NEHRP Final Technical Report

USGS Award Number: G09AC00464

Title of award: Investigations of tectonic deformation in the Yakima River canyon

Authors and affiliations:

Harvey M. Kelsey Dept. of Geology Humboldt State University Arcata, CA 95521 707 826 3991; fax 707 826 5241 [email protected]

Tyler Ladinsky Dept. of Geology Humboldt State University Arcata, CA 95521 707 826 3991; fax 707 826 5241 [email protected]

Award Period: 3/01/2010 through 02/28/2011

1 TITLE OF FINAL TECHNICAL REPORT:

Investigations of tectonic deformation along the Manastash Ridge range front

Title of award: “Investigations of tectonic deformation in the Yakima River canyon”, USGS Award Number: G09AC00464

Kelsey, H. M., Department of Geology, Humboldt State University, Arcata CA 95521 Ladinsky, T., Department of Geology, Humboldt State University, Arcata CA 95521

1. ABSTRACT

The Manastash Ridge range front on the south edge of the Kittitas Valley near Ellensburg, Washington is a prominent north-facing range front within the Yakima fold belt that hosts a suite of landforms that may reflect active faulting. Quaternary mapping on LiDAR imagery of the northern limb of the Manastash anticline provides evidence for episodic uplift and/or baselevel lowering that may be associated with crustal shortening of the Manastash anticline. The geomorphic evolution of the Manastash front is preserved through uplifted alluvial fan and uplifted river deposits. Field verification of the LiDAR mapping corroborated a series of fan and stream deposits. The fans record periods of sedimentation from short, steep drainages issuing north off the Manastash range front. The stream alluvium, which was deposited by the Yakima River, occurs on uplifted terraces. The fans and river deposits have been uplifted relative to base level in the Yakima River valley, forming perched fans and strath terraces respectfully. The sequence of Quaternary alluvial and fan deposits suggest a minimum of three baselevel-lowering events at the Manastash front. From the lack of well developed loess cover on lowest fan, we infer that the most recent baselevel lowering event was latest Pleistocene or Holocene in age. The youngest fan deposit also is cut by a Holocene fault scarp from which we infer the uplift of the range front is Holocene-active. Abandoned fan deposits are consistent with the interpretation that the Manastash Ridge is translating upward relative to the Kittitas Valley. Each baselevel lowering event may be a manifestation of one, or more likely several, co-seismic slip events (earthquakes) on a fault underlying the range front.

1. INTRODUCTION AND GEOLOGIC SETTING The Yakima fold belt encompasses a region east of the Cascade arc in Washington and northern Oregon where generally east-west to northwest-southeast tending anticlines document north-directed contraction in the latter part of the Tertiary (Bentley, 1977; Reidel, 1984; Reidel et al., 1994; Wells et al., 1998). The fold belt deforms the Columbia River Basalt, which extruded onto the continental margin in Miocene time. The north central part of the fold belt (Figure 1) includes the Kittitas Valley and the three prominent anticlines that occur between Kittitas and Yakima Valleys, the Manastash, Umtanum and Yakima anticlines (Figure 1). A compelling structural model for the form and style of growth of the Yakima fold belt fold is needed. Lack of such a compelling model to date is due in part to a lack of imagery of a fold and to a lack of mapping that is focused within an area with excellent imagery. To this end, our project will address Yakima-fold deformation using LiDAR imagery and field mapping. The objective of this research is to investigate whether the northern front of the Manastash Ridge, where it transitions to the Kittitas Valley, has evidence for Holocene age deformation. This investigation is prompted first, by the specific observation that several folds in the Yakima fold belt are associated with active faults that have Holocene scarps (Campbell and Bentley, 1981; West et al., 1996), and second, by the general observation that anticlines may develop in the hanging wall of reverse faults, either as fault bend folds or fault propagation folds (Suppe, 1983; Yeats, 1986). If the folds or associated

