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Green Mountains
Illuminating geology in areas of limited exposure using texture shading of lidar digital terrain models
Timing of tectonometamorphism across the Green Mountain anticlinorium, northern Vermont Appalachians: 40 Ar/ 39 Ar data and correlations with southern Quebec
The Prospect Rock thrust: western limit of the Taconian accretionary prism in the northern Green Mountain anticlinorium, Vermont
Tectonic and regional metamorphic implications of the discovery of Middle Ordovician conodonts in cover rocks east of the Green Mountain massif, Vermont
FROM GEOSYNCLINAL TO GEOSYNCLINE
Trondhjemitic, 1.35–1.31 Ga gneisses of the Mount Holly Complex of Vermont: evidence for an Elzevirian event in the Grenville Basement of the United States Appalachians
Transmission electron microscopy of chloritoid; intergrowth with sheet silicates and reactions in metapelites
Reconstructions of mountain glacier profiles, northeastern United States
Slope movements in the Cheshire Quartzite, southwestern Vermont
Slope movements in the Lower Cambrian Cheshire Quartzite of the western Green Mountains in Vermont are characterized by block slides, rock falls, and more rarely, by toppling failures. Slides and falls occur on steep hillslopes underlain by massive quartzite, whereas topples are unique to thin-bedded, tectonically deformed quartzite containing interbeds of graphitic schist. Freeze-thaw mechanisms dominate displacements of massive blocks, while rainfall induces toppling displacements. Movement of massive blocks occurs primarily in early spring and late fall. Bedrock discontinuities, including microfractures, joints, and bedding surfaces, are of primary importance in facilitating initial slope breakup and in controlling the subsequent mode of downslope rock-mass movement. The results of investigations at three sites in the Cheshire-Quartzite show that movement rates are controlled by structural conditions and slope-development patterns. A typical freeze cycle during testing of a physical block model in the laboratory produced a displacement of 0.13 mm, which agrees reasonably well with the 0.26 mm annual displacements measured at two cliff-edge blocks at a rock-fall site. Gravity-induced toppling movements in much less massive quartzite are more rapid.
Heat transfer and fault geometry in the Taconian thrust belt, western New England
Tectonic models of the Taconian orogeny in western New England must account for the rapid metamorphism of the Taconic klippen after thrusting. The most likely source of heat for this metamorphism is an overlying hot thrust sheet of accretionary wedge material, which overrode the continental margin of ancient North America, culminating in a continent-island arc collision. Thermal calculations indicate that rapid conductive heat transfer from such a sheet is possible. The dimensionless Peclet number suggests that conductive heat transfer is faster than, or operates at rates comparable to, advective heat transfer due to thrusting over a distance of at least 6 km from a thrust surface. Thus, syntectonic heating of footwall rocks below a major thrust surface is important and must be taken into account in tectonic models. The continental margin thrust system (CMTS) in western New England may have formed as a set of duplexes under a main roof thrust separating the CMTS from the overriding thrust sheet of accretionary wedge material and above a main floor thrust along which the CMTS was transported over autochthonous continental margin rocks. Thrust sheets in this system are composed of Middle Proterozoic Grenville basement and/or upper Proterozoic to Middle Ordovician cover rocks of a western shelf sequence or eastern slope-rise sequence. According to this duplex model, thrust faults tended to develop sequentially toward the foreland, in the transport direction. The relative timing of thrusting and metamorphism is an important constraint on tectonic models, but metamorphism is not a reliable datum with which to compare the timing of events in different parts of the thrust belt. As an example, synmetamorphic thrusting in the eastern internal part of the belt may have preceded brittle faulting to the west near the foreland. P-T paths of rocks from different thrust sheets separated by major faults will be qualitatively different, and detailed petrologic studies to determine and compare P-T paths from different thrust sheets may be useful in identifying faults along which the greatest displacement has occurred.