Project No. 93-1350 [nc. April 1996

1 1 Public Reading Room U. S. Department of Energy Idaho Operations Office

Report Siting Feasibility of Locations For Dry Storage Facility on the MEL That are Removed From Over the Snake River Plain Aquifer a Idaho National Engineering Laboratory

Westinghouse Electric Corporation 0 West Mifflin, Pennsylvania 0

rl-s-cov-1350/96 REPORT SITING FEASIBILITY OF LOCATIONS FOR DRY STORAGE FACILITY ON THE INEL THAT ARE REMOVED FROM OVER THE 01 SNAKE RIVER PLAIN AQUIFER

PROJECT No. 93-1350 APRIL 22, 1996

DI

PAUL C. RIZZO ASSOCIATES 300 OXFORD DRIVE MONROEVILLE, PENNSYLVANIA 15146 TELEPHONE: (412) 856-9700 TELEFAX: (412) 856-9749

r1-24.1350/96 TABLE OF CONTENTS

PAGE

LIST OF FIGURES ii

1.0 INTRODUCTION 1 1.1 THE SNAKE RIVER BASIN 2 1.2 THE SNAKE RIVER.BASIN AQUIFERS 2

2.0 ROCK UNITS OF THE SNAKE RIVER BASIN 3 2.1 BLOCK-FAULTED MOUNTAINS AND TERTIARY D VoLcAmaAsncs 3 2.2 ESRP DEPOSITS 4

3.0 HYDROGEOLOGY OF TIM SNAKE RIVER BASIN AQUIFERS 6 3.1 ALLUVIAL AQUIFER 6 3.1.1 Lemhi Range Area 8 3.1.2 Birch Creek Area 8 3.2 SNAKE RIVER PLAIN AQUIFER 9 3.2.1 Recharge 9 3.2.2 Matrix Properties 10 3.2.3 Water-Table Gradient 11 o 3.2.4 Aquifer Velocity and Yield 11 I 4.0 SEISMICITY 12 5.0 TOPOGRAPHY 13

6.0 CONCLUSIONS 14

GLOSSARY REFERENCES of FIGURES rl -too-1350/96 LIST OF FIGURES

FIGURE NO. TITLE

1 LOCATION OF STUDY AREA

2 MAP OF INEL SHOWING LOCATIONS OF SELECTED FACILITIES,PLAYAS, AND EPHEMERAL STREAMS

3 STRUCTURAL AND TECTONIC FEATURES IN INEL AREA

4 GENERALIZED SOIL TYPES

5 MAP OF INEL SHOWING AREAS NOT ABOVE SNAKE RIVER PLAIN AQUIFER

6 ALTITUDE OF THE WATER TABLE AQUIFER AND GENERAL DIRECTION OF GROUND WATER 9 MOVEMENT,JULY 1988 7 MAP OF INEL SHOWING AREAS THAT ARE LESS THAN ONE MILE FROM A CAPABLE FAULT

8 PROBABILISTIC SEISMIC HAZARD MAP FOR THE INEL-PEAK HORIZONTAL ACCELERATION. AT ROCK FOR A RETURN PERIOD OF 5,000 YEARS

of a-too-1350/96 REPORT SITING FEASIBILITY OF LOCATIONS FOR DRY STORAGE FACILITY ON THE INEL THAT ARE REMOVED FROM OVER THE SNAKE RIVER PLAIN AQUIFER

1.0 INTRODUCTION

The agreement between the State ofIdaho and the federal government involving the shipment of additional spent nuclear fuel to the Idaho National Engineering Laboratory (INEL)includes a provision that all spent nuclear fuel at INEL will be transferred from wet storage to dry storage (U. S. District Court, 1995; Paragraph E.8). The agreement also states that "DOE shall, after consultation with the State ofIdaho, determine the location of the dry storage facilities within the INEL, which shall, to the extent technically feasible, be at a point removed from above the Snake River Plain Aquifer." The purpose of this report is to address locations at INEL that might be removed from above the Snake River Plain Aquifer(SRP Aquifer) and to compare them to locations at INEL that are over the SRP Aquifer. As part of the search for a technically feasible location at a point removed from above the SRP Aquifer, this report also addresses the recharge to the SRP Aquifer, the magnitude of potential earthquakes, and topography and foundation 0 conditions of the area. In addressing siting considerations for a new dry storage facility at the INEL, this report places particular emphasis on the hydrogeologic characteristics of the aquifers that comprise the Snake River Basin. In discussing the Snake River Basin aquifers, it is important to recognize the relationship of the SRP Aquifer with other aquifers in the Snake River Basin. Accordingly, the Report addresses the geologic characteristics and aquifer hydrogeologic properties of the SRP Aquifer within the context of the larger Snake River Basin.

Et For the convenience of the reader, a glossary has been provided at the end of this Report. of Of 2

0 1.1 THE SNAKE RIVER BASIN

The Snake River Basin is that tract of southern Idaho that gathers water originating as precipitation and discharges it to the Snake River (Figure 1). The Eastern Snake River El Plain(ESRP), with its characteristically low topographic relief consists of about 10,800 square miles and is located within the east-central part of the Snake River Basin. Almost all of the INEL is located in the ESRP. Two relatively small areas of the INEL appear to be outside the ESRP, but they are still within the Snake River Basin (Figure 1). These two areas are of interest for use as possible sites for a new dry storage facility because they might offer locations with less risk to the Snake River Basin aquifers. One of these areas in the northern portion ofthe INEL will be referred to as the Birch Creek Area, and CI the other area on the west side of the INEL will be referred to as the Lemhi Range Area (Figure 1).

1.2 THE SNAKE RIVER BASIN AQUIFERS

The Snake River Basin encompasses at least four regional aquifers, namely:

• The unlithified and unconsolidated intermontane basin B fill which is actually a group of aquifers called the 0 Alluvial Aquifer herein; • The SRP Aquifer;

J • The Basin-and-Range Physiographic Province which consists of normal block-faulted Precambrian, Paleozoic, and Mesozoic sedimentary rocks (referred to as the Uplifts); and

• The saturated Tertiary rhyolitic rocks of the Mt. Bennett Frills Area.

