Technical Basis Document No. 3: 
Water Seeping into Drifts 
Revision 2 
Prepared for: 
U.S. Department of Energy 
Office of Civilian Radioactive Waste Management 
Office of Repository Development 
P.O. Box 364629 
North Las Vegas, Nevada 89036-8629 
Prepared by: 
Bechtel SAIC Company, LLC 
1180 Town Center Drive 
Las Vegas, Nevada 89144 
Under Contract Number 
DE-AC28-01RW12101 
QA: NA 
October 2003
Revision 2 
October 2003 No. 3: Water Seeping into Drifts
Revision 2 

1. INTRODUCTION 
1.1 OVERVIEW 
This technical basis document provides a summary of the conceptual understanding of water 
seepage into waste emplacement drifts, which is a process affecting the prediction of the 
postclosure performance of the high-level nuclear waste repository at Yucca Mountain. This 
document is one in a series that is being prepared for each component of the Yucca Mountain 
repository system relevant to predicting its likely postclosure performance. The relationship of 
drift seepage to the other components is illustrated in Figure 1-1. Drift seepage is affected by the 
processes that will be described in technical basis documents on climate and infiltration, 
unsaturated zone flow, mechanical degradation and seismic effects, low probability seismic 
events, and volcanic events. Seepage is affected by and affects the in-drift environment 
discussed in the technical basis document on in-drift chemical environment. The amount of 
seepage water entering the waste emplacement drifts and potentially contacting waste canisters 
impacts downstream repository system components, including corrosion, waste dissolution, and 
transport of radionuclides and colloids through the engineered barrier system, the unsaturated 
and saturated zones, and the biosphere. 
Figure 1-1. Components of the Postclosure Technical Basis for the License Application 
October 2003 1-1 No. 3: Water Seeping into Drifts Revision 2 
The information presented in this document, along with the associated references, forms an 
outline of the seepage-related studies supporting the ongoing development of the postclosure 
safety analysis that will comprise the license application (LA). This information is also used to 
respond to several open Key Technical Issue (KTI) agreements between the U.S. Nuclear 
Regulatory Commission (NRC) and the U.S. Department of Energy (DOE); detailed responses to 
these KTI agreements are provided in Appendices A through E, as shown in Table 1-1. 
TEF 2.08, 
GEN 1.01 (15) 
TSPAI 3.25 
USFIC 4.01 
USFIC 4.06 
RT 3.06, SDS 3.02 
Table 1-1. Seepage-Related Key Technical Issues Agreements Addressed in This Report 
Short Description KTI Agreement/AIN Appendix 
Effects of heterogeneity on thermal seepage 
Using test data to reduce uncertainty in TSPA seepage abstraction 
In situ field testing results and analyses 
Justification of continuum approach for seepage modeling 
Alcove 8Niche 3 pretest predictions 
October 2003 1-2 
A
B
C
D
E 
Water is one of the principal agents determining corrosion of engineered barriers, waste 
dissolution, and radionuclide transport from the repository to the accessible environment. The 
amount and chemical composition of water seeping into waste emplacement drifts thus affects 
the long-term safety of the repository system at Yucca Mountain. 
In the unsaturated zone, percolating water encountering a large underground opening is partly 
diverted around the cavity. This effect reduces the amount of liquid water entering the waste 
emplacement drift or prevents dripping altogether (i.e., the seepage flux is expected always to be 
smaller than the local percolation flux). This effect is referred to as a capillary barrier; it is an 
attribute of the unsaturated zone at Yucca Mountain. Moreover, during the early stages after 
closure, the heat from decaying radionuclides will vaporize water that approaches the waste 
emplacement drift. Both mechanisms limit the amount of water that potentially contacts the 
waste packages. 
Characterizing and predicting seepage requires addressing a variety of processes and factors, 
including the distribution of water percolating through the mountain, the hydrogeologic 
properties of the fractured rock in the vicinity of a waste emplacement drift, the temperature and 
humidity conditions near and within the drift, the drift geometry, and the drift wall structure. 
These processes and factors are discussed in more detail in Section 2. A comprehensive testing 
program was designed and executed to understand seepage at Yucca Mountain and to obtain data 
supporting the models developed to predict drift seepage during the postclosure period. The 
testing program and data are presented in Section 3. Various process models were developed to 
analyze data from seepage experiments and to predict seepage into waste emplacement drifts 
under ambient and thermally elevated conditions. Experimental and modeling studies were 
performed to evaluate how seepage is affected by repository heat, mechanical deformation of the 
rock and the drift itself, changes in the chemical environment, and other perturbations. These 
modeling studies are summarized in Section 4. 
Uncertainties and variabilities in the predicted seepage rates are examined and accounted for in a 
simplified but reasonable representation of seepage in a probabilistic total system performance 
No. 3: Water Seeping into Drifts Revision 2 
assessment (TSPA) analysis. The testing and modeling program undertaken to understand and 
characterize seepage from fractured rock is considered suitable to provide an adequate basis for 
predicting seepage into waste emplacement drifts under ambient and thermally elevated 
conditions at Yucca Mountain. 
1.2 SIGNIFICANCE OF SEEPAGE FOR REPOSITORY PERFORMANCE 
The number of waste packages contacted by water, the corrosion performance of the engineered 
barriers, the dissolution and mobilization of radionuclides, and the release and migration of 
radionuclides to the accessible environment depend on the rate, chemical composition, and 
spatial and temporal distribution of water seeping into the emplacement drifts. 
Percolating water encountering a waste emplacement drift is partly diverted around the opening 
because of the capillary barrier effect, which refers to the tendency of water to be held in the 
pores of unsaturated rock rather than dripping into a large opening. As a result, the seepage flux 
is expected to be smaller than the local percolation flux. This capillary barrier effect is an 
attribute of the unsaturated zone at Yucca Mountain. 
While seepage is determined by features and processes occurring above the drift, the flow 
diversion phenomenon and reduction or prevention of water inflow into the drifts also affects the 
conditions below the repository, specifically the reduced saturation in the matrix and the 
fractures immediately beneath the drift. This is referred to as the drift shadow zone (see 
Figure 1-2). The saturation and flow conditions in the shadow zone impact diffusive releases at 
the interface between the drift invert and natural environment and the potential for the absence of 
fast advective transport of radionuclides through the fracture network. 
A scientific research program has been undertaken to understand and characterize the 
fundamental processes contributing to seepage into underground openings excavated in the 
unsaturated, fractured formations at Yucca Mountain. In addition, a research program was 
designed to characterize the seepage-related properties of the repository host rock, providing the 
basis for the site-specific seepage predictions. Seepage was examined using theoretical, 
experimental, numerical, and natural analog studies. The key factors affecting seepage were 
identified, and site-specific, seepage-relevant parameters were determined through in situ testing. 
Numerical models were developed and calibrated against data that contain seepage-relevant 
information. These models were extensively tested to gain confidence in their ability to make 
predictions of drift seepage. Natural analogs were studied to corroborate the water-exclusion 
concept under unsaturated conditions. 
Based on this research program, an understanding of the process of seepage into waste 
emplacement drifts has been gained. Seepage tests in the repository host units were performed to 
obtain site-specific characterization data related to seepage. A consistent and systematic 
approach to analyzing these data for use in subsequent seepage prediction models was 
developed. 
October 2003 1-3 No. 3: Water Seeping into Drifts Revision 2 
Figure 1-2. Schematic Showing Reduced Seepage and the Development of a Shadow Zone as a 
Result of the Flow Diversion Capability of the Capillary Barrier in the Unsaturated Zone 
While the seepage processes and controlling mechanisms are well understood, seepage 
predictions under both ambient and thermal conditions remain uncertain, primarily because of 
natural variability. These uncertainties were assessed through the abstraction process and will be 
propagated in a probabilistic TSPA calculation. 
1.3 PURPOSE AND SCOPE 
The purpose of this document is to provide an overview of the current understanding of drift 
seepage, including a summary description of seepage testing and modeling activities. It presents 
the technical basis for addressing seepage KTIs. The report summarizes the lines of reasoning 
used to arrive at the conclusion that (1) reduction or prevention of water seepage into 
underground openings under both ambient and elevated temperature conditions is an attribute of 
the unsaturated zone barrier at Yucca Mountain, (2) the extensive testing conducted in the 
Exploratory Studies Facility (ESF) and the Enhanced Characterization of the Repository Block 
(ECRB) Cross-Drift provided critical seepage-related characterization data, (3) the 
comprehensive data analysis and modeling approach yields reasonable, site-specific seepage 
predictions, and (4) remaining uncertainties and process understanding issues are recognized. 
The report describes the process of seepage from the fractured repository units in the Topopah 
Spring welded tuff into a waste emplacement drift and presents the factors affecting seepage 
(see Section 2). This discussion covers a range of spatial and temporal scales from the 
near-steady, mountain-scale distribution of percolation flux to episodic, small-scale flow events 
within individual fractures to film flow along the drift surface. In addition to describing seepage 
processes under ambient conditions, the report also includes a discussion of coupled thermal, 
October 2003 1-4 No. 3: Water Seeping into Drifts Revision 2 
hydrologic, chemical, and mechanical processes as they occur under increased temperature 
conditions and their impact on seepage. 
The report provides a summary description of field tests performed at Yucca Mountain to obtain 
site-specific data that characterize seepage-relevant features and processes (see Section 3). It 
also discusses the suite of models developed to analyze these data, to predict seepage into waste 
emplacement drift sections, and to abstract the simulation results for use in probabilistic TSPA 
calculations (see Section 4). 
This report does not describe in-drift processes that are affected by seepage water, which will be 
discussed in a technical basis document on the in-drift chemical environment. In-drift processes 
(specifically evaporation and condensation effects) are discussed here with respect to the 
interpretation of seepage test data. 
1.4 DEFINITIONS 
In the context of this report, seepage is defined as dripping of liquid water from the formation 
into an underground opening, such as a niche, alcove, access tunnel, or waste emplacement drift. 
According to this definition, seepage does not include advective or diffusive vapor flow into the 
opening or condensation of water vapor on surfaces, which may lead to drop formation and drop 
detachment. Some of the water entering an underground opening may evaporate or flow along 
the wall, thus not contributing to seepage in the sense defined here. In-drift moisture 
redistribution and potential condensate accumulation will be discussed in the technical basis 
document on in-drift chemical environment. 
The seepage threshold is defined as the minimal percolation flux required to initiate seepage. 
A nonzero seepage threshold indicates the existence of effective water exclusion (Philip et al. 
1989) capability of the formation. The presence of a seepage threshold can be directly observed 
from liquid-release tests conducted at different rates, which show that seepage ceases at a 
nonzero release rate. 
1.5 CAPILLARY AND VAPORIZATION BARRIERS 
In the unsaturated zone, percolating water encountering a waste emplacement drift tends to be 
diverted around the opening because of the capillary barrier effect. This effect is referred to as 
the water exclusion phenomenon (Philip et al. 1989), which reduces the amount of liquid water 
entering an underground opening or prevents dripping altogether, that is, the seepage flux 
averaged over a sufficiently large area (e.g., that of a drift section with the length of a waste 
package) will always be equal to or smaller than the local percolation flux. This effect is an 
attribute of the unsaturated zone barrier at Yucca Mountain. 
The water-exclusion phenomenon has been extensively described in the literature (see Philip 
et al. 1989). The related water diversion capability is utilized in practical applications for the 
protection of landfills and hazardous waste sites. These standard engineering applications 
consider porous materials rather than fractured rocks. However, since the key factors affecting a 
capillary barrier are permeability and capillarity, properties also relevant for fractured rocks, the 
same effect applies to Yucca Mountain. 
October 2003 1-5 No. 3: Water Seeping into Drifts Revision 2 
Water exclusion from drifts has been extensively tested through the in situ seepage experiments 
described in In Situ Field Testing of Processes (BSC 2001a, Sections 6.2 and 6.11) and Seepage 
into an Underground Opening Constructed in Unsaturated Fractured Rock Under Evaporative 
Conditions (Trautz and Wang 2002). The experiments show that the seepage rate is less than the 
injection rate. Because of storage effects and evaporation, the reduced seepage rate by itself 
does not conclusively prove that water is diverted around the opening, which would directly 
assess the barrier capability of the natural system at Yucca Mountain. However, a combination 
of observed and simulated contributions to the water balance during a seepage test indicates that 
a substantial amount of water is diverted around the opening, confirming this water-exclusion 
phenomenon in the unsaturated zone at Yucca Mountain under ambient conditions (see 
Section 3.1.5). 
After the emplacement of radioactive waste, the heat generated by the decay of the radionuclides 
will result in elevated rock temperatures for thousands of years after emplacement. For the 
current design, these temperatures are high enough to cause boiling in the rock. The thermally 
driven changes in water saturation affect the seepage potential. For above-boiling rock 
temperatures, vaporization of percolating water in the fractured rock overlying the repository 
will provide another effective process that greatly reduces (and most likely eliminates) seepage 
into the emplacement drifts during the thermal period, despite potentially increased reflux from 
the redistribution of water associated with vaporization and condensation of moisture above the 
drift. This additional process, referred to as the vaporization barrier, and its effect on seepage 
during the thermal period are further discussed in Sections 2.6.4 and 4.5. 
The term capillary barrier will be used throughout this technical basis document to refer to the 
flow diversion phenomenon occurring at the interface between two media with different capillary 
properties, where the medium with stronger capillarity overlies that of weaker capillarity. The 
term vaporization barrier will be used throughout this technical basis document to refer to the 
reduction of flow towards drifts as a result of vaporization occurring around a heated waste 
emplacement drift (BSC 2003a, Section 6.1.3). In these technical terms, the word barrier is 
used to describe the combined effect of a physical process occurring in a system with specific 
properties. This usage is slightly different from that in the definitions of natural and engineered 
barriers as given in Total System Performance AssessmentLicense Application Methods and 
Approach (BSC 2002a, Section 8.3.1). 
In summary, partial or complete diversion of water around underground openings due to the 
capillary barrier effect in combination with vaporization during the thermal period will reduce 
seepage or even prevent water from dripping into waste emplacement drifts. In addition, the 
extent of a potential low-saturation and low-flux shadow zone beneath the drift (see Figure 1-2) 
and its potential effectiveness in delaying radionuclide transport from the invert of the waste 
emplacement drift to the accessible environment is related to the seepage-exclusion 
phenomenon. The capability of the capillary barrier to divert flow around underground openings 
in unsaturated fractured formations has been established theoretically, as well as through 
modeling and extensive field testing at Yucca Mountain. Natural analogs further confirm the 
existence and effectiveness of the capillary barrier effect. 
October 2003 1-6 No. 3: Water Seeping into Drifts Revision 2 
1.6 SUMMARY OF MODELING APPROACH 
Seepage into an opening in unsaturated fractured rock depends on the percolation flux, the 
formation characteristics, the geometric features of the opening, and the thermodynamic 
conditions in the rock and the opening itself (for details, see Section 2). Specifically, the 
processes that need to be combined in a comprehensive conceptual model of seepage include 
(1) the mountain-scale distribution of percolation flux; (2) the intermediate-scale channeling of 
flow in the fracture network; (3) the drift-scale capillary-barrier effect; and (4) the micro-scale 
phenomena of evaporation, film flow, drop formation, and drop detachment at the drift surface 
where water leaves the formation and enters the drift. In addition, the thermodynamic 
environment in the opening (e.g., temperature, relative humidity, preclosure ventilation regime) 
will also affect seepage. 
The analysis and modeling approach used to explain and reproduce seepage rates measured 
during liquid-release tests (see Section 3.1) and to predict seepage into waste emplacement drifts 
is described in detail in Section 4. The approach described in Section 4 is based on a process 
model of seepage in combination with effective parameters that are determined from in situ 
seepage experiments. Detailed predictions of drip frequency and individual seepage locations 
are not made; rather, calculated seepage rates are averaged in time and over a drift section of the 
approximate length of a waste package (i.e., they refer to the temporal and spatial scale of 
interest for a probabilistic assessment of seepage into a representative waste package). To 
support this approach, liquid-release tests were performed at rates below and above the seepage 
threshold. They covered the critical range of conditions expected under natural percolation 
conditions (which are most likely below the seepage threshold where no seepage occurs) and 
under localized, high flux conditions (as a result of wet climates combined with significant flow 
focusing) that may induce seepage. To summarize, the chosen approach focuses on the relevant 
drift- and waste-package scale and eliminates the need for auxiliary models and large spatial and 
temporal extrapolations from micro-scale models or low-resolution interpretation from site-scale 
models. 
A key advantage of this approach is that it relies directly on seepage-rate data that contain 
information about the relevant processes. Moreover, the type of data used for calibration 
(i.e., seepage rates from liquid-release tests collected in a drift section, see Section 3.1) are 
conceptually very similar to the variable of interest (i.e., average seepage rates from a natural 
percolation) that needs to be predicted with the calibrated model. This consistency between 
calibration and prediction data minimizes potential conceptual differences between the 
calibration and prediction model. The appropriateness of this approach is further discussed in 
Appendix D. Finally, uncertainties and variabilities inherent in the seepage process are 
addressed by a probabilistic treatment of seepage in TSPA (see Section 4). 
1.7 NOTE REGARDING THE STATUS OF SUPPORTING TECHNICAL 
INFORMATION 
This document was prepared using the most current information available at the time of its 
development. This technical basis document and its appendices providing KTI agreement 
responses that were prepared using preliminary or draft information reflect the status of the 
Yucca Mountain Projects scientific and design bases at the time of submittal. In some cases this 
October 2003 1-7 No. 3: Water Seeping into Drifts Revision 2 
involved the use of draft analysis and model reports and other draft references whose contents 
may change with time. Information that evolves through subsequent revisions of the analysis 
and model reports and other references will be reflected in the LA as the approved analyses of 
record at the time of LA submittal. Consequently, the Project will not routinely update either 
this technical basis document or its KTI agreement appendices to reflect changes in the 
supporting references prior to submittal of the LA. 
October 2003 1-8 No. 3: Water Seeping into Drifts Revision 2 
2. PROCESSES AND FACTORS AFFECTING SEEPAGE 
2.1 SUMMARY DESCRIPTION OF SEEPAGE PROCESS 
The seepage process has been studied as part of the Yucca Mountain site characterization effort. 
The following section summarizes the processes and factors affecting seepage into waste 
emplacement drifts. 
Seepage is a process that occurs at the interface between the natural and engineered system. The 
repository design (drift geometry), and its construction (excavation effects, and drift surface 
roughness), and the operating conditions within the drifts, (e.g., heat load and ventilation) affect 
the amount and distribution of seepage. The following sections qualitatively discuss the seepage 
process and the important factors affecting seepage, which are schematically depicted in 
Figure 2-1 for both an intact and partially collapsed waste emplacement drift. 
Figure 2-1. Schematic Showing Seepage Processes and Factors Affecting Seepage 
October 2003 2-1 No. 3: Water Seeping into Drifts Revision 2 
The majority of the precipitation on Yucca Mountain is removed by runoff and 
evapotranspiration. The remaining water penetrates the ground surface and starts to percolate 
downwards, driven by gravity and capillary forces (details will be discussed in the upcoming 
technical basis document on climate and infiltration). As this water percolates to depth, it is 
spatially redistributed (for details see the upcoming technical basis document on unsaturated 
zone flow and transport). Seepage into a section of waste emplacement drift is given by the local 
percolation flux minus the water that is diverted around the drift due to the capillary and 
vaporization barrier effects, minus water that flows as a film along the drift surface or that 
evaporates. 
The detailed flow path is determined by the degree of fracturing, fracture geometry, orientation, 
connectivity, and the hydrogeologic properties of the fractures and the matrix. Depending on 
these factors, the water phase in the unsaturated fracture network will either disperse or 
concentrate along the flow path. Tilted contacts between hydrogeologic units (especially 
between welded and nonwelded tuffs) may affect the overall flow pattern or lead to a change in 
the frequency and spacing of flow channels. As flow concentration continues to occur, the 
distance between the individual channels carrying focused flow increases. As a result, the 
likelihood of two channels meeting and merging decreases with depth. Flow concentration and 
dispersion of flow paths also occurs within a rough-walled fracture where asperity contacts and 
locally larger fracture openings lead to small-scale redistribution of water within the fracture. 
A general discussion of channeling effects under unsaturated flow conditions can be found in 
Solute Channeling in Unsaturated Heterogeneous Porous Media (Birkholzer and Tsang 1997). 
Flow focusing is important for seepage because seepage depends on the local (rather than 
average) percolation flux. These issues are further discussed in Section 2.2. 
As water approaches an emplacement drift (at a distance of one to several meters above the drift 
ceiling), conditions change in several ways that affect the amount of water that can seep into the 
opening. At early times after repository closure, the water will first encounter a dryout zone 
(defined as the zone of reduced saturation caused by preclosure drift ventilation or by boiling due 
to radioactive decay heat). Under boiling conditions, the dryout zone will be surrounded by a 
two-phase zone in which vapor-liquid counterflow (heat-pipe effect) occurs and a condensation 
zone with increased saturation. Preclosure ventilation and elevated temperatures are limited in 
time and do not affect long-term seepage. 
Formation properties around the openings will be altered as a result of stress redistribution 
during drift excavation, which will lead to local opening or partial closing of fractures and 
potentially the creation of new fractures. Additionally, thermal expansion of the rock matrix will 
also induce changes in apertures. Finally, the local chemical environment, which is altered by 
evaporation and thermal effects, will lead to dissolution and precipitation of minerals, affecting 
flow properties of the fracture system and fracture-matrix interaction (see the technical basis 
document on in-drift chemical environment). These conditions lead to a flow pattern around a 
waste emplacement drift that is different from that in the undisturbed formation under ambient 
conditions (i.e., before excavation and waste emplacement). 
When water penetrates the boiling zone (BSC 2003b, Sections 6.2 and 6.3) and reaches the 
immediate vicinity of the drift wall, it will still be prevented from seeping into the drift because 
of the capillary barrier effect (Philip et al. 1989). This effect leads to a local saturation build-up 
and, thus, the development of a higher water potential in the formation immediately adjacent to 
October 2003 2-2 No. 3: Water Seeping into Drifts Revision 2 
the drift. If the permeability tangential to the drift wall (i.e., permeability in the direction along 
the ceiling) and the capillarity of the fracture network within this region are sufficiently high, all 
or a portion of the water will be diverted around the drift under partially saturated conditions. 
Alternatively, however, the water potential in the formation may be higher than that in the drift, 
allowing water to exit the formation. At the drift surface, the water will either evaporate or 
follow the inclined, rough wall in a film or form a drop that may grow and eventually detach (Or 
and Ghezzehei 2000). Only this last mechanism is considered drift seepage according to the 
definition of Section 1.4. 
The rate of water dripping into an opening in the unsaturated zone is expected to be significantly 
less than the local percolation rate because (1) the dryout zone around the drift reduces liquid 
water flow, potentially preventing water from reaching the drift surface, (2) the capillary barrier 
diverts water around the drift, thus bypassing the waste package, (3) water may flow along the 
drift surface without dripping into the opening, and (4) water may evaporate from the drift 
surface. Even if the seepage threshold were exceeded and seepage occurred, the seepage flux 
would be lower than the local percolation flux (i.e., the unsaturated zone at Yucca Mountain acts 
as a fully or partially effective barrier to water seeping into the waste emplacement drift). 
2.2 FACTORS AND PROPERTIES AFFECTING SEEPAGE 
Seepage is a process that occurs at the interface between the natural and engineered systems. 
Consequently, seepage is not only affected by hydrogeological factors (percolation flux, 
formation properties), but also by the design of the repository and waste emplacement drifts 
(location and geometry), the method of construction (excavation effects, drift surface roughness, 
ground support), and the conditions within the drifts (heat load, preclosure ventilation, and drift 
degradation). 
The following sections describe the key factors affecting drift seepage and how they are included 
in the base-case conceptual model. The most important factors are the magnitude of the local 
percolation flux in relation to the formations permeability, the strength of the capillary forces in 
the fractures, the connectivity of the fracture network in the immediate vicinity of the opening, 
the local topography of the rough drift wall, and the thermodynamic conditions in the drift. 
Percolation FluxThe magnitude of the percolation flux is a key factor determining seepage. 
Seepage is initiated if the local percolation flux in individual flow channels and the accumulation 
of water from these channels near the drift ceiling exceeds the diversion capacity of the capillary 
barrier, the evaporation potential of the atmosphere in the drift, and the capacity of films to carry 
water along the drift surface. It is the local (rather than average) percolation flux that controls 
the onset of seepage. 
The source of percolation flux at Yucca Mountain is net infiltration at the ground surface, 
stemming from precipitation events. Net infiltration is the fraction of precipitation that moves 
through the ground surface to a depth where the liquid water can no longer be removed by 
evaporation or transpiration. Net infiltration varies in space (as a result of several factors, such 
as vegetation, morphology, soil and bedrock, and runoff and runon conditions) and in time 
(USGS 2001). Time variations are short-term as a result of daily or seasonal fluctuations and 
long-term as a result of climatic changes. As infiltrating water percolates through the 
unsaturated zone, driven by gravity and capillary forces, the initial infiltration and flow patterns 
October 2003 2-3 No. 3: Water Seeping into Drifts Revision 2 
change depending on the hydrogeologic properties and their heterogeneities. On a large scale, 
several stratigraphic units of volcanic rock with significant differences in fracture frequency and 
matrix porosity can be distinguished at Yucca Mountain. Variations between units reflect the 
type of volcanic eruption, the rate of cooling, and the intensity of postdepositional processes. 
In general, percolation flux through the Tiva Canyon welded (TCw) hydrogeologic unit, the first 
fractured bedrock unit below alluvial deposits, is governed by the imposed distribution of net 
infiltration. Flow in this unit occurs mostly in the fractures before entering the underlying 
Paintbrush nonwelded (PTn) hydrogeologic unit. This unit corresponds to the lithostratigraphic 
units from the top of the Tiva Canyon Tuff crystal poor member vitric zone moderately welded 
subzone (Tpcpv2) to the bottom of the Topopah Spring Tuff crystal rich member vitric zone 
moderately welded subzone (Tptrv2). With its characteristics of high matrix porosity and low 
fracture frequency and the existence of tilted layers of nonwelded vitric and bedded tuff, the PTn 
can effectively divert percolating water into intercepting faults and fault zones (BSC 2003c). 
Also, the PTn unit dampens and homogenizes downward-moving transient pulses from surface 
infiltration events. Therefore, the percolation distribution below the PTn unit is considerably 
different from the distribution of net infiltration, both spatially and temporally. Additional 
information on flow diversion and dampening in the PTn will be presented in the technical basis 
document on unsaturated zone flow. The hydrogeologic unit below the PTn is the Topopah 
Spring welded (TSw) hydrogeologic unit, a thick, densely fractured unit corresponding to the the 
Topopah Spring Tuff upper lithophysal (Tptpul), middle nonlithophysal (Tptpmn), and lower 
lithophysal (Tptpll) zones, which will host the repository. The Tptpll will host the majority of 
the repository. 
On an intermediate scale, there is also considerable heterogeneity within stratigraphic units. This 
kind of heterogeneity can focus water toward one drift location while diverting it away from 
another. Flow concentration on this scale (i.e., across the interface between a mountain-scale 
model and drift-scale models) is referred to as flow focusing. Flow channeling and diversion 
of flow paths also happen within each rough-walled fracture where asperity contacts and locally 
larger fracture openings lead to small-scale redistribution of water within the fracture. In 
addition, asperity-induced flow instabilities may cause small-scale episodic flow within 
fractures, leading to high-frequency fluctuations. These factors are considered in the 
development of a prediction and abstraction for seepage quantification. 
Flow concentration effects on various scales are schematically shown in Figure 2-2. Flow 
concentration, flow focusing, and channeling effects are uncertain. Flow simulations using a 
two-dimensional discrete fracture network model (see Figure 2-3) show that the average spacing 
between flow paths in a layered system tends to increase with depth (i.e., flow becomes more 
concentrated with the increase of depth under gravity-driven flow conditions). (The flow 
characteristic may change abruptly at interfaces between hydrogeologic units, leading to some 
local flow dispersion on a smaller scale in the unit with higher fracture density.) 
Temporal fluctuations superimpose the spatial flow-channeling effects described above. The 
flux in a flow channel may be near steady state or episodic with a wide frequency spectrum, 
ranging from high-frequency fluctuations triggered by small flow instabilities to intermediate 
variabilities in percolation fluxes in response to changing weather conditions to long-term 
variations from climate changes. 
October 2003 2-4 No. 3: Water Seeping into Drifts Revision 2 
Figure 2-2. Schematic of Flow-Channeling Effects on Various Scales 
October 2003 2-5 No. 3: Water Seeping into Drifts Revision 2 
measured fracture data from Yucca Mountain (nonconnected fractures excluded). 
NOTE: This two-dimensional fracture network was generated based on statistical information derived from the field 
Figure 2-3. Two-Dimensional Fracture Network at Yucca Mountain (a) and Simulated Steady-State 
October 2003 
Flux Distribution in the Fracture Network (b) 
The local (rather than average) percolation flux reaching the drift is the most important factor 
determining where and when seepage occurs, and the seepage rate. The spatial distribution of 
flow channels may change with the average percolation flux and may also change with time. 
Flow focusing could concentrate water onto a particular drift segment and lead to a flux that 
exceeds the seepage threshold. On the other hand, if flow is concentrated in one location, flow 
will be reduced in other areas leading to little or no seepage. The details of flow distribution on 
multiple scales are a major source of seepage prediction uncertainty, as discussed below. This 
uncertainty is accounted for in probabilistic TSPA calculations. 
The distribution of percolating water will be discussed in the technical basis document on 
unsaturated zone flow. The percolation flux used as a boundary condition for the seepage 
models is derived from UZ Flow Models and Submodels (BSC 2003c). Flow focusing factors 
estimated from an intermediate-scale flow focusing model (BSC 2001b, Section 6.4.2) are 
employed to account for intermediate-scale heterogeneity that is not represented in the 
layer-averaged UZ Flow Models and Submodels (BSC 2003c). Flow channeling due to 
small-scale heterogeneity is explicitly included, as discussed in Section 4.2. 
Formation PropertiesThe key formation properties determining the effectiveness of the 
capillary barrier are (1) the capillary strength and (2) the permeability tangential to the drift wall. 
Geologic formations with stronger capillarity and higher tangential permeability exhibit a higher 
seepage threshold (i.e., low seepage); whereas, a weaker capillary barrier effect (i.e., higher 
seepage) is expected if water retention is smaller or if the tangential permeability is insufficient 
to promote flow diversion. 
Porous formations with strong capillarity tend to have low permeability and vice versa, which is 
a correlation that reduces the probability of encountering parameter combinations conducive to 
extreme (low or high) seepage behavior, making seepage relatively uniform across different 
geologic units. However, this negative correlation between permeability and capillary strength 
2-6 No. 3: Water Seeping into Drifts Revision 2 
may not necessarily apply to a fractured system, specifically if considering the seepage process 
on the scale of a waste emplacement drift. A given permeability may result from a network 
consisting of a few large fractures or, alternatively, a network of many small, well-connected 
fractures. The first network with few large fractures would exhibit relatively weak capillarity, 
whereas the second network with many small fractures would have stronger capillarity. 
Moreover, if the predominant fracture orientation is aligned with the drift axis (see Section 4.2, 
Figure 4-2a), little or no tangential permeability is available and seepage is increased. For flow 
diversion to occur, the fracture system must have sufficient connectivity and permeability to 
provide the necessary effective diversion pathways in tangential direction around the drift. 
Heterogeneities in formation properties on the scale of a drift diameter or smaller may enhance 
seepage if they promote flow channeling and increase the probability of locally exceeding the 
seepage threshold. Intermediate-scale heterogeneities (from approximately 100 m to a drift 
diameter) may focus water into flow channels that either encounter or bypass the waste 
emplacement drifts. Large-scale heterogeneities may divert water (e.g., along contacts between 
hydrostratigraphic units) or concentrate it into local features (such as faults). Heterogeneities on 
these scales thus have roles in determining the fraction of waste packages encountering seepage 
and the seepage amount. The heterogeneous nature of the formation implies that certain regions 
are more prone to seepage than others, with some areas exhibiting properties that are strongly 
adverse to seepage. 
The impact of lithophysal cavities on flow and seepage is twofold: (1) lithophysal cavities are 
essentially obstacles to water flow because they act as capillary barriers, focusing the water that 
flows around them, and (2) lithophysal cavities intersected by the drift lead to a rough drift 
ceiling, potentially creating seepage points at local low points on the ceiling. Both effects tend to 
promote seepage. 
The capillarity and permeability of the fracture network alone do not determine seepage. Water 
emanating from the fracture network may not drip but be transported as film flow along the drift 
surface or evaporate (see Section 2.4). Hence, seepage is not only affected by the characteristics 
of the host rock but also by factors unrelated to the hydrogeologic properties of the fracture 
system. 
Drift Geometry and Drift-Wall PropertiesThe overall drift size and geometry can change the 
seepage threshold and the seepage amount. Generally, a large drift exhibits a significantly lower 
seepage threshold. More water accumulates in the high-saturation region near the drift boundary 
because it needs to move over a longer diversion distance around the wider opening. In a 
heterogeneous, fractured formation, the importance of drift shape and drift geometry may be 
diminished relative to that of flow channeling and local ponding (Birkholzer et al. 1999, pp. 372 
to 379). 
The effectiveness of a capillary barrier is greatest if the shape of the cavity follows an 
equipotential surface. In a homogeneous medium, parabolic cavities are more efficient in 
preventing seepage than circular or flat-roofed openings. Breakouts in the drift ceiling, caused 
by rockfall and drift degradation, may change the overall drift geometry and lead to local low 
points in the ceiling, which may trap water, reduce or prevent flow diversion, and initiate 
seepage. In addition, small-scale surface roughness tends to increase seepage if the amplitude of 
October 2003 2-7 No. 3: Water Seeping into Drifts Revision 2 
the irregularity is comparable to the boundary-layer thickness. The boundary-layer thickness is 
determined by the capillary rise in the fractures (i.e., it is on the order of a few centimeters). 
2.3 THERMAL, HYDROLOGIC, CHEMICAL, AND MECHANICAL IMPACTS ON 
SEEPAGE 
2.3.1 Introduction 
As outlined in Section 2.2, hydrogeologic properties (specifically permeability and capillary 
strength) and their spatial heterogeneity determine the flow diversion capacity of the fracture 
network and, thus, seepage behavior. Initially, the undisturbed rocks in the repository host units 
are likely to be altered as a result of stress redistribution during drift excavation, which typically 
leads to local opening of fractures and potentially the creation of new microfractures in the drift 
vicinity (BSC 2001a, Section 6.1.2.2; Wang and Elsworth 1999, pp. 752 to 756). These changes 
affect porosity, permeability, and capillarity of the fracture system in the vicinity of 
emplacement drifts. Later, the heat emanating from the radioactive material will induce changes 
as a result of coupled thermal-hydrologic-mechanical and thermal-hydrologic-chemical effects. 
Thermal expansion of the rock matrix will induce thermal stresses and associated aperture 
changes. Also, thermal effects will lead to dissolution and precipitation of minerals, affecting 
the porosity, permeability, and capillarity of the fracture system. 
2.3.2 Excavation Effects 
Because of excavation, stress is redistributed and fractures are generally expected to dilate near 
the crown of the drift. Such fracture dilation depends on the orientation of the fracture set and 
generally occurs within one drift radius. An increase in fracture aperture generally causes an 
increase in fracture permeability and a decrease in capillary strengthboth key parameters 
affecting seepage. The measured increase in permeability from preexcavation to postexcavation 
values reflects this excavation effect (Wang et al. 1999). 
2.3.3 Drift Degradation 
It is possible that the initially circular-shaped open emplacement drifts will degrade with time as 
a result of thermal stress, seismic ground motion, and time-dependent degradation of rock 
strength (BSC 2003d). Thermal stresses are caused by the heat generated from the decaying 
nuclear waste. Significant stresses can also be caused by seismic ground motions. 
Time-dependent degradation of rock strength (joint mechanical properties) may be a result of 
over-stressing from thermal heating and of static fatigue of the rock resulting from stress 
corrosion mechanisms. These effects may lead to rock mass damage and rockfall into 
emplacement drifts, changing the drift shape and size. Depending on the type of rock, the stress 
conditions, and the time-dependent rock mechanical properties, damage to the drifts may be 
small, with sparse local rockfall from the ceiling of otherwise intact drift openings, or (in 
extreme cases) damage may result in partial or complete drift collapse, with rubble rock material 
filling the enlarged drifts. These changes affect the potential for drift seepage. Local breakouts 
in the drift ceiling may lead to geometry changes that can either increase seepage by reducing or 
preventing flow diversion around the opening (e.g., by creating low points) or reduce seepage by 
resulting in a drift geometry that promotes flow diversion (e.g., by creating a more parabolic drift 
shape through breakouts near the apex of the drift). The larger size and potentially different 
October 2003 2-8 No. 3: Water Seeping into Drifts Revision 2 
shape of collapsed drifts can also reduce the potential for flow diversion; furthermore, the larger 
footprint of the collapsed drift leads to an increase in the total amount of percolation flux arriving 
at the drifts, which, in turn, can affect the total amount of seepage. In addition, the 
capillary-barrier effect at the drift wall may be affected by the rubble rock particles filling the 
opening because the capillary strength inside the opening will be different from the 
zero capillarity condition in the initially open drift. 
2.3.4 Seepage under Thermal Conditions 
The heat generated by the decay of radioactive wastes will result in rock temperatures elevated 
for thousands of years after emplacement. For average rock properties, percolation flux, and 
heat load, the drift wall will be at above-boiling temperatures for approximately 1,000 years. 
Elevated temperatures (below boiling, but above ambient conditions) will prevail throughout the 
compliance period (BSC 2003b, Section 8). For the current repository design concept, these 
temperatures will be high enough to cause boiling conditions in the drift vicinity, giving rise to 
local water redistribution and altered flow paths. Key thermal-hydrologic processes occurring 
around a drift are shown schematically in Figure 2-4 for an idealized, circular-shaped drift. The 
figure indicates that heating of the rock will cause pore water in the rock matrix to boil and 
vaporize. The vapor will move away from the drift through the permeable fracture network, 
driven primarily by a pressure increase caused by boiling. In cooler regions away from the drift, 
the vapor will condense in the fractures, where it can drain either toward the heat source from 
above or shed around the drift into the zone below the heat source. Condensed water can also 
imbibe from fractures into the matrix, leading to increased liquid saturation in the rock matrix. 
With continuous heating, a superheated (above-boiling temperature) dryout zone will develop 
closest to the heat source, separated from the condensation zone by a nearly isothermal zone 
maintained nominally at the boiling temperature. This nearly isothermal zone is characterized by 
a continuous process of boiling, vapor transport, condensation, and migration of water back 
toward the heat source (vaporliquid counter flow resulting from capillary forces or gravity 
drainage), a process often referred to as a heat pipe (Pruess et al. 1990). 
For the current repository design concept, the dryout zone around drifts will extend to a distance 
of approximately 5 to 10 m from the drift wall (BSC 2003b, Section 6.2). Boiling conditions in 
the rock are expected to exist for about 1,000 years after emplacement. While these values 
reflect average conditions, there may be significant spatial and temporal variability of the 
thermal-hydrologic conditions within the repository. One factor causing heterogeneity is the 
spatial and temporal variability directly related to the thermal load in different drift sections, 
stemming from heat output variations between individual waste packages and different 
emplacement times. Another factor is the heterogeneity of the formation properties and spatial 
distribution of the local percolation fluxes. Thermal rock properties, such as thermal 
conductivity, directly affect the conductive transport of heat. Hydrologic properties and local 
percolation fluxes, on the other hand, affect the significance of thermal-hydrologic coupling as 
they determine the effectiveness of convective heat transport. While heat conduction is the 
major component of energy transport in Yucca Mountain tuff, the impact of thermal-hydrologic 
coupling can be quite large. For example, a large percolation flux above a drift segment, 
combined with relatively high permeability, may cause heat-pipe effects that give rise to rock 
temperatures much lower and boiling periods much shorter than at average conditions (BSC 
2003b, Section 6.2.1.4). 
October 2003 2-9 No. 3: Water Seeping into Drifts Revision 2 
Repository Heating 
Figure 2-4. Schematic of Thermal-Hydrologic Processes Occurring in the Drift Vicinity as a Result of 
Heating of the rock in the drift vicinity can affect seepage in two different ways: 
1. Boiling of water in the rock directly affects the seepage-relevant flow processes close 
to the drift wall. For above-boiling conditions, vaporization of percolating water in the 
fractured rock overlying the repository further reduces the potential for seepage. 
Percolating water is expected to boil off in the superheated rock zone before reaching 
the drift crown. Therefore, seepage is unlikely as long as boiling conditions exist. On 
the other hand, condensation forms a zone of elevated water saturation above the 
dryout zone. Water from this zone may be mobilized to flow rapidly down toward the 
drift, in particular during later stages with reduced heat output from the waste 
packages when the effect of vaporization has diminished. This flow mobilization may 
promote seepage. 
2. Rock properties relevant for seepage may be affected from reversible and irreversible 
thermal, hydrologic, chemical, and mechanical effects. Thermal stress-induced 
changes tend to close existing fractures, leading to a general decrease in fracture 
permeability and porosity combined with an increase in fracture capillary strength. 
Aperture changes that occur during the thermal period could be fully reversible 
(i.e., these properties would recover to preemplacement values after the temperature 
has declined to ambient conditions). Thermal stresses could also induce permeability 
enhancement through fracture shear slip with accompanying shear dilation opening. 
Such permeability changes would be irreversible and remain after the temperature has 
declined to ambient conditions. Coupled thermal-hydrologic-chemical processes, such 
as mineral precipitation and dissolution in fractures and matrix, also have the potential 
to irreversibly modify permeability, porosity, and capillary strength of the system. 
The molar volumes of minerals created by hydrolysis reactions (i.e., anhydrous phases, 
such as feldspars, reacting with aqueous fluids to form hydrous minerals, such as 
October 2003 2-10 No. 3: Water Seeping into Drifts Revision 2 
zeolites or clays) are commonly larger than the molar volumes of the primary reactant 
minerals. Consequently, dissolution-precipitation reactions commonly lead to porosity 
and permeability reductions. The extent of mineral-water reaction is controlled by the 
surface areas of the mineral phases in contact with the aqueous fluid, as well as 
heterogeneity in the initial distribution of minerals in the fractures. Therefore, changes 
in porosity and permeability caused by these processes may also be heterogeneously 
distributed. Typically, chemical effects on hydrologic properties are irreversible. 
As mentioned in Section 2.3.3, emplacement drifts may completely collapse in extreme cases as 
a result of thermal and seismic stresses and degradation of joint mechanical properties. The 
thermal conditions in a collapsed drift will be different from those in an open drift, mainly 
because the thermal-hydrologic processes in a drift filled with rock fragments are different from 
those in an open, air-filled drift. The extent to which these differences can be important for 
seepage under thermally elevated conditions is governed by the time at which significant drift 
collapse occurs. Significant differences should only be expected when drift collapse occurs 
during the boiling period. 
