45. Bird, P. (2002) Stress-direction history of the western United States and Mexico since 85 Ma, Tectonics, 21(3), doi:10.1029/2001TC001319.

Abstract. 369 paleostress direction indicators (sets of dikes, veins, or fault slip vectors) are collected from previous compilations and the geologic literature. Like contemporary data, these stress directions show great variability, even over short distances. Therefore, statistical methods are helpful in deciding which apparent variations in space or in time are significant. First, the interpolation technique of Bird and Li [1996] is used to interpolate stress directions to a grid of evenly-spaced points in each of seventeen 5-m.y. time steps since 85 Ma. Then, a t-test is used to search for stress direction changes between pairs of time windows whose sense can be determined with some minimum confidence. Available data cannot resolve local stress provinces, and only the broadest changes affecting country-sized regions are reasonably certain. During 85-50 Ma, the most compressive horizontal stress azimuth was fairly constant at about 68 (United States) to 75 (Mexico). During 50-35 Ma, both counterclockwise stress changes (in the Pacific Northwest) and clockwise stress changes (from Nevada to New Mexico) are seen, but only locally and with about 50%-confidence. A major stress-azimuth change by ~90 occurred at 332 Ma in Mexico and at 302 Ma in the western United States. This was probably an interchange between and caused by a decrease in horizontal compression and/or an increase in vertical compression. The most likely cause was the roll-back of horizontally-subducting Farallon slab from under the southwestern United States and northwest Mexico, which was rapid during 35-25 Ma. After this transition, a clockwise rotation of principal stress axes by 36-48 occurred more gradually since 22 Ma, affecting the region between latitudes 28N and 41N. This occurred as the lengthening Pacific/North America transform boundary gradually added dextral shear on northwest-striking planes to the previous stress field of SW-NE extension.

Entire paper as a 12-page black/white .pdf file (2.6 MB)

The paleostress direction data base (3 small text files, via FTP)

 

Figure 1. Schematic and qualitative tectonic history, based on Engebretson et al. [1985], de Cserna [1989], Axen et al. [1993], and Bird [1998]. No palinspastic restoration is attempted (except in the Pacific basin). Regions of highest strain-rate at each epoch are shown with shading. Only the strain-rate axes in the northern part of (B) and the southern part of (C) result from formal computations [Bird, 1998]; other axes are drawn perpendicular to the mean trend of dip-slip faults active at that time. Distribution of high strain-rates in (E) is based primarily on historical seismicity.

 

Figure 2. Comparison of 39 paleostress direction data [left, from the most recent 5-m.y. time window] with 706 quality "A", "B", or "C" contemporary stress direction data from the World Stress Map [right, from Mueller et al., 1997]. Each data set has been interpolated with the same algorithm (Appendix B). All symbols show the azimuth of , the most compressive horizontal principal stress direction. Because stress direction data are noisy, statistical interpolation by the method of Bird and Li [1996] gives only limited weight to the nearest data, and results in very smooth fields of interpolated directions (gray bars). An alternative view is that most high-quality data are basically correct, and that the stress-direction field is separated into small provinces by sharp transitions [Zoback and Zoback, 1980]. The difference in interpolated azimuths from the United States portion of the left map to the right map is about 12, which could be an artifact of the limited amount of paleostress data. (The difference would be within the 90%-confidence limits shown.) However, this paper argues that the effect is real, because it is the continuation of a gradual clockwise rotation of stress directions that began about 22 Ma.

 

Figure 3. Geologic data on the direction of the most-compressive horizontal principal stress (solid or open-box bars) and interpolated directions (gray bars) during the time step 70-65 Ma (Late Cretaceous: Maastrichtian). Data are plotted at present coordinates, without palinspastic restoration. Oblique Mercator projection, which is conformal. Open-box symbols indicate data which have only fractional relevance to this time step. Note that data in Nevada, Utah, and Colorado could be interpreted as establishing a different (E-W) direction. However, most of these data have fractional relevance and large uncertainties.

 

Figure 4. Stress change map, comparing "early Laramide" time step 70-65 Ma (Late Cretaceous: Maastrichtian) with "late Laramide" time step 40-35 Ma (Middle-Late Eocene). Triangles merely show the geographic region associated with each interpolation grid point. Color of triangle indicates the amount of rotation of from the earlier time to the later. Triangles are only plotted around grid points where rotation is significant with 50% or greater confidence, according to a t-test. The most common rotations are 10-30 clockwise, in scattered areas such as east-central Nevada, Wyoming, and New Mexico. Counterclockwise rotation is seen mainly in the areas of the Eocene dike swarm of Hyndman et al. [1988] in Idaho-Montana. Oblique Mercator projection, showing present state lines without palinspastic restoration.

 

Figure 5. Stress change map, comparing the 40-35 Ma (Middle-Late Eocene) time step with the 30-25 Ma (mid-Oligocene) time step. Conventions as in Figure 4, except that here all rotations shown are significant with 90%-confidence. A dramatic change in azimuth by nearly 90 (the greatest possible change) has affected the whole region. This is interpreted as an interchange of the most-compressive and least-compressive stress axes.

 

Figure 6. Geologic data on the direction of the most-compressive horizontal principal stress (solid or open-box bars) and interpolated directions (gray bars) during the time step 30-25 Ma (mid-Oligocene). Conventions as in Figures 2 and 3.

 

Figure 7. Possible causes for the two greatest stress reorientations found in this study. Grey lines labeled 35, 30, and 25 Ma mark the western limits of arc volcanism at each of those times, according to Dickinson and Snyder [1978] and Urrutia-Fucugauchi [1986]. Lands to the southwest of these lines were underlain by oceanic lithosphere of the Farallon plate, subducting horizontally to the northeast. The progressive loss of contact with the Farallon plate decreased horizontal coupling to North America and decreased the northeast-ward compression, while simultaneously causing uplift and increased vertical compression. Solid lines labeled 24, 16, 8, and 0 Ma show the latitudinal extent (but not the correct longitude) of the Pacific/North America transform margin (ref. Figure 1 D-E), according to Engebretson et al. [1985]. Increasing transform length probably caused increased transmission of northwestward tractions from the Pacific plate to North America. Superposed on the pre-existing NE-SW extensional stress field, this caused a clockwise rotation of principal stress axes.

 

Figure 8. Stress change map, comparing the 25-20 Ma (Late Oligocene-Early Miocene) time step with the 5-0.01 Ma (Pliocene-Pleistocene) time step. Conventions as in Figure 4, except that here all rotations shown are significant with 90%-confidence. This reveals the cumulative effects of a slow clockwise rotation of .

 

Figure 9. History of most-compressive horizontal principal stress () azimuth at "Four Corners" (37N, 109W) in the southwestern United States since 85 Ma. Fine bounding lines show 90%-confidence limits at each time step. (Smooth curves are drawn through discrete values computed for 5 m.y. steps, although it was necessary to assume constant azimuth within each time step in order to do the calculations.) Diamond at (0 Ma, 11) shows the result from the contemporary stress field of Figure 2.