0 Two of these aquifers, the SRP Aquifer and the Alluvial Aquifer, provide most of the water that is in storage under the Snake River Basin. The Alluvial Aquifer includes a unconsolidated intermontane clastic debris north and west of the ESRP. It is of rl-.-1331196 a! 3

characterized by a relatively shallow water table elevation and it discharges into the SRP Aquifer. The SRP Aquifer is the principal groundwater storage and water source for the Snake River Basin.

The other two regional aquifers that charge the SRP Aquifer are not well described in the literature, but they are nevertheless included in this discussion for completeness. Uplifts recharge the Alluvial Aquifer which, in turn, recharges the SRP Aquifer. Groundwater within the Tertiary rhyolitic rocks of the Mt. Bennett Hills Area discharges into the SRP Aquifer downgradient of the INEL and thus has no impact on the INEL.

This report focuses on the SRP Aquifer and the Alluvial Aquifer; both of which occur in the vicinity of INEL. Section 2.0 briefly describes the rock units comprising the Snake River Basin and develops a backdrop for the hydrogeologic discussion in Section 3.0 with respect to movement of groundwater through the geologic deposits and the respective aquifer recharge. Section 4.0 briefly presents the seismicity of the ESRP and areas of INEL that are outside of the ESRP. Section 5.0 briefly describes the topography and foundation conditions of the siting areas under consideration. Finally, Section 6.0 presents conclusions with respect to the recharge from various sites to the SRP Aquifer and their relationship to the potential dry storage sites under consideration.

2.0 ROCK UNITS OF THE SNAKE RIVER BASIN

The Snake River Basin consists of clastic limestone, and igneous rocks. The two-principal rock units of interest with regard to groundwater storage and flow are the intermontane unconsolidated clastic sediments located north of the ESRP and the igneous and sedimentary suites that characterize the ESRP. Other formations that impact the recharge of the aquifers in the Snake River Basin include the Uplifts principally north and west of the ESRP and the Tertiary volcaniclastics west and south of the ESRP.

2.1 BLOCK-FAULTED MOUNTAINS AND TERTIARY VOLCANICLASTICS

The Basin-and-Range normal-block-faulted mountains (the Uplifts) lying to the north and west of the ESRP contribute to the groundwater resources, principally as a watershed area of rl-a-1350196 a! 4

(i.e., collection and distribution, not as storage). The block-faulted mountains consist of Precambrian, Paleozoic, and Mesozoic sedimentary deposits. The Uplifts north of the ESRP were generated as part of the Basin-and-Range extensional forces and include from east to west the Bitterroot Range, Beaverhead Range, Lemhi Range, and Lost River Range (Figure 2). These Uplifts were created by enormous offsets ofPrecambrian, Paleozoic and Mesozoic rocks with the faulting occurring on the west side of the ranges (Figure 3).

The throws on the normal faults associated with the Uplifts have been reported to be thousands of meters (King et al., 1987). Movement on these faults has been active within the last 4.7 million years with a mean slip rate of0.3 mm/year at the center of the Uplift and 0.1 nun/year at the southeastern ends where they intersect the ESRP (Scott et al., D 1985). Witkind (1975) classified the normal faults north of the INEL Area as Pleistocene or older and several display Holocene activity. These Uplifts have deposited enormous volumes of clastic debris into the intermontane basins.

The Tertiary rhyolitic volcaniclastic deposits of Mt. Bennett Hills in northern Blaine County, Idaho Falls have storage capacity; however, their subaerial position relegates them to be predominantly unsaturated. The aquifer associated with these deposits has no bearing upon the INEL Area because its recharge is down-gradient (i.e., south and west) o ofthe INEL and does not affect the groundwater beneath the INEL. 2.2 ESRP DEposrrs

Miocene basalt and silicic volcanic rocks, chiefly Idavada Volcanics are overlain by basalts of the Snake River Group. The Tertiary-aged Snake River Group consists of intercalated basalt and sediments. The basalt of the Snake River Group has a cumulative thickness of approximately 1,500 meters (Whitehead, 1985a; Whitehead 1986b).

The eastern part of the ESRP is bounded by Cenozoic, Mesozoic, and Paleozoic rocks, chiefly limestone, sandstone, and shale of the Basin-and-Range Physiographic Province (Rodgers and Janecke, 1992). Tertiary rhyolitic rocks bound the western part of the ESRP north of Twin Falls(Mt. Bennett Hills) and Cretaceous granitic rocks of the Idaho batholith are north of the Mt. Bennett Hills (Pierce and Morgan, 1992).

a-a-1350/96 5

Basalt of the Snake River Group was extruded from a series of volcanic vents that are aligned along volcanic rift zones (Kuntz and Dalrymple, 1979). The rift zones are parallel to and are generally aligned with normal faults that flank Basin-and-Range type structures on both sides of the ESRP (Pierce and Morgan, 1992). Basalt is thickest near the center of the ESRP and thins toward the borders where it is intercalated with sedimentary rocks.

Single basaltic lava flows generally range from 1 to 20 m in thickness and average about 4m in thickness(Kuntz, 1978). These individual flows cover 130 to 300 km2 and are as much as 30 km in length. A typical flow consists of a basal layer of oxidized, fine-grained scoriaceous basalt, usually less than 1 m thick; a massive central layer coarser-grained basalt with a thickness of several meters to 20 m thick; and a fine-grained, intensely jointed, vesicular, clinkery basalt top layer that is less than 2 m thick (Kuntz et al., 1980). The volcanic and sedimentary units form a complex overlapping and interlocking depositional unit.

Separation of the Snake River Group into discrete rock units in the subsurface is generally difficult; however, it has been moderately successful on a local scale at the INEL site where basalt sequences have been divided into several groups of flows on the basis of stratigraphic, radiometric, and paleomagnetic information (Anderson, 1991; Kuntz et al., 1992). Flow groups typically are separated by sedimentary interbeds. A deep test hole by the U. S. Geological Survey at the INEL site demonstrated the intercalation of sediments and volcaniclastics (Doherty et al., 1979).