2 faults are active, then the frontal region of the fold, at its juncture with the adjacent lowland, is often the site of uplifted Holocene deposits or Holocene-active fault scarps. Therefore the objective of this work is to evaluate whether the Manastash Range front at the southern margin of the Kittitas Valley has evidence for Holocene-active faults. 2. RESEARCH APPROACH LiDAR. The two LiDAR data sets employed are first, the Plate Boundary Observatory LiDAR data, which is a 5.5-km-wide strip down the Yakima canyon from Ellensberg to south of the city of Yakima, and, second, an Army Corp of Engineers LiDAR data set that both includes the canyon and a broader region of the fold belt to the east and west of the canyon. The LiDAR data sets have been incorporated into Arc GIS. Within ArcMap, we have defined attribute layers based on the digital elevation model (DEM), including hillshade, slopeshade and contour intervals. Figures 2 and 3 show hillshade images of the study area. Geologic mapping. We constructed a LiDAR-based neotectonic map that maps fans, terraces, scarps and landslides. The map product (Figure 4) shows landscape features and geologic units that have left a neotectonic signature on the landscape. Terrace and fan landforms are classified by relative age based on surface morphology and elevation. Clast inventories of alluvial deposits. We inventoried the lithology of clasts in alluvial deposits along the base of the Manastash range front to determine whether the clast composition was entirely Columbia River basalt or whether the clasts were a mixture of Columbia River basalt and lithologic types derived from the west in the Cascades Mountains. If entirely Columbia River basalt lithology, then the origin of the deposits would be locally-derived streamside gravel from the Manastash Range. If the lithologic composition was both Columbia River basalt and Cascade-Mountain-derived lithologic units, then the clast origin would be mainstem Yakima River in origin. The “streamside” versus “mainstem” gravel distinction was introduced by Waitt (1979) and is significant because such compositional differences separate locally derived “streamside” fan gravels (Columbia River basalt) that originate in steep, short drainages of the Manastash anticline from far-traveled, “mainstem” gravels that must have been transported from the Cascade Range by the Yakima River and its upstream tributaries. Geochronology. An age estimate of tephra from one of the exposures of fan deposits is pending; Elmira Wan of the USGS is doing the analyses. Additional ages of fan surfaces are pending based on luminescence dating of loess material collected on the fans surfaces. Shannon Mahan of the USGS is doing the luminescence work.

3. RESULTS The northern edge of the Manastash Range front has an abrupt, clearly defined transition northward to the southern edge of the Yakima River valley (Figure 2). At the southeast edge of the study area, this abrupt transition from range front to valley floor is the product of recent lateral erosion by the Yakima River. However, along most of the range front, the modern river is separated from the uplands at tributary junctions by alluvial fans that are the product of deposition at the mouths of steep tributaries that drain northward off the range front. These fans do not gradually merge with the valley floor to the north but rather have abrupt truncation marked by west-northwest-trending scarps (Figure 2). Annotations on the LiDAR image (Figure 3) depict the location of these scarps. Similarly, stream gravel deposits of the Yakima River (“mainstem gravel”) are perched above the Yakima River floodplain (units Quf and Plt, Figure 4). There are three generations of uplifted Quaternary fan deposits (Ladinsky et al., 2010) (Figure 4). The most recent fan (Qf1, Figure 4) is graded to the Yakima River valley alluvium. A subset of this fan deposit (Qf1a, Figure 4) is defined where surface roughness indicates the fan is younger than Qf1. Recent faulting has cut a fault scarp across this youngest fan deposit.

3 Units Qf2 and Qf3 (Figure 4) are older fan deposits that have been uplifted relative to the modern base level of the Yakima River. Good preservation of uplifted alluvial fan and stream deposits can be seen at Long Tom Canyon, Spring Canyon, Dead Cow Gulch North and Dead Cow Gulch South (Figures 3 and 4).

4. DISCUSSION The Manastash Range, at the juncture with the south margin of the Kittitas valley, displays two sets of geologic evidence for Holocene-active faulting. The first data set consists of alluvial fan deposits that are displaced upward relative to the modern alluvial-fan base level within the Kittitas Valley (Figure 4). And the second data set is a series of fault scarps that cut across the base of the range front and are discernable on LiDAR imagery (Figures 2 and 3). Based on the terraced sequence of Quaternary alluvial fan deposits, we infer a minimum of three baselevel-lowering events at the Manastash range front. The baselevel lowering events document periods of time when fan deposits were displaced upwards relative to the Yakima Valley. We infer such time periods encompass intervals when several range-front earthquakes elevated the range relative to the valley, forcing the short, steep tributary streams draining north off the range front (Long Tom Canyon, Spring Canyon, Dead Cow Gulch North and Dead Cow Gulch South) to cut through their alluvial fan debris in order to maintain grade with the Yakima River valley. The fault scarps visible on LiDAR imagery are meters to ten meters high and probably are the net result of multiple earthquakes. However a 1.5-meter-high scarp at the mouth of Dead Cow Gulch North appears to be a single- or two-event scarp. This scarp will the focus of an exploratory trench investigation in summer 2011 or summer 2012.