The impact of repository heat on the hydrologic, chemical, and mechanical conditions was 
examined in a heater experiment referred to as the Drift Scale Test (DST). A short description of 
the DST can be found in Section 3.3.1. The related modeling documented in Drift-Scale 
Coupled Processes (DST) and TH Seepage Models (BSC 2003b) is mainly used to corroborate 
the abstraction of coupled processes on the evaluation of seepage under thermal conditions, as 
discussed in Sections 4.6 and 4.8. 
2.4 IN-DRIFT CONDITIONS 
Preclosure ventilation will cause partial rock drying in the drift vicinity and will also remove a 
significant amount of heat and moisture. While this relatively short ventilation period is 
expected to have minor impact on the postclosure performance of the repository, in-drift 
moisture conditions are important during seepage testing (see Sections 3.1 and 3.2) and the 
analysis of seepage-rate data (see Section 4.3). 
Reduced relative humidity in the underground opening leads to evaporation of water at the drift 
surface and the development of a dryout zone in the vicinity (5 to 10 m) of the cavity. In a 
liquid-release test at ambient conditions (or natural percolation during the ventilated period), part 
or all of the water reaching the ceiling of the opening may evaporate, depending on the 
evaporation potential in the drift and the wet area exposed to evaporation. The evaporation 
potential depends on the relative humidity in the opening and the thickness of a diffusive 
boundary layer at the drift surface, which in turn is governed by the air velocity in the ventilated 
drift. Total evaporation depends on the evaporation potential and the wetted area available for 
evaporative mass transfer. 
Wetting of the drift ceiling depends on the formation properties, the spreading mechanism along 
the drift surface, and evaporation itself. Under natural percolation conditions, evaporation in a 
ventilated drift prevents sufficient wetting at the drift surface and thus seepage. However, the 
development of a wet spot and its relation to in-drift conditions has been studied during the 
seepage tests conducted in several niches and along the ECRB Cross-Drift (see Section 3.1). 
October 2003 2-11 No. 3: Water Seeping into Drifts Revision 2 
Temporal reduction of the wet spot size during continued water release can be correlated to 
increased evaporation as a result of changes in the ventilation regime, highlighting the coupled 
nature of the processes. 
The importance of evaporation effects on the interpretation of seepage data from liquid-release 
tests conducted under ambient temperature conditions has been recognized. The issue has been 
addressed by (1) increasing relative humidity in the testing area (using bulkheads, end curtains, 
and humidifiers), (2) monitoring relative humidity and evaporation from a free water surface 
(pan experiments), and (3) inclusion of evaporation into the process model used to analyze 
seepage-rate data. 
If evaporation is significantly reduced, wetting of the drift surface is expected. Wet surfaces and 
film flow are an integral part of the capillary barrier concept, providing evidence that the 
capillary barrier is engaged. Wet surfaces were observed in the passive Cross-Drift hydrologic 
test (see Section 3.2). 
Additional discussion of evaporation issues can be found in Appendix C. 
October 2003 2-12 No. 3: Water Seeping into Drifts Revision 2 
3. FIELD OBSERVATIONS AND SEEPAGE TESTING DATA 
3.1 LIQUID-RELEASE TESTING 
3.1.1 Description of Liquid-Release Tests 
Drift-scale liquid-release tests were initiated in 1997 to investigate potential seepage into an 
underground opening representing a waste emplacement drift. Short drifts (ranging from 6.3 m 
to 15.0 m in length and referred to as niches) were constructed at various locations along the ESF 
and the ECRB Cross-Drift. Boreholes were installed prior to and after the niches were excavated 
to facilitate characterization of the rock using air-injection tests and investigation of seepage 
processes using liquid-release tests. The locations of the niches were chosen so that they 
represent different hydrogeologic units and rocks with different fracture statistics. A second 
study, referred to as the systematic borehole testing program, was initiated in 2000 to 
complement the niche seepage experiments. The purpose of the program is to provide broad, 
systematic coverage and characterization of the host rock by performing air-injection and 
liquid-release tests in approximately 20-m-long boreholes drilled at a 15 angle upward and 
parallel to the drift axis into the ceiling every 30 m along the ECRB Cross-Drift. Test locations 
are illustrated in Figure 3-1. 
The purpose of these experiments was to release water from borehole intervals located above 
drift sections or niches and to collect the water that seeps into the openings. These seepage-rate 
data contain information about the seepage process reflecting most of the factors discussed in 
Section 2. They have been analyzed to infer seepage-relevant, model-related effective 
parameters on the drift scale. The tests were generally performed by (1) injecting air to 
characterize the permeability distribution, (2) introducing water from a borehole interval above 
the opening, (3) recording the induced seepage, (4) monitoring temperature and relative 
humidity, (5) observing the formation and growth of the wetted spot at the ceiling and 
(6) studying the general seepage behavior. 
Multiple liquid-release tests were performed in the niches and along the ECRB Cross-Drift to 
observe, document, and quantify any water migrating to and seeping into the underground 
openings. The tests were performed by sealing a short section of the borehole above the opening 
using an inflatable packer system and then releasing water at a specified rate into the test 
interval. Any water that migrated from the borehole to the ceiling and dripped into the opening 
was captured and measured. Qualitative observations during the tests helped provide an 
understanding and corroboration of flow diversion and seepage concepts. Moreover, a 
quantitative analysis of the seepage-rate data provided calibrated values of seepage-relevant 
formation parameters (see Section 4.3). 
The effectiveness of the capillary barrier and the presence of a seepage threshold can be directly 
observed from liquid-release tests conducted at different rates, which show that seepage ceases at 
a nonzero injection rate, referred to as a seepage threshold. 
Seepage tests are further described in Appendices B and C. 
October 2003 3-1 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003e, Figure 4. 
NOTE: The shape of the openings is approximate. (In this and other figures, niches are labeled by their construction 
station number (i.e., Niche 2 is designated as Niche 3650, Niche 3 is Niche 3107, Niche 4 is Niche 4788, 
and Niche 5 is Niche 1620). ECRB = Enhanced Characterization of the Repository Block. 
Figure 3-1. Schematic Geologic Map Showing Approximate Location of Niches and Systematic Testing 
October 2003 3-2 
Boreholes SYBT-ECRB-LA#13 
3.1.2 Air-Permeability Testing 
The purpose of the air-injection tests was to estimate permeabilities as input data for the 
stochastic generation of heterogeneous permeability fields. The tests were performed by 
isolating a short section of a borehole using an inflatable packer system and then injecting 
compressed air at a constant rate into the isolated injection interval. The pressure buildup in the 
injection interval and in nearby similarly isolated observation intervals was monitored with time 
until steady conditions were reached, typically within a few minutes. Air injection was 
terminated after reaching steady pressures, and the decline in air pressure was then monitored as 
it recovered to its initial pretest condition. Air-permeability values were derived from the steady 
pressure data by means of a commonly used analytical solution (BSC 2001a, Section 6.1.2.1). 
No. 3: Water Seeping into Drifts Revision 2 
Permeabilities determined from air-injection tests are considered representative of the absolute 
permeability of the excavation-disturbed zone around the opening. Since air-injection tests are a 
standard method to obtain permeability values, the use of these values as the basis for model 
calibration, seepage prediction, and the development of probability distributions for TSPA 
ensures consistency and reduces a potential bias that would likely be introduced by relying on 
different measurement methods. 
Air permeabilities were measured before and after mining of the niches. The results showed that 
permeability around the niches and the ECRB Cross-Drift was affected by excavation (BSC 
2001a, Section 6.1.2.2; Wang and Elsworth 1999, pp. 752 to 756). Since seepage is determined 
by the formation properties and excavation effects in the immediate vicinity of the opening, it is 
reasonable to use postexcavation air-permeability data for seepage calculations. 
3.1.3 Relative-Humidity Monitoring 
Reduced relative humidity in the underground openings leads to partial evaporation of the water 
that reaches the cavity wall, potentially affecting seepage. To diminish, control, and quantify 
this effect, relative humidity in the closed-off niches was artificially increased to reduce the 
evaporation potential, and relative humidity was monitored. Figure 3-2 shows an example of 
temperature and relative humidity data measured in Niche 4 (also referred to as Niche 4788). 
Source: BSC 2001a, Figure 6.2.1-5. 
Figure 3-2. Temperature and Relative Humidity Measurements in Niche 4 
No. 3: Water Seeping into Drifts October 2003 3-3
Revision 2 
In a closed-off and humidified niche, potential evaporation at the wall or in the capture system is 
expected to be small compared to the amount of water being released. Seepage experiments in 
the middle nonlithophysal zone (Tptpmn) of the Topopah Spring welded unit were conducted in 
niches that were closed off by a bulkhead, which reduces air circulation and thus leads to 
comparatively high relative humidity. Moreover, a humidifier was used in some of the 
experiments to increase relative humidity to a value close to 100 percent. The measured 
evaporation rates and a related sensitivity analysis indicate that evaporation effects in the 
closed-off niches are insignificant and can be neglected in the analysis of seepage-rate data (BSC 
2003e, Section 6.7). On the other hand, relative humidity in the open ECRB Cross-Drift is 
significantly lower and exhibits relatively strong fluctuations depending on weather and 
ventilation conditions. Evaporation-rate data from pan experiments were used to estimate the 
thickness of the diffusive boundary layer, which affects the evaporation potential. Evaporation 
in the ventilated ECRB Cross-Drift was found to be a greater fraction of the observed seepage 
rate, compared to the niche tests and was taken into account for the analysis of seepage tests 
conducted in the open drift. 
The monitoring of relative humidity is further discussed in Appendix C. 
3.1.4 Liquid-Release Tests in Niches and along the Enhanced Characterization of the 
Repository Block 
Multiple liquid-release tests were performed in Niches 2, 3, 4, and 5 (also referred to as 
Niches 3650, 3107, 4788, and 1620, respectively), as well as in the systematic testing boreholes 
SYBT-ECRB-LA#1 to 3. Water was released at various rates from a short section of the 
borehole above the opening. Any water that migrated from the borehole to the ceiling and 
dripped into the opening was captured and measured. In many intervals, multiple liquid-release 
tests were conducted using different release rates with different durations of inactivity between 
individual test events. Only a very small amount of water was released in early tests conducted 
in Niche 2. To reduce the impact of storage effects and to test a more representative portion of 
the fracture network involved in flow diversion around the opening, later tests in Niches 3, 4, 
and 5 and along the ECRB Cross-Drift used significantly more water in an attempt to reach 
near-steady seepage conditions. These later tests were used for parameter estimation purposes, 
as described in Section 4.3. 
Figure 3-3 shows contours of the wetting front spreading across the niche ceiling during a 
liquid-release test. Water issued from the formation through fractures and micro-cracks and 
spread along the rough and dusty surface. Dripping was initiated at discrete points. As indicated 
in Figure 3-4, seepage rates measured during a representative liquid-release test appear to 
stabilize after about 4 days of continuous water injection. In this example, the high release rate 
resulted in a near-steady seepage rate that was approximately half the release rate. 
Appendices B and C contain additional information on seepage testing. 
October 2003 3-4 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2001a, Figure 6.2.1-7. 
NOTE: Blue contours are outlines of wetting fronts. Red numbers indicate ordering of the wetting fronts in time. 
The pink bar indicates the approximate position of the release interval in the borehole above the niche, 
projected onto the crown. 
Figure 3-3. Wetting-Front Sequences Overlying Fracture Map of Niche 4 Crown for a Representative 
Liquid-Release Test 
October 2003 3-5 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2001a, Figure 6.2.1-6. 
Figure 3-4. Seepage Rates Observed during a Representative Liquid-Release Test Conducted in 
October 2003 3-6 
Niche 4 
3.1.5 Mass Balance in Niche 5 
The flow-diversion capability of the capillary barrier is the mechanism of interest for the 
estimation of reduced seepage into waste emplacement drifts. The fate of water during a 
transient liquid-release test is difficult to assess (i.e., the difference between the release rate and 
seepage rate cannot be attributed to flow diversion with certainty unless all the water used in a 
liquid-release test is accounted for in a full mass balance). Obtaining a complete mass balance in 
a transient test requires estimation of the amount of water that (1) is injected, (2) seeps into the 
opening, (3) evaporates from the rock surface and the collection system, (4) is stored in the 
formation between the injection point and the opening, (5) bypasses the opening through known 
and unknown geologic features, and (6) is diverted around the opening on account of the 
capillary-barrier effect. 
Components 1 and 2 can be directly measured with sufficient accuracy. Reliable estimates of 
Component 3 can be obtained from relative-humidity or evaporation-rate measurements. 
Alternatively, the evaporation potential can be minimized, as described in Section 3.1.3. For 
Component 4, the amount of water stored in the formation, is difficult to obtain. However, the 
tests can be run to near-steady-state conditions, and a rate balance (as opposed to a mass balance) 
can be performed. Finally, measuring Components 5 and 6 requires capturing the water in a 
secondary water collection system. 
No. 3: Water Seeping into Drifts Revision 2 
Performing such a water mass balance was considered for the Alcove 8Niche 3 test (see 
Section 3.1.6) but was not performed due to the large scale of the test and the correspondingly 
large secondary collection system that would be required. Instead, an attempt was made to 
obtain a mass balance in the Niche 5 seepage tests. The main element of this attempt was the 
construction of a slot on the side of the niche to capture the water that is diverted around the 
opening (i.e., Component 6). Relative humidity in Niche 5 was increased to reduce the 
contribution of Component 3, and a long-term liquid-release test was performed to minimize 
storage effects (Component 4). The relatively close proximity of the injection point to the drift 
ceiling reduces the risk that water bypasses the niche through unknown, unique geologic features 
(Component 5). Since near seepage conditions were achieved, a rate balance (rather than total 
mass balance) was performed, which is more appropriate in light of the eventual estimation of 
near steady seepage rates under repository conditions. 
Water was collected at the side of the niche during two seepage tests conducted in Niche 5. 
However, because of difficulties in excavating the slot and installing the capture system, it was 
not possible to visually confirm that the water collected in the slot near the wall was derived 
entirely from seepage into the slot. While qualitative evidence was obtained that the capillary 
barrier was capable of diverting water around the niche, a quantitative mass or rate balance based 
on the measured data alone could not be obtained. The seepage predictions, therefore, continue 
to rely on (1) established understanding of the physics underlying flow diversion around a 
capillary barrier, (2) extensive site-specific and seepage-related characterization data, 
(3) qualitative evidence demonstrating flow diversion and water exclusion, (4) calibration and 
validation of a physically based process model that captures all components of the mass balance 
(storage, evaporation, flow diversion, and seepage), and (5) propagation of uncertainties and 
variabilities and probabilistic treatment of seepage in TSPA calculations. 
The mass-balance issue is further described in Appendix C. 
3.1.6 Alcove 8Niche 3 Testing 
Evaluation of seepage is among the multiple objectives of the ongoing testing at 
Alcove 8-Niche 3. Alcove 8 (located in the ECRB Cross-Drift, see Figure 3-5) was excavated 
and prepared to perform liquid-releases tests into a fault and a network of fractures. 
Approximately 20 m below Alcove 8, Niche 3 (located in the main drift of the ESF at 
construction station 3107) serves as the site for monitoring of seepage. The interior of the niche 
was instrumented with trays for seepage collection. In addition, a series of boreholes 
surrounding Niche 3 was instrumented with sensors to detect the arrival of the wetting front. 
Liquid water and tracers were released at the floor of Alcove 8 (located in the upper lithophysal 
zone, Tptpul) along approximately 5 m of an exposed fault. The amount of water seeping from 
the fault into Niche 3 (which is located in the middle nonlithophysal zone, Tptpmn) and tracer 
concentrations were monitored as functions of time. An example is presented in Figure 3-6, 
showing the seepage rate is approximately 10 percent of the injection rate. 
Seepage-related issues are further discussed in Appendix C. Pretest predictions are described in 
Appendix E. 
October 2003 3-7 No. 3: Water Seeping into Drifts Revision 2 
Figure 3-5. Schematic Illustration of the Alcove 8Niche 3 Test Configuration 
October 2003 3-8 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003c, Figures 7.6-1 and 7.6-2. 
Figure 3-6. Infiltration Rate in Alcove 8 (a) and Seepage Rate in Niche 3 Test (b) 
3.2 MOISTURE MONITORING IN NONVENTILATED DRIFT SECTIONS 
3.2.1 Description of Passive Cross-Drift Hydrologic Tests and Alcove 7 
The terminal section of the ECRB Cross-Drift was closed off by a series of bulkheads to 
minimize ventilation effects (see Figure 3-7). The 918-m-long drift section is located in the 
Topopah Spring lower lithophysal (Tptpll) and the lower nonlithophysal (Tptpln) tuff units; the 
drift section is intersected by the Solitario Canyon fault. Within the isolated sections between 
bulkheads, barometric pressure, relative humidity, and temperature are currently being measured 
at various stations to provide information on moisture dynamics. Psychrometers were installed 
along seven boreholes to measure the water potential and, thus, the initial extent and later 
rewetting of the dryout zone in the fractured rock. Electrical resistance probes were laid out at 
0.5 m intervals to measure saturation changes along the drift wall. Six water collection units 
were installed. Periodically, the bulkhead doors sealing the nonventilated sections have been 
opened for observations. These observations have included sampling of liquid water from these 
water-collection units. Although the quantity of water has not been measured, water samples 
have been collected and subsequently analyzed to evaluate whether the water originated from 
seepage or condensation (see Section 3.2.4). 
An experiment similar to that described above has been conducted in Alcove 7 since 1998. 
Bulkhead doors were installed 64 m and 132 m from the entrance of the alcove. Ambient 
temperature, barometric pressure, and relative humidity were monitored. The bulkheads were 
opened after being closed for extended periods of time. Evidence of moisture was observed, 
including drip spots on the drip collection sheets, moisture drops on the utility lines and on the 
shotcrete around the bulkheads, and moisture spots in the dust on one instrument enclosure. The 
rock in the crown had a dark, moist appearance, and the fractures in the rib appeared wet. 
Although moisture was present, it was not possible to collect water for analysis. The Alcove 7 
test results are summarized in Appendix C. 
3-9 No. 3: Water Seeping into Drifts October 2003
Revision 2 
NOTE: TBM = tunnel boring machine; ERP = electrical resistance probe. 
Figure 3-7. Schematic Illustration of the Location of Monitoring Stations in the Enhanced 
Characterization of the Repository Block and the Tunnel Boring Machine 
Results of in situ moisture monitoring since the construction of the ESF and ECRB Cross-Drift 
and the DST (see Section 3.3.1) indicate no direct observations of seepage. However, moisture 
has been observed in nonventilated sections of the ECRB Cross-Drift and Alcove 7. The origin 
of these moisture observations is uncertain. It is expected that moisture will be released from the 
partially saturated rockmass in contact with the drift wall by evaporation processes. Given the 
drifts are ventilated, the relative humidity in the drifts prior to the ventilation being turned off is 
significantly less than 100 percent; therefore, a potential gradient exists to allow moisture vapor 
to be transported from the rock matrix into the drift. This moisture vapor flux, once it enters the 
drift, can be transported along the drift and condense on cooler surfaces. This gradient and the 
resultant net influx of rock moisture into the drifts are transient phenomena related to the change 
in moisture and thermal conditions in the drift. At steady state, after the drifts have been 
removed from transient humidity and pressure conditions, the relative humidity is expected to 
stabilize at 100 percent. At steady state, the principal source of liquid water is expected to be 
derived from seepage water. Prior to steady state, when in-drift conditions are less than 
100 percent humidity, moisture in the drift derived from evaporation in the rock wall may exceed 
the seepage influx. This moisture may condense on cooler surfaces, leading to liquid water. 
October 2003 3-10 No. 3: Water Seeping into Drifts Revision 2 
3.2.2 Evidence of Ventilation Effects 
The observations of changes in water potential, saturation, and in-drift atmospheric conditions 
after closure of the bulkheads confirm the strong impact of ventilation and reduced relative 
humidity on the hydrologic conditions in the immediate vicinity of the drift. The matrix is 
partially dried out up to a few meters from the drift surface. Even though the relative humidity 
increases rapidly after closing of the bulkheads, the water potential data indicate that the 
rewetting of the matrix is a slow process. Figure 3-8 shows water potentials as a function of time 
and distance from the drift surface. Low water potentials up to a distance of about 1.5 m from 
the borehole collar indicate the extent of the dryout zone as a result of drift ventilation. After 
installation of the bulkheads, water potentials increase over a period of 1.5 years. 
In-drift conditions (temperature, relative humidity, and barometric pressure) not only show 
temporal variations but also spatial differences along the tunnel section, particularly when heat 
sources are present. The resulting gradients constitute driving forces for in-drift moisture 
redistribution. Figure 3-9 shows temperature fluctuations as a function of time at four stations 
along the nonventilated section of the ECRB Cross-Drift. 
Source: BSC 2003f, Figure 6.10.2-2b. 
Figure 3-8. Water Potential Measurement as a Function of Time and Distance from the Drift Surface 
October 2003 3-11 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003f, Figure 6.10.2-4. 
Figure 3-9. Temporal and Spatial Variations in Temperature within Nonventilated Section of the 
October 2003 
Enhanced Characterization of the Repository Block 
3.2.3 Observations Related to Wet Zones 
Wet zones observed in the closed-off sections of the ECRB Cross-Drift provide information 
regarding potential seepage and in-drift moisture redistribution. During the entries behind the 
bulkheads, droplets and other moisture conditions were observed on rock bolts, ventilation ducts, 
utility conduits, wire meshes, and painted patches of tunnel walls. Puddles of water were 
observed on the conveyor belt, and drip cloths showed evidence of dripping. Observed rust spots 
and organic growths indicate the prolonged presence of moisture. 
The observations of moisture on impervious (nonporous) surfaces suggest that, at least partially, 
the moisture originated from condensation. The near100 percent relative humidity in the ECRB 
Cross-Drift and local thermal gradients (partly induced by electrical equipment in the closed-off 
drift sections) are the likely causes for the observed condensation. Although it is possible that 
the dripping may have resulted from seepage of formation water, the geochemical analyses 
presented below support the conclusion that this is most likely condensation water. 
3-12 No. 3: Water Seeping into Drifts Revision 2 
3.2.4 Chemical and Isotopic Water Analyses 
Determining the origin of the moisture observed in the closed-off sections of the ECRB Cross- 
Drift is of interest because it relates to the process inducing dripping (condensation or seepage) 
and affects the chemistry of the water potentially contacting waste packages. Chemical analyses 
and isotopic measurements were conducted on the water samples collected during the periodic 
entries into the nonventilated sections of the ECRB Cross-Drift. The chemical analyses included 
major anionic and cationic constituents (such as bromide, chloride, and lithium). 
The initial water samples collected from the puddles on the conveyor belt were dark in color. 
Because the surface of the conveyor belt was covered by dust and rock fragments, the chemical 
analyses of these samples were not expected to provide meaningful signature about the source of 
water found in the puddles. Subsequent samples were taken from clean containers placed on top 
of the conveyor belt. These samples were found to be low in chloride and silica content, 
characteristic of condensates. The samples were also found to lack the chemical signature of the 
construction water that was spiked with 20 mg/L of lithium bromide. While these data clearly 
show that part of the observed moisture originated from condensation, they do not rule out the 
possibility that some of these waters are of mixed origins. 
The hydrogen (D) and oxygen (18O) isotope compositions were also analyzed. The D values 
range from .48 to .9, and the 18O values range from .3 to .10.7. These values are 
higher than those found in construction water. The lag time between opening of bulkheads and 
sample collection (3 to 4 hours) is sufficient to result in a significant degree of evaporation of the 
samples. As seen in Figure 3-10, all samples from the ECRB Cross-Drift are shifted from the 
global meteoric water line. The offset is characteristic of waters that have undergone some 
degree of evaporation. The same degree of shifts for both the contaminated samples and the 
relatively clean samples may indicate that approximately the same amount of evaporation 
occurred. 
The geochemical and isotopic analyses of water collected in the nonventilated ECRB Cross-Drift 
seem to indicate that condensation is a source of the dripping water. 
3.2.5 Summary 
Moisture monitoring in nonventilated sections of the ECRB Cross-Drift and ESF is an ongoing 
part of the field testing program. Observations of hydrologic and thermodynamic conditions in 
the drift itself and in the nearby rock lead to the following seepage-related findings: 
1. Ventilation effects in ventilated drift sections have a significant impact on seepage, 
mainly through evaporation of potential seepage water at the drift surface but also 
through the development of a dryout zone around the opening. 
2. Once ventilation effects are reduced or eliminated, the relative humidity of the initially 
dry in-drift environment generally increases in a short time period. 
3. The high relative humidity in closed-off drift section leads to conditions that facilitate 
in-drift moisture redistribution processes, which may be associated with condensation 
October 2003 3-13 No. 3: Water Seeping into Drifts Revision 2 
of water on surfaces, inducing dripping. These processes are likely to occur even in 
the presence of only small temperature gradients. 
4. The presence of water on nonporous surfaces and the chemistry and isotopic 
composition of water samples suggest that the water accumulations in the ECRB 
Cross-Drift originated from condensate. However, minor contributions from seepage 
water, masked by condensate, are possible based on currently available information. 
The observations in the nonventilated section of the ECRB Cross-Drift are presented in 
Appendices B and C. Appendix C also summarizes results from the tests in Alcove 7. 
Source: BSC 2003f, Figure 6.10.2-9. 
NOTE: Also plotted is the isotopic composition of construction water, two pore water samples extracted from core 
samples from Alcove 5 and the Global Meteoric Water Line. 
Figure 3-10. Plot of the Hydrogen and Oxygen Isotope Compositions of Water Samples Collected from 
October 2003 
the Enhanced Characterization of the Repository Block 
3-14 No. 3: Water Seeping into Drifts Revision 2 
3.3 COUPLED PROCESSES TESTING 
3.3.1 Drift Scale Test 
As discussed in Sections 2.4 and 2.6, seepage is partly determined by the properties of the 
fractured rock. The properties may be altered as a result of coupled effects induced by heating of 
the repository. For example, increased temperatures lead to mechanical deformations that 
change the hydrologic properties of the fracture network (BSC 2003g). Moreover, mineral 
dissolution and precipitation during the thermal period may temporarily or permanently affect 
the apertures of fractures in the immediate vicinity of the waste emplacement drifts (BSC 
2003h). These coupled effects during repository heating have been studied using numerical 
simulation and the DST, which is the largest underground thermal test carried out to date in the 
ESF. 
The purpose of the DST is to evaluate the coupled thermal, hydrologic, chemical, and 
mechanical processes that take place in unsaturated fractured tuff over a range of temperatures 
(approximately 25C to 200C). Details regarding the DST layout, borehole orientations, 
operation of the test, and measurements performed (as well as their uncertainties) are discussed 
in the Thermal Testing Measurements Report (BSC 2002b, Section 6.3) and Drift Scale Test 
As-Built Report (CRWMS M&O 1998). In brief, the DST consists of an approximately 
50-m-long drift that is 5 m in diameter. Nine electrical canister heaters were placed in this drift 
to simulate nuclear-waste-bearing containers. Electrical heaters were also placed in a series of 
horizontal boreholes (wing heaters) drilled perpendicularly outward from the central axis to both 
sides of the drift. These heaters were emplaced to simulate the effect of adjacent emplacement 
drifts. The DST heaters were activated on December 3, 1997, with a planned period of 4 years 
of heating, followed by 4 years of cooling. After just over 4 years, the heaters were switched off 
on January 14, 2002, and since that time the test area has been slowly cooling. Figure 3-11 
shows a schematic view of the test layout with the main heater tunnel, the wing heaters, and the 
array of observation boreholes monitoring temperature, as well as chemical, mechanical, and 
hydrologic variables. Data on the evolution of gas phase, liquid phase and solid phase 
compositions, changes in water content and air permeabilities, and rock deformations collected 
during the DST were used to validate the related coupled models on thermal, hydrologic, 
chemical, and mechanical processes, as discussed in Sections 4.6 and 4.8. 
No seepage has been observed during the DST. This observation is consistent with the effect of 
the vaporization barrier described in Section 1.5. However, the absence of observed seepage 
should not be directly used to evaluate seepage into repository drifts because the potential for 
seepage in the DST may have been reduced as a result of vapor losses through the bulkheads 
(BSC 2003b, Section 6.4.3.2). 
Property changes induced by elevated temperatures as inferred from direct observations and 
associated modeling of the DST were examined for their impact on seepage, as discussed in 
Sections 4.6 and 4.8. 
October 2003 3-15 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2002b, Figure 6.3-2. 
Note: ERP = electrical resistance probe; ESF = Exploratory Studies Facility 
Figure 3-11. Three-Dimensional Perspective of the As-Built Borehole Configuration of the Drift Scale 
October 2003 3-16 
Test 
3.3.2 Fracture Sealing Experiment 
A laboratory fracture sealing experiment was designed to evaluate the effects of condensate 
reflux through a fracture network and into a boiling environment. Two saw-cut blocks of welded 
rhyolite ash-flow tuff, measuring 31.7 cm tall, 16.2 cm wide, and 3.2 cm thick, were separated to 
create a vertical planar fracture. Heating was accomplished through the use of electrical 
resistance heaters mounted directly on the sides of the blocks. A vertical temperature gradient 
was established within the block assembly, with a temperature of 80C at the top and 130C at 
the bottom. Temperatures were monitored throughout the experiment. 
After steady-state chemical conditions were attained in a plug-flow reactor, a portion of the 
water generated from the reactor was flowed at a rate of 10.8 mL/hr into the top of the fracture. 
After 5 days, the fracture began to seal, as evidenced by a declining outflow rate, leaks in the 
inlet side of the fracture, and the need for increased pressure to maintain a constant inlet flow 
rate. The aperture was effectively sealed. 
No. 3: Water Seeping into Drifts Revision 2 
After cooling, the fracture was opened and examined to determine the location and nature of 
secondary mineral formation (Figure 3-12). The precipitate (identified as mainly amorphous 
silica) was deposited almost exclusively at temperatures exceeding 100C. Bridging structures 
of amorphous silica that formed during the experiment in both the saw-cut fracture and a natural 
fracture appear to obstruct fluid flow within the fracture system. These same processes could 
result in the development of a precipitation cap above the heated drift, potentially reducing 
seepage (see also discussion in Section 4.8). The fast and complete sealing seen in this 
laboratory experiment may be a result of the fact that a single fracture has been tested. The high 
thermal gradient imposed on the sample may also have accelerated the sealing phenomenon. 
Source: BSC 2002b, Figure 7.3-2. 
NOTE: Scale bars are 0.5 mm. 
Figure 3-12. Bridging Structures (a) in an Opened Planar Fracture and (b) in a Crosscutting Fracture 
3.4 MINERAL DEPOSITIONS IN LITHOPHYSAL CAVITIES 
Observations of naturally occurring calcite and opal precipitation in lithophysal cavities (BSC 
2002c, Section 6.10.1; Paces et al. 2001; Marshall et al. 2003) can be used to estimate long-term 
seepage rates into these small openings. Calcite precipitates from downward-percolating 
meteoric water because of (1) evaporation, (2) CO2 outgassing as a result of the geothermal 
gradient, and (3) interaction with a gas phase containing less CO2 than the gas with which the 
water was last equilibrated. Considering these calcite-precipitation mechanisms and using 
certain water-to-calcite ratios, seepage into lithophysal cavities was estimated from 
calcite-deposition data. 
October 2003 3-17 No. 3: Water Seeping into Drifts Revision 2 
The calcite depositions on lithophysal cavity floors may not originate from dripping water 
(i.e., seepage); in fact, there is a lack of evidence of dripping from cavity ceilings (absence of 
stalactites or stalagmites at any scale), even where fractures containing coatings intersect 
lithophysae ceilings (Whelan et al. 2002, p. 744). This observation is consistent with the 
capillary barrier concept. Even if making the assumption that all calcite deposited in lithophysal 
cavities originated from seepage, the data indicate that (1) not all lithophysal cavities 
encountered seepage, and (2) seepage flux derived from mineral deposits is a very small fraction 
of percolation flux. Both conclusions corroborate the general concept of a capillary barrier 
reducing seepage below the value of the percolation flux. 
Additional discussion of the analysis of secondary minerals in Appendix C. 
3.5 ABSENCE OF SEEPAGE IN VENTILATED DRIFTS 
So far, no dripping of natural percolation water has been observed in any of the ventilated 
openings at Yucca Mountain (Trautz and Wang 2002). While this finding can be considered 
consistent with the current understanding of the capillary diversion capacity of the fractured 
formation, the absence of seepage can also be explained by evaporation effects. The significant 
evaporation potential of the dry drift atmosphere is evident not only from theoretical 
considerations, but also from temporal observations of wet spots observed at the drift ceiling 
during liquid-release tests conducted in the ECRB Cross-Drift (see discussion of Figure 3-3 
above) and the fact that a damp looking feature observed immediately after the dry excavation of 
Niche 1 (also referred to as Niche 3566) dried up before a bulkhead could be installed to increase 
the relative humidity in the opening. The damp looking feature was observed along a vertical 
wall; that is, it did not induce seepage. The feature did not reappear after sealing the niche with a 
bulkhead. 
Because the evaporation potential in ventilated openings at Yucca Mountain evidently exceeds 
the seepage potential, an effort has been made to maximize relative humidity in the niches 
designated for seepage testing (see Section 3.1.3) in Alcove 7 and in the ECRB Cross-Drift (see 
Section 3.2). These tests and the related modeling studies confirm the impact of evaporation on 
the determination of seepage. 
3.6 NATURAL ANALOGS 
Natural analogs, such as those reported in Natural Analogue Synthesis Report (BSC 2002d, 
Section 8), provide evidence that the concept of water exclusion from underground openings is 
consistent with the process that actually occurs in caves, lava tubes, rock shelters, and buildings. 
The qualitative evidence for water exclusion and flow diversion was substantiated by 
quantitative seepage measurements in limestone caves. These studies show that seepage is 
considerably smaller than the pertinent percolation flux (BSC 2002d, Section 8.2), corroborating 
the seepage testing and modeling results at Yucca Mountain. Calcite-deposition data in 
lithophysal cavities (see Section 3.4) can be considered a natural analog at Yucca Mountain itself 
that further corroborates the concept. 
October 2003 3-18 No. 3: Water Seeping into Drifts Revision 2 
4. SEEPAGE MODELING AND ABSTRACTION 
4.1 PURPOSE AND GENERAL APPROACH 
A number of conceptual, analytical, and numerical models have been developed to help 
understand seepage-related processes and phenomena and to determine site-specific, 
seepage-relevant formation parameters. Some of the models are concerned with simulating 
in situ seepage tests (BSC 2003e), while others were developed for the prediction of seepage into 
intact and degraded waste emplacement drifts under ambient and thermal conditions (BSC 2003i; 
BSC 2003h; BSC 2003a). These drift-scale seepage models are linked to other models on 
different scales, specifically the mountain-scale model of the unsaturated zone at Yucca 
Mountain (BSC 2003c), models considering the coupled thermal-hydrologic-chemical (BSC 
2003h) and thermal-hydrologic-mechanical (BSC 2003g) processes, scale-transition models 
providing flow-focusing factors (BSC 2001b, Section 6.4.2), as well as small-scale models 
evaluating flow within individual fractures (BSC 2003h). Quantitative and qualitative results 
from these process models are used in the seepage abstraction step (BSC 2003a) to arrive at a 
reasonable approach to handling seepage in TSPA calculations. 
The general approach followed to analyze data from seepage experiments conducted at Yucca 
Mountain and to arrive at a calibrated and validated predictive seepage model is based on the 
recognition that (1) detailed simulation of individual seeps is not necessary to estimate average 
seepage rates into waste emplacement drifts, (2) certain factors affecting seepage can be lumped 
into effective parameters, (3) calibrating and validating a model against data from seepage 
experiments provides confidence that the model captures the relevant processes, (4) estimating 
effective parameters partly compensates for processes and features that are not explicitly 
considered in the model, and (5) the estimated parameters can be directly used in a predictive 
model that uses a consistent conceptualization. 
The main advantage of this approach is that it relies directly on seepage-rate data, which 
inherently contain information about the relevant processes. Also, the calibration data (seepage 
rates on the scale of a drift section) are very similar to the quantity of interest for the subsequent 
predictions. The consistency between the calibration model used to derive seepage-relevant 
parameters and the predictive model used to forecast seepage minimizes conceptual differences. 
The appropriateness of the selected method and its potential advantages over alternative 
approaches are further discussed in Appendix D. 
As discussed above, the seepage models are based on data showing seepage-relevant processes 
under in situ conditions; these data were described in Section 3. Some of these data were 
directly used to develop and calibrate the models. For example, air permeabilities (see 
Section 3.1.2) were used to generate and condition heterogeneous permeability fields for the 
seepage model. They were also used to derive statistical measures representing uncertainty and 
variability of this important, seepage-relevant parameter (see Section 4.9). Evaporation-rate and 
relative-humidity data (see Section 3.1.3) were used to determine the evaporative boundary layer 
thickness, which is part of a submodel used for the interpretation of seepage tests conducted in 
the ventilated ECRB Cross-Drift. Seepage-rate data measured during liquid-release tests (see 
Section 3.1.4) were the main data used for calibration of a drift-scale seepage model. Additional 
seepage-rate data were used for testing the capability of the calibrated model to make predictions 
October 2003 4-1 No. 3: Water Seeping into Drifts Revision 2 
under different conditions and at different locations. Data from the DST were used to 
corroborate the conceptual model supporting the abstraction of thermal-hydrologic-mechanical 
and thermal-hydrologic-chemical effects (see Sections 4.6 and 4.8 below). 
The development of the seepage models involves the following steps: 
1. Geostatistical parameters of the permeability field are determined from the results 
of air-injection test data. 
2. Multiple realizations of the permeability field are generated, each of which is 
consistent with the geostatistical properties of the measured air permeabilities 
representing the excavation-disturbed zone in the drift vicinity and are mapped onto 
the computational grid. 
3. A numerical model is developed for the simulation of liquid-release tests conducted 
in niches and along the ECRB Cross-Drift. 
4. Seepage-relevant, model-related capillary-strength parameters are determined by 
calibrating the models against data from liquid-release tests. 
5. The model is tested by comparing predicted seepage rates to observed data from 
seepage experiments not used for model calibration. This step provides confidence 
that the model is capable of predicting the seepage behavior above and below the 
seepage threshold. 
6. A conceptually consistent model is developed for simulating seepage into waste 
emplacement drifts. Drift seepage is evaluated for ranges of percolation flux and 
other seepage-relevant hydrogeologic properties. 
7. Sensitivity analyses are performed to examine the impact of drift degradation, 
ground support, above-boiling conditions during the thermal period, and 
thermal-hydrologic-chemical effects. 
8. The results from Steps 6 and 7, along with other information on uncertainty and 
variability, are combined in the abstraction, providing the basis for a probabilistic 
evaluation of seepage in TSPA calculations. 
Issues related to the general modeling approach are addressed in Appendix D. 
The following sections describe the drift-scale models developed to estimate seepage-relevant 
formation parameters and to make predictive seepage calculations for TSPA. 
4.2 CONCEPTUAL AND NUMERICAL MODELS 
The drift-scale numerical seepage models consider three-dimensional flow through the 
unsaturated fracture network and seepage into the niches or the ECRB Cross-Drift. The 
fractured rock is conceptualized as a heterogeneous continuum with effective fracture 
permeabilities assigned to each grid block. A number of processes affecting seepage (such as 
film flow along the drift surface, impact of drift-wall roughness, and small-scale effects of 
October 2003 4-2 No. 3: Water Seeping into Drifts Revision 2 
discrete fractures terminating at the drift ceiling) are not explicitly modeled but are lumped into 
an effective capillary-strength parameter determined by calibrating the model against 
seepage-rate data, which contain the relevant information about these effects. This 
conceptualization and approach are considered a suitable basis for a model designed to make 
predictions of seepage averaged over a drift section of the length of a waste package. 
The numerical process model used for reproducing seepage-rate data from liquid-release tests 
and to predict seepage into waste emplacement drifts solves the Richards equation (Richards 
1931) for saturated-unsaturated flow through porous materials. The van Genuchten-Mualem 
constitutive relations (van Genuchten 1980) describe the capillary pressure and relative liquid 
permeability in the fracture continuum as a function of liquid saturation. This approach captures 
the main driving forces (gravity, viscous, and capillary forces) and physical phenomena (phase 
interference) relevant for modeling unsaturated flow and seepage in a geologic medium. 
To appropriately include small-scale heterogeneity, the spatial structure of the air-permeability 
data was analyzed, and the resulting geostatistical parameters were used to generate multiple 
realization of a spatially correlated permeability field, which were conditioned on the 
permeabilities measured in borehole intervals. The permeability fields were eventually mapped 
onto the numerical grid; an example is shown in Figure 4-1. The numerical grids created for the 
simulation of liquid-release tests represent an appropriate section of the formation around the 
injection interval, including the underground opening. 
Evaporation from the drift surface is accounted for by specifying a time-dependent 
water-potential boundary condition based on Kelvins equation, where the thickness of the 
diffusive boundary layer was determined from evaporation experiments at the seepage test 
location. 
October 2003 4-3 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003e, Figures 15b and 14. 
NOTE: In Figure 4-1a, the mesh is split into two parts to expose the boreholes (indicated by a thick black lines) and 
the injection interval (thick white line). 
Figure 4-1. Examples of the Numerical Grid and One Realization of the Underlying Heterogeneous 
Permeability Field for the Simulation of Liquid-Release Tests (a) in a Niche, and (b) in the 
October 2003 
Enhanced Characterization of the Repository Block 
Although the permeability structure comprises a network of discrete fractures, the continuum 
approach is appropriate for simulating unsaturated flow and seepage because it is capable of 
predicting observed seepage behaviors and seepage rates. In a network of randomly oriented 
fractures, flow diversion around drift openings occurs primarily within fracture planes. 
Diversion of water through multiple fractures arises only if a fracture is too short and the flow 
path within a fracture plane is interrupted. In this case, water is diverted into the next connected 
fracture, if available. This fracture is again unlikely to be perfectly parallel to the drift axis, 
allowing the in-plane flow-diversion process to continue. The situation is schematically 
illustrated in Figure 4-2, which shows two fractures intersected by a drift. In Figure 4-2a, the 
two fractures are aligned with the drift axis. As an artifact of this specific and unlikely fracture 
orientation, in-plane flow diversion is prevented, and the resulting impact of discreteness on 
seepage is accentuated. In Figure 4-2b, the fractures are approximately perpendicular to the drift 
axis. Flow diversion occurs within the fracture plane, a process that is appropriately captured by 
4-4 No. 3: Water Seeping into Drifts Revision 2 
a heterogeneous fracture continuum model even for a single fracture (which can be considered 
most discrete case). In-plane flow occurring in multiple fractures can be readily combined and 
described by an effective fracture continuum. Given the significance of in-plane flow diversion 
around the drift in combination with relatively high fracture density, a three-dimensional, 
heterogeneous fracture continuum model is an appropriate conceptualization and is, thus, used as 
the basis for the numerical models developed to analyze seepage data from liquid-release tests 
and to predict seepage into waste emplacement drifts. The appropriateness of using a continuum 
model for seepage prediction and its comparison to an approach based on a discrete fracture 
network model are further discussed in Appendix D. 
