Deformations associated with relaxation of residual stresses in a sample of Barre Granite from Vermont

Nichols, Thomas C.

doi:10.3133/pp875

Cited by 21 publications

(13 citation statements)

References 10 publications

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“…Since residual strain investigation is very limited, there is a lack of data on how it is in granite. Nichols (1975) and Wolter (1987) analyzed the locked-in stress with the over-coring method. Nichols (1975) obtained extension strain of 0.33 9 10 -3 and compressional strain of -0.27 9 10 -3 , whereas Wolter (1987) obtained much lower strain values by the overcoring method of about 32 lm/m (corresponding to 0.03 9 10 -3 ).…”

Section: Discussionmentioning

confidence: 99%

“…Nichols (1975) and Wolter (1987) analyzed the locked-in stress with the over-coring method. Nichols (1975) obtained extension strain of 0.33 9 10 -3 and compressional strain of -0.27 9 10 -3 , whereas Wolter (1987) obtained much lower strain values by the overcoring method of about 32 lm/m (corresponding to 0.03 9 10 -3 ). In the case of the investigated granitoids residual strain values were detected by neutron diffraction, ranging from -1.7 9 10 -3 (compression) to 0.59 9 10 -3 (expansion).…”

Section: Discussionmentioning

confidence: 99%

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The bowing potential of granitic rocks: rock fabrics, thermal properties and residual strain

et al. 2007

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The bowing of natural stone panels is especially known for marble slabs. The bowing of granite is mainly known from tombstones in subtropical humid climate. Field inspections in combination with laboratory investigations with respect to the thermal expansion and the bowing potential was performed on two different granitoids (Cezlak granodiorite and Flossenbürg granite) which differ in the composition and rock fabrics. In addition, to describe and explain the effect of bowing of granitoid facade panels, neutron time-of-flight diffraction was applied to determine residual macro-and microstrain. The measurements were combined with investigations of the crystallographic preferred orientation of quartz and biotite. Both samples show a significant bowing as a function of panel thickness and destination temperature. In comparison to marbles the effect of bowing is more pronounced in granitoids at temperatures of 120°C. The bowing as well as the thermal expansion of the Cezlak sample is also anisotropic with respect to the rock fabrics. A quantitative estimate was performed based on the observed textures. The effect of the locked-in stresses may also have a control on the bowing together with the thermal stresses related to the different volume expansion of the rock-forming minerals.

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Section: Discussionmentioning

confidence: 99%

Section: Discussionmentioning

confidence: 99%

The bowing potential of granitic rocks: rock fabrics, thermal properties and residual strain

et al. 2007

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“…The terms 'residual stresses' and 'residual strains' are often used interchangeably in the literature. Upon rock excava-Tectonic and residual stresses 65 tion, drilling or coring, some of the residual stresses contribute to instantaneous deformation and the rest to time-dependent deformation (Voight, 1966a;Nichols and Savage, 1976;Bielenstein and Barron, 1971). Upon rock excava-Tectonic and residual stresses 65 tion, drilling or coring, some of the residual stresses contribute to instantaneous deformation and the rest to time-dependent deformation (Voight, 1966a;Nichols and Savage, 1976;Bielenstein and Barron, 1971).…”

Section: Residual Stressesmentioning

confidence: 99%

“…Hyett, Dyke and Hudson (1986) have suggested three fundamental requirements for generating residual stresses in rock: '(1) a change in the energy level, e.g., a stress or temperature change, (2) a heterogeneity caused by different constituent parts of the material, and (3) compatibility (at least partial) of these constituent parts'. In order to separate the short-term deformations associated with residual stresses from the short-term deformations associated with active tectonic and gravitational stresses, overcoring or undercoring of overcored or undercored specimens or specimens cut from a rock mass can be carried out (Bielenstein and Barron, 1971;Friedman, 1972;Gentry, 1973;Lang, Thompson and Ng, 1986;Nichols, 1975;Nichols and Savage, 1976;Russell and Hoskins, 1973;Sbar et al, 1979). In order to separate the short-term deformations associated with residual stresses from the short-term deformations associated with active tectonic and gravitational stresses, overcoring or undercoring of overcored or undercored specimens or specimens cut from a rock mass can be carried out (Bielenstein and Barron, 1971;Friedman, 1972;Gentry, 1973;Lang, Thompson and Ng, 1986;Nichols, 1975;Nichols and Savage, 1976;Russell and Hoskins, 1973;Sbar et al, 1979).…”

Section: Residual Stressesmentioning

confidence: 99%

Estimating in situ Stresses

Amadei

Stephansson

1997

Rock Stress and Its Measurement

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Several of these different phenomena are discussed in this chapter. The reader should be aware that no agreement has yet been reached with certainty on this matter and that there is still room for discussion. VARIATION OF INSITU STRESSES WITH DEPTH Several authors have proposed expressions for the variation of the magnitude of the vertical and horizontal in situ stresses with depth at specific sites or for different regions of the world. Most data are for depths of less than 3000 m. Examples of stress profiles and stress variations with depth can be found in Hast

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“…The first method applied to test the residual stress system 'drill core' was the secondary overcoring technique (e.g. Nichols 1975;Engelder, Sbar & Kranz 1977;Engelder & Geiser 1984;Lang, Thompson & Ng 1986). We initiated strain relief in the drill core (diameter 66 mm) by cutting out a smaller rock cylinder of 30mm diameter.…”

Section: Secondary Overcoringmentioning

confidence: 99%

Residual stress features in drill cores

Zang

Berckhemer

1989

Geophysical Journal International

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S U M M A R Y The features caused by residual stresses in carboniferous sandstone drill cores from 5300 m depth were investigated by various methods: strain redistribution after secondary overcoring, anisotropy of ultrasonic wave velocity and its pressure dependence, as well as fracture tests. This was complemented by microscopic inspection of thin sections. Comparison of the different methods applied revealed a remarkably good correlation between principal stress directions. All effects observed can be explained by one common feature of stress redistribution-the formation of microcracks. The crack-closing pressure derived from acoustic velocity measurements, as well as the tensile strength resulting from the Brazilian test, gave an estimate of the magnitude of residual stresses.

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Deformations associated with relaxation of residual stresses in a sample of Barre Granite from Vermont

Cited by 21 publications

References 10 publications

The bowing potential of granitic rocks: rock fabrics, thermal properties and residual strain

The bowing potential of granitic rocks: rock fabrics, thermal properties and residual strain

Estimating in situ Stresses

Residual stress features in drill cores

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