Hydrofracturing stress measurements in the Iceland Research Drilling Project drill hole at Reydarfjordur, Iceland

Abstract

Two independent suites of hydrofracturing stress measurements were conducted in the top 600 m of the Iceland Research Drilling Project deep hole at Reydarfjordur, east Iceland. As indicated by the continuously extracted drill core, the tested section consists of tertiary subaerial tholeiitic lava flows cut by many basaltic dikes. The density of the basalt was used to estimate the vertical stress σV (in megapascals) at depth D (in meters): σV = 0.027D. In the 33‐ to 270‐m depth range the horizontal principal stresses (σHmax and σHmin) as calculated from hydrofracturing results increase gradually with depth but at a lower rate than the vertical stress: σHmin = 2.1 + 0.016D; σHmax = 3.3 + 0.016D. In the 300‐ to 550‐m depth range a major perturbation occurs with both horizontal stress magnitudes rapidly rising between 300 and 400 m and then uniformly decreasing between 400 and 550 m to a level apparently predictable by the relationships obtained in the top 270 m. Conditions favoring normal faulting (σV σHmax σHmin) were established in the 540‐ to 580‐m range and are conjectured to persist at greater depths since the vertical stress gradient is higher than that of σHmax and σHmin This would be in accord with the predominant fault type in east Iceland. The relative low horizontal stress values and the small difference between them are supportive of ocean floor spreading theories and contradict near‐surface high compressive stresses previously determined by Hast (1973) in east Iceland. The large increase in horizontal stress in the range of 300‐ to 500‐m depth is not understood. A correlation appears to exist between the zone of almost unintruded thick lava flows (200–500 m) and that of high stresses. An intuitive model suggesting ‘locked in’ stresses in this zone is proposed. The hydrofracturing‐determined overall mean direction of σHmax is N50°E, while a more selective sampling of results yields N40°E. The measured stress directions appear to be reasonably compatible with the local structure such as dike direction (NNE) and lava dip (WSW). Significantly, σHmax direction is subparallel to the N20°E trend of the nearest fissure swarms in the axial rift zone. This almost coincidence of directions, like the measured stress magnitudes, is also in agreement with the model of spreading lithospheric plates being pulled apart.

Effects of mechanical layering on hydrofracture emplacement and fluid transport in reservoirs

“…Since the in situ tensile strength of common solid rocks varies from 0.5 to 6 MPa (Haimson and Rummel, 1982;Schultz, 1995;Amadei and Stephansson, 1997), the above results from analytical and numerical models indicate that theoretical tip tensile stresses are from one hundred to ten thousand times greater than the tensile strength of the host rock through which these hydrofractures propagate. Similar results follow from other models of hydrofractures in homogeneous, isotropic rocks (Weertman, 1971;Secor and Pollard, 1975).…”

“…p e is equal to local in situ tensile strength T 0 (Equation 3) and σ d normally cannot be greater than 4T 0 . Common in situ tensile strengths T 0 of solid rocks are 0.5-6 MPa, most frequently 2-3 MPa (Haimson and Rummel, 1982;Schultz, 1995 and Stephansson, 1997). Using these values, Equation (6) gives the depth of the water source from 213 to 568 m. Using extreme variations of all the included parameters yields a maximum depth of 1200 m (cf.…”

The volcano‐electric effect

“…Assuming that the confining pressure is equal to the lithostatic pressure, the breakdown fluid overpressure is given by dp F = g(P À p H ) + T S , where P is the lithostatic pressure, p is the initial pore fluid pressure in the rock volume, g is the fracture coefficient for the rock ($1.04 [e.g., Natale et al, 1998]), and T S is the tensile strength of the rock. In poorly compacted volcanic ashes T S $ 0 while jointed basaltic lava flows have in situ tensile strengths in the range 0.2-6 MPa with the most common values $2-3 MPa [Haimson and Rummel, 1982;Schultz, 1995]. At 2 km depth, taking p = 20 MPa, T S = 10 MPa as an upper bound, g = 1, and P = 40 MPa yields dp F % 30 MPa.…”

Evolution of vertical faults at an extensional plate boundary, southwest Iceland

“…(Cartwright et al, 1995;Cartwright and Mansfield, 1998) that a regionally-distributed, absolute tensile stress at the surface was responsible for the initiation and downward propagation of the tension fractures. However, in situ stress measurements made in extensional tectonic environments (Haimson, 1979;Haimson and Rummel, 1982;Zoback and Healy, 1984;Stock et al, 1985) do not show a tendency for absolute tensile stresses to exist at or near the surface. Nonetheless, the fact remains that on the Reykjanes Peninsula in southwest Iceland, there exist at the surface both vertical tension fractures and vertical faults, the surface portions of which appear to have initiated as tension fractures.…”