NOTE: (a) A two-dimensional fracture network model assumes that all fractures are parallel to the drift axis, 
perpendicular to the drift axis. 
preventing flow diversion within the fracture plane; (b) a two-dimensional (and three-dimensional) fracture 
continuum model considers flow diversion occurring within multiple fracture planes that are approximately 
October 2003 
Figure 4-2. Schematic Showing Two Fractures Intersecting a Drift 
In summary, the process model described above captures the forces, processes, and features 
relevant for simulating unsaturated flow and seepage into underground openings at Yucca 
Mountain. The processes are captured either explicitly by solving the physically based 
governing equations or implicitly through an effective parameter that is determined from data 
that include the respective seepage process. The degree of complexity of the model is 
appropriate for its purpose, (i.e., for the prediction of average seepage on the scale of an 
approximately 5-m-long drift segment). Small-scale features and processes, including discrete 
fracture-flow behavior, surface roughness, and film flow, are captured in effective model-related 
parameters determined from site-specific data that reflect the seepage process on the appropriate 
scale (see Section 4.3). Calibration and validation against seepage-rate data and the consistent 
conceptualization in the downstream models make this a valid and reasonable approach to 
characterizing and predicting seepage at Yucca Mountain. 
4-5 No. 3: Water Seeping into Drifts Revision 2 
4.3 MODEL CALIBRATION AND VALIDATION 
Models of niches and the ECRB Cross-Drift (summarily referred to as the seepage calibration 
model) are calibrated against late-time seepage-rate data from numerous liquid-release tests 
conducted in several boreholes at locations in both the middle nonlithophysal zone and the lower 
lithophysal zone (see Figure 3-1). Early-time seepage data are discarded because they are 
affected by storage effects and the properties of a few fractures connecting the injection interval 
with the opening. These fractures are not necessarily representative of the fracture network that 
is activated in flow diversion around the entire opening under steady-state conditions. Late-time 
data are more representative of near-steady conditions and are less influenced by storage effects. 
Moreover, the relatively large amount of released water at late time has likely encountered a 
larger portion of the capillary barrier. Consequently, the late-time seepage data better reflect 
average conditions on the scale of interest. 
Eighty-one liquid-release tests conducted in Niches 2, 3, 4, and 5 as well as the systematic 
testing area in the ECRB Cross-Drift were simulated with the seepage calibration model, a 
numerical process model that captures transient unsaturated flow through a heterogeneous 
fracture continuum and seepage into the underground openings. In addition, evaporation effects 
were accounted for when deemed significant (i.e., when simulating seepage into the open, 
ventilated ECRB Cross-Drift). The simulated saturation distribution at the end of liquid-release 
tests conducted in Niche 5 and the ECRB Cross-Drift are depicted in Figure 4-3. 
Source: BSC 2003e, Figures 26a and 21d. 
Figure 4-3. Saturation Distributions at the End of a Liquid-Release Test Conducted in (a) Niche 5 and 
(b) the Enhanced Characterization of the Repository Block as Simulated with the Calibrated 
Seepage Process Model 
No. 3: Water Seeping into Drifts October 2003 4-6
Revision 2 
Measured seepage-rate data from 22 liquid-release tests performed in boreholes above Niches 3, 
4, and 5 and along the ECRB Cross-Drift were used to calibrate the seepage calibration model 
and to estimate the seepage-relevant, model-related van Genuchten capillary-strength 
parameter 1/. The remainder of the seepage-rate data was used to validate the seepage 
calibration model, (i.e., to determine whether it is appropriate and adequate for its intended use). 
The choice of the tests used for calibration and validation is discussed in Seepage Calibration 
Model and Seepage Testing Data (BSC 2003e, Section 6.6.3.2) 
Examples of calibrated liquid-release tests conducted along the ECRB Cross-Drift and in 
Niche 5 are shown in Figure 4-4. For the tests conducted along the ECRB (Figure 4-4a, b, 
and c), a significant component of the fluctuations in both the simulated and observed seepage 
rates are a result of variations in the relative humidity and, thus, evaporation potential in the 
ventilated drift; the effect is appropriately captured by the model. No such fluctuations are 
observed in the Niche 5 test, where relative humidity was approximately constant at 85 percent. 
Figure 4-5 shows examples of validation runs, in which seepage rates for liquid-release tests 
conducted in Niche 3 were predicted with the calibrated model using a single parameter set and 
compared to measured data that had not been used for model calibration. Linear error 
propagation analysis yielded the uncertainty of the model prediction as a result of uncertainty in 
the input parameters. The data fall within the range of predicted seepage rates. Based on the 
acceptance criteria outlined in Seepage Calibration Model and Seepage Testing Data (BSC 
2003e, Section 7.2), seven of the eight test predictions are considered acceptable. In 
Test UM 4.885.18, the observed late-time seepage rates are slightly larger than the relatively 
narrow uncertainty band. The prediction would be considered acceptable if the chosen 
uncertainty in the input parameters were marginally increased (e.g., to account for uncertainty as 
a result of the stochastic nature of the underlying heterogeneous permeability field). This 
uncertainty will be included in TSPA calculations. 
October 2003 4-7 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003e, Figures 19, 22, 23, and 25. 
NOTE: The gray line is the measured release rate, which is approximated in the model by the black line. Blue 
symbols represent measured seepage-rate data; the red line is calculated with the calibrated models. The 
green line is the relative humidity used to prescribe the evaporation boundary condition. Relative humidity in 
Niche 5 was constant at approximately 85 percent. 
Figure 4-4. Calibration of Seepage-Rate Data from Liquid-Release Tests in Zone 2 of Boreholes 
(a) SYBT-ECRB-LA#1, Zone 2, (b) SYBT-ECRB-LA#2, Zone 2, (c) SYBT-ECRB-LA#2, 
Zone 3, and (d) Borehole #4 in Niche 5 
October 2003 4-8 No. 3: Water Seeping into Drifts Source: BSC 2003e, Figure 43. 
NOTE: Linear uncertainty propagation analysis was used to calculate the uncertainty band of the model predictions. 
Figure 4-5. Validation of Seepage Model and Tptpmn Seepage-Relevant Parameters Using Data from 
Niche 3 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 4-9
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The capillary-strength parameter for each tested borehole interval was determined by calibrating 
the model against multiple tests using different liquid-release rates. Some of these release rates 
induced a local percolation flux that was above the seepage threshold (i.e., water dripped into the 
opening and yielded seepage-rate data valuable for calibration). However, tests were also 
performed below the seepage threshold. Moreover, the model was validated against tests 
conducted above and below the seepage threshold. The system was probed and the model was 
validated for the critical range of percolation rates about the seepage threshold. Seepage 
predictions for natural percolation fluxes that are even less than the low fluxes (below the 
seepage threshold) induced during the low-rate tests will yield the correct result, namely, 
zero seepage. A high-infiltration climate or strong flow focusing can cause the natural local 
percolation flux to exceed the seepage threshold. 
In summary, the capillary strength parameters determined from relatively high-rate liquid-release 
tests provide a solid basis for seepage predictions under low and high natural percolation fluxes. 
The validation approach demonstrates that the seepage process model is capable of predicting the 
behavior above and below the seepage threshold. 
The analysis of seepage-rate data for the determination of seepage-relevant parameters can be 
summarized as follows: 
1. The testing and modeling approach is considered adequate for providing the 
conceptual basis and parameters for predictive seepage models. The approach consists 
of analyzing seepage by means of a numerical process model that is calibrated against 
seepage-rate data from liquid-release tests conducted within the repository host units. 
2. The estimation of seepage-relevant, model-related, effective parameters on the scale of 
interest is an appropriate methodology provided that the structure of the prediction 
model (see Sections 4.4 and 4.5) is consistent with the model used for calibration (the 
seepage calibration model). 
3. Seepage properties are spatially variable. The variability has been examined by 
performing liquid-release tests at various sites along the ESF and the ECRB. Spatial 
variability in the estimated van Genuchten capillary-strength parameter  / 1 is 
relatively large compared to the estimation uncertainty at a given location. The main 
contribution to the estimation uncertainty is small-scale heterogeneity that can only be 
described stochastically. Random fluctuations in seepage-rate data lead to 
insignificant uncertainty in the parameter estimates. 
4.4 PREDICTION OF AMBIENT SEEPAGE 
While the seepage calibration model described in Section 4.3 simulates liquid-release tests and 
seepage into niches and the ECRB for calibration and validation purposes, the seepage model for 
performance assessment was developed to predict total seepage into a section of a waste 
emplacement drift under ambient percolation conditions (BSC 2003i). Isothermal flow 
simulations were performed over wide ranges of selected key parameters. The key parameters 
affecting ambient seepage are the effective capillary-strength parameter, the reference 
permeability, and the local percolation flux imposed at the upper model boundary. Conceptually 
October 2003 4-10 No. 3: Water Seeping into Drifts Revision 2 
consistent with the seepage calibration model, the predictive seepage model for performance 
assessment is a three-dimensional drift-scale model, employing a stochastic continuum 
representation of the small-scale heterogeneity of fractured rock in the drift vicinity. Applying a 
percolation flux at the top of the model, the steady-state seepage flux is obtained. As an 
example, Figure 4-6 shows the resulting saturation distribution for one realization. The 
calculation is repeated for different parameter combinations and different realizations of the 
underlying stochastic permeability field. Results are provided in the form of a lookup table, that 
gives seepage rates and related seepage estimation uncertainty as a function of these key 
parameters. During a probabilistic TSPA calculation, values of input parameters will be sampled 
from their respective probability distributions (see Section 4.6), and the corresponding seepage 
rate will be extracted from the lookup table. Sensitivity analyses were performed to examine the 
impact of the stochastic parameters (standard deviation and correlation) describing the 
small-scale heterogeneity of the permeability field. 
Source: BSC 2001b, Figure 6.4-8. 
NOTE: The development of a shadow zone is shown. 
Figure 4-6. Simulated Liquid Saturation Distribution in Heterogeneous Fracture Continuum in the 
October 2003 
Vicinity of a Waste Emplacement Drift 
4-11 No. 3: Water Seeping into Drifts Revision 2 
The seepage model assumes that the relative humidity within the drift is constant and 
100 percent. This assumption is appropriate for times significantly following the cessation of 
ventilation that steady state humidities in the drift are appropriate. This assumption effectively 
forces all incoming moisture into the drifts to be liquid water (i.e., seepage). Observations made 
in the ECRB (presented in Section 3.2) described the possible effects associated with transient 
moisture flux from the drift wall into the drift and the subsequent redistribution of that moisture 
due to small temperature differences along the drift. 
The systematic simulations performed by the seepage model performance assessment cover a 
wide range of capillary-strength values 1/ (from 100 Pa to 1,000 Pa), mean permeability values 
log10(k[m2]) (from -14 to -10), and local percolation flux (from 1 to 1,000 mm/yr). For each 
parameter combination, 20 realizations of the heterogeneous permeability fields were simulated. 
The range of results from the 20 realizations provides information about the estimation 
uncertainty in the predicted seepage rates because of uncertainty in the stochastic small-scale 
heterogeneity. 
Example results from the seepage model performance assessment are illustrated in Figure 4-7. 
The figure gives contours of the simulated seepage percentage into a drift with a diameter of 
5.5 m as a function of the capillary-strength parameter 1/ and the mean fracture permeability 
for selected percolation fluxes between 1 mm/yr and 1,000 mm/yr. (These percolation fluxes are 
local; they include potential flow focusing effects.) The seepage percentage (the ratio between 
the seepage rate and percolation flux over the drift area) indicates the flow diversion capability 
of the capillary barrier at the drift surface. As expected, the seepage percentage is large for small 
capillary strength, small permeability, and large percolation flux. In these cases, seepage may 
approach 100 percent (i.e., there is no flow diversion at the drift wall), and the entire percolation 
flux seeps into the drift. In contrast, the seepage percentage is small for all cases with strong 
capillarity, large permeability, and small percolation flux. In many of these cases, there is no 
seepage at all; the entire percolation flux is diverted around the drift by capillary forces because 
the percolation flux is below the seepage threshold for the given parameters. 
October 2003 4-12 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003i, Figure 6-8. 
Figure 4-7. Mean Seepage Percentage as a Function of Capillary-Strength Parameter and Mean 
Permeability for a Percolation Flux of 1,10, 50, 200, 400, 600, 800, and 1,000 mm/yr 
4.5 PREDICTION OF SEEPAGE UNDER THERMAL CONDITIONS 
A thermal-hydrologic seepage model (BSC 2003b) was developed to evaluate the coupled 
thermal-hydrologic processes; and their impact on seepage; in the vicinity of waste emplacement 
drifts during the heating phase of the repository. This drift-scale process model is designed to 
analyze the combined effect of the two barriers that may prevent seepage into drifts at elevated 
temperatures: (1) the capillary barrier, which is independent of the thermal conditions, and 
(2) the vaporization barrier (see Section 1.5), which is effective while temperature is elevated 
above the boiling point. While incorporating the conceptual framework for ambient seepage, the 
thermal-hydrologic seepage model accounts for important flow and energy transport processes in 
response to the emplacement of heat-generating waste, including the movement of both gaseous 
and liquid phases, transport of latent and sensible heat, phase transition between liquid and 
vapor, and vapor pressure lowering. The fractured rock is treated as a dual-permeability domain, 
accounting for the fractures and the rock matrix as two separate, overlapping continua. The 
active fracture model (Liu et al. 1998, p. 2,636) is employed to account for the fact that 
October 2003 4-13 No. 3: Water Seeping into Drifts Revision 2 
unsaturated flow may be restricted to a limited number of (active) fractures and that flow within 
a fracture is likely to be channelized. A stochastic continuum model is implemented for fractures 
near the drift that considers the small-scale variability of permeability to account for flow 
channeling. The capillary-strength parameter close to the drift wall was derived from the 
properties provided by the calibration against seepage-rate data (see Section 4.3). 
Transient simulations in a two-dimensional cross section (extending from the ground surface to 
the water table; see Figure 4-8) were performed explicitly to calculate percolation to the drift 
during the heating phase of the repository, and to calculate directly transient seepage rates into 
the drift under elevated temperature conditions. Relevant parameters varied in the evaluation of 
thermal seepage are the thermal operating mode, the local percolation flux, and selected rock 
properties. Results of this model were used in the seepage abstraction to develop an appropriate 
methodology of adjusting the seepage model performance assessment results to account for 
thermally perturbed conditions. 
The thermal-hydrologic seepage model was validated by comparison with in situ heater tests 
conducted at Yucca Mountain (BSC 2003b, Section 7), with particular focus on the DST. The 
model validation included quantitative evaluation of continuously measured temperature data 
with a detailed analysis of subtle temperature signals indicative of thermal-hydrologic coupling, 
as well as qualitative evaluation of periodic measurements that monitored moisture redistribution 
processes using geophysical methods, air-injection data, and withdrawal of liquid water in 
packed-off boreholes. 
The thermal hydrologic seepage model predictions regarding the effectiveness of the 
vaporization barrier were also tested by comparison with an alternative conceptual model of 
water flow in the superheated rock environment (BSC 2003b, Section 6.3). In this alternative 
model, the thermally perturbed downward flux from the condensation zone toward the 
superheated rock zone is conceptualized to form episodic preferential-flow events (finger flow). 
The effectiveness of the vaporization barrier was then tested for the extreme conditions where 
downward flux in small fingers is fast and large in magnitude compared to average flow. 
A semi-analytical solution (Birkholzer 2003) was employed to simulate the complex flow 
processes of episodic finger flow in a superheated fracture. With this solution, the maximum 
penetration distance into the superheated rock was determined for specific episodic flow events 
and thermal conditions, and the amount of water arriving at the drift crown was calculated. It 
was shown that finger flow is not likely to penetrate through the superheated rock during the first 
several hundred years of heating, when rock temperature is high and boiling conditions exist in a 
sufficiently large region above the drifts. Only later, when the boiling zone is small and the 
impact of vaporization is limited, may channelized water arrive at the drift crown. This issue is 
further discussed in Appendix A. 
The thermal-hydrologic seepage model was applied to simulate the thermal-hydrologic coupled 
processes for a period of 4,000 years after waste emplacement. A series of selected simulation 
cases was conducted for the Tptpmn and Tptpll submodels, comprising different thermal loads, 
various percolation flux scenarios, different capillary-strength parameters, and different 
conceptual models for fracture-matrix interaction (see overview of simulation cases in BSC 
2003b, Section 6.2.1.6). The simulation results relevant for seepage abstraction are briefly 
discussed below. 
October 2003 4-14 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003b, Figure 6.2.1.2-1. 
NOTE: The emplacement drift is located in the middle nonlithophysal zone Tptpmn, which is bounded by the upper 
lithophysal (Tptpul) and lower lithophysal (Tptpll) zones. 
Figure 4-8. Example of Numerical Grid for the Thermal-Hydrologic Seepage Model 
The predicted thermal-hydrologic conditions are strongly driven by the thermal load placed into 
the drifts and by the local percolation flux. For the reference thermal mode, the heat generated 
from the waste canisters results in maximum rock temperatures at the drift wall between 120C 
and 140C, depending on the hydrogeologic unit and the amount of percolation considered. The 
period of above-boiling rock temperature is about 1,000 years for the base-case flux scenario, 
and rock temperature at the end of the simulation period is still as high as 65C. Elevated 
percolation leads to cooler temperatures and a shorter boiling period with stronger flux activity 
(liquid-vapor counter flow in the boiling-temperature zone). 
October 2003 4-15 No. 3: Water Seeping into Drifts Revision 2 
In general, seepage under thermal conditions (thermal seepage) is possible only when (a) water 
arrives at the drift wall (depending on the vaporization impact), and (b) the saturation at the drift 
wall exceeds a given threshold value, defined by the capillary barrier effect at the rock-drift 
interface. The modeling results consistently demonstrate that the thermal perturbation of the 
flow field, causing increased downward flux from the condensation zone toward the drifts, is 
strongest during the first few hundred years after closure, corresponding to the time period when 
rock temperature is highest and the vaporization barrier is most effective. Even for high 
percolation fluxes into the model domain and strong flow channeling as a result of fracture 
heterogeneity, water cannot penetrate far into the superheated rock during the time that rock 
temperature is above boiling. Thus, the potential for seepage is small. The majority of the 
mobilized water is diverted around the dryout zone and drains away from the drift, as shown in 
Figure 4-9a. At the time when temperature has returned to below-boiling conditions (see 
Figure 4-9b), fractures start to be rewetted at the drift wall. However, while the vaporization 
barrier has become less effective, the capillary barrier at the drift wall will continue to reduce (or 
prevent) water seepage into the drift. 
Transient seepage rates were explicitly calculated by the thermal-hydrologic seepage model to 
quantify the potential for seepage during the thermally perturbed time period. These transient 
seepage rates were compared with results from ambient (steady-state) simulations to evaluate the 
vaporization barrier. Example results illustrating the evolution of thermal seepage for 
one realization and a flow-focusing factor of 10 are given in Figure 4-10. No water arrives at the 
drift during the boiling period (i.e., even without heating of the repository). The capillary barrier 
at the drift wall is predicted to be fully effective during the first 600 years after waste 
emplacement. As rock temperature decreases during cool down and the first stepwise change in 
infiltration occurs at 600 years, the saturation values build up strongly. The change to 
monsoonal climate at 600 years (from 60 to 160 mm/yr) brings the saturation up to the threshold 
value for seepage at about 1,400 years after emplacement while still in the monsoon climate 
period. With the stepwise increase of infiltration at 2,000 years, the seepage percentage 
increases strongly, and water starts to seep at a second location along the drift wall in the model. 
At the end of the simulation period, the thermal seepage percentage is at about 17 percent, only 
slightly smaller than the long-term ambient value of 19.5 percent for a 250 mm/yr percolation 
flux. This provides additional confidence because as two simultaneously acting barriers prevent 
seepage. 
October 2003 4-16 No. 3: Water Seeping into Drifts Source: BSC 2003b, Figures 6.2.2.2-3a and 6.2.2.2-4a. 
NOTE: SL = liquid saturation. 
Figure 4-9. Fracture Saturation and Liquid Flux for Tptpmn Submodel with Heterogeneous Permeability 
Field at (a) 100 Years and (b) 1,000 Years 
4-17 No. 3: Water Seeping into Drifts 
Revision 2 
October 2003
Revision 2 
Source: BSC 2003b, Figure 6.2.2.2-7b. 
Figure 4-10. Seepage Percentage for Tptpmn Submodel at Reference Thermal Mode and Tenfold 
October 2003 4-18 
Percolation Flux 
The different simulation cases studied with the thermal-hydrologic seepage model show 
considerable variability with respect to the thermal-hydrologic conditions in the rock. Despite 
this variability, there were several important observations with respect to thermal seepage that 
are common to all cases (BSC 2003b, Sections 6.2.4 and 8.1): 
1. Thermal seepage was never observed in simulation runs where the respective ambient 
seepage was zero. 
2. Thermal seepage never occurred during the period of above-boiling temperatures in 
the rock close to the emplacement drifts. 
3. In simulation cases where ambient seepage was obtained, thermal seepage was 
initiated at several hundred to a few thousand years after rock temperature has returned 
below boiling. 
4. Thermal-seepage rates were always smaller than the respective ambient reference 
values. Thus, the ambient seepage values provide an asymptotic upper limit for 
thermal seepage. 
No. 3: Water Seeping into Drifts Revision 2 
4.6 EVALUATION OF COUPLED THERMAL, HYDROLOGIC, AND MECHANICAL 
EFFECTS ON SEEPAGE 
A drift-scale thermal-hydrologic-mechanical model (BSC 2003g) was developed to assess the 
magnitude and distribution of stress-induced changes in hydrologic properties and to analyze the 
impact of such changes on the percolation flux in the rock mass around a repository drift. 
Heating of the rock will cause thermal expansion of the rock, which in turn will change the stress 
field around emplacement drifts. Thermally induced changes in the stress field will act upon 
preexisting fractures, with the result of changing the hydrologic properties of the rock mass. 
The modeling framework for the thermal-hydrologic-chemical processes is similar to the 
thermal-hydrologic seepage model described in Section 4.5. However, while the 
thermal-hydrologic seepage model focuses on the thermal-hydrologic conditions to evaluate 
seepage rates for various seepage-relevant parameter cases, the thermal-hydrologic-mechanical 
simulations concentrate on the heat-induced stress changes and resulting impact on the flow field 
and formation properties. The model was validated by comparison with rock-mass displacement 
data (for thermal-mechanical processes) and air-permeability data (for thermal-hydrologicmechanical 
processes) measured during the heating phase of the DST (BSC 2003g, Section 7). 
Figure 4-11a shows the predicted changes in air permeability (a seepage-relevant parameter) as a 
result of both thermal expansion and saturation changes (dryout and condensation effects) during 
the DST. The overall favorable comparison with measured air permeabilities (see Figure 4-11b) 
provides confidence that the model predictions can be used as a basis for assessing the impact of 
property changes induced by coupled thermal, hydrologic, and mechanical processes on seepage. 
Predictive simulations of thermal-hydrologic-mechanical effects for the Tptpmn and Tptpll units 
(BSC 2003g, Sections 6.5 and 6.6) generally show a decrease in vertical permeability in the 
immediate drift vicinity as a result of temperature-induced stresses, while the horizontal 
permeabilities remain essentially unchanged from the initial postexcavation values. These 
anisotropic property changes suggest that flow is more easily diverted around the drift, 
decreasing the potential for seepage. 
The impact of these permeability changes on the flow field was investigated by comparison of 
the fully coupled thermal-hydrologic-mechanical simulations with thermal-hydrologic 
simulations (in which the stress-induced property changes were neglected). This analysis 
indicated that the flow field differences are small to moderate. The reduction in vertical 
permeability appeared to give rise to less water reaching the drift crown, suggesting that the 
anisotropic thermal-hydrologic-mechanical property changes would increase the likelihood of 
flow being diverted around the drift and, thus, decrease the potential for seepage. To confirm 
this point, ambient seepage calculations were conducted with the thermal-hydrologic-mechanical 
model using the initial postexcavation permeability field without thermal-hydrologic-mechanical 
changes and the permeability field at 10,000 years after emplacement, including thermalhydrologic-
mechanical changes. Results from these simulations indicate that 
thermal-hydrologic-mechanical effects lead to slight reduction in seepage (on the order of less 
than 10 percent), and that an ambient seepage model without consideration of anisotropic 
thermal-hydrologic-mechanical property changes conservatively predicts seepage rates with 
sufficient accuracy. 
October 2003 4-19 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003g, Figures 7.4.3-2b and 7.4.3-4c. 
NOTE: Changes in absolute air permeability in (a) shown at the Drift Scale Test after 12 Months of Heating, and 
expressed in terms of permeability correction factor (Fk =ratio of changed to initial permeability), 
TH = thermal-hydrologic; THM = thermal-hydrologic-mechanical; TM = thermal-mechanical. 
Figure 4-11. (a) Simulated Changes in Absolute Air Permeability Caused by the Combined Effect of 
Moisture Redistribution and Stress-Induced Changes in Intrinsic Permeability and (b) an 
Example of a Comparison to Measured Data 
October 2003 4-20 No. 3: Water Seeping into Drifts Revision 2 
4.7 EVALUATION OF DRIFT DEGRADATION EFFECTS ON SEEPAGE 
As discussed in Section 2.3.3, waste emplacement drifts may degrade with time as a result of 
thermal stress, seismic ground motion, and time-dependent degradation of rock strength. 
Damage to the drifts may be rather small, with local rockfall at the ceiling of otherwise intact 
drift openings, or, in extreme cases, may result in partial or complete drift collapse, with rubble 
rock material filling the enlarged drifts. These changes affect the potential for drift seepage. 
Various drift degradation models were developed for both nonlithophysal and lithophysal rock 
types (BSC 2001c; BSC 2003d). Degradation in the nonlithophysal units is primarily controlled 
by geologic structure. Drift damage due to rockfall in the nonlithophysal rock will be relatively 
minor even for low-probability seismic ground motions and strongly reduced joint cohesion and 
friction angle. An example of a resulting drift profile based on a discrete key-block analysis is 
shown in Figure 4-12. Flow and seepage calculations were performed for selected representative 
drift profiles (an example is shown in Figure 4-13) to examine the impact of changes in drift 
shape on seepage. The simulation results indicate that the relatively small rockfall volume and 
the correspondingly minor drift shape changes will lead to limited effects on seepage (less than 
10 percent) for all degradation cases expected to occur in the middle nonlithophysal zone. 
On the other hand, given the weaker rock in the lithophysal zones, strong seismic events and 
reduction in joint cohesion and tensile strength may lead to a complete collapse of the opening. 
Collapsed drifts are predicted to approximately double in size and fill with rock fragments. 
Complete drift collapse may lead to significantly different seepage behavior. However, even 
though the collapsed drifts are filled with rubble material, capillary barrier effects will still give 
rise to considerable flow diversion at the interface between the standing rock and the 
rubble-filled drift, because of the large scattered voids between the fragmented rock particles. 
Also, a gap can be expected between the ceiling and the collapsed, consolidated rubble material. 
Therefore, capillary-driven flow diversion remains an important mechanism reducing seepage in 
collapsed drifts. A worst-case drift profile was selected as representative of the drift collapse 
scenarios depicted in Drift Degradation Analysis (BSC 2003d), and systematic seepage 
simulations for the collapsed drift were conducted. Comparison with results from the 
nondegraded drift scenario (see Figure 4-7) indicate a moderate increase in seepage percentage 
caused by the larger size of the collapsed drift (reducing the effectiveness of flow diversion 
around the drift) and by the nonzero capillary strength in the drift (reducing the effectiveness of 
the capillary barrier). The simulation results demonstrate that most of the percolation flux is still 
diverted around the collapsed drift for most of the considered parameter range; actual seepage 
fluxes, however, are increased more because of the larger footprint of the collapsed drift. 
October 2003 4-21 No. 3: Water Seeping into Drifts Source: BSC 2001b, Figure 6.4.1. 
Figure 4-12. Calculated Drift Shape Changes as a Result of Rockfall in the Nonlithophysal Zone 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 4-22
Revision 2 
Source: BSC 2001b, Figure 6.4-8. 
Figure 4-13. Simulated Liquid Saturation Distribution in Heterogeneous Fracture Continuum in the 
Vicinity of a Waste Emplacement Drift with Changed Shape due to Rockfall 
4.8 EVALUATION OF COUPLED THERMAL, HYDROLOGIC, AND CHEMICAL 
EFFECTS ON SEEPAGE 
The thermal-hydrologic-chemical seepage model (BSC 2003h) is a drift-scale process model for 
predicting (1) the composition of gas and water flowing towards waste emplacement drifts and 
(2) the effects of mineral alteration on flow in rocks surrounding drifts, potentially forming 
precipitation caps of calcite, silica, and other minerals above emplacement drifts. 
The thermal-hydrologic-chemical seepage model is based on the thermal-hydrologic model 
introduced in Section 4.5. The model includes a wide range of major and minor aqueous species 
and minerals. Sensitivity studies have been performed to evaluate the impact of, for example, 
alternative geochemical systems, initial water compositions, and reaction rates. The model was 
validated by comparing predicted with measured gas compositions, water chemistry, and mineral 
composition obtained in the DST (BSC 2003h, Section 7). The model predicted calcite and 
amorphous silica precipitation in the zone above the heaters, consistent with coring data. 
Predicted calcite dissolution in the drainage and condensation zone was consistent with measured 
carbon isotope ratios in gas samples. The trends of the observed CO2 partial pressure, which is 
sensitive to degassing and boiling, are well captured by the model. The modeled fracture water 
pH matches the trend in the measured pH, which shows an initial decrease due to the increasing 
CO2 partial pressure followed by an increase as dryout occurs as a result of boiling. 
October 2003 4-23 No. 3: Water Seeping into Drifts Revision 2 
Model results were also compared with measured water compositions from a laboratory 
plug-flow dissolution experiment. In addition, a fracture-sealing laboratory experiment was 
simulated to compare precipitation data (see Section 3.3.2). In general, the model captured the 
trends in gas composition, water chemistry, and mineral precipitation reasonably well. 
The simulation results suggest that a thin region of significantly decreased fracture permeability 
will form several meters above the crown of waste emplacement drifts, created by mineral 
deposition at the boiling front (mainly silica, and to a lesser extent calcite). There is no 
indication that significant precipitation occurs immediately at the drift wall. This means that the 
local permeability and porosity in the boundary layer above the drift wall, important for the 
capillary barrier behavior, are not significantly affected by rock alterations induced by coupled 
thermal, hydrologic, and chemical effects. Figure 4-14 illustrates the spatial distributions of 
permeability changes and demonstrates its impact on the flow conditions at 2,400 years after 
waste emplacement. While the permeability values directly at the drift wall remain unchanged, 
there is a permeability decrease by a factor of 10 in an area 7 to 8 m above the drift. As a result, 
percolating water will be partially deflected sideways at this low-permeability zone, so that less 
water arrives at the drift crown (BSC 2003h, Figure 6.8-42). Since the amount of seepage is 
correlated to the local percolation flux, this kind of umbrella effect would give rise to less 
seepage compared to a simulation without permeability changes. Note that the permeabilities 
shown at 2,400 years remain essentially unchanged for the rest of the simulation period of 
100,000 years, because the silica solubility decreases with declining temperature. The 
thermal-hydrologic-chemical induced changes of hydrologic properties are essentially 
irreversible, potentially reducing the long-term percolation flux reaching the drift wall. 
Drift-Scale Coupled Processes (DST and THC Seepage) Models (BSC 2003h, Section 6.8.5.4) 
presents several sensitivity cases for mineral alteration results using different initial water 
compositions, which show significantly different permeability changes. Fracture-porosity 
changes in these simulations depend strongly on the initial porosity estimate for the fracture 
continuum, which is uncertain (BSC 2003h, Section 8.2). It is also expected that variability in 
the thermal-hydrologic conditions (e.g., stemming from thermal-load differences and 
percolation-flux variability) and model dimensionality would bring out other differences in the 
precipitation patterns and the effectiveness of the diversion effect described above. The 
substantial variability and uncertainty in predicted porosity and permeability changes do not 
justify the explicit inclusion of the diversion effect resulting from mineral precipitation into the 
seepage abstraction. Note that the abstraction does include a wide range of uncertainties in 
percolation flux, flow focusing, permeability, and capillary strength. 
October 2003 4-24 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003h, Figure 6.8-40. 
NOTE: Contour plot of modeled (a) permeability changes and (b) liquid saturation and temperature contours (C) at 
2,400 years. 
Figure 4-14. Example of Effects of Mineral Alteration as Predicted by the Thermal-Hydrologic-Chemical 
as follows: 
2 
October 2003 4-25 
Seepage Model 
The findings from the thermal-hydrologic-chemical seepage model regarding the chemical 
composition of gas and water flowing towards the waste emplacement drift can be summarized 
1. The models used to predict the coupled thermal, hydrologic, and chemical processes 
that could affect seepage are validated against an array of data measured during the 
2 partial pressure, pH, DST. Data used include temperature, moisture change, CO 
chloride concentration, calcite and silica dissolution and mineral precipitation. 
2. Water in the condensation zone above the drift is relatively dilute (less than 
1,000 ppm) and in the pH range from 7 to 9. Elevated concentrations of aqueous 
species (between 1,000 and 10,000 ppm) are predicted only for a short period at onset 
of rewetting in regions exhibiting very small liquid saturation; no seepage is expected 
during this period (see Section 4.5). 
3. The general trends in the temporal evolution of gas phase CO2 and aqueous species 
concentrations are relatively independent of the scenario considered. The relative 
spread in predicted major cation and anion concentrations and gas phase CO 
concentration is approximately one order of magnitude. This spread arises mainly 
No. 3: Water Seeping into Drifts Revision 2 
from the natural variability of the initial pore water composition. The chemistry of 
potential seepage water is at all times similar to that of the initial, dilute pore waters. 
4. It is unlikely that CaCl2 waters will evolve. The presence of CaCl2 brines with their 
high boiling point would have increased the potential for seepage and corrosion. 
5. Heterogeneity in fracture permeability has an insignificant effect on predicted water 
composition. 
4.9 SEEPAGE ABSTRACTION 
An abstraction model was developed for evaluating the future amount and distribution of 
seepage into the waste emplacement drifts at Yucca Mountain (BSC 2003a). The purpose of the 
seepage abstraction is to provide the necessary methodology, tools, parameter distributions, 
lookup tables, and simplifications needed for TSPA to perform a probabilistic analysis of 
seepage rate (amount of seepage per time) and the seepage fraction (the fraction of waste 
packages affected by seepage) as functions of time and location in the repository. 
The information generated by the seepage process models is compiled into a form that can be 
used in probabilistic TSPA calculations. The following three process models, which are 
consistent in their conceptual treatment of flow diversion and capillary barrier behavior, provide 
the basis for seepage abstraction: 
1. The seepage calibration model provides the conceptual basis for seepage modeling and 
derives seepage-relevant parameters through calibration of the model against 
seepage-rate data from liquid-release tests (BSC 2003e; see also Section 4.3). 
2. The seepage model for performance assessment predicts drift seepage rates for 
long-term ambient conditions at Yucca Mountain, for a wide range of seepage-relevant 
parameters, and for potentially important perturbing effects. The latter include the 
effect of rock bolts on flow paths and the impact of drift shape changes caused by 
degradation (BSC 2003i; see also Section 4.4). Drift degradation is expected as a 
result of thermal stresses, seismic events, and time-dependent decrease in rock 
strength. 
3. The thermal-hydrologic seepage model predicts drift seepage during the period when 
water-flow processes in the drift vicinity are perturbed by heating of the rock (BSC 
2003b; see also Section 4.5). 
Additional input from scientific analyses or from process models is required to define probability 
distributions that appropriately cover uncertainty and spatial variability of seepage-affecting 
parameters. In addition to the capillary strength in the fractures close to the drift calibrated with 
the seepage calibration model, the most important parameters defining the amount of seepage are 
the local percolation flux and the formations permeability close to the drifts (BSC 2003e). 
Information on these parameters is derived mainly from the following sources: 
1. Site-scale and intermediate-scale unsaturated zone flow simulationsThe unsaturated 
zone flow and transport model provides three-dimensional site-scale flow fields to 
October 2003 4-26 No. 3: Water Seeping into Drifts Revision 2 
derive the local percolation flux (BSC 2003c). In addition, flow-focusing factors 
account for intermediate-scale heterogeneity that is not represented in the 
layer-averaged unsaturated zone flow and transport model. These are estimated from 
an intermediate-scale flow-focusing model (BSC 2001b, Section 6.4.2). 
2. In situ testing at Yucca MountainAir-injection tests performed at different scales and 
locations provide estimates of local fracture permeability (BSC 2001a). 
Finally, results from the coupled thermal-hydrologic-mechanical and thermal-hydrologicchemical 
models are utilized to assess whether seepage-relevant parameters may be affected by 
mechanical and (or) chemical processes. These processes occur in response to the heat generated 
in the repository (BSC 2003h; BSC 2003g). The relation and the information flow between the 
suite of primary process models important for seepage and the seepage abstraction are 
schematically illustrated in Figure 4-15. 
Source: BSC 2003a, Figure 1-1. 
NOTE: TSPA = total system performance assessment; PA = performance assessment; TH = thermal-hydrologic; 
THC = thermal-hydrologic-chemical; THM = thermal-hydrologic-mechanical; UZ = unsaturated zone 
Figure 4-15. Relation and Information Flow between Primary Process Models and Seepage Abstraction 
The information resulting from the abstraction process takes the form of probability distributions 
for seepage events, taking into account the spatial and temporal variability and inherent 
October 2003 4-27 No. 3: Water Seeping into Drifts Revision 2 
uncertainty of seepage-relevant properties and processes. Seepage is variable in space because 
of variability in percolation flux and heterogeneity in key hydrologic properties, specifically 
fracture permeability and capillary strength. In addition, seepage may be affected by heat output 
from the decaying radioactive waste, from changes in hydrologic properties as a result of 
mechanical and chemical effects, from changes in the drift shape due to drift degradation, and 
from the presence of rock bolts used for ground support. Several of these factors are also 
time-dependent, such as percolation flux and thermal effects. The methodology of incorporating 
each of these factors in seepage abstraction is directly based on the process-model results 
described in Sections 4.3 through 4.8. The general procedure has two main steps, as follows: 
1. The ambient seepage results (see Section 4.4) provide the basis for the quantitative 
evaluation of seepage as a function of key hydrologic properties. The key hydrologic 
parameters defining ambient seepage (capillary-strength, permeability, and local 
percolation flux) are described by appropriate probability distributions. Depending on 
the considered geologic unit, the selected nominal or disruptive scenarios, and the 
assumed rock strength reduction case, seepage rates will be sampled either from the 
lookup table for nondegraded drifts or from the lookup table for collapsed drifts (for 
details, see BSC 2003a, Section 6.5.1.5). 
2. The parameters and (or) ambient seepage rates are then adjusted to account for 
potentially important factors, such as thermal, mechanical, and chemical effects on 
properties and seepage, and other factors (see Figure 2-2). 
In Step 1, it is recognized that the amount of seepage is sensitive to key hydrologic properties 
that are both spatially variable and uncertain. For ambient seepage, these key hydrologic 
properties are the capillary-strength parameter, the permeability, and the local percolation flux. 
One of the main tasks of the seepage abstraction model is to define appropriate probability 
distributions. The probabilities assigned to the relevant parameters distinguish explicitly 
between spatial variability and uncertainty, using separate distributions. For example, spatial 
variability of the capillary-strength parameter 1/  is described by a uniform distribution, whereas 
the uncertainty is represented by a triangular distribution, with a mean of zero and a range value 
defining the uncertainty of the parameter. Potential sources of uncertainty included in this 
triangular distribution are (1) measurement uncertainty, (2) spatial variability uncertainty, 
(3) conceptual model uncertainty, and (4) estimation uncertainty. A schematic illustration of the 
random sampling procedure is given in Figure 4-16. During a TSPA calculation, the triangular 
distribution is randomly sampled (labeled R), providing an adjusted mean value to account for 
uncertainty. Next, random sampling (labeled r) from the spatial variability distributions are 
added to the adjusted mean at each location in the repository area. Details of the procedure and 
the development of the underlying probability distributions can be found in Abstraction of Drift 
Seepage (BSC 2003a, Section 6.6). 
October 2003 4-28 No. 3: Water Seeping into Drifts Revision 2 
Source: BSC 2003a, Figure 6.5-2. 
Figure 4-16. Schematic Illustration of Random Sampling Procedure for Capillary-Strength Parameter 
1/, Using Probability Distributions for Uncertainty (Triangular) and Spatial Variability 
(Uniform) 
The procedure for sampling of local percolation fluxes is slightly different from sampling of the 
other parameters. The flux variability is provided for three different climate stages (present-day 
climate, monsoonal climate, and glacial transition climate) by model results from the unsaturated 
zone flow and transport model (BSC 2003c, Section 6.6). For each time step, the local fluxes at 
several thousand locations in the repository area are interpolated from the simulated flux 
distributions. Uncertainty inherent in these flux distributions is expressed by using several 
alternative scenarios of spatial flux distributions, each of them associated with a certain 
probability of occurrence. These scenarios are the mean, the upper-bound, and the lower-bound 
scenarios. The local flux values need to be multiplied with flow-focusing factors that lead to 
increased fluxes in some areas, while reducing them in others. These factors, also spatially 
variable and thus randomly sampled, account for intermediate-scale heterogeneity not 
represented in the flux distributions calculated with the site-scale model. Multiplication of the 
local fluxes from the site-scale model with the flow-focusing factors gives the local percolation 
flux to be used in the TSPA calculation. Once a parameter set is randomly sampled, the 
October 2003 4-29 No. 3: Water Seeping into Drifts Revision 2 
corresponding seepage rate is extracted from the lookup tables generated for intact or collapsed 
waste emplacement drifts. 
In Step 2, the impact of additional factors affecting seepage is evaluated. These factors include 
the ground support with rock bolts, the expected transient changes in hydrologic properties as a 
result of thermal, mechanical, and chemical effects, and the thermal perturbation of the flow field 
as a result of boiling in the rock. The method proposed in the seepage abstraction is to account 
for these factors in a simplified form using the ambient seepage results as a basis and adjusting 
them as suggested by the relative importance of each factor. To incorporate uncertainty, the 
simplifications made in this process are usually conservative yet strive to be as realistic as 
possible. 