Joints in the massive central parts offlows are typically vertical and form polygonal columns of basalt. Tension joints formed by cooling and contraction are characteristic of basalt of the Snake River Group. Other less regular fractures developed along the leading edges of flows and as collapse features (Lindholm and Vaccaro, 1988). Joints, open fissures, and minor displacement faults are concentrated in rift zones. Depths offractures visible at the surface are unknown, but the presence of cinder cones, lava cones, fissure flows, and other volcanic landforms along rift zones suggest that the fractures may have been healed at depth by movement of magma subsequent to fracturing. Open fissures in basalt are common on pressure ridges (i.e., top of basalt flows) and are located near the of rl-a-1350/96 6

surface (Lindholm and Vaccaro, 1988). Open fissures promote rapid vertical transport of precipitation.

Voids in basalt differ greatly in size and degree of interconnection. Permeability is significantly enhanced by fracturing of void-bearing volcanic rock. Macroporosity consists of lava tubes as much as 5 m or more in diameter and 1,000 m or more in length (Mace et al., 1975). Vesicles may exceed 25 percent of total rock volume, and 10 to 20 percent is common in the upper parts of flows(Lindholm and Vaccaro, 1988). Total rock porosity in the SRP Aquifer ranges between 6 and 37 percent, and effective porosity (i.e., interconnected) ranges from 4 to 22 percent (reported in Lindholm and Vaccaro, 1988).

3.0 HYDROGEOLOGY OF THE SNAKE RIVER BASIN AQUIFERS

Precipitation that falls on the Snake River Basin and does not evaporate or transpire, either flows to the SRP Aquifer to be discharged to the Snake River, or is transmitted by streams to the Snake River. The Snake River discharges flow to the Columbia River at Kennewick, Washington.

The SRP Aquifer and the adjacent intermontane valley-fill saturated sediment sequences (i.e., the Alluvial Aquifer) dominate the Snake River Basin with regard to storage and ground water availability (Lindholm and Vaccaro, 1988). The Tertiary volcanic aquifer on the western portion of the ESRP is not a major source of recharge to the SRP Aquifer under the INEL since it is located downgradient ofthe INEL; therefore, it is not important to the discussions herein.

3.1 ALLUVIAL AQUIFER

The Alluvial Aquifer lies north and northwest of the[NEL and is located in the valleys of the Basin and Range mountains (Figure 2). The Alluvial Aquifer transmits ground water from the mountainous areas adjacent to the ESRP to the SRP Aquifer. Little has been written about this aquifer since it is very heterogeneous, occurs in complex settings such as alluvial plains and fluvial settings and the specific capacity of water wells is lower than the specific capacity of wells in the SRP Aquifer. This aquifer occurs in intermontane

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deposits that are coarse-grained, poorly sorted, and largely unconsolidated. These rock sequences are up to several hundred meters thick (Lindholm and Vaccaro, 1988).

The mountainous areas north and northwest of the ESRP receive more precipitation than the ESRP. These areas direct sheetflow and groundwater to the intermontane valley-fill areas (Alluvial Aquifer) where recharge of the SRP Aquifer occurs. These mountainous areas adjacent to the intermontane valleys normally receive 20 to 30 inches of precipitation per year. As a contrast, the ESRP receives only 8 to 10 inches of precipitation per year, and the SRP Aquifer in the INEL Area only receives a recharge of less than one inch per year (Garabedian, 1992). Therefore, the recharge to the SRP Aquifer from the Alluvial Aquifer is significant.

The INEL is located in an enclosed basin that drains three of these northern tributaries; Big Lost River, Little Lost River, and Birch Creek (Irving, 1992). These tributaries and underflows capture precipitation from the adjacent mountain watersheds located to the north and northwest ofINEL (Lost River Range, Lemhi Range, and Bitterroot Range) and discharge groundwater and surface water to the SRP Aquifer.

The Big Lost River is impounded west ofINEL at Mackay Dam and is the major surface water feature on the INEL (Figure 1). The flow in the Big Lost River travels past Arco through Box Canyon and reaches the INEL, where it is either diverted into man-made playas or flows northward to the Lost River Sinks, a natural playa (Figure 2). At the Lost River Sinks, flow is lost to evaporation and infiltration (Irving, 1992). The ponded water at the Lost River Sinks provides recharge to the SRP Aquifer.

The Little Lost River is 35 miles long and drains the Lemhi and Lost River ranges. During the summer, flow is diverted for irrigation north of Howe, Idaho or lost to evaporation. Preiumably, underflow reaches the INEL and recharges the SRP Aquifer. Subaerial channelized flow that travels to the ESRP undergoes evaporation and provides recharge to the SRP Aquifer.

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3.1.1 Lemhi Range Area

The Lemhi Range Area encompasses the southern extension of the Lemhi Mountain Range. As seen in Figure 5, part ofthe Lemhi Range Area is not over the SRP Aquifer. Even though this area is not over the Aquifer, it is adjacent to the aquifer and the run-off from this area drains to the SRP Aquifer and recharges the aquifer. Therefore, this area cannot be considered to be hydrologically removed from over the SRP Aquifer. This conclusion is consistent with the position of the U.S. Geological Survey's field office for INEL (Telephone Conversation, K.D. Willie to L. Mann, 1996). The Lemhi Range Area contains intermittent streams (erosion channels) due to its close proximity to the Lemhi Mountains. Much ofthe flatter sections are on the western side ofthe Lemhi Range and are also adjacent to private land on the[NEL boundary. This private land is down gradient with respect to ground water flow from the Lemhi Range Area (Taylor et al., 1994). a. 3.1.2 Birch Creek Area The 40-mile long Birch Creek has its origins in the springs below Gilmore Summit in the Beaverhead Mountains north of BsTEL. Birch Creek flows south between the Lemhi and the Bitterroot ranges, providing drainage for adjacent slopes of these ranges, and is captured north ofINEL for irrigation and hydropower.

