Peter J. Hudleston

University of Minnesota

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Labao Lan

Columbia University

Morgan E. Monz

University of Minnesota

Elisa Fitz-Díaz

Universidad Nacional Autónoma de México

Gustavo Tolson

Universidad Nacional Autónoma de México

Susan H. Treagus

University of Manchester

Robert L. Bauer

University of Missouri

Roger LeB. Hooke

University of Maine

D.L. Southwick

European Organization for Nuclear Research

David J. Prior

University of Cambridge

Zachary Michels

University of Arizona

Cooperative Institutions

University of Minnesota

Universidad Nacional Autónoma de México

Twin Cities Orthopedics

University of Michigan–Ann Arbor

Stanford University

ETH Zurich

University of Nottingham

United States Geological Survey

British Geological Survey

University of Dundee

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Estimacion de acortamiento en pliegues chevron que han experimentado deformacion post flexion

Revista Mexicana de Ciencias Geológicas (2019)

Alberto Vásquez-Serrano Gustavo Tolson Elisa Fitz-Díaz Peter J. Hudleston

Los pliegues son estructuras geológicas que se presentan en muchos medios geológicos. Analizar su geometría nos permite obtener una aproximación de la deformación que acomodaron. Los pliegues tipo chevron son útiles para hacer estimaciones de acortamiento en sistemas orogénicos debido a su particular geometría. A pesar de esto, no se ha propuesto un método para calcular la deformación total (dinámica y cinemática) que experimentan estas estructuras. En el presente trabajo se expone un método para el cálculo del acortamiento en pliegues chevron que han sufrido una deformación post flexión o post pandeo, el cual toma como base el modelo propuesto por Ramsay en 1974. El método propuesto es conceptualmente sencillo y general, lo que permite su aplicación para estimar el acortamiento en sistemas orogénicos alrededor del mundo.

Chevron (anatomy)

10.22201/cgeo.20072902e.2019.3.1493

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The effects of rheology on the strain distribution in single layer buckle folds

Journal of Structural Geology (1995)

Labao Lan Peter J. Hudleston

Buckle

Finite strain theory

10.1016/0191-8141(94)00095-h

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Citations (32)

Structures and fabrics in glacial ice: A review

Journal of Structural Geology (2015)

Peter J. Hudleston

Ice wedge

10.1016/j.jsg.2015.09.003

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Citations (129)

Deformation at an Archean subprovince boundary, northern Minnesota

Canadian Journal of Earth Sciences (1991)

John R. Tabor Peter J. Hudleston

Structural analysis in the northern margin of the Quetico subprovince (part of the Archean Superior Province of the Canadian Shield) in Minnesota reveals that the main deformation involved polyphase folding (F 1 recumbent and nappe-like, and F 2 upright, east–west trending, and tight to isoclinal) during regional ductile transpression and amphibolite-facies metamorphism. A younger deformation, developed during the latter stages of regional transpression, resulted in the generation of localized ultraphyllonites along the steeply dipping Rainy Lake – Seine River fault (RLSRF), the major fault separating the Quetico subprovince from the Rainy Lake wrench zone (a wedge-shaped block between the Quetico and Wabigoon subprovinces). The transpression involved north–south shortening and east–west dextral shear. The presence of shear zones in amphibolite-facies wall rock south of the fault and in lower grade ultraphyllonites within the RLSRF suggests that localization of shear occurred by work and (or) reaction softening, possibly enhanced by the influx of fluids during regional cooling. The youngest structures in the wall rock are conjugate brittle faults oriented similarly to the youngest ductile shear structures in the RLSRF, indicating that the zone of transpression widened following the stage of strain localization, possibly due to work hardening during continued regional cooling. Widening of the zone of deformation was accompanied by an increase in the relative intensity of the north–south shortening component of transpression, revealed by chloritized necks of boudinaged quartz ribbons, quartz and calcite microfabrics, and flattening strains. Protracted ductile flow and localized greenschist-facies conditions in the RLSRF, which occurred during widening of the zone of deformation and rotation of the kinematic frame (to produce north–south shortening structures), are best explained by an influx of fluid phases.Mesostructures and quartz microfabrics in late tectonic (but synkinematic) peraluminous leucogranitoid intrusions and host schist 10 km south of the RLSRF record north–south shortening, but not east–west dextral shear, and further support late north–south shortening across the RLSRF.Tectonic settings for the RLSRF include (i) a suture between distinct lithotectonic terranes or (ii) a zone of localization of deformation within the northern margin of the Quetico subprovince following collision between the Quetico and Wabigoon terranes.