The expected time-dependent alterations of seepage-relevant properties, stemming from 
thermal-hydrologic-mechanical and thermal-hydrologic-chemical effects in response to the 
elevated temperatures in the repository, can be neglected in the seepage simulations conducted in 
the TSPA. The thermal-hydrologic-mechanical simulations discussed in Section 4.6 suggest that 
temperature-induced stress changes give rise to changes in the vertical fracture permeability in 
the vicinity of waste emplacement drifts. However, these permeability changes do not result in 
significant changes in the flow fields. In particular, the seepage rates calculated for a 
permeability field including thermal-hydrologic-mechanical permeability changes were similar 
to, but slightly smaller than those calculated for a permeability field representative of the initial 
postexcavation conditions. The seepage model performance assessment simulation results 
provide reasonably accurate (slightly conservative) estimates of the expected seepage rates at 
long-term conditions with coupled thermal-hydrologic-mechanical property changes. Therefore, 
the impact of thermal-hydrologic-mechanical property changes is neglected in the seepage 
abstraction (i.e., the seepage abstraction model uses the ambient seepage rates without 
accounting for the transient thermal-hydrologic-mechanical changes in seepage-relevant 
properties). 
The thermal-hydrologic-chemical simulations discussed in Section 4.8 suggest formation of a 
precipitation cap about 7 to 8 m above the drift crown. The zone of decreased fracture 
permeability acts as an umbrella that partially deflects percolating water sideways, limits the 
amount of flux at the drift crown, and reduces seepage. Seepage abstraction does not incorporate 
this effect, considering the considerable uncertainty and potential variability in these simulated 
results. It should be recognized, however, that the simulated trend of a precipitation cap forming 
at some distance above the drift crown appears to be reliable in a qualitative sense. This adds 
confidence in the seepage abstraction results. The amount of seepage is likely to be smaller than 
the abstracted seepage because of thermal-hydrologic-chemical effects. 
Two alternative abstraction models are proposed for seepage during the period of strong thermal 
perturbation at Yucca Mountain. The first (simple) model does not take credit for the 
vaporization barrier that prevents seepage at above-boiling rock temperatures. In the second 
(more realistic) abstraction model, thermal seepage is set to zero for the period of above-boiling 
rock temperatures in the drift vicinity. 
In summary, the abstraction is based on seepage predictions from detailed process models that 
have been validated in previous analyses to ensure appropriate representation of the physical 
October 2003 4-30 No. 3: Water Seeping into Drifts Revision 2 
processes and relevant parameters. These results are either propagated to the TSPA without 
changes (i.e., seepage lookup table) or have been simplified within the abstraction process 
(i.e., thermal seepage, thermal-hydrologic-chemical and thermal-hydrologic-mechanical 
alterations, and drift degradation). 
From the seepage look-up tables and the respective simplifications for additional factors, 
probabilistic seepage rates and uncertainties can be calculated as a function of seepage-relevant 
parameters. In the abstraction, appropriate spatial variability and uncertainty distributions have 
been developed for these parameters, based on either process model results (i.e., capillary 
strength or percolation flux) or in situ measurements (permeability). 
4.10 SEEPAGE IN TOTAL SYSTEM PERFORMANCE ASSESSMENT 
The purpose of the seepage component in TSPA is to calculate the seepage rate (amount of 
seepage per time) and the seepage fraction (the fraction of waste packages affected by seepage) 
as functions of time and location in the repository. The calculation is performed using a 
probabilistic approach that accounts for the spatial and temporal variability and inherent 
uncertainty of seepage-relevant properties and processes. The resulting information takes the 
form of probability distributions for seepage events. These distributions are used for subsequent 
TSPA calculations that may handle, for example, waste form degradation or radionuclide 
transport. 
The TSPA procedure of calculating seepage is schematically illustrated in Figure 4-17. The 
TSPA calculation runs over several time steps to account for the temporal variability of relevant 
processes. Within each time step, random sampling of uncertainty distributions is conducted for 
a sufficiently large number of realizations (labeled R). Within each realization, the seepage rate 
is evaluated at a sufficiently large number of spatial locations (labeled r) in the repository area. 
Over all locations, the resulting number of locations with seepage, relative to the total number of 
locations, defines the fraction of waste packages encountering seepage for the realization and the 
time considered. 
For illustration of the expected seepage behavior in the repository, a probabilistic seepage 
calculation was conducted following the abstraction method described in Abstraction of Drift 
Seepage (BSC 2003a, Section 6.8). Summary results indicate the importance of the natural 
barrier formed by the unsaturated rock at and above the repository horizon. For drifts located in 
the main geological unit of the repository (Tptpll) and assuming the expected (mean) infiltration 
climate scenario, the mean seepage percentage is about 8 percent during the glacial transition 
climate, when most seepage is expected. This means that, on average, more than about 
92 percent of the percolating water is diverted around the emplacement drifts. The calculation 
procedure was also applied to various sensitivity cases. Note that the calculation results from 
Abstraction of Drift Seepage (BSC 2003a, Section 6.8) are not directly utilized in the 
performance assessment; the seepage component in the TSPA simulations will conduct a similar 
seepage calculation embedded in the TSPA Monte Carlo simulation procedure. 
October 2003 4-31 No. 3: Water Seeping into Drifts Source: BSC 2003a, Figure 6.5-1. 
Figure 4-17. Probabilistic Total System Performance Assessment Procedure for Calculating Seepage at 
Selected Time Steps 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 4-32
Revision 2 
Finally, it is useful to qualitatively compare the observations made in the ECRB Cross-Drift and 
Alcove 7, with the representation of seepage in the abstraction model for TSPA (BSC 2003a, 
Section 6.8). The abstraction model for drift seepage was prepared for use in TSPA, and tested 
by substituting recommended parameter distribution functions for the independent variables: 
focused percolation flux, permeability, and capillary strength. The results show that 
approximately 8 percent of waste packages (averaged over the entire repository layout area) are 
predicted to experience seepage, for the mean infiltration case and present-day climate 
conditions (BSC 2003a, Table 6.8-1). In addition, the seepage abstraction results in an average 
of 1.7 L/yr per waste package, or about 20 L/yr per waste package with a seep. Percolation flux 
is greater in some parts of the site area (BSC 2003c, Section 6.6, Figure 6.6-6) and is above 
average in the host rock under Yucca Crest that is traversed by the ECRB Cross-Drift. 
Accordingly, the seepage abstraction model predicts at least an 8 percent likelihood that seepage 
will occur (at rates of about 20 L/yr) in any 5.1-m long drift interval, through several hundred 
meters of the Cross-Drift. Similar conclusions were reached in the pretest predictions for the 
ECRB Cross-Drift passive monitoring test (BSC 2001d, Section 6.1). 
These results are not inconsistent with the possibility that the source of liquid water in the ECRB 
is seepage. However, as noted in Section 3.2, it is probable that these observations are the result 
of condensation from the humid air in the drift. This humid air was primarily derived from 
moisture in the form of water vapor coming into the drift following the cessation of ventilation. 
This moisture flux is not explicitly quantified in the seepage model (which, as noted in 
Section 4.4, assumes 100 percent relative humidity at the drift wall) and is generally a small 
fraction of the seepage amount for relative humidities approaching 100 percent (BSC 2003e, 
Figure 33). 
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4-34 No. 3: Water Seeping into Drifts 
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5. SUMMARY 
Seepage into waste emplacement drifts affects the performance of the high-level radioactive 
waste repository at Yucca Mountain, Nevada. The number of waste packages contacted by 
water, the dissolution and mobilization of radionuclides, and the release of radionuclides depend 
on the rate, chemical composition, and the spatial and temporal distribution of water seeping into 
the emplacement drifts. Seepage will also affect the conditions below the drift, specifically the 
saturation reduction in the matrix and the fractures (referred to as the drift shadow zone) which, 
in turn, can affect diffusive releases from the drift to the natural environment and the potential 
for (or absence of) fast advective transport of radionuclides through the fracture network. 
Theoretical analyses, numerical modeling studies, field experiments, and natural analogs suggest 
that seepage into underground openings excavated in unsaturated formations is smaller than the 
percolation flux at the given location. This is mainly a result of capillary pressures holding water 
in the formation, diverting it around the cavity, and preventing it from entering the underground 
opening. 
The effectiveness of this capillary barrier will depend on the percolation flux, the hydrogeologic 
properties of the formation, the geometry of the drift opening, the properties of the drift wall, and 
the in-drift conditions determining the evaporation potential. In addition, a vaporization barrier 
will develop when the emplacement drifts are ventilated or heated to above-boiling. Seepage 
may be further reduced as a result of thermal and mechanical property changes in the vicinity of 
the drifts and the development of a precipitation cap by a coupled thermal-hydrologic-chemical 
process. 
A large number of seepage experiments under ambient temperature conditions were performed in 
several niches and along the ECRB Cross-Drift. Qualitative and quantitative data were collected 
to further understand the seepage process and to estimate seepage-relevant formation parameters. 
A suite of conceptually consistent seepage process models was developed, effectively 
propagating seepage-related data and their uncertainties from the field to the probabilistic 
seepage prediction model as part of TSPA calculations. The modeling approach was designed to 
address many technical issues (including the impacts of discrete fractures, drift surface 
roughness, film flow, and evaporation) in a reasonable manner. The models were validated 
against field and laboratory data and tested against alternative conceptualizations. 
The effects of increased repository temperatures on rock properties were investigated 
experimentally (see Section 3.3) and in associated modeling studies (see Sections 4.6 and 4.8). 
The resulting impact on seepage under thermal conditions was examined (see Section 4.5) and 
included in the seepage abstraction (see Section 4.9). 
The effectiveness of the capillary barrier and the presence of a seepage threshold can be directly 
observed from liquid-release tests conducted at different rates, which show that seepage ceases at 
a nonzero injection rate. Moreover, calcite depositions in lithophysal cavities at Yucca Mountain 
(assuming that they originate from seepage) indicate that water enters only a small fraction of 
these underground openings at an average rate that is significantly smaller than the percolation 
flux. 
October 2003 5-1 No. 3: Water Seeping into Drifts Revision 2 
The data collected in the passive ECRB Cross-Drift hydrologic test, and Alcove 7, which have 
been isolated from ventilation, have been interpreted qualitatively as discussed in the previous 
sections. These data include small variations in temperature or relative humidity that reflect 
natural variation in host rock conditions, and stronger effects such as the drying and adjacent 
condensation observed in response to heat sources in the ECRB. Waters collected so far have 
chemical characteristics of condensates, without the chemical signature of tagged construction 
water. While these data clearly show that part of the observed moisture originated from 
condensation, they do not rule out or confirm the existence of formation of water seeping into the 
drifts. As discussed in Section 4.10, the existence of seepage in the ECRB Cross-Drift is not 
inconsistent with the probabilistic abstraction of drift seepage developed for use in TSPA, 
although the contribution from vapor-phase migration and subsequent condensation has not been 
quantified. 
The following general conclusions are drawn: 
 Hydrologic process simulation with a calibrated and validated model is the preferred 
means for predicting seepage, because (1) the key process relevant to seepage (i.e., flow 
of water under unsaturated conditions) is directly modeled based on established physical 
laws, (2) only a few presumptions need to be made because the model directly simulates 
the seepage process of interest, (3) the approach has the potential to simulate conditions 
that cannot be observed in the field, and (4) numerical models are flexible enough to 
accommodate the realistic initial and boundary conditions as they occur during seepage 
experiments. 
 The testing and modeling approach is adequate for providing the conceptual basis and 
parameters for the TSPA seepage model. The approach consists of analyzing seepage 
by means of a numerical process model that is calibrated against seepage-rate data from 
liquid-release tests conducted within the repository host units. Seepage experiments 
provide calibration data that reflect the process of interest. The measured data 
automatically reflect the factors and features pertinent to seepage. The effective 
parameters are capable of reproducing observed seepage data and are thus likely to yield 
reasonable seepage predictions. Moreover, the experiments test the capillary-barrier 
effect on the scale of interest. The water encountering the niche or drift is partly 
diverted around the opening, activating the relevant portion of the fracture network on 
the appropriate scale. 
 The estimation of seepage-relevant, model-related, effective parameters on the drift 
scale is an appropriate methodology provided that the structure of the prediction model 
is consistent with the model used for calibration. 
 Seepage properties are spatially variable. The variability has been examined by 
performing liquid-release tests at various sites along the ESF and the ECRB Cross-Drift. 
Available permeability data haven been analyzed to develop appropriate distributions 
reflecting spatial variability as well as uncertainty. 
 It is recognized that the amount of seepage is sensitive to key hydrologic properties that 
are both spatially variable and uncertain. For ambient seepage, these key hydrologic 
October 2003 5-2 No. 3: Water Seeping into Drifts Revision 2 
properties are the capillary-strength parameter, the permeability, and the local 
percolation flux. Appropriate probability distributions have been defined in the seepage 
abstraction (see Section 4.9), representing the spatial variability and uncertainty inherent 
in these parameters in a realistic manner. Relevant sources of uncertainty have been 
identified, described, and accounted for in this process, including measurement 
uncertainty, conceptual model uncertainty, estimation uncertainty, and spatial variability 
uncertainty. 
 Property changes as a result of coupled thermal-hydrologic-mechanical and 
thermal-hydrologic-chemical effects will have minor and generally beneficial impacts on 
seepage; they were conservatively neglected in the seepage abstraction. Larger 
perturbations (such as a drift collapse as a result of seismic events or cohesion loss of the 
fractured rock) can lead to more substantial changes in seepage; they were analyzed and 
appropriately captured in the seepage abstraction. 
In summary, the extensive testing and modeling program undertaken to understand and 
characterize seepage from fractured rock provides an adequate basis for predicting seepage into 
waste emplacement drifts under ambient and thermal conditions at Yucca Mountain. 
The report summarizes responses to certain seepage-related KTI agreements between the DOE 
and the NRC. The KTI agreements addressed in this report are listed in Table 1-1. 
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5-4 No. 3: Water Seeping into Drifts 
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Marshall, B.D.; Neymark, L.A.; and Peterman, Z.E. 2003. Estimation of Past Seepage Volumes 
from Calcite Distribution in the Topopah Spring Tuff, Yucca Mountain, Nevada. Journal of 
Contaminant Hydrology, 62-63, 237-247. [New York, New York]: Elsevier. TIC: 254210. 
Or, D. and Ghezzehei, T.A. 2000. Dripping into Subterranean Cavities from Unsaturated 
Fractures under Evaporative Conditions. Water Resources Research, 36, (2), 381-393. 
Washington, D.C.: American Geophysical Union. TIC: 246982. 
Paces, J.B.; Neymark, L.A.; Marshall, B.D.; Whelan, J.F.; and Peterman, Z.E. 2001. Ages and 
Origins of Calcite and Opal in the Exploratory Studies Facility Tunnel, Yucca Mountain, 
Nevada. Water-Resources Investigations Report 01-4049. Denver, Colorado: U.S. Geological 
Survey. TIC: 251284. 
Philip, J.R.; Knight, J.H.; and Waechter, R.T. 1989. Unsaturated Seepage and Subterranean 
Holes: Conspectus, and Exclusion Problem for Circular Cylindrical Cavities. Water Resources 
Research, 25, (1), 16-28. Washington, D.C.: American Geophysical Union. TIC: 239117. 
Pruess, K.; Wang, J.S.Y.; and Tsang, Y.W. 1990. On Thermohydrologic Conditions Near 
High-Level Nuclear Wastes Emplaced in Partially Saturated Fractured Tuff, 2. Effective 
Continuum Approximation. Water Resources Research, 26, (6), 1249-1261. [Washington, 
D.C.]: American Geophysical Union. TIC: 224854. 
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Richards, L.A. 1931. Capillary Conduction of Liquids Through Porous Mediums. Physics, 1, 
318-333. [New York, New York: American Physical Society]. TIC: 225383. 
Trautz, R.C. and Wang, J.S.Y. 2002. Seepage into an Underground Opening Constructed in 
Unsaturated Fractured Rock Under Evaporative Conditions. Water Resources Research, 38, 
(10), 6-1 through 6-14. [Washington, D.C.]: American Geophysical Union. TIC: 253348. 
USGS (U.S. Geological Survey) 2001. Simulation of Net Infiltration for Modern and Potential 
Future Climates. ANL-NBS-HS-000032 REV 00 ICN 02. Denver, Colorado: U.S. Geological 
Survey. ACC: MOL.20011119.0334. 
van Genuchten, M.T. 1980. A Closed-Form Equation for Predicting the Hydraulic 
Conductivity of Unsaturated Soils. Soil Science Society of America Journal, 44, (5), 892-898. 
Madison, Wisconsin: Soil Science Society of America. TIC: 217327. 
Wang, J.S.Y. and Elsworth, D. 1999. Permeability Changes Induced by Excavation in 
Fractured Tuff. Rock Mechanics for Industry, Proceedings of the 37th U.S. Rock Mechanics 
Symposium, Vail, Colorado, USA, 6-9 June 1999. Amadei, B.; Kranz, R.L.; Scott, G.A.; and 
Smeallie, P.H., eds. 2, 751-757. Brookfield, Vermont: A.A. Balkema. TIC: 245246. 
Wang, J.S.Y.; Trautz, R.C.; Cook, P.J.; Finsterle, S.; James, A.L.; and Birkholzer, J. 1999. 
Field Tests and Model Analyses of Seepage into Drift. Journal of Contaminant Hydrology, 
38, (1-3), 323-347. New York, New York: Elsevier. TIC: 244160. 
Whelan, J.F.; Paces, J.B.; and Peterman, Z.E. 2002. Physical and Stable-Isotope Evidence for 
Formation of Secondary Calcite and Silica in the Unsaturated Zone, Yucca Mountain, Nevada. 
Applied Geochemistry, 17, ([6]), 735-750. [New York, New York]: Elsevier. TIC: 253462. 
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APPENDIX A 
EFFECTS OF HETEROGENEITY ON THERMAL SEEPAGE 
(RESPONSE TO TEF 2.08 AND GEN 1.01 (COMMENT 15)) 
. 
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Note Regarding the Status of Supporting Technical Information 
This document was prepared using the most current information available at the time of its development. This 
Technical Basis Document and its appendices providing Key Technical Issue Agreement responses that were 
prepared using preliminary or draft information reflect the status of the Yucca Mountain Projects scientific 
and design bases at the time of submittal. In some cases this involved the use of draft Analysis and Model 
Reports (AMRs) and other draft references whose contents may change with time. Information that evolves 
through subsequent revisions of the AMRs and other references will be reflected in the License Application 
(LA) as the approved analyses of record at the time of LA submittal. Consequently, the Project will not 
routinely update either this Technical Basis Document or its Key Technical Issue Agreement appendices to 
reflect changes in the supporting references prior to submittal of the LA. 
No. 3: Water Seeping into Drifts October 2003
Revision 2 
APPENDIX A 
EFFECTS OF HETEROGENEITY ON THERMAL SEEPAGE 
(RESPONSE TO TEF 2.08 AND GEN 1.01 (COMMENT 15)) 
This appendix provides a response for Key Technical Issue (KTI) agreement Thermal Effects on 
Flow (TEF) 2.08 and General Agreement (GEN) 1.01, Comment 15. These agreements relate to 
the effects of spatial heterogeneity on thermal seepage. 
A.1 KEY TECHNICAL ISSUE AGREEMENTS 
A.1.1 TEF 2.08 and GEN 1.01 (Comment 15) 
Agreement TEF 2.08 was reached during the U.S. Nuclear Regulatory Commission (NRC)/U.S. 
Department of Energy (DOE) Technical Exchange and Management Meeting on Thermal 
Effects on Flow held January 8 to 9, 2001, in Pleasanton, California (Reamer and Williams 
2001). The agreement resulted from the technical discussion of Subissue No. 2: Thermal effects 
on temperature, humidity, saturation, and flux. Work in progress to determine the effects of 
heterogeneity on the potential for thermally driven seepage was discussed, including (1) using 
further refinement of the grid for the heterogeneous field, (2) using three-dimensional effects 
since preliminary assessment indicates that the two-dimensional models are conservative, and 
(3) evaluating the effect of high-permeability features (e.g., fault) crossing the drift. 
Agreement GEN 1.01 was reached during the NRC/DOE Technical Exchange and Management 
Meeting on Range of Thermal Operating Temperatures, held September 18 to 19, 2001 (Reamer 
and Gil 2001). At that meeting, NRC provided additional comments, resulting in GEN 1.01 
(Comment 15), which relates to the effects of spatial heterogeneity on thermal seepage 
(TEF 2.08). The specific page number referral cited below as part of GEN Comment 15 is from 
FY 01 Supplemental Science and Performance Analyses, Volume 1: Scientific Bases and 
Analyses (BSC 2001). 
The wording of these agreements is as follows: 
TEF 2.08 
Provide the Mountain-Scale Coupled Processes AMR, or another appropriate 
AMR, documenting the results of the outlined items on page 20 of the OI 7 
presentation (considering the NRC suggestion to compare model results to the 
O.M. Phillips analytical solution documented in Water Resources Research, 
1996). The DOE will provide the updated Mountain-Scale Coupled Processes 
Model AMR (MDL-NBS-HS-000007) Rev 01 to the NRC in FY 02, documenting 
the results of the outlined items on page 20 of DOEs Open Item 7 presentation at 
this meeting. The DOE will consider the NRC suggestion of comparing the 
numerical model results to the O.M. Phillips analytical solution documented in 
WRR (1996). 
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Note that page 20 of DOEs Open Item (OI) 7 presentation includes the following: 
Refined Grid Case: Mountain Scale Model (Continued) 
Spatially Heterogeneous Fracture Permeability 
 Work is in progress to determine the effects of heterogeneity on the 
potential for thermally driven seepage: 
- Using further refinement of grid for heterogeneous field 
- Using three-dimensional effects since preliminary assessment 
indicates that the two-dimensional models are conservative 
- Evaluating the effect of high-permeability features (e.g., fault) 
crossing the drift. 
GEN 1.01 (Comment 15) 
The analytical approach in this section moves in the direction of resolving part of 
agreement TEF 2.08 that states, The DOE will consider the NRC suggestion of 
comparing the numerical model results to the O.M. Phillips analytical solution. 
However, this approach should factor into consideration changes in water 
properties such as increased boiling temperatures of concentrated solutions. Also, 
taking u in this approach to be condensate drainage in the reflux zone instead of 
net infiltration would give a transient period of increased seepage for a few 
hundred years after closure. 
Basis - Increased boiling temperatures of concentrated solutions will increase the 
distance a liquid rivulet can flow into the above-boiling region. This would have 
the effect of increasing seepage into drifts during the thermal period of the HTOM 
as modeled using the approach developed in the section starting on page 4-58. 
Evidence from the DST indicates some condensate drainage could have high 
concentrations of dissolved solids. 
DOE Initial Response to GEN 1.01 (Comment 15): 
The analytical approach was used as an alternative conceptual model for thermal 
seepage. DOE will compare the analytical model with numerical model results, 
consistent with existing agreement TEF 2.08. Should the site be approved, the 
DOE will, as appropriate, re-evaluate the impact of a lower-temperature operating 
mode upon existing KTIs, which were established on the basis of the 
higher-temperature operating mode. The changes in water properties, such as 
increased boiling temperatures of concentrated solutions, may only be significant 
for the high-temperature operating mode. Preliminary data concerning boiling 
temperature in the DST indicates that this effect is not significant. 
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Note that data from DST geochemical sampling have not shown high 
concentrations of dissolved solids. 
A very limited number of samples from a single borehole did show high Cl 
content (but low silica content). These samples were taken early in the heating 
cycle of the DST and are believed to be contaminated from the drilling of the 
sampling boreholes. This will be documented in the AMR Unsaturated Zone 
Thermal Testing Analysis, expected to be issued in FY 2003. 
A.1.2 Related Key Technical Issue Agreements 
None. 
A.2 RELEVANCE TO REPOSITORY PERFORMANCE 
As discussed in the previous section, TEF 2.08 relates to DOE providing documentation on the 
results of work to determine the effects of heterogeneity on the potential for thermally driven 
seepage, which was discussed during the January 2001 NRC/DOE Technical Exchange (Reamer 
and Williams 2001). NRC was concerned that the heterogeneity of fracture permeability, as 
reflected in the test-derived tsw34 values that span several orders of magnitude within a single 
geological layer, may not be adequately represented in the model. NRC requested the 
documentation of spatially heterogeneous fracture permeability using refinement of the grid for 
the heterogeneous fields in three dimensions and to evaluate the effect of high-permeability 
features (e.g., faults) crossing the drifts (NRC 2002, p. 3.3.6-12). 
In addition, NRC stated that a rigorous demonstration that the seepage model for total system 
performance assessment abstraction is valid for its intended purpose would require testing model 
results against relevant data not used in the original development of the model. However, NRC 
recognized that such data might not be available for the model. For thermally driven seepage, 
NRC suggested comparing the numerical model results with the Phillips (1996) analytical 
solution as a means of model validation (NRC 2002, p. 3.3.6-24). 
The agreement TEF 2.08 is relevant to the repository performance because the evaluation of 
thermally driven seepage is affected by heterogeneity and the thermal seepage results from the 
thermal-hydrologic simulations will be abstracted for use in the total system performance 
assessment. 
A.3 RESPONSE 
This KTI reflects the NRC concern that thermal flux perturbation with boiling and subsequent 
condensation of water may give rise to enhanced reflux toward waste emplacement drifts, 
thereby increasing the possibility of thermally driven seepage. This could be particularly 
important in strongly heterogeneous flux, where flow channeling or flow fingering may occur. 
This concern was addressed in Drift-Scale Coupled Processes (DST and TH Seepage) Models 
(BSC 2003a). A drift-scale thermal-hydrologic process model was developed 
(thermal-hydrologic seepage model), which incorporates all relevant thermal-hydrologic 
processes and accounts for small-scale heterogeneity in the drift vicinity. The 
thermal-hydrologic seepage model was applied to explicitly simulate thermally perturbed 
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channelized fluid flow down to the drift and to directly calculate transient seepage rates during 
the period of elevated temperatures (see Section A.3.1). The numerical results of the thermalhydrologic 
seepage model were compared to an improved semianalytical solution based on the 
Phillips solution (Phillips 1996) that was introduced as an alternative conceptual model in 
Drift-Scale Coupled Processes (DST and TH Seepage) Models (BSC 2003a). The alternative 
semianalytical model is discussed and results are presented in Section A.3.2. GEN 1.01 
Comment 15 is addressed in Section A.3.3. 
The information in this report is responsive to agreements TEF 2.08 and GEN 1.01 
(Comment 15) made between the DOE and NRC. The report contains the information that DOE 
considers necessary for the NRC to review for closure of these agreements. 
A.3.1 Effects of Heterogeneity on Thermally Driven Seepage 
As mentioned above, the effects of heterogeneity on thermal seepage are documented in 
Drift-Scale Coupled Processes (DST and TH Seepage) Models (BSC 2003a, Section 6.2). 
Grid Refinement for Heterogeneous Field A.3.1.1 
The thermal-hydrologic seepage model was developed to simulate thermal seepage into the 
waste emplacement drifts at Yucca Mountain (BSC 2003a). The drift-scale model explicitly 
accounts for small-scale fracture permeability heterogeneity as developed for ambient seepage 
simulations (BSC 2003b) and also applies other important model concepts from ambient seepage 
(small fracture capillarity, seepage boundary condition treatment at the rock-drift interface). The 
small-scale heterogeneity is based on air permeability measurements conducted on a 1-foot 
measurement scale in various boreholes above niches in both the lower lithophysal and the 
middle nonlithophysal unit. Small-scale heterogeneity may lead to channelized reflux from the 
condensation zone back to the heated drift and is also an important factor for ambient seepage, as 
explained in Drift-Scale Coupled Processes (DST and TH Seepage) Models (BSC 2003a). 
Variability of rock properties and boundary conditions on a larger scale (i.e., variability between 
different repository sections) is accounted for by simulating various sensitivity cases primarily 
for factors known to impact thermal seepage. These factors are, for example, the 
thermal-operating mode, the local percolation flux, and selected drift-scale rock properties. 
The thermal-hydrologic behavior of fractured rock is simulated in two-dimensional vertical 
domains perpendicular to the drift axis. 
The gridblock size is kept sufficiently small in the vicinity of the drift and at geologic contacts 
but is coarser elsewhere to achieve computing efficiency. At the drift wall, gridblocks are about 
20 cm in the radial direction (i.e., the grid block size is sufficiently small to describe the 
small-scale heterogeneity). The area within approximately 50 m above the drift is more finely 
discretized than areas beyond to better capture thermal-hydrologic effects important for seepage 
into drifts. The inside of the drift is also finely discretized to accurately capture the heat transfer 
from the waste package to the drift surface. 
Further details on the thermal-hydrologic seepage model are provided in Section A.4.1.1. 
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Three-Dimensional Effects A.3.1.2 
A fully three-dimensional simulation of drift-scale thermal seepage has not been performed. 
Several simulation cases must be studied with the thermal-hydrologic seepage model to account 
for the variability in rock properties and boundary conditions important for thermal seepage; 
therefore, a full three-dimensional simulation of the coupled processes is not feasible because of 
computational limitations. Similar to the ambient seepage models, the thermal-hydrologic 
seepage model focuses on near-drift conditions, using a refined discretization in the drift vicinity. 
However, at the same time, the thermal-hydrologic simulation requires a large vertical model 
domain because the thermally disturbed zone extends far into the overlying and underlying 
geological units. The main deviations between a three-dimensional and a two-dimensional 
model occur at the end of each emplacement drift and at the edges of the repository. Such 
effects are accounted for in Drift-Scale Coupled Processes (DST and TH Seepage) Models (BSC 
2003a, Sections 6.2.2.1.3 and 6.2.4.2) by considering several sensitivity cases for the thermal 
load. Also note that, with respect to the effectiveness of the capillary barrier for seepage into 
drifts, a two-dimensional representation gives a conservative prediction of seepage for most 
cases of heterogeneous fracture permeability fields because the potential diversion of flow in the 
third dimension is neglected (BSC 2003c, Section 6.4.3.1). 
Effect of High-Permeability Features Crossing the Drift A.3.1.3 
The impact of faults has not been examined specifically for thermal seepage. The impact of 
large-scale features on the temperature distribution is captured by the mountain-scale 
thermal-hydrologic models, which provide the boundary conditions for the thermal seepage 
models. Sensitivity studies performed to analyze the impact of increased mean permeability on 
thermal-hydrologic processes are summarized in FY 01 Supplemental Science and Performance 
Analyses, Volume 1 (BSC 2001, Table 5.4.3-1). Virtually no changes in rock temperature occur 
for the cases with one-standard-deviation permeability variation above and below the mean and 
for the case with a two-standard-deviations smaller permeability. Significant impact was 
predicted, however, for the case with permeability two standard deviations above the mean, 
where the predicted peak temperature was about 11C lower and the duration of the boiling 
period was a few hundred years shorter than in the other cases. However, calculation of local 
seepage from a fault is considered less important as it is unlikely that waste packages will be 
placed in known fault locations. 
A.3.2 Comparison of Model Results to the Phillips Analytical Solution 
Unsaturated fracture flow may occur in fast-flowing preferential pathways (thin fingers) that 
drain downward intermittently. Water buildup in the condensation zone above heated waste 
emplacement drifts can provide a potential source of such downward finger flow, carrying water 
at flow rates much larger than the average infiltration. Such conditions may promote the 
potential of seepage during the thermal period at Yucca Mountain because finger flow may 
penetrate far into the superheated rock zone (i.e., rock temperature above boiling point of water) 
around waste emplacement drifts. It is not clear whether process models using a continuum 
representation, such as the thermal-hydrologic seepage model, are able to capture such 
small-scale processes, even though small-scale heterogeneity in fracture permeability has been 
October 2003 A-5 No. 3: Water Seeping into Drifts
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incorporated. Therefore, an alternative conceptual model was applied (see Section A.4.2) to 
investigate the potential impact of episodic finger flow on thermal seepage. 
Phillips (1996) developed an analytical solution for the infiltration distance of a liquid finger 
flowing in a super-heated fractured rock as a function of time. This solution provides an 
asymptotic approximation of the long-term behavior, but it predicts unrealistic flow velocities at 
early times because of simplifying assumptions used to derive this solution. (The flow velocities 
are much larger than the gravity-driven flow velocity in the absence of vaporization.) An 
improved semianalytical solution (Birkholzer 2003; BSC 2003a) was developed, resolving the 
inability of Phillips solution to describe early-time behavior (BSC 2003a). This solution replaces 
the conservative Phillips (1996) solution. 
The improved semianalytical solution (see Section A.4.2) is used as an alternative conceptual 
model for thermal seepage, referred to as the thermal-hydrologic model for episodic finger flow, 
confirming the results of the thermal-hydrologic seepage model. The thermal-hydrologic model 
for episodic finger flow uses a simplified conceptualization of unsaturated fracture flow that is 
very conservative with respect to the potential for thermal seepage (BSC 2003a, Section 6.3.4). 
The assumed finger-flow events in the thermal-hydrologic model for episodic finger flow are fast 
and intense compared to the average flow conditions generally considered in process models like 
the thermal-hydrologic seepage model, and vaporization effects are limited as a result of the 
small cross-sectional area between the draining water and the hot rock. Also, finger flow is 
assumed to occur in vertical continuous fractures directly connecting the condensation zone 
above drifts with the drift crown. The fracture apertures used in the thermal-hydrologic model 
for episodic finger flow reflect the range of typical fracture apertures at Yucca Mountain (see 
Section A.4.2.3). Extreme aperture cases (such as large cracks or faults) were not used since the 
thermal-hydrologic model for episodic finger flow is already very conservative. In spite of this 
conservatism, the thermal-hydrologic model for episodic finger-flow results are fairly consistent 
with the process model results obtained with the thermal-hydrologic seepage model. Most 
importantly, the thermal-hydrologic model for episodic finger flow demonstrates that finger flow 
is not able to penetrate through the superheated rock during the first several hundred years of 
heating, when rock temperature is high and boiling conditions exist in a sufficiently large region 
above the drifts. These are the conditions when the potential for episodic finger flow is highest. 
Section A.4.2 provides additional details. 
A.3.3 Response to GEN 1.01, Comment 15 
The analytical approach described in Section A.3.2 (thermal-hydrologic model for episodic 
finger flow) was used as an alternative conceptual model for thermal seepage and compared with 
the results of the thermal-hydrologic seepage model. The thermal-hydrologic model for episodic 
finger flow explicitly accounts for condensate drainage in the reflux zone. This model 
demonstrates that vaporization reduces the impact of flux perturbation in the condensation zone 
by a large percentage. For the first several hundred years of heating, vaporization is so effective 
that water is not able to penetrate through the superheated rock, even when the flux is 12 times 
greater than the ambient flux of 6 mm/yr. These results clearly demonstrate that the time period 
of strongly elevated vertical flux in the condensation zone coincides with the time period of very 
effective vaporization. Additional details are provided in Section A.4.2.3. 
October 2003 A-6 No. 3: Water Seeping into Drifts
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Increased boiling temperatures of concentrated solutions are not considered important. This is 
justified because the data from the Drift Scale Test geochemical sampling generally show that 
concentrations of dissolved solids are relatively low (BSC 2002, Section 6.3.4). The liquid 
saturation generally has to be much less than 1 percent to produce concentrations that are 
significantly higher (BSC 2003d, Section 6.4.6.1). Under such conditions, the liquid is nearly 
immobile because of the very small relative permeability for the liquid phase. 
Although relatively low concentrations of dissolved solids were measured in many of the 
samples collected from the Drift Scale Test, some water samples showed relatively high 
concentrations of dissolved solids and low pH values relative to background values. The 
samples were limited to regions where the rock was well above the boiling temperature, and 
generally above 140C. A series of field and laboratory tests were conducted to determine 
whether the high concentrations of dissolved solids were due to degradation of the packer 
materials or because of water-rock interactions under thermal load (YMP 2002; Williams 2003). 
The results of the field test confirmed that the source of elevated fluoride was due to the packer 
materials and not the host rock. The laboratory tests supported this finding and also 
demonstrated that the volcanic tuff is not a source of hydrofluoric gas. Laboratory tests also 
demonstrated that neoprene can release significant quantities of chloride, especially when reacted 
with a higher temperature vapor system. Because of this potential problem, precautions will be 
taken to not introduce such packer materials into an operating repository, especially in regions of 
elevated temperatures. 
A.4 BASIS FOR THE RESPONSE 
A.4.1 Effects of Heterogeneity on Thermally Driven Seepage 
The following sections describe the modeling analysis using a drift-scale process model for 
thermal seepage influenced by small-scale heterogeneity. The numerical grid and the 
heterogeneity structure used in the thermal-hydrologic seepage model, as well as simulation 
results, are presented in Section A.4.1.1. In addition, Sections A.3.1.2 and A.3.1.3 have 
discussed the dimensionality of the model and the explicit consideration of high-permeability 
features crossing the drift. 
Grid Refinement for Heterogeneous Field A.4.1.1 
Information for this section is based on Drift-Scale Coupled Processes (DST and TH Seepage) 
Models (BSC 2003a, Section 6.2). 
Numerical Grids for Thermal-Hydrologic Simulations A.4.1.1.1 
The thermal-hydrologic seepage model was developed using TOUGH2 (LBNL 2003) to simulate 
thermal seepage into the waste emplacement drifts at Yucca Mountain. This model is based on a 
continuum assumption simulating the average flow behavior in the fractured rock. The model 
features small-scale fracture permeability heterogeneity as developed for ambient seepage 
simulations and also applies other important model concepts from ambient seepage (small 
fracture capillarity, seepage boundary condition treatment at the rock-drift interface). 
October 2003 A-7 No. 3: Water Seeping into Drifts
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To account for the two main host rock units of the repository, two two-dimensional submodels 
with slightly different spatial discretization and different stratigraphy were studied. The first 
one, the Tptpmn submodel, considers a drift located in the Topopah Spring Tuff middle 
nonlithophysal unit (Tptpmn unit). The second one, the Tptpll submodel, considers a drift 
located in the Topopah Spring Tuff lower lithophysal unit (Tptpll unit). 
The origin of the mesh coordinate system is the center of the drift. Figures A-1 and A-2 show 
the grid design at different scales. According to the dual-permeability method, the fractured rock 
is discretized with two identical overlapping numerical grids for the fracture and the matrix 
continuum, respectively, and only one of these is shown in the figures. Figures A-1 and A-2 
show that the gridblock size is kept sufficiently small to provide enough resolution in the vicinity 
of the drift and at geologic contacts but is coarser elsewhere in order to achieve computational 
efficiency. 
Source: BSC 2003a, Figure 6.2.1.2-1. 
NOTE: The top of the mesh is at +221 m; the bottom at -335 m. Blue lines show the interfaces between the host 
rock unit, the Topopah Spring Tuff middle nonlithophysal (Tptpmn) and the adjacent units, the Topopah 
Spring Tuff upper lithophysal (Tptpul) and the Topopah Spring Tuff lower lithophysal (Tptpll) units. The 
contact between the Tptpmn and the Tptpul was slightly raised compared to the USW SD-9 data to provide 
for better continuity at the interface. 
October 2003 
Figure A-1. Tptpmn Submodel Mesh with Closeup View of Drift Vicinity 
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Figure A-2. Discretization inside the Drift and in the Immediate Drift Vicinity 
Source: BSC 2003a, Figure 6.2.1.2-2. 
Heterogeneous Fracture Permeability Fields A.4.1.1.2 
The modeling framework for thermal seepage represents small-scale fracture permeability 
heterogeneity in the drift vicinity. In the thermal-hydrologic seepage model, fracture 
permeability is varied within a radius of 20 m from the drift centerline. The heterogeneity within 
20 meters is considered sufficient for the purpose of seepage modeling (BSC 2003a, 
Section 6.2). Similar to the ambient seepage models, the structure of the heterogeneous fracture 
permeability fields used is based on small-scale air-permeability test data. For the Tptpmm unit, 
data are available from Niches 2, 3, and 4 (also referred to as Niches 3650, 3107, and 4788, 
respectively) in the Exploratory Studies Facility. For the Tptpll unit, data from borehole 
SYBT-ECRB-LA#2 in the Enhanced Characterization of the Repository Block Cross-Drift and 
from Niche 5 (also referred to as Niche 1620) are used. Based on these data, log-normally 
distributed fracture permeability fields were generated for both the Tptpll and the Tptpmm with a 
standard deviation for the log-permeability of 0.84 (BSC 2003a, Section 4.1.1.1). This value is 
slightly smaller than the value used in the current revisions of the ambient seepage predictions 
(BSC 2003e). No spatial correlation is implemented because the variograms developed from the 
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air-permeability data show either short correlation length or a nugget effect close to the sill value 
(BSC 2003b, Section 6.6.2.1), i.e., the permeability is essentially random without a noticeable or 
significant correlation. 
The mean permeabilities of the random fields are based on the unsaturated zone drift-scale 
calibrated property set, derived from calibration against pressure and saturation data from several 
boreholes (BSC 2003f). The respective mean values used for the Tptpmn unit and the Tptpll unit 
are 0.33  10-12 m2 and 0.91  10-12 m2 (BSC 2003g, Table 6). 
As an example, Figure A-3 shows the permeability distribution of Realization 1 of the Tptpmn 
unit in the drift vicinity. Fracture permeabilities were randomly sampled from a lognormal 
distribution and assigned to individual grid blocks. The apparent correlation length of the 
heterogeneity field increases with distance from the drift as a result of an increase in grid-block 
size. However, in a region within the first few meters from the drift wall, where an appropriate 
random field representation is most important for seepage, the uncorrelated variability as derived 
from the air-permeability data on a comparable support scale is appropriately captured. 
Source: BSC 2003a, Figure 6.2.2.2-1. 
NOTE: The permeability within each grid block is constant. The contour plot shows the values as interpolated by the 
visualization software. 
Figure A-3. Fracture Permeability Distribution in Log(k) for Heterogeneous Realization 1 
October 2003 A-10 No. 3: Water Seeping into Drifts
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Modeling Results A.4.1.1.3 
The drift-scale thermal model was applied to a wide range of sensitivity cases to study the 
potential for thermally driven seepage (BSC 2003a, Sections 6.2.2.2 and 6.2.3.2). 
The thermal modes and the percolation fluxes considered cover a wide range of the variability 
and uncertainty in thermal-hydrologic conditions expected in the repository. For a given set of 
thermal-hydrologic rock properties, the predicted thermal conditions (maximum rock 
temperature, extent of the superheated rock zone, and duration of the boiling period) are mainly 
driven by the assumed heat load and the magnitude of percolation. One thermal mode, the 
low-temperature mode, results in rock temperatures that never reach boiling conditions. It was 
shown that thermal effects on flow and seepage are negligible in this case so that the potential for 
thermal seepage can be estimated from ambient seepage results. The other thermal modes give 
rise to boiling of water in the fractured rock close to waste emplacement drifts. Simulation 
results demonstrate that the thermal perturbation of the flow field (causing increased downward 
flux from the condensation zone toward the drifts) is strongest during the first few hundred years 
after closure, corresponding to the time period when rock temperature is highest and the 
vaporization barrier is most effective. Even for high percolation fluxes into the model domain 
and strong flow channeling as a result of fracture heterogeneity, water cannot penetrate far into 
the superheated rock during the time that rock temperature is above boiling, and model results 
show no seepage. The majority of the vaporized (and subsequently condensed) matrix water is 
diverted around the dryout zone and drains away from the drift, as shown in Figure A-4. The 
magnitude of percolation affects the temperature conditions in the fractured rock. For a given 
thermal load, high percolation fluxes tend to cool the rock temperatures, result in a shorter 
boiling period, and cause more distinct heat-pipe effects compared to small percolation fluxes. 