REFERENCES Bentley, R. D., 1977, Stratigraphy of the Yakima basalts and structural evolution of the Yakima ridges in the western Columbia Plateau, in Brown, E.H. and Ellis, R.C., editors, Geological Excursions in the Pacific Northwest: Western Washington University, p. 339-390. Published as a geology field guide in conjunction with the 1977 annual meeting of the Geological Society of America. Campbell, N. P. and Bentley, R.D., 1981, Late Quaternary deformation of the Toppenish Ridge uplift in south-central Washington, Geology, 9, 519-524. Ladinsky, T. C., Kelsey, H. M., Sherrod, B. L. and Pratt, T. L., 2010, Range-front deformation on the northern limb of the Manastash anticline, Yakima Fold belt, Washington, EOS Trans., AGU, EP53B-0620. Reidel, S.P., 1984, The Saddle Mountains: the evolution of an anticline in the Yakima fold belt, American Journal of Science, 284, 942-978. Reidel, S. P. Campbell, N.P., Fecht, K.R., and Lindsey, K.A., 1994, Late Cenozoic structure and stratigraphy of south-central Washington, in Lasmanis, R. and Cheney, E.S., conveners, Regional Geology of Washington State: Washington Division of Geology and Earth Resources Bulletin 80, 159-180. Suppe, J., 1983, Geometry and kinematics of fault-bend folding, American Journal of Science, 283, 684-721. Waitt, R. B., 1979, Late Cenozoic deposits, landforms, stratigraphy and tectonism in Kittitas Valley, Washington, U. S. Geological Survey Professional Paper 1127, 18 p. Wells, R. E., C. S. Weaver, R. J. Blakely, 1998. Forearc migration in Cascadia and its neotectonic significance. Geology 26, 759-762. West, M.W., Ashland, F.X., Busacca, A.J., Berger, G.W., and Shaffer, M.E., 1996, Late Quaternary deformation, Saddle Mountains anticline, south-central Washington, Geology, 24, 1123-1126.

4 Yeats, R. S., 1986, Active faults related to folding: Washington, D.C., Geophysics Study Committee, National Research Council, National Academy Press, 63-79.

PUBLICATIONS RESULTING FROM THE WORK PERFORMED Ladinsky, T. C., Kelsey, H. M., Sherrod, B. L. and Pratt, T. L., 2010, Range-front deformation on the northern limb of the Manastash anticline, Yakima Fold belt, Washington, EOS Trans., AGU, EP53B-0620.

ACKNOWLEDGMENTS Brian Sherrod (USGS) provided input in all phases of this project and arranged for the use of the Army Corps of Engineers LiDAR data. Tom Pratt (USGS) discussed with us a seismic line through Shushuskin Canyon within the study area. Elizabeth Barnett, USGS, contributed the base data for Figure 1.

FIGURE CAPTIONS Figure 1. Location map of the Manastash Ridge study area in the context of the Kittitas Valley and the lower Yakima River canyon. The lower Yakima River canyon is incised into the Manasatash Ridge anticline. Figure 2. LiDAR image of the northern front of the Manastash Ridge to the east of the head of the lower Yakima River canyon. See location of image on Figure 1. The image depicts the transition from the Kittitas Valley lowland southward to the front of Manastash Ridge. At the transition from the lowland to the foothills of the Manastash upland, there are a series of linear topographic features that are delineated as faults on Figure 3. Figure 3. Annotated LiDAR image of the northern front of the Manastash Ridge to the east of the head of the lower Yakima River canyon. See location of image on Figure 1. Red lines delineate inferred traces of reverse faults that border the base of Manastash Ridge. Figure 4. Geologic map of the northern front of the Manastash Ridge to the east of the head of the lower Yakima River canyon. Contour interval is 5 meters.

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