Transpression

Greenschist

10.1139/e91-028

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Citations (27)

Influence of initial fabric on fractures developed in shear zones in clay

AGU Fall Meeting Abstracts (2012)

Christopher Zahasky Peter J. Hudleston

Abstract We examine the influence of initial fabric on the development of fractures in experiments in which clay cakes are sheared over two horizontal base plates that move past each other in wrench-fault motion. An anisotropic fabric in the kaolinite was produced during the preparation of the clay cakes for these experiments. To produce the fabric, the clay was either screeded perpendicular to the underlying fault, screeded parallel to the underlying fault, or molded to develop a cake-parallel fabric that is isotropic in the horizontal plane. The influence of the initial fabric is striking. With cake-parallel fabric, both Riedel (R) and conjugate Riedel (R′) shears develop, the former being much more pronounced than the latter. With a fault-parallel fabric, only R shears developed, while with a cake- and fault-perpendicular fabric, only closely spaced high-angle shears developed initially, with more widely spaced R shears forming later. There is a difference in the orientation of the R shears in the three types of fabric, with the angle being smallest for a fault-parallel fabric (mean of initial fractures of 15°) and largest for a fault-perpendicular fabric (mean of initial fractures of 25°). The high-angle shears have an initial average angle of 80° for cake-parallel fabric and 100° for fault-perpendicular fabric. Only in the case of the high-angle fractures for a fault-perpendicular fabric is there significant rotation after formation. It is likely that the difference in fracture orientation attributed to anisotropy of the initial fabric of the clay also has its counterpart in nature and is not confined to fractures formed in shear zones.

Normal fault

Fault gouge

Horizontal plane

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Non-ellipsoidal inclusions as geological strain markers and competence indicators

Journal of Structural Geology (1996)

Susan H. Treagus Peter J. Hudleston Labao Lan

Ellipsoid

10.1016/0191-8141(96)00039-9

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Citations (21)

Development of Fabric and Structures in Shear Zones

Proceedings of the International Conferences on Basement Tectonics (1995)

Peter J. Hudleston

Cataclastic rock

Brittleness

Upper crust

Pure shear

10.1007/978-94-017-0831-9_33

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Ice Fabrics in a Vertical Flow Plane, Barnes Ice Cap, Canada

Journal of Glaciology (1980)

Roger LeB. Hooke Peter J. Hudleston

Abstract At a depth of about 75 m in the lower part of the accumulation area of the Barnes Ice Cap there is a change from fine-grained ice with a weakly-oriented c -axis fabric to coarser ice with a broad single-maximum fabric. At a depth of about 150 m the single maximum becomes elongate perpendicular to the direction of bubble elongation, and then splits into two distinct maxima making an angle of about 40–45° with respect to one another. At greater depths a third and finally a fourth maximum appear, forming the well known diamond pattern. Mean crystal size does not seem to increase in the transitions from one to two and thence to three maxima, but it may become more uniform. Crystal size does increase in the transition from three to four maxima, however. At the base of the glacier there is a 10–20 m thick layer of unusually-bubbly, fine-grained white ice with a strong single-maximum fabric. The depths to the transitions increase up-glacier and in place of the single-maximum fabric a small-circle pattern is found. Down-glacier the depths to the transitions decrease, systematically eliminating the higher zones. Thus in the lower part of the ablation area, ice with a four-maximum fabric appears at the surface. The independent variables governing these fabric transitions appear to be temperature T , stress τ , and cumulative strain ³ oc . In a tentative stability diagram showing the fields in which given fabrics are stable in T – τ – ³ oc space, multiple-maximum fabrics occur at high temperatures (> —10°C) and at moderate to high stresses, weakly-oriented fabrics at low stresses or low cumulative strains, broad single-maximum fabrics at moderate stresses or moderate cumulative strains, and strong single-maximum fabrics at high stresses or large cumulative strains.