At the time when temperature has returned to below-boiling conditions and fractures start 
rewetting at the drift (for mean infiltration without flow focusing around 1,000 years after 
emplacement), the capillary barrier at the drift wall continues to operate, reducing (or 
preventing) water seepage into the drift. Since the thermal and hydrological conditions in the 
fractured rock will be perturbed from heating for a long time, simulation of thermal seepage was 
performed for 4,000 years after waste emplacement. The performance of the capillary barrier 
during this time period was evaluated in comparison to results from long-term ambient seepage 
(steady-state) simulations that were conducted to provide reference values for seepage at 
different percolation rates. The results indicate that thermal seepage never occurs in simulation 
cases where the respective long-term ambient seepage is zero. In cases where long-term ambient 
seepage is obtained (typically, cases with high percolation fluxes, heterogeneous fracture 
permeability fields, small fracture-capillary strength parameter in the drift vicinity, and inclusion 
of the effect of discrete fractures in the immediate drift vicinity using a specific drift wall 
boundary condition) thermal seepage is possible. These are cases that have been identified as 
promoting seepage in ambient seepage studies (Birkholzer et al. 1999; BSC 2003e). In such 
cases, seepage is predicted to begin several hundred to a few thousand years after rock 
temperature has returned below boiling, the delay caused by the slow saturation buildup in 
fractures; there is no seepage during the time period of above-boiling temperatures in the rock. 
Thermal-seepage percentages are always smaller than the respective ambient reference values 
(Figure A-5), indicating that there is no enhanced seepage as a result of reflux of water (because 
most of the condensate has long drained down away from the drift), and that the long-term 
October 2003 A-11 No. 3: Water Seeping into Drifts
ambient seepage values provide an asymptotic upper limit for thermal seepage. Note that these 
general conclusions apply for all above-boiling thermal operating modes and for both the 
Tptpmn and the Tptpll repository horizons. 
Source: BSC 2003a, Figure 6.2.2.2-3. 
NOTE: SL denotes liquid saturation. 
Figure A-4. Fracture Saturation and Liquid Flux for Tptpmn Submodel with Heterogeneous Permeability 
Field (Simulation Case MN-HET-01, Realization 1) at 100 Years after Waste Emplacement 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 A-12
Revision 2 
Source: BSC 2003a, Figure 6.2.2.2-7b. 
Figure A-5. Thermal-Hydrologic Conditions for Tptpmn Submodel with Flow Focusing Factor 10 
(Simulation Case MN-HET-03, Realization 1): Seepage Percentage for Thermal Run and 
A.4.1.1.4 
October 2003 A-13 
Long-Term Ambient Runs 
Sensitivity to rock properties was explicitly studied with the thermal-hydrologic seepage model 
by assessing seepage in two host rock units with different thermal and hydrological properties 
and by varying the seepage-relevant fracture capillary-strength parameter. In all these cases, the 
main conclusions regarding thermal seepage were similar, in that no seepage is predicted to 
occur during the period of above-boiling temperatures in the rock and that thermal seepage is 
always less in magnitude compared to the respective long-term ambient values. While the 
potential variability of other relevant thermal-hydrologic properties (thermal conductivity and 
fracture permeability) is expected to result in considerably different thermal-hydrologic 
conditions, the above main conclusions on thermal seepage should not be affected. This is 
because the range of thermal-hydrologic conditions expected from the variability of these 
properties is smaller than the range of thermal-hydrologic conditions explicitly addressed in the 
modeling analysis. 
Conclusions 
The following conclusions were reached from the thermal-hydrologic modeling analysis of 
thermal seepage (BSC 2003a, Section 6.2): 
 The vaporization barrier is effective as long as boiling conditions persist in the rock 
close to the drifts. Even for high infiltration fluxes, channelized fast flow cannot 
penetrate into the superheated rock during the hot time period. 
No. 3: Water Seeping into Drifts
Revision 2 
 The period of above-boiling temperature coincides with the period of present-day mean 
infiltration, which is significantly smaller than infiltration during monsoon or glacial 
transition climate. This means that two effective barriers (the vaporization barrier and 
the capillary barrier) are operating simultaneously during the first several hundred years 
after waste emplacement. 
 Thermal seepage is always smaller than the long-term ambient seepage percentage 
calculated from steady-state simulation runs using the respective infiltration rate of the 
three climate periods. 
 In general, thermal seepage may start to occur when the rock temperature is below 
boiling. Whether thermal seepage occurs (after the vaporization barrier has vanished) 
depends on the effectiveness of the capillary barrier, as evaluated by the long-term 
ambient seepage simulations for the steady state. The time when thermal seepage starts 
to occur depends on the time-dependent rewetting of the fractures at the drift wall. 
 The Tptpll unit shows a higher peak temperature at the drift wall, a larger superheated 
zone, and a longer period of above-boiling temperature compared to the Tptpmn unit. 
Three-Dimensional Effects A.4.1.2 
These effects are discussed in Section A.3.1.2. 
Effect of High-Permeability Features Crossing the Drift A.4.1.3 
These effects are discussed in Section A.3.1.3. 
A.4.2 Comparison of Model Results to the Phillips Analytical Solution 
Information for this section is based on Drift-Scale Coupled Processes (DST and TH Seepage) 
Models (BSC 2003a, Section 6.3). 
As discussed in Section A.3.2, an alternative conceptual model was developed to support the 
findings of the thermal-hydrologic seepage model. The alternative model is an improved version 
of the model developed by Phillips (1996). Phillips model was modified because it yielded an 
unrealistic solution at early times. The alternative conceptual model is described in more detail 
in the following sections. The alternative conceptualization is highly simplified and therefore 
conservative, particularly because (1) it is not clear if such finger-flow behavior is characteristic 
for Yucca Mountain, and (2) the solution assumes fracture geometries that are not realistic 
(vertical continuous fracture connecting high-saturation condensation zone with drifts). 
Alternative Conceptual Model A.4.2.1 
An alternative conceptual model is used to corroborate the results and conclusions of the 
thermal-hydrologic seepage model. The alternative conceptual model considers the possibility 
that unsaturated fracture flow may occur in fast-flowing preferential pathways (thin fingers) that 
drain downward intermittently. Water buildup in the condensation zone above waste 
emplacement drifts can provide a potential source of such downward finger flow, carrying water 
October 2003 A-14 No. 3: Water Seeping into Drifts
Revision 2 
at flow rates much larger than the average percolation under ambient conditions. Such high-flux 
conditions may promote the potential of seepage during the thermal period at Yucca Mountain, 
because finger flow may penetrate far into the superheated rock zone (i.e., rock temperature 
above the boiling point of water) around waste emplacement drifts. 
The alternative conceptual model, referred to as the thermal-hydrologic model for episodic finger 
flow, is applied to investigate the potential impact of episodic finger flow on thermal seepage. 
The thermal-hydrologic model for episodic finger flow analyzes the fate of episodic preferential 
flow events that originate somewhere in the condensation zone above the repository and 
percolate downward towards the emplacement drifts. Figure A-6 shows an illustration of 
episodic fingers flowing through fractures and penetrating into the superheated rock in the 
vicinity of waste emplacement drifts. As flow arrives at the superheated rock region around 
drifts, water begins to boil off. Depending on magnitude and duration of each flow event as well 
as on the temperature and pressure conditions in the fractured rock, the water may completely 
vaporize above the drift crown, or it may penetrate far into the superheated region and reach the 
drift. 
Modeling Procedure A.4.2.2 
The first step in applying the thermal-hydrologic model for episodic finger flow is to derive 
estimates for the possible characteristics of episodic finger flow at Yucca Mountain. 
Experimental data from a comprehensive laboratory study by Su et al. (1999) are used for that 
purpose, and a simplified finger-flow model for downward drainage is developed 
(Section A.4.2.3). The second step is to simulate the fate of such episodic finger-flow events 
when the flow penetrates into the superheated rock region above waste emplacement drifts, using 
the semianalytical solution of Birkholzer (2002; BSC 2003a). The conceptual model and the 
semianalytical solution are presented in Section A.4.2.4. The solution is implemented at several 
discrete times after waste emplacement to cover the range of rock temperature conditions and 
extent of superheated zone around drifts. The third and final step is to evaluate the results; 
namely, the relative percentage of water arriving at the drift crown at different times after 
emplacement, in relation to the perturbed flow situation above the drifts at these times (i.e., the 
elevated downward flux from the condensation zone towards the drift). 
October 2003 A-15 No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003a, Figure 6.3-1. 
NOTE: The drip shield above waste packages is not shown here for simplicity. 
Figure A-6. Schematic Illustration of Conceptual Model for Finger Flow in a Vertical Fracture above a 
Drift with Heat Conduction from the Adjacent Rock (a) and Episodic Finger Flow in 
A.4.2.3 
October 2003 
Unsaturated Fractured Rock in the Vicinity of Waste Emplacement Drifts (b) 
Characteristics of Episodic Preferential Flow 
Episodic preferential flow in unsaturated fractures has been experimentally observed in flow 
visualization experiments using fracture replicas (e.g., Nicholl et al. 1994; Persoff and Pruess 
1995; Su et al. 1999). (Note that such conditions have never been observed in the ambient 
natural environment at Yucca Mountain.) Although constant inlet flow conditions were applied 
in these experiments, intermittent flow behavior was caused by small-scale capillary barriers 
within the fracture plane, forming in areas of smaller apertures located above regions of larger 
apertures. As a result, water accumulated in the small-aperture regions until the water potential 
A-16 No. 3: Water Seeping into Drifts
Revision 2 
exceeded the capillary-force difference. Once this occurred, a large portion of the accumulated 
water moved rapidly downward in a thin finger. When the capillary pool emptied, the finger 
snapped and reformed at some later time. Typically, the observed water volumes per event were 
small, of the order of milliliters. 
Interestingly, Su et al. (1999, p. 1032, Table 4) report a small range of water volumes 
accumulating in and draining from capillary pools for the entire suite of experiments, fairly 
unaffected by the order-of-magnitude variation in flow rate imposed at the inlet boundary. Also, 
the width of the rivulets was observed to be independent of the applied flow rate, while the 
temporal frequency of flow events correlated well with the flow rate imposed at the inlet 
boundary. These observations are consistent with the concept of capillary-induced episodic flow 
patterns, in which the accumulation and flow distribution of water depends on local aperture 
variation, while the time required between subsequent flow events (required for water 
accumulation) depends on the rate of overall downward percolation in the fractured rock. 
Adopting this concept for the thermal conditions at Yucca Mountain, it is assumed that the 
thermally perturbed percolation fluxes in the condensation zone (as predicted by the 
thermal-hydrologic seepage model) drain downward in episodic finger-flow patterns. The 
characteristics of individual fingers (i.e., finger geometry, water volume per flow event and flow 
rate) are assumed to be independent of the actual percolation flux magnitude. Their frequency, 
however, is directly correlated to the percolation flux (i.e., strongly elevated downward fluxes at 
early stages of heating should result in finger flow that occurs more often in time and space). 
In this study, it is assumed that such intermittent flow behavior can also occur in the unsaturated 
fractures at Yucca Mountain, particularly during the thermal period when condensate above the 
superheated zone is expected to provide a significant source of water above waste emplacement 
drifts. Since there are neither experimental studies with fracture test samples from Yucca 
Mountain nor replicas mimicking Yucca Mountain fractures, the flow characteristics observed in 
the above experiments were used as estimates for potential episodic preferential flow in 
unsaturated fractures at Yucca Mountain. The fracture replica analysis of Su et al. (1999) is 
probably the best suited for this purpose because the realistic geometry of natural fractures is 
accounted for and detailed quantitative measurements are provided in their analysis. The 
fracture replica in this experimental work was taken from the granitic rock of the Stripa Mine in 
Sweden. Differences between fractures from the Yucca Mountain tuff and the Stripa Mine 
granite (with respect to aperture distributions, surface roughness, and contact angle) will bring 
out differences in flow behavior and distribution. This approach is valid for a qualitative 
analysis intended to demonstrate the impact of an alternative flow concept on water arrival at the 
drift during the thermal period at Yucca Mountain. 
Basic characteristics defining episodic finger flow (namely, water volume of individual flow 
events, V, fracture aperture b, and finger width w), are directly extracted from the experimental 
results described by Su et al. (1999). Using representative values for these parameters, 
additional parameters are derived from a simplified conceptual flow model, assuming 
gravity-driven, laminar, and fully developed flow in vertical one-dimensional channels of 
uniform width, in fractures of uniform aperture and infinite extent. This simplified flow model is 
conservative because it provides a direct fast-flow connection between the condensation zone 
and the heated drift. These derived parameters (flow velocity vP, mass flow rate mP, and duration 
October 2003 A-17 No. 3: Water Seeping into Drifts
Revision 2 
of flow tP) are input to the semianalytical solution. (The flow duration denotes the time period 
needed for the finger to flow past a given location.) 
The experimental data of Su et al. (1999, Sections 2 and 3) suggest the following representative 
values for fracture aperture b, water volume V, and finger width w. Assuming log normal 
distribution, the geometric mean aperture of the fracture replica investigated by Su et al. (1999, 
p. 1024) is 0.141 mm, while the standard deviation is 0.559 in natural log space. Comparison of 
these statistical parameters with conditions at Yucca Mountain is difficult, since comparable 
small-scale measurements are not available for the fractures in the Tptpmn and the Tptpll. 
However, first-order estimates of hydraulic aperture can be derived from fracture frequency and 
fracture permeability data. Following Particle Tracking Model and Abstraction of Transport 
Processes (CRWMS M&O 2000, Section 6.2.1, Equation 25, Table 4), the geometric mean of 
fracture hydraulic aperture in the Tptpmn unit is approximately 0.1 mm with a standard deviation 
of 0.479 in natural log space. These mean and standard deviation values are slightly smaller than 
the mean aperture and standard deviation reported by Su et al. (1999, p. 1024). Data on water 
volumes are derived using the 17 (out of 21) flow visualization experiments by Su et al. (1999, 
Table 4) that exhibit episodic behavior, giving a geometric mean of 0.161 mL and a standard 
deviation of 0.438 (in natural log). The geometric mean values of fracture aperture and water 
volume are applied as base cases. In addition, uncertainty is covered in a sensitivity analysis in 
which these base-case values are varied by adding or subtracting the respective standard 
deviation (in log space). For finger geometry, Su et al. (1999, p. 1032) report a fairly consistent 
finger width of about 1 mm, often forming behind advancing water drops that are slightly larger, 
on the order of 4.5 mm. Since these two values are not sufficient to derive statistical properties, 
two equally probable cases with w = 1 mm and w = 4.5 mm are considered. Therefore, the range 
of apertures used in the thermal-hydrologic model for episodic finger flow reflects the range of 
typical fracture apertures at Yucca Mountain. 
Table A-1 lists the input properties and the calculated flow characteristics of all simulation cases 
studied in the analysis below. Case 1, for example, uses the geometric mean values of fracture 
aperture and water volume with a finger width of 1 mm, which gives a downward flow velocity 
of 0.054 m/s, a mass flow rate of 7.3  10-6 kg/s, and a flow event duration of 21.2 seconds. 
Using the same aperture and water volume, but a wider (4.5 mm) finger, the downward flow 
velocity is still 0.054 m/s, but mass flow rate is larger at 3.3  10-5 kg/s, while the flow duration 
is smaller at 5.2 s (Case 2). In the sensitivity cases, either fracture aperture is varied (Cases 1a 
and 2a for larger aperture, Cases 1b and 2b for smaller aperture) or the water volume is adjusted 
(Cases 1c and 2c for larger water volume, Cases 1d and 2d for smaller water volume). Changes 
in aperture invoke changes in flow velocity, mass flow rate, and duration of flow event, while 
changes in water volume affect only the flow duration. Typically, a larger aperture is associated 
with a fast, intense, and short flow event. Larger water volumes are related to longer flow 
duration. 
October 2003 A-18 No. 3: Water Seeping into Drifts
Finger Flow 
Simulation Cases 
Case 1 
(uses geometric mean of b 
and V, w = 1 mm) 
Sensitivity Cases to Case 1 
Case 1a (large aperture) 
Case 1b (small aperture) 
Case 1c (large volume) 
Case 1d (small volume) 
Case 2 
(uses geometric mean of b 
and V, w = 4.5 mm) 
Sensitivity Cases to Case 2 
Case 2a (large aperture) 
Case 2b (small aperture) 
Case 2c (large volume) 
Case 2b (small volume) 
Table A-1. Suite of Episodic Flow Events Analyzed with the Thermal-Hydrologic Model for Episodic 
Input extracted from Su et al. (1999) 
Fracture 
Aperture 
b 
Finger 
Width 
w 
(mm) (mL) (mm) 
1.0 0.141 
1.0 0.247 
1.0 0.081 
1.0 0.141 
1.0 0.141 
4.5 0.141 
4.5 0.247 
4.5 0.081 
4.5 0.141 
4.5 0.141 
Water 
Volume 
V 
A-19 
0.161 
0.161 
0.161 
0.249 
0.104 
0.161 
0.161 
0.161 
0.249 
0.104 
Output derived using b, V, and w as 
input 
Flow 
Velocity 
vP 
(m/s) 
0.054 
0.164 
0.018 
0.054 
0.054 
0.054 
0.164 
0.018 
0.054 
0.054 
tP 
Mass Flow 
Rate 
mP 
(kg/s) 
7.3  10-6 
3.9  10-5 
1.4  10-6 
7.3  10-6 
7.3  10-6 
3.3  10-5 
1.8  10-4 
6.1  10-6 
3.3  10-5 
3.3  10-5 
Flow 
Duration 
21.2 
4.0 
32.9 
13.7 
4.7 
0.9 
25.2 
7.3 
3.0 
(s) 
113.4 
October 2003 
Source: BSC 2003a, Table 6.3.1.2-1. 
Water Penetration into Superheated Rock A.4.2.4 
The semianalytical solution of Birkholzer (2002, BSC 2003a) is used to determine the maximum 
penetration distance of episodic fingers subject to vigorous vaporization from the hot rock. In 
case the flow from these events penetrates through the entire superheated zone above drifts, the 
solution also gives the total amount of water arriving at the drift crown. A brief review of the 
mathematical formulation and solution procedure is given below. This solution provides an 
exact simulation method for early and late time periods of flow events that can be episodic or 
continuous. 
The basic conceptual model for the semianalytical solution of finger penetration into superheated 
rock is schematically depicted in Figure A-4, showing a superheated region of length L above the 
crown of a waste emplacement drift. Here, the ambient rock water has long been boiled off, and 
fractures and rock are essentially dry. The rock temperature in the superheated zone is above the 
boiling temperature at prevailing pressure. Initially, before finger flow occurs, the temperature 
field is uniform in the lateral x-direction and a function of location in the vertical z-direction. 
Episodic flow events of given mass flow rate mP, duration tP, and finger width w enter the 
superheated region at z = 0 and t = 0. The infiltrating water is already heated up to almost 
boiling temperature TP upon arrival at the superheated region and begins boiling as it passes the 
boiling-point isotherm. As was presented in the previous section, the downward flow of the 
finger is gravity-driven and strictly one-dimensional. Upon contact with the water, the rock 
No. 3: Water Seeping into Drifts 
Revision 2
surface cools to boiling temperature, and a steep temperature gradient is established in the 
surrounding matrix when the liquid front in the fractures reaches the considered position. With 
time, the thermal perturbation penetrates farther into the rock, the thermal gradient decreases, 
and heat flow from the matrix to the fracture is reduced. As conduction in the matrix is slow 
compared to the vertical movement of the liquid pulse, the conductive heat flow within the 
matrix and from the matrix to the fracture is considered as strictly lateral, perpendicular to the 
fracture plane. Note that the accumulation time between two consecutive episodic flow events is 
usually longer than the flow duration tP, so that for all practical purposes the rock temperature 
has equilibrated to its initial state before the next flow event arrives. 
The downward flow rate at a location z in the superheated region can be derived from an energy 
balance between the energy required for vaporization of water and the energy supplied by heat 
conduction from the rock. Using an analytical solution of Carslaw and Jaeger (1959, pp. 58 to 
62) to solve for the lateral temperature distribution in the rock matrix, this energy balance is as 
follows (Birkholzer 2002, p. 5, Eq. 9) 
T P RI 
h z ΃t 
T
t0 (z) .
. 
( ) 
Here, m(z,t) is mass flow rate at location z, time t, dry is dry thermal conductivity of the rock 
matrix, h is specific enthalpy of vaporization, TRI is the initial rock temperature, and  is rock 
thermal diffusivity. The period t0(z) denotes the time interval after initial entry of the water 
finger into the superheated zone until the arrival of the tip of the liquid finger at location z. 
Equation A-1 is valid as long as the thermal gradient in the rock is nearly uniform across the 
width of the liquid finger. Since thermal perturbation distance of the thermal calculation into the 
rock grows with (  t)1/2, the maximum time period tm associated with a uniform thermal gradient 
is of order 
m( ) z,t 2w dry . = 
w2 
m 
A.4.2.5 
 
For t > tm, the nearly one-dimensional heat flow perpendicular to the fracture-rock interface 
transforms to a more circular spreading of heat and Equation A-1 can no longer be applied. 
However, in most cases of practical concern, tm is much larger than the timescale of interest. 
A simple Lagrangian solution scheme is used to solve Equation A-1 for episodic flow events of 
given flow rate and duration (Birkholzer 2002, pp. 10 to 12; BSC 2003a). A time-marching 
procedure tracks the movement of finite water masses traveling downwards while part of the 
water boils off. The semianalytical solution scheme is shown to be accurate, robust, and 
extremely fast. For details on the numerical methods, for verification and validation of the 
solution (in comparison with TOUGH2 modeling results and an analytical solution), refer to 
Birkholzer (2002, pp. 10 to 12 and 42 to 44). 
Thermal-Hydrologic Model for Episodic Finger-Flow Results 
The long-term evolution of thermal-hydrological conditions in the rock is accounted for by 
applying the thermal-hydrologic model for episodic finger flow at 11 selected times after waste 
t = 
A-20 No. 3: Water Seeping into Drifts 
Revision 2 
(Eq. A-1) 
(Eq. A-2) 
October 2003
Revision 2 
emplacement, covering the time period during which repository temperatures remain above 
boiling (about 1,000 years). The thermal parameters required as input for the thermal-hydrologic 
model for episodic finger flow, namely the vertical temperature profile and the extent of the 
superheated region, are obtained from the thermal-hydrologic seepage model. Figure A-5 
provides results of the thermal-hydrologic model for episodic finger flow considering 11 discrete 
times and using the flow event referred to as Case 1 in Table A-1 (i.e., finger width is 1 mm). 
The red symbols give the maximum penetration distance into the superheated rock, while the 
blue symbols show the relative amount of water arrival at the drift. The maximum penetration 
distance should be compared to the dotted curve showing the extent of the superheated region 
above the drift crown. According to this figure, no water would reach the drift for the first 
450 years after emplacement because of intense heat in a sufficiently large hot region. At later 
times, the possible maximum penetration (in the absence of the drift opening) becomes larger 
than the boiling zone (i.e., water would arrive at the drift crown). The relative amount of water 
reaching the drift increases significantly between 450 years and 750 years after emplacement, as 
a result of the decreasing rock temperature and the smaller superheated rock zone. Eventually, 
after 950 years, the effect of vaporization becomes marginal so that the water mass arriving at 
the drift is almost equal to the initial mass of the episodic flow event. 
In Figure A-6, the relative rates of water arrival at the drift crown at given times are related to the 
flux perturbation in the condensation zone at these times. The red line shows the so-called flux 
elevation factor, which is defined as the maximum downward flux in the condensation zone 
divided by the undisturbed ambient percolation of 6 mm/yr. The maximum downward flux is 
calculated at the 11 selected times from the thermal-hydrologic seepage model. As the circular 
symbols indicate, the most significant flux elevation occurs at 75 years of heating, where the 
maximum downward flux is 73.2 mm/yr, more than 12 times that of the ambient flux of 
6 mm/yr. With time progressing, this effect declines rapidly and is essentially negligible at 
1,500 years after waste emplacement. (Increasing infiltration, resulting from climate changes at 
600 years, causes the spike at 650 years (BSC 2003a, Section 6.3).) The blue line gives the 
water flux arriving at the drift crown when the combined effect of flux perturbation and 
vaporization barrier is considered. Note that this flux is given relative to the undisturbed ambient 
percolation at the respective time and is obtained by multiplying the flux-elevation factor with 
the relative mass-arrival rate given in Figure A-7. If the displayed values are larger than one, the 
amount of water potentially arriving at the drift wall exceeds the ambient percolation flux. 
It is obvious from Figure A-8 that vaporization reduces the impact of flux perturbation in the 
condensation zone by a large percentage. For the first 450 years of heating, vaporization is so 
effective that the amount of water arriving at the drift crown is zero. Between 450 and 
650 years, vaporization is still strong enough to reduce the elevated fluxes to values smaller than 
the ambient percolation (i.e., the resulting flux ratio is smaller than one). These are important 
results, clearly demonstrating that the time period of strongly elevated vertical flux in the 
condensation zone coincides with the time period of very effective vaporization. Thus, even if 
the downward flux from the condensation zone towards the drift would flow entirely in episodic 
finger-type patternsan extreme flow conceptualization that has never been observed at Yucca 
Mountainthe vaporization barrier would be fully effective for several hundred years. Only at 
later times, when vaporization effects diminish, is the flux arriving at the drift slightly higher 
than the natural ambient percolation. However, note that these results are based on various 
simplifications that tend to promote the potential amount of water reaching drifts, most of them 
October 2003 A-21 No. 3: Water Seeping into Drifts
Revision 2 
related to the idealized conceptual model of finger flow and heat transport. Also, the capillary 
barrier capability of the drift opening, which has not been considered in this analysis, will most 
likely prevent seepage from occurring (see BSC 2003e, Section 6.6.1), even if the fluxes arriving 
at the drift crown were taken from the alternative thermal-hydrologic model for episodic finger 
flow instead of the thermal-hydrologic seepage model. 
Source: BSC 2003a, Figure 6.3.2.1-4. 
Figure A-7. Maximum Penetration Distance (Red Line; Left Y-Axis) and Ratio of Water Mass Arriving at 
Drift Crown (Blue Line; Right Y-Axis) for Case 1 (Tptpmn Unit), at 11 Different Times after 
October 2003 A-22 
Waste Emplacement 
No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003a, Figure 6.3.2.1-5. 
NOTE: The red line shows flux ratio in the condensation zone, simulated with the thermal-hydrologic seepage 
model. The blue line shows the flux ratio of water at the drift crown, including the effect of vaporization. 
Figure A-8. Ratio of Thermally Perturbed Vertical Flux and Ambient Percolation for Case 1 (Tptpmn 
A.4.2.6 
October 2003 
Unit), at 11 Different Times after Waste Emplacement 
Thermal-Hydrologic Model for Episodic Finger-Flow Sensitivity Cases 
Several sensitivity cases are studied to analyze the uncertainty of water arrival at the drift caused 
by the potential variability in the flow characteristics of episodic finger flow. Of all input 
parameters required for the semianalytical solution, those properties related to the small-scale 
finger-flow characteristics, as extracted from Su et al. (1999), are the most uncertain and 
variable. The sensitivity cases performed are summarized in Table A-1. Case 1a is the most 
critical of all the cases (large fracture aperture and small finger width; see Figure A-9). In this 
case, the episodic flow event is comparably fast and intense, while the effect of vaporization is 
small, because of the small interface area available for heat conduction and the reduced contact 
time between water and hot rock. Even then, however, vaporization in the superheated zone is 
strong enough to significantly reduce the effect of elevated vertical fluxes draining down from 
the condensation zone, particularly at early times when the thermal perturbation is largest. The 
maximum flux elevation ratio at the drift crown is about 3 at 550 years after emplacement 
(i.e., the amount of water potentially arriving at the drift would be 18 mm/yr, compared to 
6 mm/yr at ambient). For all sensitivity cases, the effect of variation in finger-flow 
characteristics is noticeable. All cases, however, exhibit a vaporization barrier that is fully 
effective for several hundred years, covering the time period of strong thermal perturbation when 
this barrier capability is most critical. In addition to this vaporization barrier, the capillary 
A-23 No. 3: Water Seeping into Drifts
Revision 2 
barrier at the drift surface is in effect, which significantly suppresses the seepage potential for the 
fluxes calculated with the alternative thermal-hydrologic model for episodic finger flow. 
Source: BSC 2003a, Figure 6.3.2.2-1a. 
NOTE: The red line shows flux ratio in the condensation zone, simulated with the thermal-hydrologic seepage 
model. The other lines show the flux ratio of water at the drift crown, including the effect of vaporization. 
The black line is Case 1a and the green line is Case 1b. The dashed blue line is the mean case. 
Figure A-9. Ratio of Thermally Perturbed Vertical Flux and Ambient Percolation, Showing Sensitivity of 
A.4.2.7 
October 2003 
Model Results to Fracture Aperture (Cases 1, 1a, 1b). 
Summary 
The alternative conceptual model was used to corroborate the results and conclusions of the 
thermal-hydrologic seepage model. The thermal-hydrologic model for episodic finger flow used 
a conceptualization of unsaturated fracture flow that is very conservative with respect to the 
potential for thermal seepage. The assumed finger-flow events are fast and intense compared to 
the average flow conditions generally considered in process models like the thermal-hydrologic 
seepage model, and vaporization effects are limited as a result of the small cross-sectional area 
between the draining water and the hot rock. These conditions, along with a simplified onedimensional 
finger-flow model representing continuous vertical fractures, create an adverse 
environment for the vaporization barrier above heated waste emplacement drifts. The most 
favorable conditions for episodic finger flow to occur are the early stages of heating, when 
moisture redistribution processes are most active. Water builds up in the condensation zone 
above drifts, providing a potential source for downward drainage of fingers. Note that such flow 
conditions are not expected at ambient state. 
A-24 No. 3: Water Seeping into Drifts
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In spite of this conservatism, the thermal-hydrologic model for episodic finger-flow results were 
fairly consistent with the process model results obtained with the thermal-hydrologic seepage 
model. Most importantly, the thermal-hydrologic model for episodic finger flow demonstrated 
that finger flow is not able to penetrate through the superheated rock during the first several 
hundred years of heating, when rock temperature is high and boiling conditions exist in a 
sufficiently large region above the drifts. These are the conditions in which the largest thermal 
perturbation occurs, i.e., when the potential for episodic finger flow is highest. Only later, when 
the boiling zone is small and the impact of vaporization is limited, can finger flow arrive at the 
drift crown. The fact that water can reach the drift during the period of above-boiling 
temperatures makes the alternative conceptual model distinct from the thermal-hydrologic 
seepage model. However, the strong thermal perturbation observed at early heating stages has 
already diminished during this time period, and the net result of water arrival at the 
driftconsidering the combined impact of water buildup in the condensation zone and 
vaporization in the superheated zoneis similar to ambient percolation. These findings are 
consistent over a wide range of finger-flow characteristics studied in a sensitivity analysis 
(Section A.4.2.6), covering the potential uncertainty in finger-flow patterns. Thus the thermalhydrologic 
model for episodic finger-flow model results clearly support the main findings of the 
thermal-hydrologic seepage model, adding confidence into the model and reducing the 
conceptual model uncertainty. Of the two host rock units, the Tptpll unit allows less water to 
arrive at the drift wall, as a result of the higher rock temperature and the larger superheated rock 
zone above the drift. This again is consistent with the thermal-hydrologic seepage model. The 
water fluxes potentially arriving at the drift surface during the cooldown period are most likely 
significantly below the seepage threshold (see BSC 2003e, Section 6.6.1), even though these 
fluxes are calculated using a conservative alternative model for episodic finger flow. It is, 
therefore, reasonable to assume that no seepage will occur during the boiling period. 
Because no seepage experiments under elevated temperature conditions have been performed at 
Yucca Mountain, this alternative conceptual model makes use of experimental data from a 
granite fracture from the Stripa mine (Section A.4.2.3). The thermal-hydrologic model for 
episodic finger flow is inherently conservative and thus considered suitable for a bounding 
calculation that corroborates the thermal-hydrologic seepage model in a qualitative manner. 
A.5 REFERENCES 
A.5.1 Documents Cited 
Birkholzer, J.T. 2002. TH_PULSE: Program for Calculating Infiltration of Episodic Liquid 
Fingers in Superheated Rock Fractures, Theory, Users Manual, and Sample Applications. 
LBNL/PUB-277. Berkeley, California: Lawrence Berkeley National Laboratory. TIC: 53581. 
Birkholzer, J. 2003. Penetration of Liquid Fingers into Superheated Fractured Rock. Water 
Resources Research, 39, (4), 9-1 through 9-21. [Washington, D.C.]: American Geophysical 
Union. TIC: 254362. 
Birkholzer, J.; Li, G.; Tsang, C-F.; and Tsang, Y. 1999. Modeling Studies and Analysis of 
Seepage into Drifts at Yucca Mountain. Journal of Contaminant Hydrology, 38, (1-3), 
349-384. New York, New York: Elsevier. TIC: 244160. 
October 2003 A-25 No. 3: Water Seeping into Drifts
Revision 2 
BSC (Bechtel SAIC Company) 2001. FY 01 Supplemental Science and Performance Analyses, 
Volume 1: Scientific Bases and Analyses. TDR-MGR-MD-000007 REV 00 ICN 01. 
Las Vegas, Nevada: Bechtel SAIC Company. ACC: MOL.20010801.0404; 
MOL.20010712.0062; MOL.20010815.0001. 
BSC 2002. Thermal Testing Measurements Report. ANL-NBS-HS-000041 REV 00. 
Las Vegas, Nevada: Bechtel SAIC Company. ACC: MOL.20021004.0314. 
BSC 2003a. Drift-Scale Coupled Processes (DST and TH Seepage) Models. MDL-NBS-HS- 
000015 REV 00C. Las Vegas, Nevada: Bechtel SAIC Company. ACC: MOL.20030910.0160. 
BSC 2003b. Seepage Calibration Model and Seepage Testing Data. MDL-NBS-HS-000004 
REV 02. Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030408.0004 
BSC 2003c. Abstraction of Drift Seepage. MDL-NBS-HS-000019 REV 00. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: DOC.20030826.0001. 
BSC 2003d. Drift-Scale Coupled Processes (DST and THC Seepage) Models. MDL-NBS-HS- 
000001 REV 02. Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030804.0004. 
BSC 2003e. Seepage Model for PA Including Drift Collapse. MDL-NBS-HS-000002 REV 02. 
Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030709.0001. 
BSC 2003f. Calibrated Properties Model. MDL-NBS-HS-000003 REV 01. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: DOC.20030219.0001. 
BSC 2003g. Analysis of Hydrologic Properties Data. MDL-NBS-HS-000014 REV 00. 
Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030404.0004. 
Carslaw, H.S. and Jaeger, J.C. 1959. Conduction of Heat in Solids. 2nd Edition. Oxford, Great 
Britain: Oxford University Press. TIC: 206085. 
CRWMS M&O (Civilian Radioactive Waste Management System Management and Operating 
Contractor) 2000. Particle Tracking Model and Abstraction of Transport Processes. 
ANL-NBS-HS-000026 REV 00. Las Vegas, Nevada: CRWMS M&O. 
ACC: MOL.20000502.0237. 
Nicholl, M.J.; Glass, R.J.; and Wheatcraft, S.W. 1994. Gravity-Driven Infiltration Instability in 
Initially Dry Nonhorizontal Fractures. Water Resources Research, 30, (9), 2533-2546. 
Washington, D.C.: American Geophysical Union. TIC: 243493. 
NRC (U.S. Nuclear Regulatory Commission) 2002. Integrated Issue Resolution Status Report. 
NUREG-1762. Washington, D.C.: U.S. Nuclear Regulatory Commission, Office of Nuclear 
Material Safety and Safeguards. TIC: 253064. 
Persoff, P. and Pruess, K. 1995. Two-Phase Flow Visualization and Relative Permeability 
Measurement in Natural Rough-Walled Rock Fractures. Water Resources Research, 31, (5), 
1175-1186. [Washington, D.C.]: American Geophysical Union. TIC: 229697. 
October 2003 A-26 No. 3: Water Seeping into Drifts
Revision 2 
Phillips, O.M. 1996. Infiltration of a Liquid Finger Down a Fracture into Superheated Rock. 
Water Resources Research, 32, (6), 1665-1670. [Washington, D.C.]: American Geophysical 
Union. TIC: 239025. 
Reamer, C.W. and Gil, A.V. 2001. Summary Highlights of NRC/DOE Technical Exchange and 
Management Meeting of Range on Thermal Operating Temperatures, September 18-19, 2001. 
Washington, D.C.: U.S. Nuclear Regulatory Commission. ACC: MOL.20020107.0162. 
Reamer, C.W. and Williams, D.R. 2001. Summary Highlights of NRC/DOE Technical Exchange 
and Management Meeting on Thermal Effects on Flow. Meeting held January 8-9, 2001, 
Pleasanton, California. [Washington, D.C.]: U.S. Nuclear Regulatory Commission. 
ACC: MOL.20010202.0095 through MOL.20010202.0108. 
Su, G.W.; Geller, J.T.; Pruess, K.; and Wen, F. 1999. Experimental Studies of Water Seepage 
and Intermittent Flow in Unsaturated, Rough-Walled Fractures. Water Resources Research, 35, 
(4), 1019-1037. Washington, D.C.: American Geophysical Union. TIC: 245798. 
Williams, N.H. 2003. Contract No. DE-AC28-01RW1210  Transmittal of White Paper, 
Effects of Neoprene on Water in the Drift Scale Test. Letter from N.H. Williams (BSC) to J.D. 
Ziegler (DOE/ORD), February 4, 2003, 0129035843, with enclosure. 
ACC: MOL.20030206.0211. 
YMP (Yucca Mountain Site Characterization Project) 2002. Effects of Introduced Materials in 
the Drift Scale Test. North Las Vegas, Nevada: Yucca Mountain Site Characterization Office. 
ACC: MOL.20020304.0044. 
A.5.2 Software Code 
LBNL (Lawrence Berkeley National Laboratory) 2003. Software Code: TOUGH2. V1.6. 
PC/MS-DOS under Windows 98, Sun UltraSparc OS 5.5.1, DEC-Alpha OSF1 V4.0. 
10007-1.6-01. 
October 2003 A-27 No. 3: Water Seeping into Drifts
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A-28 No. 3: Water Seeping into Drifts 
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October 2003
APPENDIX B 
USING TEST DATA TO REDUCE UNCERTAINTY IN 
TOTAL SYSTEM PERFORMANCE ASSESSMENT SEEPAGE ABSTRACTION 
(RESPONSE TO TSPAI 3.25) 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003
Revision 2 
Note Regarding the Status of Supporting Technical Information 
This document was prepared using the most current information available at the time of its development. This 
Technical Basis Document and its appendices providing Key Technical Issue Agreement responses that were 
prepared using preliminary or draft information reflect the status of the Yucca Mountain Projects scientific 
and design bases at the time of submittal. In some cases this involved the use of draft Analysis and Model 
Reports (AMRs) and other draft references whose contents may change with time. Information that evolves 
through subsequent revisions of the AMRs and other references will be reflected in the License Application 
(LA) as the approved analyses of record at the time of LA submittal. Consequently, the Project will not 
routinely update either this Technical Basis Document or its Key Technical Issue Agreement appendices to 
reflect changes in the supporting references prior to submittal of the LA. 
No. 3: Water Seeping into Drifts October 2003
Revision 2 
APPENDIX B 
USING TEST DATA TO REDUCE UNCERTAINTY IN 
TOTAL SYSTEM PERFORMANCE ASSESSMENT SEEPAGE ABSTRACTION 
(RESPONSE TO TSPAI 3.25) 
This appendix provides a response to Key Technical Issue (KTI) agreement Total System 
Performance Assessment and Integration (TSPAI) 3.25. This KTI agreement relates to the 
seepage abstraction and associated parameters used in total system performance assessment 
(TSPA). 
B.1 KEY TECHNICAL ISSUE AGREEMENT 
B.1.1 TSPAI 3.25 
Agreement TSPAI 3.25 was reached during the U.S. Nuclear Regulatory Commission 
(NRC)/U.S. Department of Energy (DOE) Technical Exchange and Management Meeting on 
Total System Performance Assessment and Integration held August 6 to 10, 2001, in 
Las Vegas, Nevada (Reamer 2001), which was convened to discuss four TSPAI KTI subissues: 
(1) system description and demonstration of multiple barriers; (2) scenario analysis within the 
TSPA methodology; (3) model abstraction within the TSPA methodology; and (4) demonstration 
of the overall performance objective. During the course of the technical exchange, TSPAI 3.25 
was reached in the area of Subissue 3. 
The wording of the agreement is as follows: 
TSPAI 3.251 
DOE should use the Passive Cross Drift Hydrologic test, the Alcove 8Niche 3 
tests, the Niche 5 test, and other test data to either provide additional confidence 
in or a basis for revising the TSPA seepage abstraction and associated parameter 
values (e.g., flow-focusing factor, van Genuchten alpha for fracture continuum, 
etc.), or provide technical basis for not using it (UZ2.3.4). DOE will utilize field 
test data (e.g., the Passive Cross Drift Hydrologic test, the Alcove 8Niche 3 tests, 
the Niche 5 test, and other test data) to either provide additional confidence in or a 
basis for revising the TSPA seepage abstraction and associated parameter values 
(e.g., flow-focusing factor, van Genuchten alpha for fracture continuum, etc.), or 
provide technical basis for not using it. This will be documented in Seepage 
Calibration Model and Seepage Testing Data AMR (MDL-NBS-HS-000004) 
expected to be available to NRC in FY 2003. 
1UZ2.3.4 refers to the TSPAI Technical Exchange and Management Meeting held August 6 through 10, 2001, in 
Las Vegas, Nevada, regarding flow paths in the unsaturated zone, Acceptance Criterion 3, Item 4 (Reamer 2001). 
October 2003 B-1 No. 3: Water Seeping into Drifts
Revision 2 
B.1.2 Related Key Technical Issue Agreements 
KTI agreement Unsaturated and Saturated Flow Under Isothermal Conditions (USFIC) 4.01 is 
related to TSPAI 3.25 in that it also requires documentation of test plan and test results, 
including the Passive Cross-Drift Hydrologic test, the Alcove 8Niche 3 (also referred to as 
Niche 3107) tests, and the Niche 5 (also referred to as Niche 1620) test. USFIC 4.01 is 
addressed in Appendix C. 
B.2 RELEVANCE TO REPOSITORY PERFORMANCE 
This KTI agreement relates to gaining additional confidence in the seepage abstraction and in 
associated parameter values. Data from hydrologic tests such as the Passive Cross-Drift 
Hydrologic test, Alcove 8Niche 3 tests, the Niche 5 test, and the Systematic Hydrologic 
Characterization tests are available for seepage model calibration and validation and to provide 
additional confidence in the seepage abstraction. 