In the Birch Creek Area, the boundary between the Alluvial Aquifer and the SRP Aquifer is poorly defined in part because the Alluvial Aquifer is interfingered with the SRP Aquifer. The Alluvial Aquifer provides significant recharge to the SRP Aquifer and in the Birch Creek Area, the Alluvial Aquifer is hydrologically connected to the SRP Aquifer. Therefore, the Birch Creek Area cannot be considered to be removed from above the SRP Aquifer. This conclusion is based on the Environmental Protection Agency(EPA) report on the SRP Aquifer as a Sole Source Aquifer(EPA, 1990) and is consistent with the judgement of the United States Geological Survey personnel (Telephone Conversation, K.D. Wille to L. Mann, 1996). 91 rl-a-1350/96 UI Siting a facility over the Alluvial Aquifers in the Birch Creek Area is undesirable relative to siting over the SRP at the ICPP or NRF for the following reasons:

• The vertical hydraulic conductivity through the Alluvial Aquifer at Birch Creek is inferred to be higher than that of the SRP Aquifer, implying that, for the same gradient, a contaminant would travel at a higher velocity down through the Alluvial Aquifer than down through the uppermost strata and comprising the ESRP at the ICPP or NRF.

• The vertical distance to the water table at Birch Creek is estimated to be on the order of 250 feet below grade as compared to 370 feet at the NRF and 450 feet at ICPP (L. Mann, 1996; Personal Communication). Thus the distance that the contaminant must travel to the aquifer is considerably shorter.

In view of all of the above, we consider the Birch Creek Area to be relatively undesirable from a hydrologic perspective for siting a new facility where contaminant spills are postulated to occur.

3.2 SNAKE RIVER PLAIN AQUIFER

3.2.1 Recharge

The SRP Aquifer has been greatly affected by anthropogenic factors. Diversion of surface water from rivers for irrigation over the past 100 years has increased recharge to the SRP Aquifer and now supplies about two-thirds of the total recharge (Lindholm and Vaccaro, 1988). Garabedian (1992; Plate 4) reported that since the 1950s, the groundwater withdrawal for irrigation caused a yearly drawdown of the SRP Aquifer of nearly 10 feet which is recharged in the winter and spring. Interestingly, Well 3N-29E-I4ADD1, located in the central portion ofINEL, has not displayed significant yearly variations in the water table elevation.

Basalt devoid of soil and vegetation cover composes the land surface for about 10 percent ofthe Snake River Plain (Lindholm and Goodell, 1986). In much of the rest of the plain,

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soil and sedimentary rocks, one to several hundred meters thick, overlie or are syndepositional to the basalt. They consist of sediments shed from the bordering mountains and lacustrine deposits.

The irregular, broken upper parts of basalt flows and vertical fractures in the basalt flows provide conduits for water to infiltrate vertically to recharge the unconfined aquifer. Therefore, infiltration is controlled by the texture and thickness of sediment overlying the more permeable basalt. Fine-grained sediments intercalated with basalt greatly impedes the vertical downward movement of water.

Garabedian (1992; Figure 10, Table 12) divided the ESRP into three types of recharge areas depending upon the amount of sedimentary fill overlying the basalt (Figure 4). Those areas with thickness of soil cover greater than lm had recharge rates one-third that of areas with thin soil cover (i.e., less than 1m)and an order of magnitude less than areas of recent lava flows. At ICPP the soil thickness is 5 to 15 m and at an NRF seismic station the soil thickness is 10m (Wong et al., 1990); consequently, infiltration at ICPP and NRF will be much lower than areas with less than lm of soil thickness. Under these conditions, infiltrating water may be temporarily perched by fine-grained sediment (Cecil et al., 1991).

3.2.2 Matrix Properties

The structure and hydraulic conductivity ofthe SRP Aquifer vary considerably within individual basalt flows. The fractured top of an individual basalt flow is typically very porous and has high horizontal hydraulic conductivity. The central part of an individual basalt flow may have moderately high porosity depending on the degree of vesicularity and jointing, but vertical and horizontal hydraulic conductivities of sediment between individual basalt flows are considerably lower than in the interflow zones of the SRP Aquifer. The base of a basaltic flow is typically scoriaceous and, locally, has high hydraulic conductivity (Lindholm and Vaccaro, 1988).

Horizontal hydraulic conductivity of basalt in the Snake River Group is as high as 10,000 ft/day and most commonly ranges from 500 to 5,000 ft/day (Garabedian, 1992). Although water moves vertically through fractures in basalt, the preferred direction of water

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movement is lateral, along interflow zones. Basalt flows at the INEL site have a reported ratio of horizontal to vertical hydraulic conductivity of 3.7 to 1, due to the massive central portion of the flow restricting vertical movement (Barraclough et al., 1976). Robertson (1976) reported that horizontal hydraulic conductivity for basalt ranges from 1 to 7,000 ft/day and vertical hydraulic conductivity of sedimentary interbeds ranges from 0.00001 to 7 ft/day. Consequently, fine-grained sedimentary interbeds generally behave as confining units. Lateral hydraulic gradients in the basalt generally range from 0.002 to 0.012 ft/ft (Garabedian, 1992).

3.2.3 Water-Table Gradient

At INEL, the water table elevation ranges from 200 feet below grade in the north-central part ofthe site to about 900 feet below grade in the southeastern part of rNEL. This gives a vertical drop across INEL of approximately 1 to 15 ft/mi (Orr and Cecil, 1991). At NRF and ICPP the water tables is at approximately 370 feet and 450 feet below grade, respectively.

3.2.4 Aquifer Velocity and Yield

Saturated Quaternary basalt of the Snake River Plain in the central portion may be 3,600 feet thick (Whitehead, 1986b) and at INEL, the aquifer is between 840 and 1,220 feet thick (Mann, 1986). Porosity and hydraulic conductivity decrease with depth and most water moves through the upper 200 ft to 500 ft ofthe aquifer. As determined by model studies, transmissivity of the upper 100 to 200 feet of the Quaternary basalt in the SRP Aquifer ranges from 1 to 56 ft2/sec (reported in Garabedian, 1992). The number and thickness of highly transmissive interflow zones are important factors in total aquifer transmissivity.

