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By Lancelot Thomas Hogben; Maureen Cartwright

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Brace and Kohlstedt (1980) poin t o ut that the limits of upper lithosphere stress can be de te rmine d on the assum ptio ns (i) that rock s are fract ured . and that friction on the fractures co ntrols the stress at shallow depths, an d (ii) t hat upper crustal st ren gth is based o n the strength of quart z. AI a given depth , depe nding o n the temperat ure grad ient , stren gth beco mes dependent on the cree p properties of mine rals , particularly quartz, o livine and feldspa r (see 2. 7).

McGarr (1980) sho ws, o n the basis o f determinatio ns from North A merica , southe rn Africa and Au str alia , that, o n average . 6M Pa/km in ha rd rock s. Brace and Kohlstedt (1980) poin t o ut that the limits of upper lithosphere stress can be de te rmine d on the assum ptio ns (i) that rock s are fract ured . and that friction on the fractures co ntrols the stress at shallow depths, an d (ii) t hat upper crustal st ren gth is based o n the strength of quart z. AI a given depth , depe nding o n the temperat ure grad ient , stren gth beco mes dependent on the cree p properties of mine rals , particularly quartz, o livine and feldspa r (see 2.

T hese are or iented WNW-ESE with a strike-slip se nse, par allel to the relative plate move me nt vecto r. Thi s resu lt is int erpreted as co nfirmation tha t t he stress syste m in an ocea nic p late near the ridge is do minated by the co mpressive ridgepush force. Regional pattern ofstress orientation The most co mplete regiona l data co verage is of North America . 20) based on over 200 measureme nts. Several distinct stress prov inces can be distinguished which can readily be correlat ed with the wellknown tecto nic prov inces.

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