The agreement stems from the NRC concern that previous seepage tests in Niche 2 (also referred 
to as Niche 3650) yielded results that may be biased by ventilation dryout, the close proximity of 
the injection boreholes to the niche ceiling, and the injection rates that are much higher than 
ambient percolation flux. The NRC was also concerned that the range of permeability developed 
from air-injection tests in Niche 2 may not include or appropriately bound the permeability 
variability in the lower lithophysal unit. NRC staff requested the DOE to provide additional 
confidence in the calibrated fracture properties and to demonstrate the estimated alpha values are 
consistent with the largest apertures typical for the grid-block scale. The NRC also requested 
further clarification on the incorporation of the alpha parameter uncertainty into the TSPA 
seepage abstraction (NRC 2002). 
The agreement is relevant to the repository performance since the abstraction of seepage and the 
associated parameter values are directly used in TSPA calculations and in the evaluation of the 
unsaturated zone barrier. 
B.3 RESPONSE 
The KTI agreement pertains to the documentation and use of subsurface seepage and tracer tests 
(1) as a basis for revising the TSPA seepage abstraction or (2) to provide additional confidence 
in the TSPA seepage abstraction and associated parameter sets. The field testing specifically 
aimed at resolving seepage-related issues has been expanded significantly since the initial 
short-term, small-volume liquid-release tests conducted in Niche 2. The new tests provide the 
relevant data of sufficient quality to address the NRC concern related to the early tests. All 
available field test data were reviewed and considered for inclusion in the seepage models. Data 
from the previous Niche 2 tests are no longer used for the determination of seepage-relevant 
parameters but only for the validation of the seepage calibration model. 
The first part of the response to this KTI agreement (Section B.3.1) addresses the direct 
quantitative use of data from subsurface tests (including the Niche 5 test and Systematic 
Hydrologic Characterization test) in revising analyses and models and subsequently the TSPA 
seepage abstraction. The second part (Section B.3.2) deals with the subsurface tests (including 
Alcove 8Niche 3 tests and Passive Cross-Drift Hydrologic tests) that provided confidence in the 
October 2003 B-2 No. 3: Water Seeping into Drifts
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seepage models and abstraction by corroborating the conceptual seepage model. These first 
two parts discuss the use of the available data in support of seepage abstraction and the 
determination of seepage-relevant parameters. The last part (Section B.3.3) discusses the 
seepage-relevant parameters that could not directly be estimated from the available test data, 
such as the flow-focusing factor. The technical basis for these responses is provided in 
Section B.4. 
B.3.1 Revision of the Total System Performance Assessment Seepage Abstraction and 
Related Parameters 
The data basis and modeling approach supporting seepage abstraction have been greatly widened 
and improved since the first revision of the TSPA seepage model, substantially reducing 
uncertainties in the seepage-relevant parameters and the subsequent predictions of seepage into 
waste emplacement drifts. Data from the Enhanced Characterization of the Repository Block 
(ECRB) Systematic Hydrologic Characterization tests and Niche 5 were used by the seepage 
calibration model for the determination of seepage-relevant parameters for the lower lithophysal 
zone (Tptpll) of the Topopah Spring Tuff. Data from Niches 3 and 4 (also referred to as 
Niches 3107 and 4788, respectively) were used for parameter estimation in the middle 
nonlithophysal zone (Tptpmn) of the Topopah Spring Tuff. Relative humidity has been 
monitored, and evaporation effects have been included in the model used to analyze the 
seepage-rate data. All estimates of air permeability and capillary strength (1/) have been 
compiled in a comprehensive analysis to determine their spatial variability and uncertainty. 
B.3.1.1 Systematic Hydrologic Characterization Tests and Niche 5 Tests (Lower 
Lithophysal Zone) 
Data from air-injection and liquid-release tests conducted in Niche 5 and in the ECRB for 
Systematic Hydrologic Characterization were used to determine seepage-relevant parameters 
(specifically permeability and capillary strength), thus providing a defensible basis for and 
additional confidence in the revision of the TSPA seepage abstraction. These data were used in a 
quantitative manner for the estimation of seepage-relevant parameters for the lower lithophysal 
zone. The data were also used to validate the process model. 
These data directly reflect the seepage process (1) in the hydrogeologic unit of interest and (2) on 
the scale of interest. In addition, their use in a procedure that yields model-related parameters 
provided the basis to quantify and reduce the uncertainty of the subsequent seepage predictions. 
Relative humidity and evaporation-rate data were incorporated into the process model to reduce 
the potential bias introduced by evaporation effects within the drifts. The data from these tests 
are described in In Situ Field Testing of Processes (BSC 2003a, Sections 6.2 and 6.11); the 
analysis of the data is discussed in Seepage Calibration Model and Seepage Testing Data (BSC 
2003b). 
Niches 3 and 4 (Middle Nonlithophysal Zone) B.3.1.2 
Part of the test data from Niches 3 and 4 were used to determine seepage-relevant parameters for 
the middle nonlithophysal zone. The remaining test data were used for model validation. An 
analysis was performed to demonstrate that evaporation in the closed-off niches with near 
October 2003 B-3 No. 3: Water Seeping into Drifts
Revision 2 
100 percent relative humidity was insignificant and did not lead to a bias in the estimated 
parameters. This additional study increased the confidence in the previously obtained estimates 
of seepage parameters for the middle nonlithophysal zone. The data from these tests are 
described in In Situ Field Testing of Processes (BSC 2003a, Section 6.2); the analysis of the data 
is discussed in Seepage Calibration Model and Seepage Testing Data (BSC 2003b). 
B.3.2 Confidence Building in the Total System Performance Assessment Seepage 
Abstraction 
The Passive Cross-Drift Hydrologic test, the Alcove 8Niche 3 Test, and liquid-release tests in 
Niche 2 were not used for the determination of seepage-relevant parameters. However, several 
aspects of these tests are used to confirm the current understanding of the seepage process and 
corroborate the corresponding conceptual models and analyses underlying the TSPA seepage 
abstraction as outlined below. 
Passive Cross-Drift Hydrologic Tests B.3.2.1 
These tests included monitoring of moisture in boreholes; measurement of in-drift temperature, 
humidity and barometric pressure; visual inspection of wetness; and chemical/isotopic analyses 
of water samples. These observations were conducted in ventilated and nonventilated sections of 
the ECRB Cross-Drift. The data available to date are not sufficient to conclusively identify the 
source of the observed moisture. However, the limited available data of temperature and relative 
humidity gradients suggest that condensation accounts for most of the observed water 
(BSC 2003a, Section 6.10). The issue is further discussed in the response to USFIC 4.01 
(Appendix D). 
Alcove 8Niche 3 Tests B.3.2.2 
In the first phase of Alcove 8Niche 3 testing, where water was injected along a fault exposed in 
Alcove 8, the observed wetting-front advance and wetting plume showed that flow occurred 
predominantly along the fault zone. This precluded the data from being used for calibration or 
validation of the drift-scale seepage model and its abstraction, which is concerned with seepage 
from fractured rocks in the lithophysal and nonlithophysal zones and specifically located in areas 
free of faults. However, these tests along with other modeling efforts (BSC 2003c) provide 
corroboration and build confidence in the seepage models. The seepage rate observed in Niche 3 
was consistently less than 10 percent of the infiltration rate (after the seepage rate had stabilized). 
This low fraction of seepage is consistent with the general seepage concept used in the seepage 
process models. 
Niche 2 Tests B.3.2.3 
The short-term tests conducted in Niche 2 were significantly influenced by storage effects and 
the local properties of a few fractures connecting the release point with the niche ceiling. Thus, 
the data were not suitable for quantitative calibration of the seepage process model. However, 
they provided qualitative seepage information that generally agrees with the conceptual model of 
seepage and were used for model validation purposes. The data from these tests are described in 
In Situ Field Testing of Processes (BSC 2003a, Section 6.2); the analysis of the data is discussed 
in Seepage Calibration Model and Seepage Testing Data (BSC 2003b). 
October 2003 B-4 No. 3: Water Seeping into Drifts
Revision 2 
B.3.3 Seepage-Relevant Parameters That Could Not Be Estimated from Test Data 
The concept of flow focusing describes potential concentration of downward flow onto a 
particular drift segment as governed by intermediate-scale heterogeneity on the order of a few 
drift diameters. It is required to relate the percolation flux calculated with the mountain-scale 
model of the unsaturated zone with the drift-scale, seepage prediction model. All the 
liquid-release test data available refer to a scale on the order of one drift diameter, and are thus 
insufficient to provide direct quantitative estimation of the flow-focusing factor. Therefore, 
flow-focusing factors for the TSPA for the license application (LA) seepage abstraction were 
derived from models that are able to describe the immediate-scale heterogeneity, bridging the 
gap between the site scale and the drift scale models (Bodvarsson et al. 2003; BSC 2003c, 
Section 6.6.3). 
The information in this report is responsive to agreement TSPAI 3.25 made between the DOE 
and NRC. The report contains the information that DOE considers necessary for the NRC to 
review for closure of this agreement. 
B.4 BASIS FOR THE RESPONSE 
B.4.1 Revision of the Total System Performance Assessment Seepage Abstraction and 
Related Parameters 
The data basis and modeling approach supporting seepage abstraction have been greatly widened 
and improved since the first revision of the TSPA seepage model, substantially reducing 
uncertainties in the seepage-relevant parameters and the subsequent prediction of seepage into 
waste emplacement drifts. Relative humidity has been monitored, and evaporation effects have 
been included in the models used to analyze the seepage-rate data. All estimates of permeability 
and capillary strength have been compiled in a comprehensive analysis to determine their spatial 
variability and uncertainty. 
Relative humidity and evaporation rate data from Niche 5 tests were utilized to calibrate a 
diffusive evaporation model under various ventilation conditions (BSC 2003b, Section 6.6.1.4). 
The calibrated evaporation boundary layer thicknesses and relative humidity measurements were 
used to model evaporation from the drift walls for the Niche 5 and Systematic Hydrologic 
Characterization tests. Analysis of seepage rates at high drift relative humidity values showed 
that the effect of evaporation on modeled evaporation rate is insignificant for relative humidity 
values greater than 85 percent (BSC 2003b, Section 6.6.1.4). As a result, evaporation was not 
modeled for the closed off and artificially humidified Niches 3 and 4. 
Data from Niche 5 tests and other tests were used to determine permeability and capillary 
strength and to provide a basis for additional confidence in the revision of the TSPA seepage 
abstraction. The air-injection data were used to generate spatially correlated permeability maps 
for the drift-scale models. At the scale of individual grid blocks of the drift-scale models, a high, 
effective (continuum) permeability may be attributed to larger fracture apertures (which implies 
low capillary strength) or to higher fracture density (which would not affect capillary strength). 
Because the potential correlation between permeability and capillary strength is unknown, the 
van Genuchten 1/ parameter is interpreted as an effective parameter taken to be constant for a 
October 2003 B-5 No. 3: Water Seeping into Drifts
Revision 2 
given test bed in the drift-scale models. The seepage calibration model was used to estimate the 
van Genuchten 1/ parameters for the lower lithophysal and middle nonlithophysal zones (Tptpll 
and Tptpmn) of the Topopah Spring tuff unit by calibrating the drift-scale seepage models 
against the field liquid-release test data. To quantify a key aspect of the uncertainty in the van 
Genuchten 1/ parameter provided to TSPA-LA seepage abstraction, the seepage calibration 
model utilized multiple realizations of permeability field for each test bed. The mean value 
computed from the multiple 1/ estimates was considered as representative for the respective test 
bed. 
Each seepage data set is obtained from a certain test bed that can be considered one realization 
from a number of statistically similar geologic systems. The lack of knowledge regarding the 
details of this specific realization makes the inversely determined van Genuchten 1/ parameter 
estimate uncertain. This estimation uncertainty was analyzed by performing multiple inversions 
of the same data set using different realizations of the underlying heterogeneous permeability 
field. The estimated 1/ parameter for each test bed was represented using probabilistic 
distributions (instead of a single value) (BSC 2003d, Section 6.34). The mean van Genuchten 
1/ values corresponding to the different test beds were compiled to provide spatial variability of 
the 1/ parameter. The uncertainty in the probability distribution chosen to represent the spatial 
variability was accounted for by varying the mean of the chosen (uniform) probability 
distribution within appropriate ranges. A symmetric triangular distribution was chosen to 
provide the random adjustment of the mean because it is an appropriate model for uncertain 
quantities whose most likely value and estimated range of parameters are known. The chosen 
uncertainty distribution also accounts for other potential sources of uncertainty such as 
measurement uncertainty (BSC 2003d, Section 6.6.1.3). 
In the drift-scale models, the van Genuchten 1/ parameter is conceptualized as an effective 
property that represents not only the average hydraulic characteristics of individual fractures but 
also the connectivity, density, geometry, and orientation of the fracture network as it relates to 
the geometry and orientation of the underground opening. The effective parameter also 
incorporates seepage processes that cannot be explicitly implemented in the conceptual model 
(such as film flow and small-scale roughness in the drift ceiling). Therefore, the estimated 
van Genuchten 1/ values are not expected to be representative of only the largest apertures on 
the drift-wall. 
The conceptual model and approach developed for the seepage calibration model were used in 
the seepage model for performance assessment to predict seepage threshold and seepage 
percentage for a variety of hydrogeologic conditions and percolation fluxes. The seepage model 
for performance assessment simulations were also performed with 20 realizations of the 
permeability map for each parameter set. 
The seepage calibration model and seepage model for performance assessment provided the 
TSPA-LA seepage abstraction with the basis for determining the distributions and uncertainties 
of the van Genuchten 1/ parameter, seepage rates, and seepage percentages. The TSPA-LA 
seepage abstraction utilizes appropriate air-injection test data to derive the spatial distribution of 
the absolute permeability. Analysis of preexcavation measurements in the middle nonlithophysal 
zone (Niches 1 (also referred to as Niche 3566), 2, 3, and 4) is provided in In Situ Field Testing 
October 2003 B-6 No. 3: Water Seeping into Drifts
of Processes (BSC 2001, Table 6.1.2-3), giving the mean and standard deviation of the 
small-scale permeabilities. Statistical parameters for preexcavation air-permeability data from 
the lower lithophysal zone (measured in Niche 5) were calculated in Abstraction of Drift Seepage 
(BSC 2003d, Attachment III). Postexcavation permeability data for the middle nonlithophysal 
zone (measured in Niches 2, 3, and 4) and the lower lithophysal zone (measured in Niche 5 and 
systematic testing borehole SYBT-ECRB-LA#2) were analyzed in Seepage Calibration Model 
and Seepage Testing Data (BSC 2003b, Section 6.5.2 and Table 10). The mean values and the 
standard deviations of all appropriate small-scale permeability data conducted at each of the test 
locations are summarized in Table B-1, for both undisturbed and disturbed conditions. Here, 
standard deviations reflect spatial variability within the test bed, on a 1-foot test interval scale. 
The intermediate-scale variability of permeability refers to the variation of this parameter and 
was determined from the means of small-scale permeability measurements within the repository 
rock units (BSC 2003d). In addition, all available permeability data from surface-based 
boreholes and underground test beds were reviewed, appropriate scaling laws were developed, 
and the data were compiled to determine the permeability distribution reflecting spatial 
variability and uncertainty. 
Niche 3 (Tptpmn) 
Niche 1 (Tptpmn) 
Niche 2 (Tptpmn) 
Niche 4 (Tptpmn) 
Niche 5 (Tptpll) 
SYBT-ECRB-LA#2 (Tptpll) 
Table B-1. Summary Statistics of Air Permeabilities Derived from Small-Scale Air-Injection Tests for 
Undisturbed and Excavation-Disturbed Conditions in the Middle Nonlithophysal Zone 
Disturbed Permeability 
Mean log(k) 
-12.14 
 
-11.66 
-11.79 
-10.95 
-10.73 
Std. Dev. 
0.80 
 
0.72 
0.84 
1.31 
0.21 
October 2003 
(Tptpmn) and the Lower Lithophysal Zone (Tptpll) 
Location 
Undisturbed Permeability 
Mean log(k) 
-13.4 
-13.0 
-13.4 
-13.0 
-11.5 
 
Std. Dev. 
B-7 
0.70 
0.92 
0.81 
0.85 
1.12 
 
Source: BSC 2003c, Table 6.6-3. 
The following sections describe the use of the liquid-release and air-injection test data from 
Niche 5, Systematic Hydrologic Characterization, as well as Niches 3 and 4 for the calibration 
and validation of the seepage calibration models for the lower lithophysal zone and middle 
nonlithophysal zone. 
B.4.1.1 Niche 5 and Systematic Hydrologic Characterization Tests (Lower Lithophysal 
Zone) 
Summaries of the test data and analyses for Niche 5 and the Systematic Hydrologic 
Characterization are provided in the responses to KTI USFIC 4.01 (Sections D.4.8 and D.4.9, 
respectively). The data from these tests are described in In Situ Field Testing of Processes (BSC 
2003a, Sections 6.2 and 6.11); the analyses of the data are discussed in Seepage Calibration 
Model and Seepage Testing Data (BSC 2003b). 
No. 3: Water Seeping into Drifts 
Revision 2
Revision 2 
A total of 61 air-injection tests were conducted in boreholes excavated above Niche 5. These 
tests provided geostatistical information of the absolute permeability (mean, standard deviation, 
and correlation length), which was used for the generation of a stochastic permeability map of 
the test zones for the seepage calibration model. The generated spatially correlated permeability 
field is conditioned on the measured postexcavation air-permeability data (Figure B-1), as shown 
in Figure B-2. 
Source: BSC 2003b, Figure 11. 
Figure B-1. Postexcavation Permeability Data of Niche 5, Borehole 3 and the Corresponding 
Generated Permeability Values from One Representative Realization, Which Honors the 
Measured Data 
Source: BSC 2003b, Figure 15b. 
NOTE: In this visualization, the mesh is split into two parts to expose the borehole (indicated by thick black line 
and the injection interval (thick white line). Multiple realizations of the permeability field are generated. 
Note the rough ceilings as well as the left and right slots. 
Figure B-2. Numerical Grid with One Realization of the Permeability Field Used for the Simulation of 
Liquid-release Tests Conducted in Niche 5 Borehole 5 
October 2003 B-8 No. 3: Water Seeping into Drifts
Revision 2 
In Niche 5, a total of 13 liquid-release tests were conducted. Of these, two long-term tests were 
used for calibration of the seepage calibration model, and five were used for model validation. 
Data from some of the test events were not used because of data logger, packer, and pumping 
problems, or because seepage partially bypassed the capture system (for details, see BSC 2003b, 
Table 11). Comparison between seepage-rate data from a liquid-release test conducted in 
borehole #5 (28 to 29 ft) and simulation results for a single realization of the calibrated model is 
given in Figure B-3. 
Source: BSC 2003b, Figure 27. 
NOTE: Blue symbols represent measured data; the red line is the calculated seepage rate. The measured release 
rates are shown in dark gray; the black solid line shows the injection rate used in the model. 
Figure B-3. Calibration of Seepage-Rate Data from Liquid-Release Tests Conducted in Interval 28 to 
October 2003 B-9 
29 ft of Borehole 5 in Niche 5 
During two concurrent liquid-release tests in borehole #5 (28 to 29 ft) and borehole #3 
(21 to 22 ft) (BSC 2003b, Figure 27), seepage water was collected from the tarp underneath the 
left batwing (slot). Note that the slot was inaccessible to visually confirm if water collected in 
the tarp was from the slots or the edges of the main niche (see response to KTI agreement 
USFIC 4.01). Seepage into the slot of comparable magnitude was also observed in the seepage 
model that was calibrated by matching the total modeled seepage rate (including seepage into the 
main niche and the slot) to the measured total seepage rate. These measurement and model 
results of seepage into the side slots (shown in Figure B-4) provide additional direct evidence 
that flow diversion around the opening occurs, corroborating the capillary barrier concept for 
openings excavated in unsaturated formations. 
No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003b, Figure 35. 
NOTE: Liquid was released in interval 28 to 29 ft of borehole 5. 
Figure B-4. Water Collected in the Slot on the Side of Niche 5, Proving Flow Diversion around the 
October 2003 B-10 
Opening 
The Systematic Hydrologic Characterization included air-injection tests in 6-ft-long 
(approximately 1.8-m-long) intervals of borehole SYBT-ECRB-LA#2, providing an estimate of 
mean log-permeability at the experimental site of -10.73 (corresponding to a permeability of 
1.86  10-11 m2) that was used in the generation of a permeability map for the test zone. A 
representative realization of the permeability map is shown in Figure B-5. 
No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003b, Figure 14. 
NOTE: Only half of the drift is simulated because of symmetry. The vertical position of the injection interval 
(indicated in light gray) is appropriately adjusted for the simulation of seepage experiments conducted in 
other test zones. 
Figure B-5. Numerical Grid with One Realization of the Permeability Field Used for the Simulation of 
Liquid-Release Tests Conducted in Zone 2 of Borehole SYBT-ECRB-LA#2 
As part of the Systematic Hydrologic Characterization tests, a total of 26 liquid release tests were 
conducted in boreholes SYBT-ECRB-LA#1, SYBT-ECRB-LA#2, and SYBT-ECRB-LA#3. Of 
these, 11 were used for calibration of the seepage calibration model and 14 were used for model 
validation. One test in SYBT-ECRB-LA#3 failed because the zone was too tight, and the test 
was not utilized. Comparison between seepage-rate data from liquid-release tests conducted in 
SYBT-ECRB-LA#2 and simulation results for a single realization of the calibrated seepage 
model is given in Figure B-6. 
October 2003 B-11 No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003b, Figure 23. 
NOTE: Blue symbols represent measured data; the red line is the calculated seepage rate. The measured release 
rates are shown in dark gray; the black solid line shows the injection rate used in the model. 
Relative-humidity data are shown as a green dashed line. 
Figure B-6. Calibration of Seepage-Rate Data from Liquid-Release Tests Conducted in Zone 3 of 
October 2003 B-12 
Borehole SYBT-ECRB-LA#2 
Evaporation, relative humidity, and temperature measurements conducted inside and outside the 
closed-off Niche 5 were used to calibrate a conceptual model of evaporation. This calibrated 
evaporation model was subsequently incorporated into the seepage calibration model developed 
for the analysis of seepage data from Niche 5 and Systematic Hydrologic Characterization tests. 
Considering the low variability of relative humidity in the closed-off Niche 5, a constant relative 
humidity value of 85 percent was used throughout the inversions and validations. For the 
Systematic Hydrologic Characterization tests, measured relative-humidity values were used as 
boundary conditions in the ECRB, driving evaporation. As shown in Figure B-6, fluctuations in 
seepage rate can be correlated to the drastic changes in relative humidity, which drives 
evaporation. The model captures this evaporation effect reasonably well, tracking increases in 
measured seepage rates as relative humidity increases and vice versa. The rather complex 
system behavior, which includes expansion and shrinkage of the liquid plume along the drift 
surface, signifies the importance of handling unsaturated flow, seepage, and evaporation in a 
fully coupled manner. This explicit consideration of evaporation in the seepage calibration 
model has reduced a potential bias in the estimated parameters, increasing the confidence in the 
parameter distributions used in the TSPA seepage calculations. The results provide confidence 
that the conceptual model represents the key processes and their interactions appropriately, 
including: 
1. Unsaturated flow using a continuum representation of fracture flow based on the 
Richards equation (BSC 2003b, Section 6.6.1.1); 
No. 3: Water Seeping into Drifts
Revision 2 
2. Seepage into the opening, accounting for the capillary-barrier effect (BSC 2003b, 
Section 6.6.1.2); 
3. Vaporization of water from the drift surface, using a simplified evaporation model 
(BSC 2003b, Section 6.6.1.3). 
In summary, the air-injection and liquid-release tests conducted in Niche 5 and the Systematic 
Hydrologic Characterization Tests were used to determine the seepage-relevant parameters 
(specifically permeability and capillary strength) of the lower lithophysal zone (Tptpll) and 
provided additional confidence in the conceptual model used to simulate seepage and related 
processes (e.g., evaporation). 
Niches 2, 3, and 4 (Middle Nonlithophysal Zone) B.4.1.2 
A total of 225 air-injection tests were performed in 10 boreholes above Niches 2, 3, and 4. The 
geostatistics of these permeabilities were used to generate stochastic permeability fields for the 
niches (BSC 2003b, Section 6.6.2.1). Meshes created for simulation of liquid-release tests in 
Niches 2, 3, and 4 are shown in Figure B-7. 
In Niche 3, liquid-release tests were conducted in two intervals, borehole UM 4.885.18 and 
borehole UL 5.495.80. Only some of the tests in UM 4.885.18 resulted in seepage and were 
suitable for calibration. Of these, three tests that resulted in seepage were simultaneously used 
for calibration to provide a single van Genuchten 1/ value of 741 Pa, representative for the 
conditions at Niche 3 (see also Section B.4.2.2). The remaining tests were used to validate the 
process model. Because Niche 3 was closed off by a bulkhead, and the relative humidity was 
expected to be high, evaporation was not explicitly considered in the calibration and validations 
models. 
In Niche 4, twelve liquid-release tests were conducted in three intervals (UL, 7.62 to 7.93 m; 
UM, 6.10 to 6.40 m; and UR, 5.18 to 5.48 m). Of these, 6 tests (2 tests per interval) were used 
for calibration to provide one van Genuchten 1/ value for each of the boreholes UL, UM, and 
UR. The remaining tests were used to validate the process model. Because Niche 4 was closed 
off by a bulkhead and artificially humidified to get close to 100 percent relative humidity, 
evaporation was not explicitly considered in the calibration and validations models. 
Comparisons between seepage-rate data from liquid-release tests conducted in three different 
borehole intervals of Niche 4 and simulation results of the calibrated seepage model are given in 
Figure B-8. 
October 2003 B-13 No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003b, Figure 16. 
NOTE: Note that the meshes are shown from an angle below horizontal to display the ceiling roughness 
incorporated into meshes (c) and (d). 
Figure B-7. Computational Meshes and Permeability Field for Three-Dimensional Seepage Calibration 
Model Used for the Analysis of Seepage Data from (a) Niche 2, Centered 4.42 m from the 
Collar of Borehole UM, (b) Niche 2, Centered 5.64 m from the Collar of Borehole UM, 
(c) Niche 3, Centered at Station 00+10.25 m, and (d) Niche 4, Centered at Station 
00+11.45 m 
In summary, liquid-release tests from Niches 3 and 4 were used in a quantitative way for 
calibration and validation of the seepage calibration model, providing four van Genuchten 1/ 
values that represent the middle nonlithophysal unit. Liquid-release test data from Niche 2 were 
not used in the calibration but provided qualitative support to the seepage models and were used 
for model validation, as outlined in Section B.4.2.3. 
October 2003 B-14 No. 3: Water Seeping into Drifts
Source: BSC 2003b, Figure 31. Data from a given interval are inverted simultaneously. 
Figure B-8. Comparison between Simulated and Measured Seepage Rates from Six Liquid-Release 
Tests Conducted in Three Different Borehole Intervals of Niche 4 
B-15 No. 3: Water Seeping into Drifts 
Revision 2 
October 2003
Revision 2 
B.4.2 Confidence Building in the Total System Performance Assessment Seepage 
Abstraction 
The data from the Passive Cross-Drift tests, Alcove 8Niche 3 tests, and Niche 2 tests can be 
used to (1) qualitatively confirm DOEs understanding of the seepage process and 
(2) corroborate the corresponding conceptual models and analyses underlying the seepage 
abstraction. These aspects are discussed in subsequent sections. 
Passive Cross-Drift Hydrologic Tests B.4.2.1 
The results of the Passive Cross-Drift Hydrologic tests are provided in detail in In Situ Field 
Testing of Processes (REV 01, BSC 2001; REV 02B, BSC 2003a, Section 6.10). Summaries of 
the major features of these tests are given in the responses to KTI USFIC 4.01. 
A long section of the ECRB close to the portal was open to the prevailing ventilation conditions 
of the tunnel. Tests under this ventilated regime were aimed at checking whether seepage could 
occur under natural percolation flux conditions. In the ventilated drift sections of the ECRB 
Cross-Drift, no continuous dripping (or seepage) was observed. The absence of seepage could 
imply (1) sufficiently strong capillary forces keeping the percolating water inside the formation 
and thus preventing seepage and (or) (2) significant evaporation removing potentially seeping 
water. Both of these aspects of seepage exclusion (strong capillary barrier and evaporation) were 
integral parts of the seepage calibration model (BSC 2003b, Section 6.3.1) that provided 
seepage-relevant formation parameters to the seepage abstraction and TSPA calculations. 
The terminal section of the ECRB Cross-Drift was closed off by a series of bulkheads to 
minimize ventilation effects. Within these isolated sections, barometric pressure, relative 
humidity, and temperature were measured at various stations. The evaporation rate was not 
monitored in the Cross-Drift. Periodically, the bulkhead doors sealing the nonventilated sections 
were opened for observations. Water samples were collected and were subsequently analyzed to 
determine if water originated from seepage or condensation. These tests are aimed at evaluating 
seepage and moisture dynamics under nonventilated conditions (i.e., when near-ambient 
conditions are re-established in the repository). 
The relative humidity values measured in the closed-off sections were almost constant from 
July 2000 to May 2001, as shown in Figure B-9a. In the two zones between the first and third 
bulkheads, the relative humidity remained close to 95 percent, with some changes observed in 
March 2001, when the humidity in the second zone gradually fell closer to 90 percent. During 
late January 2001, the relative humidity in these sections dropped drastically when the bulkheads 
were opened for visual inspection. The relative humidity recovered to its original value very 
rapidly after the bulkheads were closed again. Similar drastic declines and rises of temperature 
were also observed in the innermost section, as seen in Figure B-9b. 
October 2003 B-16 No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003a, Section 6.10.2.1. 
Note: Station 15+02 is before the first bulkhead. Stations 21+40 and 25+52 are behind the bulkheads. 
Figure B-9. (a) Relative Humidity and (b) Temperature Measured in the Enhanced Characterization of 
October 2003 B-17 
the Repository Block Cross-Drift 
During the entries behind the bulkheads (in the nonventilated sections), moisture was observed 
on rock bolts, ventilation ducts, utility conduits, wire meshes, and painted patches of tunnel 
walls. Puddles of water were observed on the conveyor belt, and drip cloths showed evidence of 
dripping. Observed rust spots and organic growths indicate the prolonged presence of water. 
These observations of moisture on impervious (nonporous) surfaces suggest that the moisture 
originated from condensation. Local thermal gradients (partly induced by electrical equipment 
No. 3: Water Seeping into Drifts
Revision 2 
in the closed-off drift sections) in the ECRB environment near 100 percent relative humidity are 
the likely causes for the observed condensation. 
The initial water samples collected from the puddles on the conveyor belt were dark in color. 
Because the surfaces of the conveyor belt were likely contaminated, the chemical analyses of 
these samples were not expected to provide meaningful signatures of the source of the puddles. 
Subsequent samples were collected from clean containers placed on the conveyor belt. These 
samples were found to be low in chloride and silica content, a characteristic feature of 
condensate. The samples were also found to lack the chemical signature of the construction 
water that is spiked with 20 mg/L of lithium bromide. While these data clearly show that part of 
the observed moisture originated from condensation, they do not rule out or confirm the 
existence of seepage of water from flow through the formation. 
Note that results of in situ moisture monitoring since the construction of the Exploratory Studies 
Facility and ECRB as well as the Drift Scale Test (see Section 3.3.1) indicate no occurrence of 
potential seepage except at the nonventilated sections of the ECRB and Alcove 7. Although the 
origin of moisture and the amount of condensate could not be conclusively determined primarily 
due to test limitations, the effects of seepage including seepage chemistry have been incorporated 
into TSPA (see Sections 4.9 and 4.10 and the technical basis document on the in-drift chemical 
environment). 
In summary, while the origin of moisture could not be conclusively determined, the available 
evidence suggests that condensation effects contributed significantly to the observed water. 
Alcove 8Niche 3 Tests B.4.2.2 
This test is aimed at evaluating unsaturated zone flow, seepage response, and matrix diffusion 
processes. Alcove 8 was excavated off the ECRB Cross-Drift in the upper lithophysal zone. 
Approximately 20 m below the floor of Alcove 8, Niche 3 was excavated off the Exploratory 
Studies Facility in the middle nonlithophysal zone. A nearly vertical fault runs from Alcove 8 to 
Niche 3. The interface between the upper lithophysal zone and middle nonlithophysal zone is 
approximately 15 m below the floor of Alcove 8. The results of Phase I tests concerned with 
infiltration of water along the 5-m-long fault line exposed in Alcove 8 are given in In Situ Field 
Testing of Processes (BSC 2003a, Section 6.12) and UZ Flow Models and Submodels 
(BSC 2003c, Section 7.6). 
In the first phase of the Alcove 8Niche 3 test, water was applied along the fault in Alcove 8 at 
three different times. In the first set, water was released from a 30-cm diameter circular 
infiltrometer. In the second set, water was released from a 70-cm by 70-cm square infiltrometer. 
In the third stage, the approximately 5-m-long fault segment was divided into four sections, and 
ponded infiltration experiments were conducted with a head of approximately 2 cm. 
Two conservative tracers (pentafluorobenzoic acid, or PFBA, and LiBr) were released along the 
fault during a 9-day period. Wetting-front advance and development of a wetting plume were 
monitored using electrical resistance probes installed in boreholes above the ceiling of Niche 3. 
Seepage into Niche 3 was collected by a series of capture trays equipped with an automated 
gauging system. 
October 2003 B-18 No. 3: Water Seeping into Drifts
Revision 2 
The total fault intake (infiltration) and seepage rates collected during the ponded infiltration test 
(Set 3) are plotted in Figure B-10. The velocity of the wetting front computed from the electrical 
resistance probe data of boreholes 9 and 10 is shown in Figure B-11. The fault is about 2 m 
away from the collars of the boreholes. Figure B-11 shows that the wetting front velocity is 
fastest along the fault. 
October 2003 B-19 No. 3: Water Seeping into Drifts
Source: BSC 2003c, Figures 7.6-1 and 7.6-2. 
Figure B-10. (a) Infiltration and (b) Seepage Rate in Alcove 8Niche 3 Test; Phase I, Set 1 (ponded 
infiltration test) 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 B-20
Revision 2 
The Alcove 8Niche 3 tests differ significantly from the niche tests and Systematic Hydrologic 
Characterization tests used in the calibration and validation of the seepage model or its 
abstraction for the following reasons. Primarily, flow of water in the Alcove 8Niche 3 tests was 
dominated by the presence of the near-vertical fault, as demonstrated by the wetting front 
velocity. Secondly, Alcove 8 is located in the upper lithophysal zone, whereas Niche 3 is in the 
middle nonlithophysal zone. Consequently, water released from Alcove 8 encountered the 
slightly dipping interface between the two zones, which may have led to flow diversion and 
potential bypassing of the capture system in Niche 3. Thirdly, the fault in Niche 3 is partially 
outside of the closed-off section behind the bulkhead, i.e., a portion of the potential seepage 
water may have bypassed the capture system in Niche 3 and evaporated. Thus, the tests 
simultaneously encounter two different evaporation regimes (ventilated and nonventilated). 
Because of these differences, the data are likely to introduce a bias in the calibrated properties if 
they are used to calibrate or validate the seepage model. However, the infiltration and seepage 
data provide qualitative corroboration to the general conceptual model of flow in unsaturated 
formations and seepage as outlined below. 
Source: BSC 2003c, Figure 7.6-3. 
(called distance from collar) to the fault is about 2 m. 
NOTE: Observation boreholes are approximately perpendicular to the fault. The distance from a borehole collar 
October 2003 
Figure B-11. Water Travel Velocity Data for Boreholes 9 and 10 
B-21 No. 3: Water Seeping into Drifts
Revision 2 
The infiltration water supplied at the bed of Alcove 8 either (1) is stored in the voids of the 
formation, (2) enters the niche in liquid form (seepage) or vapor form (evaporation), or (3) flows 
around Niche 3 and percolates down to the underlying formations. The seepage rate collected in 
all the trays in Niche 3 reached a maximum value after approximately 70 days (see 
Figure B-10b) and declined gradually afterwards. The infiltration rate also started declining at 
about the same time (see Figure B-10a). The stabilization of the seepage rate is indirect evidence 
that the storage component has reached the maximum level. The fact that flow occurred through 
a narrow range around the fault (see Figure B-11) also implies that storage occurred only in a 
restricted region surrounding the fault. The seepage percentage during this period was 
consistently less than 10 percent. The foregoing observations suggest that 90 percent of the 
infiltration water was either being diverted around Niche 3 or was evaporating. Both of these 
aspects (capillary barrier effect and evaporation) contribute to seepage exclusion; they were 
integral parts of the analysis with the seepage calibration model (BSC 2003b, Section 6.3.1) that 
provided seepage-relevant formation parameters. 
The infiltration rate, seepage rate, wetting front velocity, and tracer breakthrough data were used 
to validate the three-dimensional unsaturated zone flow models (BSC 2003c, Section 7.6). 
Inverse modeling using the seepage rate and wetting-front advance data resulted in a calibrated 
van Genuchten 1/ value of 914 Pa for the fault zone. This value is on the same order as that of 
the fracture continuum of Niche 3 (741 Pa) derived from the seepage calibration model (see 
Section B.4.1.2 above). Deviations between the predicted breakthrough curves of 
two conservative tracers and measured data were within the validation acceptance criteria. 
In summary, the Alcove 8Niche 3 test provided additional confidence in the conceptual model 
of seepage for the following reasons: (1) the low seepage percentage measured in the 
Alcove 8-Niche 3 tests was consistent with the conceptual model of seepage, and (2) the 
calibrated capillary strength parameter for the Alcove 8Niche 3 test is within the same order of 
magnitude as that determined from the analysis of liquid-release tests conducted in Niche 3. 
Niche 2 Tests B.4.2.3 
In Niche 2, liquid-release tests were conducted for short durations. These short-term tests are 
very sensitive to storage effects and the properties of a few fractures connecting the injection 
interval to the niche opening. Thus, the data were used only for validation of the seepage model 
(BSC 2003b, Section 7.3). The data qualitatively agree with the general conceptual model of 
seepage in that seepage rate is significantly less than the release rate. Fifty Monte Carlo 
simulations performed for the prediction of seepage rates in Niche 2 showed that the majority of 
the seepage data (24 out of 27 tests) fall within the range defined by the Monte Carlo simulations 
as shown in Figure B-12. 
October 2003 B-22 No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003b, Figure 45. 
NOTE: Monte Carlo Simulations were performed to estimate the prediction range. 
Figure B-12. Validation of Seepage Calibration Model and Seepage-Relevant Parameters of the Middle 
October 2003 
Nonlithophysal Zone (Tptpmn) Using Data from Niche 2 
Visual inspection of the wetting-front arrival in Niche 2 showed that water migrated along 
several exposed fine fractures from the point of initial arrival (see Figure B-13). It was observed 
that water saturation was building up for 2 minutes in the exposed fracture network in an uphill 
direction, before dripping began. These observations provide empirical evidence that an 
effective capillary barrier was formed while the arriving moisture was being redistributed. The 
barrier collapsed after full saturation was attained locally (Trautz and Wang 2002). 
B-23 No. 3: Water Seeping into Drifts
Revision 2 
Source: Trautz and Wang 2002, Figure 10. 
Figure B-13. Position and Movement of the Wetting Front after Arriving at the Niche Ceiling, Providing 
October 2003 
Evidence of Capillary Barrier Effect in Fractured Rock 
B.4.3 Seepage Related Parameter That Could Not Be Estimated from Test Data 
The concept of flow focusing describes potential concentration of downward flow onto a 
particular drift segment as governed by intermediate-scale heterogeneity. Flow-focusing factors 
should not incorporate large-scale flow distribution (along contacts or faults) nor heterogeneity 
below the spatial resolution of approximately one drift diameter, since small-scale variability (on 
a scale of less than a meter) is explicitly accounted for in the drift-scale seepage models (the 
seepage calibration model, seepage model for performance assessment, and the thermalhydrologic 
seepage models). Within the drift-scale seepage models, flow channeling is due to 
small-scale heterogeneity, which was accounted for by the underlying heterogeneous 
permeability fields. The percolation flux distributions for the TSPA-LA seepage abstraction 
were derived from model results of the unsaturated zone flow and transport model (BSC 2003c). 
These spatial distributions were given separately for three climate stages (present-day, monsoon, 
and glacial transition). Local, drift-scale percolation fluxes were obtained by adjusting the 
large-scale percolation flux using flow-focusing factors. The flow-focusing factors for seepage 
abstraction were derived from high-resolution, intermediate-scale flow models that bridge the 
gap between the site-scale and drift-scale models (Bodvarsson et al. 2003; BSC 2003c, 
Section 6.6.3). 
B-24 No. 3: Water Seeping into Drifts
Revision 2 
B.5 REFERENCES 
Bodvarsson, G.S.; Wu, Y-S.; and Zhang, K. 2003. Development of Discrete Flow Paths in 
Unsaturated Fractures at Yucca Mountain. Journal of Contaminant Hydrology, 62-63, 23-42. 
New York, New York: Elsevier. TIC: 254205. 
BSC (Bechtel SAIC Company) 2001. In Situ Field Testing of Processes. ANL-NBS-HS- 
000005 REV 01. Las Vegas, Nevada: Bechtel SAIC Company. ACC: MOL.20020108.0351. 
BSC 2003a. In Situ Field Testing of Processes. ANL-NBS-HS-000005 REV02B. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: MOL.20030915.0238. 
BSC 2003b. Seepage Calibration Model and Seepage Testing Data. MDL-NBS-HS-000004 
REV 02. Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030408.0004. 
MOL.20030728.0198. 
BSC 2003c. UZ Flow Models and Submodels. MDL-NBS-HS-000006 REV 01. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: DOC.20030818.0002. 
BSC 2003d. Abstraction of Drift Seepage. MDL-NBS-HS-000019 REV 00. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: DOC.20030826.0001. 
NRC (U.S. Nuclear Regulatory Commission) 2002. Integrated Issue Resolution Status Report. 
NUREG-1762. Washington, D.C.: U.S. Nuclear Regulatory Commission, Office of Nuclear 
Materials Safety and Safeguards. TIC: 253064. 
Reamer, C.W. 2001. U.S. Nuclear Regulatory Commission/U.S. Department of Energy 
Technical Exchange and Management Meeting on Total System Performance Assessment and 
Integration (August 6 through 10, 2001). Letter from C.W. Reamer (NRC) to S. Brocoum 
(DOE/YMSCO), August 23, 2001, with enclosure. ACC: MOL.20011029.0281. 
Trautz, R.C. and Wang, J.S.Y. 2002. Seepage into an Underground Opening Constructed in 
Unsaturated Fractured Rock Under Evaporative Conditions. Water Resources Research, 38, 
(10), 6-1 through 6-14. Washington, D.C.: American Geophysical Union. TIC: 253348. 