Although flow velocities vary due to aquifer heterogeneity, horizontal water movement through basalt ofthe Snake River Group faster than the movement of groundwater through sedimentary rock aquifers. General groundwater movement in the SRP Aquifer is to the southwest and in the INEL Area, movement is also to the southwest (Figure 6). Robertson et al.,(1974) reported that average water velocity in basalt ranges from 5 to 20 ft/day in the southern part ofthe INEL.

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Typical ofthe behavior of aquifers, hydraulic head in the basalt sequence decreases with depth in recharge areas and increases with depth in discharge areas. Groundwater in the vicinity ofthe springs moves upward as well as laterally to the Snake River. Within the discharge area, sedimentary interbeds and massive crystalline basalts act as semiconfining beds and impede upward movement of water. Decreases of head with depth in the recharge areas were verified in a U.S. Geological Survey test hole at INEL(On and Cecil, 1991).

4.0 SEISMICITY of Generally speaking, the ESRP is aseismic; however, the ESRP does experience seismic shaking associated with the rupture of faults located in the Basin-and-Range mountains (Smith and Sbar, 1974) that are near INEL. Several recent studies have been performed to predict earthquake magnitudes, locations, and timing (e.g., Wong et al., 1990, 1992 and 1993). The areas along the edge of the ESRP have been used in deterministic and probabilistic studies to model the impact of an event upon the facilities at INEL (Wong et aL, 1990 and 1992).

In the scenarios provided in Woodward-Clyde reports(Wong et al., 1990, 1992, and 1993), the maximum predicted event is postulated to occur as close to the INEL as is tectonically reasonable. Basically, a hypothetical M 7.0 Borah Peak-type event is postulated to occur in the vicinity of Howe at the southern terminus of the Lemhi Fault for the prediction of peak ground acceleration for seven facilities at the INEL. The postulated Howe epicenter is six kilometers from that portion of the Lemhi Range that is within the INEL. The Birch Creek Area is very close to the Beaverhead Fault, which would also be modeled with a M 7.0 Borah Peak-style earthquake. Further, peak ground acceleration values projected from modeling indicate that the Lemhi Range Area and the Birch Creek Area would have approximately a 70 percent higher peak ground acceleration values than those at ICPP and NRF (Figure 8).

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It is noted that the Lemhi Range Area, is a zone where surface rupture associated with fault movement is a definite siting and design consideration. It is well known that surface rupture occurred with the Borah Peak Earthquake. Since there are known capable faults within one miler of most of the Lemhi Range Area (Figure 7), a site in this zone would, in all probability, be abortive from a surface rupture perspective. The profession is not yet able to design civil structures to accommodate surface rupture even if one could characterize the nature, direction, and magnitude ofthe rupture sufficient for design. This is the reason that the NRC's Standard Review Plan (NUREG-0800) recommends an alternate location for such sites. Therefore, based upon seismic considerations the Lemhi Range Area is not considered technically acceptable for the siting of a dry storage facility.

In the Birch Creek Area, the Blue Dome Segment of the Beaverhead Fault is believed to exist within about two miles of the Birch Creek Areas that lies outside the SRP Aquifer boundary. While the Beaverhead Fault is viewed as capable, the capability ofthe Blue Dome segment is not clear. No evidence of offsets in 100,000 year old alluvium has been found. On the other hand, it is our opinion that the USNRC would postulate that the Blue Dome Segment is capable based on the fact that it is tied structurally to the capable Beaverhead Fault and thus it is subject to the potential for reactivation. Because of the proximity ofthe fault to the Birch Creek Area, we believe that the USNRC would suggest looking elsewhere for a site.

5.0 TOPOGRAPHY

Much of the ESRP has very low topographic relief and, as such, is an ideal region for the placement of the dry storage facility from a topographic perspective. Landslides, excessive earthwork, and unusual drainage conditions are generally not problems with relatively flat sites such as the NRF and ECF.

The foundation conditions on the ESRP, specifically at the NRF at ICPP are not problematic. There are no significant problems with bearing capacity, expansive soils, excessive settlements, sensitive clays or dewatering. The shear strength is adequate for l The nuclear profession generally considers a site within 5 miles of a capable fault to be in the vicinity of the capable fault_

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the magnitude of anticipated foundation loads. Indeed the flat topography, good foundation conditions, ready access, and the low risk of natural phenomena characterizing the ESRP, are unique in the tectonically-active, mountainous western portion of the United States.

The portion of the INEL that includes the southern extension of the Lemhi Range (the Lemhi Range Area) has steep topographic expression, and certain portions have a predilection towards landslides or slumps. The slopes in most of the Lemhi Range Area that are off the SRP have gradients as steep as 30 percent and several areas, through their topographic expression, appear to be slumped or deformed through landslides. Depending on the specific site considered, one might encounter colluvial soils with their inherent geotechnical characteristics inadequate for bearing capacity and/or excessive settlement. Perched water conditions could also exist that could lead to dewatering problems. Given the choice ofthe two possibilities, i.e., the Lemhi Range Area and the ESRP, it is clear that, from topographical and foundation perspectives, the ESRP at the NRF and ICPP is superior.

6.0 CONCLUSIONS

The Snake River Basin includes at least four aquifers, one of which is actually a group of aquifers referred to as the Alluvial Aquifer. The Alluvial Aquifer extends from the northern intermontane areas to the south and ends at the northern and western portion of INEL. It receives recharge from the adjacent mountains and contributes significant recharge to the SRP Aquifer. The Alluvial Aquifer is characterized by a shallow water table elevation and is more sensitive to anthropogenic effects since it is relatively shallow.

The SRP Aquifer resides entirely within the ESRP, which is characterized by having mostly low topographic relief and thick deposits of volcanic and sedimentary deposits. The water table gradient in the SRP Aquifer is relatively shallow, but the horizontal hydraulic conductivity is high and the aquifer displays channelized flow through some of its domain.

