrical anisotropy is not a local anomaly but rather may be prevalent throughout oceanic lithosphere.

This thesis deals with periodical measurements at the Tetčice polygon to confirm geological activity caused by geological shift that pass through the center of the village. This work was focused on the third phase of measurement by long static GNSS observation in summer 2013 to monitor horizontal shifts on both edges of Boskovice furrow. Points are stabilized on pillars with forced centring. Part of the thesis is summary of present results, the differences between the various stages and graphical representations of shifts. The theoretical part deals with the geological conditions in the area and description of GNSS technology.

<div> <div> <div> <p>The combination of field-based studies and numerical modeling provides a robust tool for evaluating geologic and geodynamic processes along a convergent margin. Complex and persistent tectonic activity and a novel suite of geophysical observations make the southern Alaskan convergent margin a key region to evaluate these processes through both basin analysis studies and geodynamic modeling. This conceptual approach is utilized to explore the active driving forces of surface deformation throughout southcentral Alaska, as well as the geologic record of regional Cenozoic tectonic processes. </p> <p>New sedimentologic, chronostratigraphic, and provenance data from strata that crop out within the central Alaska Range document a previously unrecognized stage of Eocene – early Miocene strike-slip basin development along the northern side of the central Denali fault system. This stage was followed by Miocene-Pliocene deformation and exhumation of the central Alaska Range, and basin development and northward sediment transport into the Tanana foreland basin. This portion of the study provides insight into Cenozoic tectonics and basin development in the central Alaska Range. </p> <p>How transpressional tectonics are manifest in the modern-day, in combination with shallow subduction processes, are not well understood for the southern Alaskan convergent margin. Simulations of the 3-D deformation of this region allow for investigation of the complex relationship between these tectonic processes and surface deformation. Results from this study display the far-field affect that strong plate coupling along the shallowly subducting Yakutat slab has on the surface deformation of southcentral Alaska. Our models also show that partitioning of this convergence is observed along the Denali fault system. Additionally, our results indicate the subducting slab is segmented into separate Pacific, Yakutat and Wrangell slab segments. This variation in slab structure exerts control on the upper plate response to shallow subduction.</p> </div> </div> </div>

archives@tulane.edu / Salt basins are complex structural systems, showing genetic relationships between salt structures, faults, and variable sediment depositional patterns. The dynamics of salt-fault interaction, the role of shale deformation, and the influence of salt evacuation on surface features have been poorly understood. A link between all these processes is the throw history of faults adjacent to and within a salt basin. In this dissertation, I interpret industry well logs and 3D seismic data from the Terrebonne Salt Withdrawal Basin (TSWB) of southeastern Louisiana, to understand these processes. The methodology includes the use of fault throw maps, throw variations along strike and with depth, and sediment expansion indices to understand fault kinematics adjacent to sediment loads and mobile material, i.e., salt or shale. I address the histories of three faults along the northern margin of the TSWB: the Lake Boudreaux, Montegut, and Isle de Jean Charles faults. Each shows Miocene and Quaternary active phases correlated with sediment loading, separated by relative inactivity during the Pliocene. The pattern of Quaternary activity and the surface projections of these faults are consistent with a fault-controlled pattern of wetland loss, suggesting that faults in southeastern Louisiana are active. Isle de Jean Charles fault and the Lake Boudreaux fault interact with the Bully Camp and Lake Barre Salt stocks, respectively. Each stock is interpreted to have grown by a different diapiric mechanism, consistent with different spatial patterns of throw variation on the two faults, despite similar temporal histories. Throw on the Isle de Jean Charles fault increases towards the Bully Camp stock, suggesting deformation inside and outside the stock. In contrast, a decrease in the throw on the Lake Boudreaux fault and an increase in diameter of the Lake Barre stock indicate that deformation exists only within the stock. Additionally, this dissertation considers throw patterns along the southern margin of the TSWB, showing that faults linking the Dog Lake and Caillou Island salt stocks are affected by shale deformation adjacent to salt. These results show that studies of fault-related subsidence and wetland loss in coastal Louisiana need to include observations from nearby salt structures. / 1 / Akinbobola Akintomide