Maxima

10.1017/s0022143000010443

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Citations (94)

Microstructural Analysis of Intensely Sheared, Coarse-Grained Marginal Ice on Storglaciären, Sweden, Using Cryo-Electron Backscatter Diffraction (EBSD)

AGU Fall Meeting Abstracts (2020)

Morgan E. Monz Peter J. Hudleston David J. Prior Zachary Michels Fan Shen

Backscatter (email)

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The tectonic significance of dikes of irregular fold-like shape

Geology (2012)

Elena Druguet Lina M. Castaño Dyanna M. Czeck Peter J. Hudleston Jordi Carreras

Research Article| July 01, 2012 The tectonic significance of dikes of irregular fold-like shape Elena Druguet; Elena Druguet * 1Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Bellaterra, Barcelona, Spain *E-mails: elena.druguet@uab.cat; linamarcela.castano@uab.cat; dyanna@uwm.edu; hudle001@umn.edu; jordi.carreras@uab.cat. Search for other works by this author on: GSW Google Scholar Lina M. Castaño; Lina M. Castaño * 1Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Bellaterra, Barcelona, Spain *E-mails: elena.druguet@uab.cat; linamarcela.castano@uab.cat; dyanna@uwm.edu; hudle001@umn.edu; jordi.carreras@uab.cat. Search for other works by this author on: GSW Google Scholar Dyanna M. Czeck; Dyanna M. Czeck * 2Department of Geosciences, University of Wisconsin, P.O. Box 413, Milwaukee, Wisconsin 53201, USA *E-mails: elena.druguet@uab.cat; linamarcela.castano@uab.cat; dyanna@uwm.edu; hudle001@umn.edu; jordi.carreras@uab.cat. Search for other works by this author on: GSW Google Scholar Peter J. Hudleston; Peter J. Hudleston * 3Department of Geology and Geophysics, University of Minnesota, Minneapolis, Minnesota 55455, USA *E-mails: elena.druguet@uab.cat; linamarcela.castano@uab.cat; dyanna@uwm.edu; hudle001@umn.edu; jordi.carreras@uab.cat. Search for other works by this author on: GSW Google Scholar Jordi Carreras Jordi Carreras * 1Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Bellaterra, Barcelona, Spain *E-mails: elena.druguet@uab.cat; linamarcela.castano@uab.cat; dyanna@uwm.edu; hudle001@umn.edu; jordi.carreras@uab.cat. Search for other works by this author on: GSW Google Scholar Author and Article Information Elena Druguet * 1Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Bellaterra, Barcelona, Spain Lina M. Castaño * 1Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Bellaterra, Barcelona, Spain Dyanna M. Czeck * 2Department of Geosciences, University of Wisconsin, P.O. Box 413, Milwaukee, Wisconsin 53201, USA Peter J. Hudleston * 3Department of Geology and Geophysics, University of Minnesota, Minneapolis, Minnesota 55455, USA Jordi Carreras * 1Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Bellaterra, Barcelona, Spain *E-mails: elena.druguet@uab.cat; linamarcela.castano@uab.cat; dyanna@uwm.edu; hudle001@umn.edu; jordi.carreras@uab.cat. Publisher: Geological Society of America Received: 25 Oct 2011 Revision Received: 20 Jan 2012 Accepted: 26 Jan 2012 First Online: 09 Mar 2017 Online ISSN: 1943-2682 Print ISSN: 0091-7613 © 2012 Geological Society of America Geology (2012) 40 (7): 579–582. https://doi.org/10.1130/G32960.1 Article history Received: 25 Oct 2011 Revision Received: 20 Jan 2012 Accepted: 26 Jan 2012 First Online: 09 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share Facebook Twitter LinkedIn Email Permissions Search Site Citation Elena Druguet, Lina M. Castaño, Dyanna M. Czeck, Peter J. Hudleston, Jordi Carreras; The tectonic significance of dikes of irregular fold-like shape. Geology 2012;; 40 (7): 579–582. doi: https://doi.org/10.1130/G32960.1 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGeology Search Advanced Search Abstract The effects of postemplacement deformation on originally nonplanar dikes were tested experimentally and compared to field data from the Rainy Lake zone (Ontario, Canada) where irregular fold-like structures are observed. The analyses reveal that two processes are responsible for the irregular dike geometries. First, dikes intrude with varying orientations as they propagate across layers with rheology contrasts, thus developing nonplanar profiles. Second, with postemplacement ductile deformation, dikes that are more competent than the host rocks are folded and refracted in variable amounts, with the amount depending on the initial dike geometry, the heterogeneities in the host, and the regional strain. Deformed dikes and veins are often used as kinematic markers to evaluate regional tectonics, using methods that generally assume that veins had planar walls prior to deformation. The experimental results indicate that caution should be taken when using this approach, and they provide criteria to distinguish between intrusive and deformation structures in intensely deformed areas where distinction between the two is not readily apparent. You do not have access to this content, please speak to your institutional administrator if you feel you should have access.

10.1130/g32960.1

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Citations (5)