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The four areas within INEL that are being considered for the dry storage facility include, the NRF,ICPP, the Birch Creek Area and Lemhi Range Area. The Lemhi Range Area is not over the SRP Aquifer. However, it is adjacent to the SRP Aquifer and recharges the SRP Aquifer. Therefore, the Lemhi Range Area cannot be considered to be hydrologically removed from over the SRP Aquifer. Most of the Lemhi Range Area is steep terrain that is not suitable for a dry storage facility. Much ofthe flatter sections is adjacent private land on the INEL boundary and is down gradient with respect to the flow ofground water. In addition, there are known capable faults within one mile of most of the Lemhi Range Area, with the potential for surface ruptures. Therefore, the Lemhi Range Area is not considered technically acceptable for the siting of a dry storage facility.

The Birch Creek Area, while situated in flat terrain, is located over part of the Alluvial Aquifer. In the Birch Creek Area, the boundary between the Alluvial Aquifer and the SRP Aquifer is poorly defined in part because the Alluvial Aquifer is interfingered with the SRP Aquifer. The Alluvial Aquifer provides significant recharge to the SRP Aquifer, and, in the Birch Creek Area, the Alluvial Aquifer is hydrologically connected to the SRP Aquifer. Therefore, the Birch Creek Area cannot be considered to be removed from above the SRP Aquifer. Also, the vertical hydraulic conductivity and the water available o for recharge are inferred to be higher in the Birch Creek Area than at the ICPP or NRF. Considering the potentially higher hydraulic conductivity and the shorter travel path, this site is undesirable. Finally, the Birch Creek Area has a predicted peak ground acceleration from seismic activity that is significantly higher than the NRF and the ICPP sites and is with a few miles of a suspected capable fault. We believe the NRC would suggest looking elsewhere for a site. Therefore, the Birch Creek Area would be less desirable than NRF or ICPP.

The NRF and ICPP sites overlie the SRP Aquifer; however, the thick soil profiles at these two locations, the low infiltration rate for the ESRP, and the depth to the water-table aquifer indicates that the NRF and ICPP are suitable for the proposed dry storage facility.

The NRF and ICPP sites are located within the seismically quiescent ESRP and these two locations would be seismically favorable for a dry storage facility. These two areas are predicted to have similar peak ground acceleration based upon a Borah Peak type of event

rl-a-1350/96 16

with a postulated epicenter at Howe. Because of the similarities in the topography and geologic profile of these two sites, it is difficult to distinguish the impact to the aquifer recharge from these two sites_ Therefore, we conclude that the NRF and the ICPP should be considered equivalent from a hydrogeological and seismologic perspective for housing the new dry storage facility.

Senior Staff Consultant

PCR/PJH/sbe

r I -a-1350196 o fr--) GLOSSARY

Anthopogenic - Caused by man.

Aquifer - A geological formation of permeable rock, gravel, or sand containing or conducting groundwater, especially one that supplies the water for wells, springs, etc.

Basalt - The dark, dense, igneous rock of a lava flow or minor intrusion, composed essentially of labradorite and pyroxene and often displaying a columnar structure.

Basin - Drainage in a geographic area defined by topography wherein the area drained by a river and all its tributaries (see WATERSHED)

Cenozoic - Noting or pertaining to the present era, beginning 65 million years ago and characterized by the ascendancy of mammals.

Clastic - Sediments that are composed of fragments or particles of older rocks or previously existing solid matter.

Conduit flow - Fluid flow within an open channel such that frictional forces acting to retard fluid flow are confined to the surface of the channel (see DIFFUSE FLOW).

Diffuse Flow - Intergranular fluid flow within an aquifer in which frictional forces act to retard fluid flow.

Discharge - the transference of groundwater from one rock unit or surface source to of another porous rock unit or surface source. Ephemeral - Stream flow that lasts a very short time.

Granite (granitic) - A coarse-grained igneous rock composed chiefly of feldspar minerals and of quartz, usually with lesser amounts of one or more other minerals, as mica, hornblende, or augite.

Hydraulic Conductivity - a proportion that describes the rate at which water can move through a permeable medium, reported in length/time. In three-dimensional space, lateral hydraulic conductivity refers the rate in a horizontal direction and vertical hydraulic a conductivity refers to the rate in a vertical direction. Intercalated - The existence of one or more layers between other layers.

r1-glom-1354/96 GLOS-1 Lava Tube - The hollow space beneath the surface of a solidified lava flow, formed by the withdrawal of molten lava after the formation of the surface crust.

Mesozoic - Noting or pertaining to a geologic era occurring between 230 million and 65 million years ago, characterized by the appearance of flowering plants and by dinosaurs.

Normal Fault - A break in the continuity of a body of rock, with dislocation along the plane of the fracture (fault plane) where the downdropped block places younger rock adjacent to older rock.

Paleomagnetic - Magnetic polarization acquired by the minerals in a rock at the time the rock was deposited or solidified. A method for dating rocks.

Paleozoic - Of or pertaining to a geologic era occurring between 570 million and 230 million years ago, when fish, insects, and reptiles first appeared.

Perched - Unconfined ground water separated from an underlying main body of groundwater by an unsaturated zone.

Permeability - A measure of the communication of pores in a porous media.

Playa - The flat, central floor of a basin with interior drainage.

Pleistocene - Of or pertaining to the geologic epoch forming the earlier half of the Quaternary Period, beginning about two million years ago and ending ten thousand years ago, the time of the last Ice Age and the advent of modern humans.

Porosity - A measure of the void spaces in a solid media.

Precambrian - Noting or pertaining to the earliest era of earth history, ending 570 million years ago, during which the earth's crust formed and life first appeared in the seas.

Quaternary - Of or pertaining to the present period of earth history forming the latter part of the Cenozoic Era, originating about two million years ago, and including the Recent and Pleistocene Epochs.

Radiometric - The measurement of geologic time by the study of parent and/or daughter isotopic abundances and known disintegration rates of the radioactive parent isotopes.