October 2003 B-25 No. 3: Water Seeping into Drifts
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B-26 No. 3: Water Seeping into Drifts 
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October 2003
Revision 2 
APPENDIX C 
IN SITU FIELD TESTING RESULTS AND ANALYSES 
(RESPONSE TO USFIC 4.01) 
October 2003 No. 3: Water Seeping into Drifts
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Note Regarding the Status of Supporting Technical Information 
This document was prepared using the most current information available at the time of its development. This 
Technical Basis Document and its appendices providing Key Technical Issue Agreement responses that were 
prepared using preliminary or draft information reflect the status of the Yucca Mountain Projects scientific 
and design bases at the time of submittal. In some cases this involved the use of draft Analysis and Model 
Reports (AMRs) and other draft references whose contents may change with time. Information that evolves 
through subsequent revisions of the AMRs and other references will be reflected in the License Application 
(LA) as the approved analyses of record at the time of LA submittal. Consequently, the Project will not 
routinely update either this Technical Basis Document or its Key Technical Issue Agreement appendices to 
reflect changes in the supporting references prior to submittal of the LA. 
No. 3: Water Seeping into Drifts October 2003
Revision 2 
APPENDIX C 
IN SITU FIELD TESTING RESULTS AND ANALYSES 
(RESPONSE TO USFIC 4.01) 
This appendix provides a response for Key Technical Issue (KTI) agreement Unsaturated and 
Saturated Flow under Isothermal Conditions (USFIC) 4.01. This KTI agreement relates to the 
performance and documentation of specific hydrologic tests conducted at Yucca Mountain. 
C.1 KEY TECHNICAL ISSUE AGREEMENT 
C.1.1 USFIC 4.01 
Agreement USFIC 4.01 was first reached during the U.S. Nuclear Regulatory Commission 
(NRC)/U.S. Department of Energy (DOE) Technical Exchange and Management Meeting on 
Unsaturated and Saturated Flow Under Isothermal Conditions held August 16 to 17, 2000, in 
Berkeley, California (Reamer and Williams 2000). During the course of this meeting, 
USFIC Subissue 4, Deep Percolation, was discussed, and KTI agreement USFIC 4.01 was 
reached. 
Subsequent to this technical exchange, NRC staff reviewed agreement USFIC 4.01 and proposed 
modifications to the agreement. This proposal was transmitted in a letter from the NRC to the 
DOE dated June 20, 2001 (Reamer 2001). The proposed revisions were later discussed at the 
NRC/DOE Technical Exchange and Management Meeting on Total System Performance 
Assessment and Integration held August 6 to 10, 2001, in Las Vegas, Nevada. At this meeting, 
an agreement was reached on the final wording of agreement USFIC 4.01 (Reamer and 
Gil 2001). The NRC originally requested some test plans as well as results from several tests 
and modeling studies (Reamer 2001). In reaching the final agreement, the DOE and NRC agreed 
to limit the agreement to test plans and test results, with related modeling issues covered in 
separate agreements. 
The wording of the final agreement is as follows. 
USFIC 4.01 
The ongoing and planned testing are a reasonable approach for a licensing 
application with the following comments: 
Consider a mass balance of water for Alcove 8Niche 3 cross over test; i. 
ii. Monitor evaporation during all testing; 
iii. Provide the documentation of the test plan for the passive cross-drift 
hydrologic test; 
iv. Provide the NRC with any cross-drift seepage predictions that may have 
been made for the passive cross-drift hydrologic test; 
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v. Provide documentation of the results obtained and the analysis for the 
passive cross-drift hydrologic test. This documentation should include the 
analysis of water samples collected during entries into the cross-drift 
(determination whether the water comes from seepage or condensation); 
vi. Provide documentation of the results obtained and the analysis for the 
Alcove 7 test. This documentation should include the analysis of water 
samples collected during entries into Alcove 7 (determination whether the 
water comes from seepage or condensation); 
vii. Provide the documentation of the test plan for the Niche 5 test; 
viii. Provide documentation of the results obtained and the analysis for the 
Niche 5 test; 
ix. Provide documentation of the results obtained and the analysis for the 
Systematic Hydrologic Characterization test; 
x. Provide documentation of the results obtained and the analysis for the 
Niche 4 test; 
xi. Provide documentation of the results obtained from the calcite-filling test. 
Include interpretation of the observed calcite deposits found mostly at the 
bottom of the lithophysal cavities; 
DOE stated that: 
1) A mass balance of water for the Alcove 8Niche 3 test has been considered, 
but is not feasible due to the size of the collection system that would be 
required. A collection system to obtain a mass balance is being developed 
for the Niche 5 test (i); 
2) Evaporation will be monitored for all tests where evaporation is a relevant 
process (ii); 
3) Test plans for Niche 5 and the cross-drift hydrologic tests are expected to be 
available to NRC FY 2002 (iii, viii); 
4) The cross-drift seepage predictions will be documented in the Seepage 
Calibration Model and Seepage Testing Data AMR (MDL-NBS-HS- 
000004) expected to be available to NRC by FY 2003 (iv); 
5) DOE will document the results for the tests identified above (except calcite 
filling observations) in the In-Situ Field Testing of Processes AMR 
(ANL-NBS-HS-000005) expected to be available to NRC in FY 2003 (v), 
(vi), (vii), (ix), (x); 
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6) Results of the calcite filling observations will be documented in Analysis of 
Geochemical Data for the Unsaturated Zone (ANL-NBS-HS-000017) and 
the UZ Flow Models and Submodels (MDL-NBS-HS-000006) expected to 
be available to NRC FY 2003 (xi). 
C.1.2 Related Key Technical Issue Agreements 
Agreement Total System Performance Assessment and Integration (TSPAI) 3.25 covers material 
related to agreement USFIC 4.01. TSPAI 3.25 deals with testing to provide additional 
confidence in, or a basis for revising the total system performance assessment (TSPA) seepage 
abstraction and associated parameter values. The response to TSPAI 3.25 (see Appendix B) is 
based on the same field test data as used in response to USFIC 4.01. 
C.2 RELEVANCE TO REPOSITORY PERFORMANCE 
This KTI agreement relates to the DOE providing more information about ambient-condition 
hydrologic testing in the unsaturated zone at Yucca Mountain. During the August 2000 USFIC 
Technical Exchange (Reamer and Williams 2000), the DOE presentations for Subissue 4, Deep 
Percolation, included a discussion of seepage into emplacement drifts and of unsaturated zone 
flow. The DOE presented the ongoing and planned testing activities to evaluate seepage into 
drifts and stated that the unsaturated zone flow and transport models were extensively calibrated 
and validated against available data. 
The NRC noted that the ongoing and planned testing was a reasonable approach for license 
application but requested the items as identified in the agreement to close this subissue 
(Reamer and Williams 2000). Of particular importance is the ongoing field test in the east-west 
cross-drift in which approximately a 1-km-long section of the tunnel has been sealed off from 
ventilation and is being allowed to return to ambient conditions (NRC 2002, p. 3.3.6-24). The 
NRC also noted that the analysis of calcite abundance would provide some constraints on 
hydrological parameters, percolation flux, and additional evidence for validation of the flow and 
transport model. The NRC acknowledged that this analysis could not give a definitive value or 
narrow range of values (NRC 2002, p. 3.3.6-24). 
The agreement USFIC 4.01 is relevant to the repository performance because results and data 
from the hydrologic tests are relied upon for the development and validation of unsaturated zone 
process models and abstraction models supporting TSPA. 
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C.3 RESPONSE 
In situ testing and monitoring studies are being conducted to directly assess and evaluate the 
proposed waste emplacement environment and the unsaturated zone natural barrier to 
radionuclide transport at Yucca Mountain. For this KTI agreement, the field activities of interest 
are Alcove 8Niche 3 (also referred to as Niche 3107), Niches 4 and 5 (also referred to as 
Niches 4788 and 1620), systematic hydrologic characterization, passive cross-drift hydrologic 
test, Alcove 7, and the calcite filling test. The responses to each aspect of the KTI agreement 
USFIC 4.01 can be summarized as follows, with supporting documentation provided in 
Section C.4: 
i) A mass balance of water was considered for Alcove 8Niche 3, but was not performed 
because the large scale of this test would have required a collection system that was 
considered infeasible. A collection system to obtain a mass balance was therefore 
developed for Niche 5, but its effectiveness was limited, so a complete mass balance 
was not obtained. Details are discussed in Section C.4.1. 
ii) Evaporation was monitored in Niche 5 and for the systematic hydrologic 
characterization tests, and this information was used for the quantitative determination 
of seepage-related parameters. Evaporation was not monitored in Niche 4, the passive 
cross-drift hydrologic test, Alcove 8Niche 3, and Alcove 7, but relative humidity 
measurements were made. Estimates of evaporation can be obtained from the relative 
humidity measurements, coupled with appropriate assumptions about evaporative 
surfaces and impacts of ventilation. Estimates of evaporation for these tests have not 
been performed, however. Evaporation was not a relevant process over the time 
period that calcite observations were performed for the calcite-filling test. See 
Section C.4.2 for more details. 
iii) The test plan for the passive cross-drift hydrologic test is provided in Test Plan for: 
Moisture Monitoring in the ECRB Bulkheaded Cross Drift (BSC 2001a). 
iv) Preliminary seepage predictions for the passive cross-drift hydrologic test are 
described in Test Plan for: Moisture Monitoring in the ECRB Bulkheaded Cross Drift 
(BSC 2001a). A summary is provided in Section C.4.4. 
v) The results and analysis of data from the passive cross-drift hydrologic test are 
provided in In Situ Field Testing of Processes (BSC 2003a) and are summarized in 
Section C.4.5. 
vi) The results from Alcove 7 are documented in In Situ Field Testing of Processes 
(BSC 2003a) and summarized in Section C.4.6. 
vii) The test plan for the Niche 5 test is provided in Test Plan for: Niche 5 Seepage 
Testing (BSC 2001b). 
viii) The results from the Niche 5 seepage tests are documented in In Situ Field Testing of 
Processes (BSC 2003a) and Seepage Calibration Model and Seepage Testing Data 
(BSC 2003b), and are summarized in Section C.4.8. 
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ix) The results from the Systematic Hydrologic Characterization test are documented in In 
Situ Field Testing of Processes (BSC 2003a), and Seepage Calibration Model and 
Seepage Testing Data (BSC 2003b), and are summarized in Section C.4.9. 
x) The results from the Niche 4 seepage tests are documented in In Situ Field Testing of 
Processes (BSC 2003a), and Seepage Calibration Model and Seepage Testing Data 
(BSC 2003b), and are summarized in Section C.4.10. 
xi) The results obtained from the calcite-filling test are documented in Analysis of 
Geochemical Data for the Unsaturated Zone (BSC 2002) and UZ Flow Models and 
Submodels (BSC 2003c) and are summarized in Section C.4.11. 
The information in this report is responsive to agreement USFIC 4.01 made between the DOE 
and NRC. The report contains the information that DOE considers necessary for the NRC to 
review for closure of this agreement. 
C.4 BASIS FOR THE RESPONSE 
C.4.1 Mass Balance 
In an attempt to obtain a mass or rate balance during a liquid-release test, a slot was excavated on 
the side of Niche 5 to capture the water diverted around the niche (see Section C.4.7 for more 
details). The intent of this effort was to demonstrate that the amount of water released to the 
formation was balanced by the amount of water (1) recovered as seepage from the niche ceiling, 
(2) diverted around the opening and recovered in the slot, (3) stored in the formation, and (4) lost 
to evaporation. Since component (3) is difficult to measure, the liquid-release test was run to 
near-steady state, allowing for the calculation of a rate balance (rather than total mass balance) in 
which component (3) becomes insignificant. Water was collected at the side of the niche during 
two seepage tests conducted in Niche 5. However, because of difficulties in excavating the slot 
and installing the capture system, it was not possible to visually confirm if the water collected in 
the tarp underneath the slot was derived entirely from seepage into the slot. Even if we assumed 
all the water collected in the side originated from the slot, the measured data were not suitable 
for model calibration because (1) water could have bypassed the incomplete slot, (2) the seepage 
rates did not reach steady state, or (3) the data were biased by interference from a liquid-release 
test simultaneously conducted in a nearby borehole. While qualitative evidence was obtained 
that the capillary barrier was capable of diverting water around the niche (see also Section C.4.7 
below), a quantitative mass or rate balance based on the measured data alone could not be 
obtained. 
C.4.2 Evaporation Monitoring during Testing 
Evaporation affects seepage-rate data collected during liquid-release tests and thus potentially 
introduces a bias in the estimates of seepage-relevant parameters. Moreover, the evaporation 
potential in the ventilated drifts may mask potential seepage observations. Therefore, an effort 
was made to (1) control relative humidity in seepage test locations, (2) monitor relative humidity 
and (or) evaporation potential, and (3) account for evaporation effects in the analysis of seepagerate 
data (if considered relevant). 
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Evaporation monitoring in the Niche 5 and the systematic hydrologic characterization tests is 
discussed below in Sections C.4.2.1 and C.4.2.2, respectively. The collected data provide a 
sufficient basis for addressing potential evaporation issues during liquid-release testing. For the 
calcite filling observations, evaporation was not a relevant process over the time period that 
calcite observations were performed. Evaporation was not monitored in the Niche 4 test, the 
passive cross-drift hydrologic test, the Alcove 8Niche 3 test, and the Alcove 7 test, but relative 
humidity measurements were made. Estimates of evaporation could be obtained from the 
relative humidity measurements coupled with appropriate assumptions about evaporative 
surfaces and impacts of ventilation. The results from the passive cross-drift test and the 
Alcove 7 test have not, however, been used in quantitative seepage modeling. In the analysis of 
the Niche 4 and Alcove 8Niche 3 test results, evaporation was not incorporated since it was 
assumed to be minimal because the bulkhead doors at the entrance to the niches were closed and 
sealed, and the air space within the niches was artificially humidified. 
Further detail on evaporation measurements during these tests can be found in In Situ Field 
Testing of Processes (BSC 2003a, Sections 6.2, 6.10, 6.11, and 6.12). 
Niche 5 Test C.4.2.1 
The evaporation flux was measured inside Niche 5 (BSC 2003a, Section 6.2.1.3.5.3). Figure C-1 
shows the evaporation flux inside and outside the niche during Test #2 9-17-02. The plot 
indicates that the average evaporation flux outside of the niche is about a factor of 20 greater 
than the average evaporation flux inside the niche. The peak evaporation rates associated with 
the sawtooth pattern observed in the evaporation pan data collected outside the niche correspond 
to refilling the evaporation container with fresh warm water from the tunnel water supply 
system. In Seepage Calibration Model and Seepage Testing Data (BSC 2003b), the evaporation 
in Niche 5 was accounted for in the simulations by calculating an evaporative boundary-layer 
thickness based on the measured evaporation data. 
Systematic Hydrologic Characterization C.4.2.2 
Evaporation pans were combined with wetted area observations to measure evaporation rates for 
the systematic hydrologic characterization (BSC 2003a, Section 6.11.3). Curtains were installed 
to minimize evaporation from the seepage face. Evaporation rates from 9 liquid release tests are 
summarized in Figure C-2. Evaporation was zero at two locations (LA3z3 and LA4z3) and 
ranged from 2.5 ml/min to 32 ml/min in the remaining seven locations. 
October 2003 C-6 No. 3: Water Seeping into Drifts
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Source: BSC 2003a. 
Figure C-1. Evaporation Fluxes Inside and Outside Niche 5 during Test #2 9-17-02 
Source: BSC 2003a, Section 6.11. 
October 2003 
Figure C-2. Measured Evaporation Rates from Systematic Hydrologic Tests 
C.4.3 Test Plan for the Passive Cross-Drift Hydrologic Test 
The test plan for the passive cross-drift hydrologic test is provided in Test Plan for: Moisture 
Monitoring in the ECRB Bulkheaded Cross Drift (BSC 2001a). This test plan is provided to the 
NRC separate from this technical basis document. 
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C.4.4 Cross-Drift Seepage Predictions 
Modeling studies of the bulkhead experiment were carried out in 1996 and 1997 to evaluate the 
changes in moisture conditions in the rock surrounding the drift. The rate and extent of rock 
dryout during the ventilation period and rewetting after installation of the bulkhead were 
evaluated using the site-scale unsaturated zone flow model. In the calculations for dryout, the 
extent of drying was found to be less than 10 m within 100 years (Ahlers et al. 1996). For the 
rewetting period after installation of the bulkhead, the models predicted that the fractures will 
resaturate within 6 months for the reference case, whereas the matrix would require more than 
6 years to completely resaturate (Bodvarsson et al. 1997). 
The probability of seepage in the bulkheaded section of the Enhanced Characterization of the 
Repository Block (ECRB) was evaluated in 2000 based on a methodology similar to that used by 
TSPA at that time. This study assumed that the ECRB had returned to undisturbed moisture 
conditions in the rock for present-day climate. The prediction results were presented at the 
unsaturated zone process model report interactive review held at the Lawrence Berkeley National 
Laboratory on January 10, 2000 (BSC 2001a). Probabilistic seepage predictions of the seepage 
fraction and the seep flow rate into the length of the ECRB cross-drift (1,800 to 2,500 m) were 
performed, with percolation fluxes calculated for present day climate conditions. Flow-focusing 
factors, permeability, and capillary-strength parameters were sampled from probability density 
functions, and seepage rates and seepage fraction extracted from lookup tables calculated by the 
seepage model for performance assessment. 
Defining one seep as water entering a 5-m section of the drift, the predictions indicated there is a 
50 percent chance that one or more seeps would occur in the bulkheaded section of the ECRB, a 
10 percent chance that four or more seeps would occur between 2,000 m and 2,200 m of the 
cross-drift, and a 10 percent chance that two or more seeps would occur between 2,400 and 
2,500 m. A large flow rate was predicted for each of these seeps. This analysis did not consider 
evaporation and associated condensation, which may also be occurring in the ECRB unventilated 
section. 
Note that the abstraction values used for these predictions are not identical to those to be used in 
TSPA-LA. However, the predictions are based on an approach consistent with that used for 
TSPA-SR. The probabilistic seepage predictions cannot be directly compared to data collected 
in the ECRB behind the bulkheads, because it is uncertain if the collected water originated from 
seepage or condensate (see Section 4.5.3.6). Nevertheless, the potential existence of seepage in 
the ECRB is not inconsistent with the probabilistic seepage predictions. 
C.4.5 Results and Analysis for the Passive Cross-Drift Hydrologic Test 
Information for the following sections is based on In Situ Field Testing of Processes 
(BSC 2003a, Section 6.10). 
Test Summary C.4.5.1 
Passive moisture monitoring along the ECRB cross-drift was performed to examine the moisture 
dynamics and distribution in the drift with and without ventilation. In the ventilated drift 
sections, no continuous dripping or confirmed seepage was observed in either the Exploratory 
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Studies Facility (ESF) loop or in the ECRB cross-drift. This lack of seepage may be explained 
by the capillary barrier mechanism, where capillary forces hold water within the rock mass, or by 
the effect of ventilation. Ventilation can remove large amounts of moisture, dry the rock behind 
the drift walls, and suppress seepage. 
C.4.5.2 Ventilation Effects in the Enhanced Characterization of the Repository Block 
Cross-Drift 
Relative humidity data from three moisture stations in the ECRB cross-drift are illustrated in 
Figure C-3 for the month of November 1998, right after the completion of the excavation by the 
tunnel-boring machine and when the ventilation was on. The moisture sensor assembly at ECRB 
cross-drift construction station CD 25+55 (2,555 m from the ECRB cross-drift entrance) is 
located near the Solitario Canyon fault on the western boundary of the repository block. The 
other two stations, at CD 14+43 and CD 21+40, measured the moisture conditions in the middle 
part of the ECRB cross-drift within the repository block. 
The figures illustrate the temporal fluctuations and the spatial distributions of moisture 
conditions along the ECRB cross-drift. The data were collected every 15 minutes. CD 25+55 
was much more humid than the other two stations under the control of the same ventilation 
system. The day shifts had more activities than the other two shifts. 
The spatial variations illustrated in Figure C-4 are based on weekly averaging over the day shifts. 
The differences in relative humidity are more clearly shown with the spatial distribution plot. 
While the magnitude varies from week to week, the spatial gradients were relatively constant. 
The average gradients for the two sections were 3.4 percent per kilometer between CD 14+35 
and CD 21+40, and 25.2 percent per kilometer between CD 21+40 and CD 25+55. The section 
near the end of the tunnel apparently had more moisture removed than the section near the 
entrance. The average relative humidity decreased over the first 3 weeks of November at each 
station, but increased during the fourth week of November. This increase in average relative 
humidity is probably correlated with the ventilation system being shut down over the long 
Thanksgiving weekend. 
C.4.5.3 Observations along Nonventilated Sections of the Enhanced Characterization of 
the Repository Block Cross-Drift 
A series of bulkheads was constructed in the terminal section of the ECRB cross-drift to 
minimize ventilation effects. Barometric pressure, humidity, and temperature are being 
measured at various stations within the drift to provide information on moisture dynamics along 
the ECRB cross-drift. Psychrometers were installed along seven boreholes to measure the water 
potential and thus the extent and rewetting of the dryout zone. The evaporation rate was not 
monitored in the cross-drift. Periodically, the bulkhead doors sealing the nonventilated sections 
were opened for observations. Water samples were also collected during these times and were 
subsequently analyzed to determine if water originated from seepage or condensation. The 
918-m-long drift section is located in the Topopah Spring lower lithophysal (Tptpll) and the 
lower nonlithophysal (Tptpln) tuff units. 
October 2003 C-9 No. 3: Water Seeping into Drifts
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Source: BSC 2003a, Section 6.10. 
NOTE: The data were collected in November 1998 after completion of excavation. The legends are the distances in 
meters from the moisture station to the ECRB cross-drift entrance. 
Figure C-3. Relative Humidity Temporal Variations in the Enhanced Characterization of the Repository 
Block Cross-Drift 
Source: BSC 2003a, Section 6.10. 
NOTE: The weekly averages of day shift data are presented for November 1998 after completion of excavation. 
Figure C-4. Relative Humidity Spatial Variations along the Enhanced Characterization of the Repository 
Block Cross-Drift 
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Barometric-Pressure Variations C.4.5.3.1 
Barometric pressure measured along four locations in the ECRB cross-drift did not show any 
spatial variability but had a pronounced change over time (Figure C-5). The range of the 
temporal variability was between approximately 870 and approximately 905 millibars (mbars). 
From May to September 2000, the barometric pressure along the ECRB cross-drift was restricted 
between approximately 880 and approximately 895 mbars. Larger fluctuations in the barometric 
pressure were observed between October 2000 and May 2001. 
Source: BSC 2003a, Section 6.10. 
Figure C-5. Barometric Pressure Measured along the Enhanced Characterization of the Repository 
C.4.5.3.2 
October 2003 C-11 
Block Cross-Drift 
Temperature Variations Between May 2000 and May 2001 
Temperature measurements along the ECRB cross-drift made over a period of 9 months, starting 
in early August 2000, show a clear temperature gradient extending through the section of the 
ECRB cross-drift behind the bulkhead doors (Figure C-6). 
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Figure C-6. Temperature Measured in the Four Enhanced Characterization of the Repository Block 
Source: BSC 2003a, Section 6.10. 
Cross-Drift Stations 
The highest temperatures were recorded in the zone behind the third bulkhead (Station 26+00), 
which houses the tunnel-boring machine. In this zone the temperature fluctuated between 
30 and 32C during most of the monitoring periods. However, there were three distinct periods 
when the temperature in this zone dropped below 30C. The first occurred in early 
September 2000 and was likely caused by power interruptions, which in turn caused the 
tunnel-boring machine to cool. The second temperature drop was in late January 2001, when all 
the bulkhead doors were opened. During this brief period, the temperature in the vicinity of the 
tunnel-boring machine dropped to approximately 22.5C. The temperature in this zone again 
dropped to below 30C in early April 2000, likely because of the powering-off of the 
tunnel-boring machine. 
In the zone between the second and third bulkheads (Station 25+52), the temperature 
continuously dropped from approximately 26.5C to approximately 24C between August 2000 
and May 2001. Significant deviations from this trend were observed in early September 2000, 
when the temperature increased briefly. These deviations coincide with the temperature 
decreases in the zone housing the tunnel-boring machine. Because similar observations were not 
recorded before the first bulkhead, it is likely this perturbation was caused when the third 
bulkhead door was left open for a few days. 
No. 3: Water Seeping into Drifts October 2003 C-12
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The temperature data collected between the first and second bulkhead (Station 21+40) shows the 
region steadily cooling immediately following the closure of the bulkhead doors in July 2000. 
(Because of the lack of temperature data from this location between late September 2000 and 
February 2001, temperature dynamics in this zone cannot be compared with the other two zones 
during this time.) Following the closure of the bulkhead doors in late January 2000, the 
temperature in this zone immediately dropped to approximately 24C and remained close to that 
value over the next 2 months. 
Temperature in the ECRB cross-drift measured immediately outside the first bulkhead shows 
diurnal and seasonal fluctuations (Station 15+02). While the diurnal fluctuations appear to be 
restricted to within 3C, the seasonal temperature changed from approximately 29C in late 
August 2000 to approximately 25C in late December 2000. 
In summary, the three zones defined by the bulkheads in the ECRB cross-drift appear to be 
partially thermally isolated from each other and also from the area outside the bulkhead when the 
doors are closed. The zone housing the tunnel-boring machine was warmer than the area outside 
the first bulkhead while the other two zones were consistently cooler when the doors were 
closed. During the period when the bulkhead doors were opened the temperature in each of the 
zones rapidly approached that of the zone outside the bulkheads. 
Relative Humidity Variations between May 2000 and May 2001 C.4.5.3.3 
The relative humidity in the three zones defined by the bulkheads shows spatial variability 
similar to the temperature data (Figure C-7). The lowest humidity was observed in the area 
before the first bulkhead, where it fluctuated between approximately 10 and 40 percent, with a 
few instances where the humidity was greater than 60 percent. In the two zones between the first 
and third bulkheads, the relative humidity remained close to approximately 95 percent, with 
some changes observed in March 2001, when the humidity in the second zone gradually fell 
closer to approximately 90 percent. 
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Source: BSC 2003a, Section 6.10. 
Figure C-7. Relative Humidity Measured in the Enhanced Characterization of the Repository Block 
C.4.5.3.4 
October 2003 C-14 
Cross-Drift Stations 
Water Potential Measurements 
Water-potential measurements along three horizontal boreholes in the ECRB cross-drift are 
summarized in Figure C-8. These three boreholes are located at CD 15+00, CD 20+00 and 
CD 25+00, and are 6 m long. The borehole at CD 15+00 is located outside the first bulkhead, 
while the boreholes at CD 20+00 and CD 25+00 are located between the first and second 
bulkheads. The matrix is partially dried out up to a few meters from the drift surface. 
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Source: BSC 2003a, Section 6.10. 
NOTE: (a) Station 15+00; (b) Station 20+00; (c) Station 25+00. 
Figure C-8. Water Potential Measurements along the Enhanced Characterization of the Repository 
C.4.5.3.5 
October 2003 C-15 
Block Cross-Drift 
Moisture Observations 
Observations of moisture were made during the periodic entries behind the bulkhead doors. 
Moisture was observed on rock bolts, utility lines, vent ducts, wire meshes, and the drift walls. 
Observed rust spots and organic growths indicate the prolonged presence of moisture. Puddles 
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of water were present on the conveyor belt. Water droplets were also observed on the surface of 
a small patch of paint, an impermeable barrier to the rock. Since the paint is impermeable, the 
observed beads are likely the result of condensation, not from seepage through the rocks below 
the paint. Condensation, and consequent dripping, could occur by water phase transitioning from 
vapor to liquid, associated with local temperature variations. 
Analysis of Collected Water Samples C.4.5.3.6 
Water samples were collected during some of the entries behind the bulkhead doors. Initial 
water samples were collected directly from pools that had formed on the conveyor belt, and these 
samples were of brownish to dark brown color, with some examples shown in Figure C-9. These 
samples are likely contaminated from the conveyor belt resulting from the belt usage and 
operation before ECRB cross-drift closure, with the degree of contamination unknown and not 
quantified. Contamination of the conveyor belt may include salt accumulated from water 
evaporation following transportation of the tuff debris, as well as other miscellaneous 
contamination. Therefore, these samples may not yield useful information about the origin of the 
water (condensate or seepage) observed in the ECRB cross-drift behind bulkheads. 
Source: BSC 2003a, Section 6.10. 
Figure C-9. Chemical Analyses of Liquid Samples Collected during Bulkhead Entries 
Three water samples were subsequently collected from containers placed on the top of the 
conveyor belt (Figure C-9). These samples were clear and were analyzed for chloride and silica 
October 2003 C-16 No. 3: Water Seeping into Drifts
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contents and to perform isotopic analyses (Figure C-10). The water collected from collection 
containers indicated that the water is low in chloride and silicate contents, characteristic of 
condensate. The water also does not have the chemical signature of construction water, which 
was spiked with approximately 20 mg/L of lithium bromide. While these data clearly show that 
part of the observed moisture may have originated from condensation, they do not rule out or 
confirm the existence of seepage of water from flow through the formation. 
Because of the uncertainty in the origin of the moisture, the test results obtained so far from the 
ECRB bulkhead monitoring program have not been used directly in the development or 
calibration of seepage models for TSPA. 
Source: BSC 2003a, Section 6.10. 
NOTE: Unit of the y-axis is in mg/L, except for the ratio of sulfate to chloride (dimensionless). 
C.4.6.1
ECRB Samples are grouped as follows: CC in collection container, DW on drift wall, and CB on conveyor 
belt. 
Construction water data presented here are an average value from seven samples. TSw PW: pore water in 
Topopah Spring welded tuff unit. 
October 2003 
Figure C-10. Comparison of Chemical Signatures 
C.4.6 Results and Analysis for Alcove 7 
Information for the following section is based on In Situ Field Testing of Processes (BSC 2003a, 
Section 6.10). 
Test Summary 
Ambient monitoring of temperature, barometric pressure, and relative humidity was performed 
inside Alcove 7, located in the ESF at station 50+64. This alcove was constructed to a depth of 
C-17 No. 3: Water Seeping into Drifts
Revision 2 
199 m and penetrated the Ghost Dance fault at 167 m. Bulkhead doors were installed 64 m and 
132 m from the entrance of the alcove. 
Results C.4.6.2 
Between September 25, 2001, and June 10, 2002, the relative humidity behind the bulkhead 
doors was less than 95 percent (dry end of the thermocouple psychrometer range) and was 
therefore not measured. Pressure monitoring indicated that the transmission of atmospheric 
pressure fluctuations across the bulkhead doors showed minimal dampening (less than 5 percent) 
and short time lags (on the order of hours). Large temperature fluctuations (between 19.5 and 
27.5C) at the monitoring station located 4 m from the entrance of the alcove were due to 
seasonal temperature fluctuations down the ESF by the ventilation system. This monitoring 
station is located outside the bulkhead doors. Diurnal temperature fluctuations due to ventilation 
were as large as 1.2C. Temperatures behind the bulkheads indicated no discernable annual 
fluctuation, and the diurnal temperature fluctuations were less than 0.05C. Abrupt temperature 
decreases (up to 1.0C) were occasionally measured behind the bulkheads. These temperature 
decreases were correlated with the pressure recovery period following a low-pressure event. The 
temperature decrease may be due to a pressure gradient driving warm-dry ESF air through the 
fractures around the bulkheads, evaporating water, and cooling the air. 
On September 18, 2001, the bulkheads were opened after being closed since October 30, 2000. 
Evidence of moisture was observed during this entry. Signs of moisture included drip spots on 
the drip collection sheets, moisture drops on the utility lines, moisture drops on the shotcrete 
around the bulkheads, moisture spots in the dust on an instrument enclosure, and the rock in the 
crown had a dark, moist appearance. The bulkhead doors were next opened on May 20, 2003. 
There were drip spots on the drip collection sheets, moisture drops on the utility lines, and 
moisture spots in the dust on an instrument enclosure. The rock in the crown had a dark, moist 
appearance and the fractures in the rib appeared wet. 
Although moisture was present, it was not possible to collect enough water for analysis. 
As in the ECRB bulkhead-monitoring program, the uncertainty regarding the source of observed 
moisture has so far precluded the use of test data from the Alcove 7 tests in quantitative seepage 
modeling. 
C.4.7 Test Plan for the Niche 5 Test 
The test plan for the Niche 5 test is provided in Test Plan for: Niche 5 Seepage Testing (BSC 
2001b). This test plan is provided to the NRC separate from this technical basis document. 
C.4.8 Results and Analysis for Niche 5 Test 
Information for the following sections is based on In Situ Field Testing of Processes (BSC 
2003a, Section 6.2) and Seepage Calibration Model and Seepage Testing Data (BSC 2003b, 
Section 6.6). 
October 2003 C-18 No. 3: Water Seeping into Drifts
Revision 2 
Test Summary C.4.8.1 
Niche 5 was constructed along the south side of the cross-drift (Figure C-11) within the lower 
lithophysal zone of the Tptpll. The main purpose of the test was to quantify the amount of water 
seeping into the drift as a basis for estimating seepage-relevant formation parameters for the 
lower lithophysal zone. In addition, a slot on the side of Niche 5 was excavated (see 
Section C.4.8.2) to demonstrate that water is diverted around the opening to the side wall of the 
niche due to the capillary barrier effect. The water collected in the slot provides one component 
of a comprehensive mass balance. The tests were performed by injecting water into a short 
interval of borehole that was sealed off using an inflatable packer system. Any water that 
migrated from the borehole to the niche ceiling and dripped into the opening was captured and 
weighed. 
Source: BSC 2003b, Section 6.5, Figure 4. 
NOTE: The shape of the openings is approximate. 
Figure C-11. Schematic Geologic Map Showing Approximate Location of Niches and Systematic Testing 
C.4.8.2 
October 2003 C-19 
Boreholes SYBT-ECRB-LA#13 
Slot Design 
Construction of slots in the east and west walls of Niche 5 was originally intended to aid in the 
collection of water to provide a mass balance. The slot design was based on the premise that 
water would move laterally around the opening because of the capillary barrier and would collect 
at a low spot and drip into the slot (point A on Figure C-12a). The unstable rock conditions at 
No. 3: Water Seeping into Drifts
Revision 2 
Niche 5 caused sections of the initial slot ceiling to collapse during its construction, resulting in 
an excavation that did not meet the original desired construction and testing specifications. Slot 
construction activities were halted after creating a 3.3-m-long irregular-shaped excavation in the 
left rib and a short (less than 1 m) excavation in the right rib of the niche. Figure C-13b shows 
the final size and shape of the slots. Note that there are five profiles numbered 2 through 6 in 
Figure C-12b showing the irregular shape of the longer slot on the left rib. Profiles 2 and 6 
define the lateral ends of the slot. The remaining profiles (3 to 5) are spaced sequentially by 
number between the two lateral ends with a distance of approximately 0.5 to 1.3 m separating the 
profiles. 
Source: BSC 2003a, Section 6.2. 
Figure C-12a. Schematic Illustration of Front View of Niche 5 Facing South Showing Location of 
October 2003 C-20 
Boreholes 1 to 7 
No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003a, Section 6.2. 
NOTE: Profile #2 is located closest to the niche entrance and #6 is farthest away. 
Figure C-12b. Schematic Illustration of Front View of Niche 5 Facing South Showing Profiles #1 to 7 of 
C.4.8.3 
C.4.8.3.1 
October 2003 C-21 
Slot C 
Results and Analysis 
Liquid Release and Seepage Rates 
Several tests performed during the study indicate that a measurable seepage threshold exists for 
the Tptpll. Water was collected in the slot in only two of these tests, Test #1 7/15/02 and Test #2 
9/17/02. Figure C-13 shows a plot of the total seepage rate into the niche (triangles) during 
Test #2 9/17/02 and the seepage rate captured by the tarp (diamonds) installed at the entrance to 
the slot (area A in Figure C-12b). Seepage captured by the tarp follows the same pattern over 
time as the total seepage, which represents water collected from all the capture compartments. 
Seepage captured by the tarp is a large component of the total seepage into the drift approaching 
80 to 90 percent of the total during specific periods. Both the total seepage and the seepage 
captured by the tarp declined and dropped off to zero as the release rate declined after 
October 20, 2002. In Test #1 7/15/02, the water collected in the slot accounted for less than 
10 percent of the total seepage. As discussed in Section C.4.1.2, a mass balance based on the 
measured data could not be obtained. The flow diversion capability of the capillary barrier was 
demonstrated qualitatively through water spreading along the side wall of the niche, as shown in 
Figure C-14. 
No. 3: Water Seeping into Drifts
Source: BSC 2003a, Section 6.2. 
Figure C-13. Total Seepage and Seepage into the Tarp Area at the Entrance to the Slot 
Source: BSC 2003a, Section 6.2. 
Figure C-14. Wetted Area Spreading down the Side Wall in Niche 5 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 C-22
Revision 2 
Relative Humidity and Temperature C.4.8.3.2 
Figure C-15 shows the relative humidity and temperature of the air inside and outside the niche 
during Test #2 9/17/02 (September 17, 2002 to October 28, 2002). The relative humidity and 
temperature inside the niche are very stable, ranging from approximately 90 to 94 percent and 
24o to 25oC, respectively. The sudden drop in relative humidity observed in middle and late 
September was caused by the exchange of cool moist air inside the drift with dry warm air 
outside the niche when the bulkhead door was opened. 
Source: BSC 2003a, Section 6.2. 
Figure C-15. Relative Humidity and Temperature of Air Inside and Outside Niche 5 during Test #2 
C.4.8.3.3 
October 2003 C-23 
9/17/02 
Analysis 
Estimates of the van Genuchten capillary-strength parameter, 1/, obtained by calibrating the 
Niche 5 seepage data, are summarized in Seepage Calibration Model and Seepage Testing Data 
(BSC 2003b). These simulations accounted for evaporation in Niche 5 by calculating an 
evaporative boundary-layer thickness based on the measured evaporation data. The calibrated 
model demonstrated that a substantial amount of water was diverted around the niche opening. 
C.4.9 Results and Analysis for the Systematic Hydrologic Characterization 
Information for the following sections is based on In Situ Field Testing of Processes 
(BSC 2003a, Section 6.2) and Seepage Calibration Model and Seepage Testing Data 
(BSC 2003b, Section 6.6). 
No. 3: Water Seeping into Drifts
Test Summary C.4.9.1 
A systematic approach of testing at regular intervals along the drift was adopted to acquire 
knowledge of the heterogeneous hydrological characteristics of the lower lithophysal zone of the 
Topopah Spring Tuff in the ECRB cross-drift, in which over 80 percent of the repository will 
reside. The size and spacing of the fractures and lithophysal cavities along this unit are highly 
variable along the drift walls (the drift is 5 m in diameter) over an 800m stretch. This indicates 
that hydrological characteristics at one particular location may not be representative of the entire 
unit. Air injection tests were performed to give a measure of fracture permeability. Liquidrelease 
tests were conducted to determine the ability of the open drift to act as a capillary barrier 
as well as the potential of the water to seep into the drift. 
Results and Analysis C.4.9.2 
Air Injection Tests C.4.9.2.1 
The air-injection tests were performed by isolating short sections of the boreholes using an 
inflatable packer system and then injecting compressed air at a constant rate into the isolated 
injection intervals. The pressure buildup in the injection interval and in nearby observation 
intervals was monitored with time until steady-state conditions were reached, which typically 
occurred within a few minutes. Air injection was terminated after reaching steady-state 
pressures, and the decline in air pressure was then monitored as it recovered to its initial pretest 
condition. Air-permeability values were derived from the steady-state pressure data based on a 
commonly used analytical solution (BSC 2001c, Section 6.1.2.1; LeCain 1995, p. 10, Eq. 15). 
Air-permeability estimates for the three zones tested in ECRB-SYBT-LA#2 from the 
steady-state pressure response to constant-flow-rate air-injection tests are tabulated in Table C-1. 
LA2 zone 1 
1.83 LA2 zone 2 
5.18 LA2 zone 3 
Table C-1. Air-Permeability Estimates for the Three Zones in Borehole LA2 
Zone Length (m) Zone ID 
1.83 
Air Permeability K(m2), 
for Packer Inflation at 
2.5 10-11 
2.7  10-11 
1.1 10-11 
C-24 
Air Permeability K(m2), 
for Packer Inflation at 
27.5 psi 32.5 psi 
2.3 10-11 
2.5 10-11 
0.95 10-11 
October 2003 
Source: BSC 2003a, Section 6.11. 
Liquid Release Tests C.4.9.2.2 
Multiple liquid-release tests were performed in the ECRB cross-drift by sealing a short section of 
the borehole above the opening using an inflatable packer system and then releasing water at a 
specified rate into the isolated test interval. Any water that migrated from the borehole and 
dripped into the opening was captured and weighed. The cumulative seepage was recorded as a 
function of time. The evaporation rate was monitored using an evaporation pan and wetted area 
observations. 
No. 3: Water Seeping into Drifts 
Revision 2
Revision 2 
A summary of 10 liquid release tests is provided in Figure C-16. The bar graph shows the 
injection rate, return rate, evaporation rate, seepage rate, and calculated diversion rate for each 
zone. For LA2 zone 1 (z1), the evaporation and diversion rates are not provided since end 
curtains and evaporation pans were not in place. 
Source: BSC 2003a, Section 6.11. 
C.4.9.2.3 
Figure C-16. Summary of Systematic Liquid Release Tests 
Analysis 
A three-dimensional, heterogeneous fracture continuum model was developed to simulate 
liquid-release tests conducted in the ECRB (see Figure C-17). The model is conditioned on the 
measured air permeabilities and accounts for evaporation effects as a function of the measured 
relative-humidity variations in the ventilated drift. Transient seepage-rate data from various 
liquid-release tests in multiple boreholes were used to calibrate the model for the determination 
of effective, seepage-relevant, model-related parameters. An example is shown in Figure C-18. 
Additional seepage-rate data were used for model validation activities. In summary, the data 
measured as part of the systematic hydraulic characterization testing (i.e., transient release rates, 
seepage rates, evaporation rates, and relative humidity data) were used to determine 
seepage-relevant parameters, which are used in subsequent seepage predictions based on a 
conceptually consistent process model. 
C-25 No. 3: Water Seeping into Drifts October 2003
Source: BSC 2003b, Section 6.6.3.3, Figure 18(b). 
Figure C-17. Simulated Saturation Distribution at the End of Liquid-Release Testing in Zone 2 of 
Borehole SYBT-ECRB-LA#1 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 C-26
Revision 2 
Source: BSC 2003b, Section 6.6.3.3, Figure 19. 
NOTE: Blue symbols represent measured data; the red line is the calculated seepage rate. The measured release 
rates are shown in dark gray; the black solid line shows the injection rate used in the model. 
Relative-humidity data are shown as a green dashed line. 
Figure C-18. Calibration of Seepage-Rate Data from Liquid-Release Tests in Zone 2 of 
October 2003 C-27 
Borehole SYBT-ECRB-LA#1 
C.4.10 Results and Analysis for Niche 4 Seepage Test 
Information for the following sections is based on In Situ Field Testing of Processes 
(BSC 2003a, Section 6.2) and Seepage Calibration Model and Seepage Testing Data (BSC 
2003b, Section 6.6). 