Range - Referring to a physiographic province formed by extensional tectonic forces that produced mountain ranges with the adjacent low land is separated by faulting. Basin-Drainage in a geographic area defined by topography wherein the area drained by a river and all its tributaries (see WATERSHED).

rl-glos-1350/96 GLOS-2 --I

Recharge - The addition of water to a porous rock media.

Rhyolite - A fine-grained igneous rock rich in silica: the volcanic equivalent of granite.

Saturated - A porous rock unit that is completely filled with water.

Scoria (scoriaceous) - A cinderlike basic cellular lava.

Sheetflow - An overland downslope movement of water in the form of a thin, continuous film over relatively smooth soil or rock surfaces and not concentrated in large channels.

Specific Capacity - The rate of discharge of a water well per unit of drawdown; it is related to the aquifer matrix properties.

Stratigraphy - A branch of geology dealing with the classification, nomenclature, correlation, and interpretation of stratified rocks.

Storativity - The volume of water released from or taken into storage per unit surface area of the aquifer per unit change in head. Represents porosity in unconfined aquifers.

Syndepositional - Two different rock types deposited at the same time.

Tertiary - Noting or pertaining to the earlier period of the Cenozoic Era, beginning about 65 million years ago, during which mammals gained ascendancy.

Throw - On a fault, the amount of vertical displacement between a broken and offset rock unit.

Transmissivity - The rate at which water is transmitted through a unit width of the aquifer under a unit hydraulic gradient. The ability of a rock body to transmit water; reported in length squared per time.

Unconfined aquifer - An aquifer that has free water table that is not confined under pressure beneath relatively impermeable rocks.

Underflow - The flow of water beneath the bed or alluvial plain of a surface stream, generally in the same direction as the surface drainage.

Vesicular - Characterized by or containing vesicles which are small cavities formed by the expansion of bubbles of gas or steam during the solidification of rock.

Watershed - The region or area drained by a river, stream, etc.

r 1 -glos-1350/96 GLOS-3 0

REFERENCES

• of al rl4m-1350/96 REFERENCES

Ackerman, D. J., 1991, Transrnissivity of the Snake River Plain Aquifer at the Idaho National Engineering Laboratory, Idaho: U. S. Geological Survey Water-Resources Investigations Report 91-4058, 35 p.

Anderson, S. R., 1991, Stratigraphy of the Unsaturated and Uppermost Part of the Snake River Plain Aquifer at Idaho Chemical Processing Plant and Test Reactors Area, Idaho National Engineering Laboratory, Idaho: U. S. Geological Survey Water-Resources Investigations Report 91-4010.

Barraclough, J. T., Robertson, J. B., and Janzer, V. J., 1976, Hydrogeology of the Solid Waste Burial Grounds, as Related to the Potential Migration of Radionucleides: U. S. Geological Survey Open-File Report 76-471, 183 p.

Cecil, L. D., Orr, B. R., Norton, T., and Anderson, S. R., 1991, Formation of Perched Ground-Water Zones and Concentrations of Selected Chemical Constituents in Water, Idaho National Engineering Laboratory, Idaho, 1968-88: U. S. Geological Survey Water- Resources Investigations Report 91-4166.

Doherty, D. J., McBroome, L. A., and Kuntz, M. A., 1979, Preliminary Geological Interpretation and Lithologic Log of the Exploratory Geothermal Test Well (INEL-1), Idaho National Engineering Laboratory, Eastern Snake River Plain, Idaho: U. S. Geological Survey Open-File Report 79-1248, 7 p.

Embree, G. F., McBroome, L. A., and Kuntz, M. A., 1982, Preliminary Stratigraphic Framework of the Pliocene and Miocene rhyolite, Eastern Snake River Plain, Idaho, in Bonnichsen, B., and Breckenridge, R. M., eds., Cenozoic geology ofIdaho, Idaho Bureau of Mines and Geology, p. 333-343.

Garabedian, S. P., 1992, Hydrology and Digital Simulation of the Regional Aquifer System, Eastern Snake River Plain, Idaho: U.S.G.S. Professional Paper; 1408-F.

Irving, J. S., 1992, Draft Environmental Resource Document for the Idaho National Engineering Laboratory: Idaho National Engineering Laboratory, EG&G Idaho, Inc. Volume 1; DE-AC07-761D01570.

King, J. J., Doyle, T. E., and Jackson, S. M., 1987, Seismicity of the Eastern Snake River Plain region, Idaho, Prior to the Borah Peak, Idaho, Earthquake: October 1972-October 1983: Bulletin of the Seismological Society of America, v. 77, no. 3, p. 809-818.

1 -ref-1350/96 REF-1 Kuntz, M. A., 1978, Geology of the Arco-Big Southern Butte Area, eastern Snake River Plain, and Potential Volcanic Hazards to the Radioactive Waste Management Complex and Other Waste Storage and Reactor Facilities at the Idaho National Engineering Laboratory, Idaho: U.S.G.S Open-File Report; 78-691.

Kuntz, M. A., Covington, H. K,and Schorr, L. J., 1992, An Overview of Basaltic Volcanism of the Eastern Snake River Plain, Idaho, in Link, P. K., Kuntz, M. A., and B Platt, L. B., eds., Regional Geology of Eastern Idaho & Western Wyoming: Boulder, CO, Geological Society of America, p. 227-267.

0 Kuntz, M. A., and Dalrymple, G. B., 1979, Geology, Geochronology, and Potential Volcanic Hazards in the Lava Ridge-Hells Half Acre Area, Eastern Snake River Plain, 0 Idaho: U.S. Geol. Sur. Open-File Rept.; 79-1657. Kuntz, M. A., Dalrymple, G. B., Champion, D. E., and Doherty, D. J., 1980, Petrography, Age, and Paleomagnetism of Volcanic Rocks at the Radioactive Waste Management Complex, Idaho National Engineering Laboratory, Idaho, With an Evaluation of Potential Volcanic Hazards: U. S. Geological Survey Open-File Report 80-388, 63 p.

Lindholm, G. F., and Goodell, S. A., 1986, Irrigated Acreage and Other Land Uses on the Snake River Plain, Idaho and Eastern Oregon: U. S. Geological Survey Hydrologic Investigations Atlas 691, scale 1:500,000.

Lindholm, G. F., and Vaccaro, J. J., 1988, Region 2, Columbia Lava Plateau, in Back, W., Rosenshein, J. S., and Seaber, P. R., eds., Hydrogeology: Boulder, CO, Geological Society of America, p. 37-50.

Mann, L. J., 1986, Hydraulic Properties of Rock Units and Chemical Quality of Water for INEL-1: A 10,365-Foot Deep Test Hole Drilled at the Idaho National Engineering Laboratory, Idaho: U. S. Geological Survey Water-Resources Investigation Report 86- 4020, 23 p.

Mann, L. J., and Cecil, L. D., 1990, Tritium in Ground Water at the Idaho National Engineering Laboratory, Idaho: U. S. Geological Survey Water-Resources Investigations Report 90-4090, 35 p.

Mann, L. J., Chew, E. W., Morton, J. S., and Randolph, R. B., 1988, Iodine-129 in the Snake River Plain Aquifer at the Idaho National Engineering Laboratory: U. S. Geological Survey Water-Resources Investigations Report 88-4165, 27 p.

Nace, R. L., Voegeti, P. T., Jones, J. R., and Deutsch, M., 1975, Generalized Geological a. Framework of the National Reactor Testing Station, Idaho: U. S. Geological Survey of Professional Paper 725-B, 49 p. rl-ref-1350/96 REF-2 Orr, B. R., and Cecil, L. D., 1991, Hydrologic Conditions and Distribution of Selected Chemical Constituents in Water, Snake River Plain Aquifer, Idaho National Engineering Laboratory, Idaho, 1986 to 1988: U. S. Geological Survey Water-Resources Investigations Report 91-4047.

Pierce, K. L., and Morgan, L. A., 1992, The track of the Yellowstone Hot Spot: Volcanism, Faulting, and Uplift, in Link, P. K., Kuntz, M. A., and Platt, L. B., eds., Regional Geology of Eastern Idaho & Western Wyoming: Boulder, CO, Geological Society of America, p. 1-54.

Robertson , J. B., 1976, Numerical Modeling of Subsurface Radioactive Solute Transport from Waste-Seepage Ponds at the Idaho National Engineering Laboratory: U. S. Geological Survey Open-File Report 76-717, 68 p.

Robertson, J. B., Schoen, R., and Barraclough, J. T., 1974, The Influence of Liquid Waste Disposal on the Geochemistry of Water at the National Reactor Testing Station, Idaho, 1952-1970: U. S. Geological Survey Open-File Report OF-73-0238, 345 p.

Rodgers, D. W., and Janecke, S. U., 1992, Tertiary Paleogeologic Maps ofthe Western Idaho-Wyoming-Montana thrust belt, in Link, P. K., Kuntz, M. A,and Platt, L. B., eds., Regional Geology of Eastern Idaho & Western Wyoming: Boulder, CO, Geological Society of America, p. 83-94.

Scott, W. E., Pierce, K. L., and Hait Jr., M. H., 1985, Quaternary Tectonic Setting of the 1983 Borah Peak earthquake, Central Idaho: Bulletin of the Seismological Society of America, v. 75, no. 4, p. 1053-1066.

Smith, R. B., and Sbar, M. L., 1974, Contemporary Tectonics and Seismicity of the Western United States with Emphasis on the Intermountain Seismic Belt. Geological Society of America Bulletin 85: pp. 1205-1218.

Taylor, D.D., Hoskinson, R.L., Kingsford, C.O., and Ball, L.W., 1994, "Preliminary Siting Activities for New Waste Handling Facilities at the Idaho National Engineering Laboratory," EG&G Idaho, Inc. Report EGC-WN-1118.

United States Environmental Protection Agency, 1990, Support Document for the EPA Designation of the Snake River Plain Aquifer as a Sole Source Aquifer, EPA910/9-90- 020.

Whitehead, R. L., 1986a, Compilation of Selected Geophysical References for the Snake River Plain, Idaho and Eastern Oregon: U. S. Geological Survey Geophysical Investigations Map 869; Scale 1:1,000,000, 3 sheets.

rl-ref-1350/96 REF-3 Whitehead, R. L., 1986b, Geohydrologic Framework of the Snake River Plain, Idaho and eastern Oregon: U. S. Geological Survey Hydrologic Investigation Atlas 681; Scale 1:1,000,000, 3 sheets.

Willie, K.D., to L. Mann, Telephone Conversation, March 21, 1996.

Witkind, I. J., 1975, Preliminary Map Showing Known and Suspected Active Faults in Idaho: USGS Open-File Report; 75-278. 71 pp.

Wong, I. G., Silva, W. J., Stark, C. L., Wright, D. H., and Darragh, R. B., 1990, Earthquake Strong Ground Motion Estimates for the Idaho National Engineering Laboratory: Final Report. Woodward-Clyde Consultants proprietary report to EG&G Idaho November 1990.

Wong, I. G., Coppersmith, K., Silva, W. J., Youngs, T., Sawyer, T., Hemphill-Haley, M., Stark, C. L., Knuepfer, P., Casstro, R., Makdisi, F., Wells, S., Chiou, S., Bruhn, R., and Daning, W., 1992, Earthquake Ground Motion Evaluations for the Proposed New Production Reactor at Idaho National Engineering Laboratory: Volume I: Deterministic Evaluation. Woodward-Clyde Federal Services proprietary report.

Wong, I. G., Hemphill-Haley, M., Sawyer, T., Coppersmith, K., Youngs, R., Silva, W. J., and Stark, C. L., 1993, Site-Specific Probabilistic Seismic Hazard Analyses for the Idaho National Engineering Laboratory. Woodward-Clyde Federal Services, Geomatrix Consultants, and Pacific Engineering and Analysis proprietary report.

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