C.4.10.1 Test Summary 
The Niche 4 test was conducted as part of the ESF Drift Seepage Test and Niche Moisture Study. 
The main purpose of the test was to quantify the amount of water seeping into the drift as a basis 
for estimating seepage-relevant formation parameters. The tests were performed by injecting 
water into a short interval of borehole that was sealed off using an inflatable packer system. Any 
water that migrated from the borehole to the niche ceiling and dripped into the opening was 
captured and weighed. Niche 4 is located in a highly fractured area in the main drift of the ESF 
(Figure C-11). 
C.4.10.2 Results and Analysis 
C.4.10.2.1 Evaporation, Relative Humidity, and Temperature 
The seepage tests were conducted with the bulkhead doors at the entrance to the niche closed and 
sealed, and the air space within the niche was artificially humidified to minimize evaporation. 
No. 3: Water Seeping into Drifts
Revision 2 
The evaporation rate inside the niche was not monitored. Figure C-19 shows the relative 
humidity and the temperatures inside of Niche 4. 
Source: BSC 2003a, Section 6.2. 
Figure C-19. Relative Humidity and Temperature inside Niche 4 
C.4.10.2.2 Seepage Tests Results 
Thirteen niche seepage tests were performed on three test intervals positioned above Niche 4 
beginning in late 1999 and ending in mid-2000. Water migrated through the rock and seeped 
into the niche from all zones tested. Water that dripped into the drift opening was collected in a 
capture system and weighed. The wetting front typically arrived at the niche ceiling directly 
below the test zone. Most of the water was captured in only one or two collection trays located 
directly beneath the test interval. The niche seepage percentage ranged from 0 percent to 
68.7 percent. 
Figure C-20 illustrates the release rate into a borehole interval, the return rate, and the 
stabilization of niche seepage rate of water collected in the niche trays. If tests were not long 
enough before niche stabilization, the niche seepage ratio was not well defined. Various 
operating conditions and niche moisture conditions may contribute to the fluctuations observed 
in the early time data. The execution of long-duration tests to ensure quasi-steady conditions 
contributed to the robustness of seepage quantification at selected borehole intervals. 
C-28 No. 3: Water Seeping into Drifts October 2003
Revision 2 
Source: BSC 2003a, Section 6.2. 
Figure C-20. Stabilized Flow Rates Observed during Test #1 1-5-00 Conducted on Test Interval UR at 
October 2003 C-29 
Niche 4 
C.4.10.2.3 Analysis 
The data from Niche 4 were analyzed in detail using the seepage calibration model (BSC 2003b, 
Section 6.6). A numerical model of Niche 4 was developed (see Figure C-21) and calibrated 
against seepage-rate data (an example is shown in Figure C-22) to determine an effective, 
seepage-relevant and model-related estimate of the van Genuchten capillary-strength parameter, 
1/. Additional data from Niche 4 were used for validating the seepage process model 
(BSC 2003b, Section 7.3). The estimated parameters were then used in Seepage Model For PA 
Including Drift Collapse (BSC 2003d) to determine the seepage threshold values and seepage 
percentages for a variety of hydrogeologic conditions and percolation fluxes. 
No. 3: Water Seeping into Drifts
Revision 2 
Source: BSC 2003b, Section 6.6.3.3, Figure 30(b). 
Figure C-21. Late-Time Saturation Distribution Calculated with Seepage Calibration Model of Niche 4 
Source: BSC 2003b, Section 6.6.3.3, Figure 31. 
Figure C-22. Example of Comparison between Calculated and Measured Seepage-Rate Data from a 
Liquid-Release Test Conducted in Niche 4 
October 2003 C-30 No. 3: Water Seeping into Drifts
Revision 2 
C.4.11 Results for the Calcite Filling Test 
Information for the following sections is based on Analysis of Geochemical Data for the 
Unsaturated Zone (BSC 2002, Section 6.10) and UZ Flow Models and Submodels (BSC 2003c, 
Section 7.9). 
C.4.11.1 Background 
Observations of calcite and opal precipitations in lithophysal cavities in the Yucca Mountain 
unsaturated zone can be used to estimate long-term seepage rates into these small openings 
(BSC 2002, Section 6.10.1; Paces et al. 2001; Marshall et al. 2003) and provide estimates of 
infiltration rates (BSC 2003c). Calcite is assumed to precipitate from downward-percolating 
meteoric water because of (1) evaporation, (2) CO2 outgassing as a result of the geothermal 
gradient, and (3) interaction with a gas phase containing less CO2 than the gas with which the 
water was last equilibrated. 
The calcite deposits mostly occur as patchy coatings on the footwalls of fracture cavities or as 
irregular to hummocky accumulations on the floors of lithophysal cavities (Paces et al. 2001; 
Whelan et al. 2002). Hanging-wall surfaces and cavity ceilings are almost devoid of 
calcitesilica deposits (Paces et al. 2001; Whelan et al. 2002). Calcitesilica deposits are present 
in only a small percentage of all fractures or lithophysae (Paces et al. 2001); more than 
90 percent of the fractures and cavities exposed in the underground workings do not contain 
secondary minerals (Whelan et al. 2002). 
C.4.11.2 Results and Interpretation 
Detailed line survey measurements of the location and thickness of calcite and opal coatings 
were made along the wall of the ESF tunnel. The volume of the coatings was estimated based on 
the measured thicknesses and the size of the cavities. Seepage rates were calculated using a 
volume fraction of calcite in the coatings of 0.9, assuming that every coating was deposited over 
10 million years, and using estimates of the ratio of the volume of water to the volume of calcite 
obtained from the literature. The calculated seepage rates ranged from 4.2  10-4 to 0.093 l/year. 
For a 5 meter long waste package inside a drift with a 5 m diameter, estimates of the seepage 
rates ranged from 0.005 l/year to 5 l/year, with corresponding seepage fluxes of 2  10-4 mm/yr 
to 0.2 mm/yr (Marshall et al. 2003). The analysis of calcite and opal precipitation data shows 
that (1) not all lithophysal cavities encountered seepage and (2) seepage flux derived from 
mineral deposits is a very small fraction of percolation flux. 
The percolation flux in the unsaturated zone depends strongly on the infiltration flux, which is a 
boundary condition of the unsaturated zone flow model (BSC 2003c). Observations of 
precipitated calcite in the unsaturated zone can also be used to constrain the infiltration flux and 
provide additional evidence for validation of the unsaturated zone model (BSC 2003c). 
One-dimensional modeling of calcite deposition in a deep surface-based borehole (WT-24) was 
performed using the reactive transport computer code TOUGHREACT (Xu and Pruess 1998, 
2001) to estimate the infiltration rate. The simulated calcite abundances generally fell within the 
range of calcite observed in the field over a range of 2 to 20 mm/yr infiltration rates. The 
20 mm/yr infiltration rate may be the upper bound for WT-24 location, whereas the base-case 
October 2003 C-31 No. 3: Water Seeping into Drifts
Revision 2 
infiltration rate of 5.92 mm/yr used for the flow model gave the closest match to the data. The 
modeled calcite abundances generally increased with increasing infiltration rate, but become less 
sensitive to infiltration at higher rates as a result of changes to the geothermal gradient. The 
calcite coating data collected from the ESF also support the validity of the active fracture 
concept for use in describing fracture flow in the unsaturated zone (BSC 2003e, Section 7.2.2). 
C.5 REFERENCES 
Ahlers, C.F.; Shan, C.; Haukwa, C.; Cohen, A.B.J.; and Bodvarsson, G.S. 1996. Calibration and 
Prediction of Pneumatic Response at Yucca Mountain, Nevada Using the Unsaturated Zone 
Flow Model. Milestone OB12M. Berkeley, California: Lawrence Berkeley National 
Laboratory. ACC: MOL.19970206.0285. 
Bodvarsson, G.S.; Bandurraga, T.M.; and Wu, Y.S., eds. 1997. The Site-Scale Unsaturated Zone 
Model of Yucca Mountain, Nevada, for the Viability Assessment. LBNL-40376. Berkeley, 
California: Lawrence Berkeley National Laboratory. ACC: MOL.19971014.0232. 
BSC (Bechtel SAIC Company) 2001a. Test Plan for: Moisture Monitoring in the ECRB 
Bulkheaded Cross Drift. SITP-02-UZ-001 REV 00. Las Vegas, Nevada: Bechtel SAIC 
Company. ACC: MOL.20011018.0011. 
BSC 2001b. Test Plan for: Niche 5 Seepage Testing. SITP-02-UZ-002 REV 00. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: MOL.20020117.0200. 
BSC 2001c. In Situ Field Testing of Processes. ANL-NBS-HS-000005 REV 01. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: MOL.20020108.0351. 
BSC 2002. Analysis of Geochemical Data for the Unsaturated Zone. ANL-NBS-HS-000017 
REV 00 ICN 02. Las Vegas, Nevada: Bechtel SAIC Company. ACC: MOL.20020314.0051. 
BSC 2003a. In Situ Field Testing of Processes. ANL-NBS-HS-000005 REV02B. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: MOL.20030915.0238. 
BSC 2003b. Seepage Calibration Model and Seepage Testing Data. MDL-NBS-HS-000004 
REV 02. Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030408.0004. 
BSC 2003c. UZ Flow Models and Submodels. MDL-NBS-HS-000006 REV 01. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: DOC.20030818.0002. 
BSC 2003d. Seepage Model For PA Including Drift Collapse. MDL-NBS-HS-000002 REV 02. 
Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030709.0001. 
BSC 2003e. Analysis of Hydrologic Properties Data. MDL-NBS-HS-000014 REV 00. 
Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030404.0004. 
LeCain, G.D. 1995. Pneumatic Testing in 45-Degree-Inclined Boreholes in Ash-Flow Tuff Near 
Superior, Arizona. Water-Resources Investigations Report 95-4073. Denver, Colorado: 
U.S. Geological Survey. ACC: MOL.19960715.0083. 
October 2003 C-32 No. 3: Water Seeping into Drifts
Revision 2 
Marshall, B.D.; Neymark, L.A.; and Peterman, Z.E. 2003. Estimation of Calcite Distribution in 
the Topopah Spring Tuff, Yucca Mountain, Nevada. Journal of Contaminant Hydrology, 
62-63, 237-247. New York, New York: Elsevier. TIC: 254210. 
NRC (U.S. Nuclear Regulatory Commission) 2002. Integrated Issue Resolution Status Report. 
NUREG-1762. Washington, D.C.: U.S. Nuclear Regulatory Commission, Office of Nuclear 
Material Safety and Safeguards. TIC: 253064. 
Paces, J.B.; Neymark, L.A.; Marshall, B.D.; Whelan, J.F.; and Peterman, Z.E. 2001. Ages and 
Origins of Calcite and Opal in the Exploratory Studies Facility Tunnel, Yucca Mountain, 
Nevada. Water-Resources Investigations Report 01-4049. Denver, Colorado: U.S. Geological 
Survey. TIC: 251284. 
Reamer, C.W. 2001. Unsaturated and Saturated Flow Under Isothermal Conditions (USFIC) 
Key Technical Issue Agreements. Letter from C.W. Reamer (NRC) to S. Brocoum 
(DOE/YMSCO), June 20, 2001, with enclosure. ACC: MOL.20010913.0149. 
Reamer, C.W. and Gil, A.V. 2001. Summary Highlights of NRC/DOE Technical Exchange and 
Management Meeting on Total System Performance Assessment and Integration, 
August 6-10, 2001, Las Vegas, Nevada. Washington, D.C.: U.S. Nuclear Regulatory 
Commission. ACC: MOL.20010921.0121. 
Reamer, C.W. and Williams, D.R. 2000. Summary of Highlights of NRC/DOE Technical 
Exchanges and Management Meeting on Unsaturated and Saturated Flow under Isothermal 
Conditions, August 16-17, 2000, Berkeley, California. Washington, D.C.: U.S. Nuclear 
Regulatory Commission. ACC: MOL.20001201.0072. 
Whelan, J.F.; Paces, J.B.; and Peterman, Z.E. 2002. Physical and Stable-Isotope Evidence for 
Formation of Secondary Calcite and Silica in the Unsaturated Zone, Yucca Mountain, Nevada. 
Applied Geochemistry, 17, ([6]), 735-750. New York, New York: Elsevier. TIC: 253462. 
Xu, T. and Pruess, K. 1998. Coupled Modeling of Non-Isothermal Multi-Phase Flow, Solute 
Transport and Reactive Chemistry in Porous and Fractured Media: 1. Model Development and 
Validation. LBNL-42050. Berkeley, California: Lawrence Berkeley National Laboratory. 
TIC: 243735. 
October 2003 C-33 No. 3: Water Seeping into Drifts
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C-34 No. 3: Water Seeping into Drifts 
Revision 2 
October 2003
JUSTIFICATION OF CONTINUUM APPROACH FOR SEEPAGE MODELING 
(RESPONSE TO USFIC 4.06) 
No. 3: Water Seeping into Drifts 
APPENDIX D 
Revision 2 
October 2003
Revision 2 
Note Regarding the Status of Supporting Technical Information 
This document was prepared using the most current information available at the time of its development. This 
Technical Basis Document and its appendices providing Key Technical Issue Agreement responses that were 
prepared using preliminary or draft information reflect the status of the Yucca Mountain Projects scientific 
and design bases at the time of submittal. In some cases this involved the use of draft Analysis and Model 
Reports (AMRs) and other draft references whose contents may change with time. Information that evolves 
through subsequent revisions of the AMRs and other references will be reflected in the License Application 
(LA) as the approved analyses of record at the time of LA submittal. Consequently, the Project will not 
routinely update either this Technical Basis Document or its Key Technical Issue Agreement appendices to 
reflect changes in the supporting references prior to submittal of the LA. 
No. 3: Water Seeping into Drifts October 2003
Revision 2 
APPENDIX D 
JUSTIFICATION OF CONTINUUM APPROACH FOR SEEPAGE MODELING 
(RESPONSE TO USFIC 4.06) 
This appendix provides a response to Key Technical Issue (KTI) agreement Unsaturated and 
Saturated Flow Under Isothermal Conditions (USFIC) 4.06. This KTI agreement relates to a 
modeling study to compare continuum versus discrete fracture network models. 
D.1 KEY TECHNICAL ISSUE AGREEMENT 
D.1.1 USFIC 4.06 
Agreement USFIC 4.06 was reached during the U.S. Nuclear Regulatory Commission 
(NRC)/U.S. Department of Energy (DOE) Technical Exchange and Management Meeting on 
Total System Performance Assessment and Integration (TSPAI) held August 6 to 10, 2001 in 
Las Vegas, Nevada (Reamer 2001), which was convened to discuss four TSPAI KTI 
subissues: (1) System description and demonstration of multiple barriers; (2) Scenario analysis 
within total system performance assessment (TSPA) and methodology; (3) Model abstraction 
within the TSPA methodology; and (4) Demonstration of the overall performance objective. 
During the course of this Technical Exchange, seven USFIC agreements were also modified or 
added, including USFIC 4.01 through 4.07. Agreement USFIC 4.06 was added at this time. 
The wording of the agreement is as follows: 
USFIC 4.06 
Provide documentation of the results obtained from the Comparison of 
Continuum and Discrete Fracture Network Models modeling study. 
Alternatively, provide justification of the continuum approach at the scale of the 
seepage model grid (formerly June 20 letter, item xiii). DOE will provide 
documentation of the results obtained from the Comparison of Continuum and 
Discrete Fracture Network Models modeling study or provide justification of the 
continuum approach at the scale of the seepage model grid. This will be 
documented in Seepage Calibration Model and Seepage Testing Data AMR 
(MDL-NBS-HS-000004) or other suitable document expected to be available to 
NRC in FY 2003. 
D.1.2 Related Key Technical Issue Agreements 
The following KTI agreements cover material related to agreement USFIC 4.06: 
Radionuclide Transport (RT) 3.05, Structural Deformation and Seismicity (SDS) 3.01, and 
USFIC 6.03: The NRC is concerned that the use of a continuum model is inappropriate when the 
spacing of flowing fractures exceeds the grid size (Schlueter 2003; NRC 2002, pp. 3.3.6-18 and 
3.3.6-19). The NRC noted that in the pretest predictions of the Alcove 8Niche 3 (also referred 
to as Niche 3107) tests, the grid size is one meter or less; however, studies have found fracture 
spacing in tsw33 to be 1.23 m (Ziegler 2002, Table 1). The NRC argued that using the active 
October 2003 D-1 No. 3: Water Seeping into Drifts
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fracture concept, the spacing of fractures in which water flows would be expected to increase 
under less than fully saturated conditions (Schlueter 2003). Therefore, the NRC has requested 
that the DOE justify its use of the continuum model when the spacing of flowing fractures 
exceeds the grid size. 
D.2 RELEVANCE TO REPOSITORY PERFORMANCE 
This KTI agreement relates to the use of the continuum approach, versus a discrete fracture 
network approach, for modeling flow and seepage processes in a fracture network at the scale of 
the seepage model grid. The NRC concern was that the use of the continuum approach might not 
be appropriate for simulating seepage processes into waste emplacement drifts at Yucca 
Mountain. It is specifically mentioned that fracture networks in the host rock may not be dense 
enough to be treated as a three-dimensional continuum. As a result, a continuum model may not 
be able to capture flow diversion and seepage that may be controlled more by fracture geometry 
than by effective hydraulic properties of a fracture network (NRC 2002). 
When water flows predominantly through fractures, a discrete fracture network model seems 
more appropriate than a continuum model for the reproduction and prediction of drift seepage. 
However, the continuum approach is adopted for the simulation of drift seepage. Justification 
for the continuum approach is provided from evaluation of seepage simulation results, supported 
by observed data from seepage experiments conducted in fractured rock on the appropriate scale. 
Comparison studies using both continuum and discrete fracture network models at the scale of 
the seepage model further strengthen the continuum approach. 
The agreement is relevant to the repository performance because it concerns drift seepage 
modeling which provides seepage-relevant parameters and their probability distributions directly 
to TSPA. 
D.3 RESPONSE 
This KTI agreement response (USFIC 4.06) consists of two parts: (1) justification for the use of 
the continuum approach for seepage analyses and predictions, and (2) comparison between 
seepage calculations with continuum and discrete fracture network models. 
Justification for the continuum approach at the scale of the seepage model grid has been 
documented in Seepage Calibration Model and Seepage Testing Data (BSC 2003a) and by 
Finsterle (2000) as well as other sources in the open literature (e.g., Nitao 1996; Jackson et al. 
2000). The arguments justifying the continuum approach for the purpose of seepage modeling 
include: 
1. The overall, integrated approach to the analysis and modeling of seepage data ensures 
that the model appropriately captures the site-specific behavior of the relevant 
processes on the scale of interest (for details, see Section D.4.1.1). 
2. The successful reproduction of observed seepage-rate datawith the adjustment of a 
single parameterprovides confidence that the modeling approach is reasonable (for 
details, see Section D.4.1.2). 
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3. The successful prediction of seepage-rate data provides confidence that the calibrated 
model is capable of capturing seepage behavior above and below the seepage 
threshold (for details, see Section D.4.1.3). 
4. The continuum approach appropriately captures in-plane flow diversion, which is the 
dominant mode of flow diversion around an opening in fractured rock (for details, see 
Section D.4.1.4). 
5. Fracture density at Yucca Mountain is high, and the fracture network is generally well 
connected, lending support for the use of the continuum approach on the drift scale 
(for details, see Section D.4.1.5) 
6. Additional studies providing justification for the continuum approach are summarized 
in Section D.4.1.6. 
The second part of the response to USFIC 4.06 (see Section D.4.2) presents comparisons 
between seepage predictions performed with continuum and discrete fracture network models. 
Use of a continuum approach can be further justified by comparing it with a discrete modeling 
approach. The comparison studies can be summarized as follows: 
1. A continuum model and a discrete fracture network model (Finsterle 2000; BSC 2003a) 
yield consistent predictions of seepage threshold and seepage rates if calibrated against 
data from liquid-release tests (for details, see Section D.4.2.2). 
2. Another two-dimensional discrete fracture network model (Liu et al. 2002; BSC 2003a) 
resulted in insignificant flow diversion, i.e., no capillary barrier effect exists for 
discrete, two-dimensional systems that neglect in-plane flow diversion (for details, see 
Section D.4.2.3). 
3. Alternative conceptual models (such as a discrete fracture network model) require 
detailed, currently unavailable characterization data. More importantly, these 
alternative models are based on additional model assumptions that are difficult to 
justify, and require a calibration step similar to that needed for the continuum approach 
(for details, see Section D.4.2.4). 
4. Comments on discretization issues are given in Section D.4.2.5. 
In summary, while the seepage models do not predict the strength of individual seeps or specific 
drip locations, the continuum approach is considered appropriate for predicting average seepage 
into waste emplacement drifts in a probabilistic framework. 
The information in this report is responsive to agreement USFIC 4.06 made between the DOE 
and NRC. The report contains the information that DOE considers necessary for NRC review 
for closure of this agreement. 
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D.4 BASIS FOR THE RESPONSE 
D.4.1 Justification for the Continuum Approach 
The process models developed to provide seepage estimates for TSPA are conceptualized as 
heterogeneous continuum models. In general, continuum seepage models can be considered 
appropriate for use in the Yucca Mountain project if they are capable of predicting average 
seepage rates into a drift segment on the scale of a waste package. Moreover, the approach must 
be demonstrated to be applicable to the conditions prevailing at Yucca Mountain. It also must be 
transparent and defensible. 
The continuum approach is considered appropriate for seepage predictions at Yucca Mountain. 
The following sections provide the rationale for this assessment. 
Overall Modeling Approach D.4.1.1 
Seepage is a complex process that involves phenomena on a wide range of spatial and temporal 
scales; from mountain-scale flow redistribution to microscale processes of film flow and drop 
detachment; from near-steady percolation to highly transient, episodic flow events within 
fractures. The processes, phenomena, and factors affecting drift seepage are described in detail 
in Seepage Calibration Model and Seepage Testing Data (BSC 2003a, Section 6.3). 
Given the complexity of the seepage process in unsaturated, fractured porous media, it is 
considered infeasible to develop a detailed process model with a deterministic calculation of 
unsaturated water flow through a fracture network that exhibits multiscale variabilities in 
hydraulic properties. Such a model would also include effects from small-scale roughness and 
small-scale heterogeneities, film flow within fractures and along the drift surface, drop formation 
and detachment, and other processes, including evaporation and in-drift moisture redistribution. 
While modeling these processes is theoretically possible, the characterization data needed are not 
available, and the computational demands are prohibitive. A more effective and equally valid 
alternative approach was therefore used in seepage modeling as described below. 
A detailed deterministic model is not needed, because it is recognized that (1) detailed simulation 
of individual seeps is not necessary to estimate average seepage rates into waste emplacement 
drifts on the scale of a waste package, (2) certain factors affecting seepage can be lumped into an 
effective parameter, (3) calibrating a model against data from seepage experiments ensures that 
the model captures the relevant processes, (4) estimating effective parameters partly compensates 
for processes and features that are not explicitly considered in the model, and (5) the estimated 
parameters are optimal for the given model structure and can be directly used in a prediction 
model that is based on a consistent model conceptualization. 
A key element of the approach chosen to obtain a defensible seepage model and to determine 
seepage-relevant parameters is the incorporation of site-specific, seepage-related data on the 
scale of interest. The data are incorporated through inverse modeling. The main advantage of 
this approach is that it relies directly on seepage-rate data, which inherently contain information 
about the relevant processes. Moreover, the calibration data (seepage rates on the scale of a drift 
section) are very similar to the measure of interest for the subsequent predictions. The 
consistency between the calibration model used to derive seepage-relevant parameters and the 
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prediction model used to forecast seepage minimizes potential conceptual differences and large 
systematic errors. 
The complexity of the model is appropriate for its purpose, i.e., for the prediction of average 
seepage on the scale of a drift segment. Small-scale features and processes, including discrete 
fracture-flow behavior, surface roughness, and film flow, are captured in effective, model-related 
parameters determined from site-specific data that reflect the seepage process on the appropriate 
scale. Calibration against seepage-rate data and the consistent conceptualization in the 
downstream models make this a valid and reasonable approach to characterizing and predicting 
seepage at Yucca Mountain. 
In summary, seepage estimates in TSPA rely on site-specific data representing the seepage 
process itself. The numerical model serves as a transfer function providing average seepage 
rates for a range of hydrogeologic conditions. This transfer function is firmly based on physical 
principles and site-specific characterization data. It is demonstrated below that the model is 
capable of reproducing and predicting observable seepage data. Moreover, theoretical analyses 
(see Section D.4.2.1) show that the continuum approach is also capable of predicting flow and 
seepage behavior that cannot be directly observed in the field. 
Reproduction of Observed Seepage Data D.4.1.2 
A seepage model based on the continuum approach can be considered appropriate if it is capable 
of reproducing observed data from seepage experiments conducted in fractured rock on the 
appropriate scale. The model should be able to reproduce the data without adjusting a large 
number of parameters (i.e., without overparameterization). Moreover, the parameter values 
estimated as a result of the calibration process should be reasonable. Under these conditions, it 
can be concluded that the continuum model appropriately captures the hydrogeological features 
and physical processes involved in the seepage phenomenon, providing a basis for and 
confidence in the subsequent model predictions. 
A numerical process model was developed for reproducing seepage-rate data from liquid-release 
tests and to predict seepage into waste emplacement drifts (BSC 2003a). The model is 
conceptualized as a three-dimensional, heterogeneous fracture continuum model based on the 
Richards equation (Richards 1931) for saturated-unsaturated flow. The van Genuchten-Mualem 
constitutive relations (van Genuchten 1980) describe the capillary pressure and relative liquid 
permeability in the fracture continuum as functions of liquid saturation. This approach captures 
the main driving forces (gravity, viscous, and capillary forces) and phenomena (phase 
interference) relevant for modeling unsaturated flow and seepage in a geologic medium. 
To appropriately include heterogeneity, the spatial structure of the air-permeability data was 
analyzed, and the resulting geostatistical parameters were used to generate multiple realizations 
of a spatially correlated permeability field, which were conditioned on the permeabilities 
measured in the borehole intervals. The permeability fields were eventually mapped onto the 
numerical grid. Multiple realizations of the underlying permeability field were generated to 
capture uncertainty related to the stochastic nature of the represented fracture network.
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The numerical grids created for the simulation of liquid-release tests represent an appropriate 
section of the formation around the injection interval, including the underground opening. 
Evaporation from the drift surface is accounted for by specifying a time-dependent water 
potential boundary condition based on Kelvin's equation, where the thickness of the diffusive 
boundary layer was determined from evaporation experiments at the seepage test location. 
The model is calibrated against late-time seepage-rate data from numerous liquid-release tests 
conducted in several boreholes and locations in both the middle nonlithophysal zone and the 
lower lithophysal zone. Early-time seepage data are discarded because they are affected by 
storage effects and the properties of a few fractures connecting the injection interval with the 
opening. These fractures are not necessarily representative of the fracture network that is 
engaged in flow diversion around the entire opening under steady conditions. Late-time data are 
more representative of near-steady conditions and are less influenced by storage effects. 
Moreover, the relatively large cumulative amount of released water at late time in these tests has 
likely encountered a significant portion of the capillary barrier. As a result, the late-time seepage 
data better reflect average conditions on the scale of interest. 
Measured seepage-rate data from 22 liquid-release tests were used to calibrate the seepage 
calibration model and to estimate the seepage-relevant, model-related van Genuchten capillarystrength 
parameter  / 1 . Examples of calibrated liquid-release tests conducted in the Enhanced 
Characterization of the Repository Block Cross-Drift are shown in Figure D-1. The fluctuations 
in both the simulated and observed seepage rates are a result of variations in the relative 
humidity and thus evaporation potential in the ventilated drift; the effect is appropriately 
captured by the model. 
Source: BSC 2003a, Figures 19 and 23. 
NOTE: Blue symbols represent measured seepage-rate data; the red line is calculated with the calibrated model. 
Figure D-1. Calibration of Seepage-Rate Data from Liquid-Release Tests in Zone 2 of Borehole 
October 2003 
SYBT-ECRB-LA#1 and Zone 3 of Borehole SYBT-ECRB-LA#2 
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As demonstrated, the seepage continuum model is capable of appropriately capturing complex 
unsaturated flow and seepage processes during a highly transient liquid-release test conducted in 
a heterogeneous, fractured formation. Only a single parameter was adjusted to match the data, 
providing confidence that the salient features of the system are appropriately represented in the 
model. The estimated capillary-strength parameter is reasonable and consistent with its use as an 
effective parameter in a drift-scale seepage process model. 
Prediction of Seepage Rates D.4.1.3 
Matching a model to observed data by adjusting a minimum number of parameters is a first step 
in demonstrating the appropriateness of the underlying model. However, the model must also be 
tested for its predictive capability under changed conditions. As outlined in Section D.4.1.1, the 
general approach was designed to minimize the extrapolation required to predict currently 
unobservable data (i.e., long-term seepage into waste emplacement drifts under natural, generally 
low percolation fluxes) from the observable data used for calibration (i.e., short-term seepage 
induced by relatively high-flux liquid-release tests). The field experiments were designed so that 
the data used for calibration reflect the process of interest on the relevant scale. Moreover, since 
the structure of the prediction model is very similar to that of the model used for calibration, the 
optimality of the model-related parameter estimates can be transferred to the prediction model. 
The appropriateness of such an extrapolation of the model beyond its tested grounds were 
assessed. While rigorous model testing is fundamentally challenging (Oreskes et al. 1994), 
validation of the model for the intended purpose of supporting TSPA has been accomplished. 
The seepage process models were tested against observable data from seepage experiments that 
were not used for model calibration. The purpose of this validation exercise was to determine 
whether the model was appropriate and adequate for its intended use (BSC 2003a, Section 7). 
Remaining uncertainty has been quantified during the seepage abstraction process and 
propagated through TSPA (BSC 2003b, Section 6). 
Model predictions are inherently uncertain as a result of uncertainty in the input parameters as 
well as conceptual model uncertainties. Uncertainty propagation methods (such as Monte Carlo 
simulations and first-order second-moment analyses) were used to estimate the prediction 
uncertainty, providing a quantitative acceptance criterion for model validation (BSC 2003a). 
Figure D-2 shows an example of a validation run, in which seepage rates for a liquid-release test 
conducted in Niche 3 were predicted with the calibrated model and compared to measured data 
that were not used for model calibration. Linear error propagation analysis yielded the 
uncertainty of the model prediction as a result of uncertainty in the input parameters. The data 
fall within the range of predicted seepage rates. 
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Source: BSC 2003a, Figure 43. 
Figure D-2. Validation of Seepage Calibration Model and Tptpmn Seepage-Relevant Parameters using 
D.4.1.4 
October 2003 D-8 
Data from Niche 3 (Niche 3107) 
The capillary-strength parameter was determined by calibrating the model against multiple tests 
using different liquid-release rates. Some of these release rates induced a local percolation flux 
that is above the seepage threshold (i.e., water dripped into the opening and yielded seepage rate 
data). However, the joint inversion of multiple data sets also included data from tests performed 
below the seepage threshold. Moreover, the model was validated against tests conducted above 
and below the seepage threshold. That is, the system was probed and the model was validated 
for the critical range of percolation rates about the seepage threshold. Seepage predictions for 
natural percolation fluxes that are even less than the low fluxes (below the seepage threshold) 
induced during the low-rate tests will yield the correct result, namely zero seepage. As a result 
of a high-infiltration climate or strong flow focusing, the natural percolation flux may be high 
and exceed the seepage threshold. These would be the critical scenarios for performance. 
Obviously, the parameters estimated from the liquid-release tests would be most suitable for 
those critical circumstances, because they were determined under similar high-rate conditions. 
In summary, the parameters determined from relatively high rate liquid-release tests are 
appropriate and provide a solid basis for seepage predictions under low and higher natural 
percolation fluxes. The validation exercise demonstrated that the fracture continuum model is 
capable of predicting the seepage behavior above and below the seepage threshold at new 
locations not used for model calibration with an acceptably low prediction uncertainty. 
In-Plane Flow Diversion 
Water flow through the Topopah Spring welded (TSw) hydrogeologic unit and seepage into 
openings at Yucca Mountain occurs predominantly through the fracture network. Flow diversion 
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around the opening occurs primarily within a fracture plane (hereafter referred to as in-plane 
diversion). Multiple fractures are involved in the flow diversion only if the fracture is too short 
and the flow path within the fracture plane is interrupted. In this case, water is diverted into the 
next connected fracture. This fracture is again unlikely to be perfectly parallel to the drift axis, 
allowing the in-plane flow-diversion process to continue. 
The situation is schematically illustrated in Figure D-3, which shows two fractures intersected by 
a drift. In Figure D-3a, the two fractures are aligned with the drift axis (which is an implicit 
assumption made in all two-dimensional fracture network models used to predict drift seepage). 
As an artifact of this specific and unrealistic fracture orientation, in-plane flow diversion is 
prevented, and the resulting impact of discreteness on seepage is exaggerated. Two-dimensional 
fracture network models (including those shown by Finsterle (2000; see Figure D-4a) and Liu 
et al. (2002, Figures 1 to 6) represent extreme cases that may not be representative of and 
appropriate for site-specific seepage modeling. 
In Figure D-3b, the fractures are approximately perpendicular to the drift axis. Flow diversion 
occurs within the fracture plane, a process that is appropriately captured by a heterogeneous 
fracture continuum model even for a single fracture. In-plane flow occurring in multiple 
fractures can be readily combined and described by an effective fracture continuum. 
Three-dimensional discrete fracture network models are also capable of capturing in-plane flow 
diversion. 
Given the significance of in-plane flow diversion around the drift in combination with relatively 
high fracture density and variable fracture orientation (see Section D.4.1.5), a three-dimensional, 
heterogeneous fracture continuum model is an appropriate conceptualization. It captures the 
relevant processes more realistically than, for example, a two-dimensional discrete fracture 
network model. Note that since a two-dimensional model strongly amplifies the effects of 
discreteness on flow and seepage, the appropriateness of the continuum model is tested by 
comparison to seepage rates generated with a two-dimensional model (see Section D.4.2.2). If 
this rigorous test is passed, the suitability of the continuum approach in three dimensions can be 
inferred. 
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Source: BSC 2003a, Figure 1. 
NOTE: (a) A two-dimensional fracture network model assumes that all fractures are parallel to the drift axis, 
preventing flow diversion within the fracture plane; (b) a two-dimensional (and three-dimensional) fracture 
continuum model considers flow diversion occurring within multiple fracture planes that are approximately 
perpendicular to the drift axis. 
Figure D-3. Schematic Showing Two Fractures Intersecting a Drift 
High Fracture Density D.4.1.5 
A continuum representation of a fracture network can be considered appropriate if the fracture 
density is high and the fracture network is well connected. 
Mongano et al. (1999, pp. 65 to 72, 76 to 79) documented in their detailed line survey report that 
fracture frequencies observed in the Topopah Spring upper lithophysal (Tptpul), middle 
nonlithophysal (Tptpmn), and lower lithophysal (Tptpll) zones range from 3.2 m-1 to 4.3 m-1 and 
fractures are predominantly developed in two or three orientations resulting in well connected 
networks. Connectivity of fractures is further enhanced by the presence of numerous 
microcracks as observed at the site. Fracture network connectivity has been determined at a drift 
scale through air-injection tests, which indicate that fractures networks are well connected within 
the moderately to densely welded rocks selected to host the repository (BSC 2001). 
Additional Supporting Studies D.4.1.6 
The appropriateness of the heterogeneous continuum approach to simulate flow through 
fractured rock was studied by Jackson et al. (2000) using synthetic and actual field data. The 
heterogeneous continuum model developed for their study has grid blocks with effective 
permeabilities appropriate to represent the network of fractures within the rock. Jackson et al. 
(2000) concluded that the heterogeneous continuum representations of fractured media are 
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self-consistent (i.e., appropriately estimated effective continuum parameters are able to represent 
the underlying fracture-network characteristics). 
Other studies on drift-scale seepage under ambient conditions have employed heterogeneous 
continuum models (Nitao 1996; Birkholzer et al. 1999). 
D.4.2 Comparison between Continuum and Discrete Fracture Network Models 
Introduction D.4.2.1 
Discrete fracture network models are considered to be conceptually and visually appealing 
alternatives to the continuum models. This approach involves the stochastic generation of 
fracture networks whose geometry is statistically similar to that seen on fracture trace maps or 
borehole logs. In addition to the geometric information, fracture hydraulic properties must be 
determined by calibration or derived from aperture-distribution data before flow and transport 
simulations can be performed. This key process and some of its pitfalls have been described in 
detail by Cacas et al. (1990) and Dverstorp and Andersson (1989). Moreover, when considering 
unsaturated flow through fracture networks, various assumptions must be made regarding phase 
occupancy of fracture segments, accessibility of certain portions of the fracture network, 
entrapment of wetting and nonwetting phases, and flow along and across fracture intersections. 
Flow channeling within a fracture planealready significant in fully saturated mediabecomes 
increasingly complex under unsaturated flow conditions. All these aspects must be 
conceptualized and implemented in a defensible discrete fracture network model if such an 
approach is chosen. 
The discreteness of unsaturated fracture flow and seepage phenomena suggests the use of a 
discrete fracture network model for seepage studies at Yucca Mountain. As outlined in 
Section D.4.1, the continuum approach was chosen because it was considered appropriate for the 
purpose of seepage prediction into waste emplacement drifts. The following sections summarize 
studies comparing the two approaches, demonstrating that the results obtained with either model 
are consistent, provided that each model is calibrated against seepage data (see Section D.4.2.2). 
Seepage Predictions with Discrete Fracture Network and Continuum Model D.4.2.2 
Finsterle (2000) compared seepage predictions calculated with a fracture continuum model to 
those obtained with a discrete fracture network model. The models were calibrated against one 
another (the discrete model providing the synthetic data) to account for the calibration step 
involved in the development of the continuum model. The study involved the following steps: 
1. A model with a complex network of discrete features was developed (see 
Figure D-4a). The purpose of the model was to produce discrete flow behavior and 
localized seepage events (see Figure D-4b). Unsaturated flow simulations performed 
with this discrete fracture network model are considered to represent the response of a 
fractured system. 
2. Air-injection tests, liquid-release experiments, and seepage under natural flow 
conditions were simulated using the discrete fracture network model to generate 
synthetic characterization, calibration, and confirmation data, respectively. 
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3. A simplified heterogeneous fracture continuum model was developed based on the 
available synthetic air-permeability data (see Figure D-5). 
4. Effective parameters were determined by calibrating the fracture continuum model 
against the synthetic liquid-release test data. 
5. Responses from additional liquid-release tests were predicted with the continuum 
model and compared to results obtained with the discrete fracture network model. 
6. The critical performance test for the continuum model is the examination of its ability 
to predict unobservable quantities (such as the seepage threshold and seepage rates 
under low percolation conditions). The fracture continuum model predictions were 
thus compared to the calculated response from the discrete system. 
The main purpose of the modeling study was to gain confidence in the appropriateness of the 
continuum model to simulate and predict seepage into underground openings excavated from 
fractured rock. However, the study inherently contains a comparison between the two modeling 
approaches. The synthetically generated data could be replaced with actual seepage-rate data 
from liquid-release tests to which both models are calibrated. Subsequently, both models are 
used to estimate the seepage threshold under natural percolation conditions. It can be concluded 
that both models yield consistent results (see Figure D-6). 
Note that the comparison between the two models uses the extreme assumption that all fractures 
are perfectly parallel to the drift axis. Even under these extreme conditions, where in-plane flow 
diversion is prevented, the calibrated continuum model yields reasonable seepage predictions for 
conditions that are different from those obtained during calibration. 
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Source: Finsterle 2000, Plate 1. 
NOTE: (a) High-resolution permeability field; (b) discrete flow path and discrete seepage behavior. 
Figure D-4. Two-Dimensional Discrete Fracture Network Model 
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Source: Finsterle 2000, Plate 2. 
NOTE: (a) Permeability field; (b) flow field at end of simulated liquid-release test. 
Figure D-5. Two-Dimensional Fracture Continuum 
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Source: Finsterle 2000, Figure 8. 
NOTE: Prediction of seepage percentage with fracture continuum model shown with solid line; results from Monte 
Carlo simulations shown with dots; seepage data provided by the discrete fracture network model shown 
with the dash-dotted line. The Xs represent the prediction based on the realization of the permeability field 
that was used to calibrate the model. 
Figure D-6. Prediction of Seepage Percentage with Fracture Continuum Model, Including Results from 
Monte Carlo Simulations, and Comparison to Seepage Data Provided by the Discrete 
D.4.2.3 
October 2003 D-15 
Fracture Network Model 
Discrete Fracture Network Modeling Study of Drift Seepage 
Liu et al. (2002) performed a drift seepage study using the discrete fracture network model 
depicted in Figure D-7a. In such a two-dimensional discrete fracture network model, flow 
diversion occurs only if the fracture density and (or) the capillary-strength parameter are high. 
Only insignificant flow diversion effects were produced with the model, as shown in 
Figure D-7b. This behavior is well understood and a direct result of the assumption that all 
fractures are perfectly parallel to the drift axis, preventing in-plane flow diversion. 
Consequently, Liu et al. (2002) concluded that fracture network models need to be 
three-dimensional for them to realistically evaluate the capillary barrier effect in fractured 
formations. Note that the synthetic fracture network and hydraulic parameters used in the 
discrete model of Finsterle (2000; see also Figure D-4) induced some flow diversion. This 
difference in flow diversion capability between the models of Finsterle (2000) and Liu et al. 
(2002) is caused by their respective parameter choices. 
No. 3: Water Seeping into Drifts
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Fracture density, network connectivity, fracture orientation with respect to the drift axis, and 
hydrologic properties of the fractures determine the effectiveness of the capillary barrier in a 
fractured formation. The sensitivity of each of these parameters and features can be examined in 
modeling studies using discrete fracture network models. While the geometrical fracture 
network information used in the model of Liu et al. (2002) is representative of the conditions at 
Yucca Mountain (with the notable exception of the assumption that all fractures are parallel to 
the drift axis), the hydrologic properties (specifically the capillary-strength parameter) are not 
seepage-related (i.e., they are not calibrated against seepage-rate data and thus do not 
compensate for the bias in seepage predictions introduced by the lack of in-plane flow 
diversion). This example therefore highlights the need for model calibration against 
seepage-related data. 
Source: Liu et al. 2002, Figures 1 and 2. 
NOTE: (a) Fracture network; (b) flow paths. 
D.4.2.4 
Figure D-7. Two-Dimensional Discrete Fracture Network Model 
Data Requirements and Need for Calibration 
The relative parsimony of the continuum model is considered a key advantage over the 
complexity of alternative conceptual models, including a discrete fracture network model. The 
continuum model is supported by relevant, conceptually consistent data from Yucca Mountain. 
For example, the air-permeability data used for the generation of the heterogeneous property 
field refer to the effective behavior of the fracture network on the scale of a computational grid 
block. A minimal number of assumptions are required to develop a continuum model, and 
remaining conceptual inconsistencies as well as unmodeled small-scale processes and features 
can be represented in a model-related parameter (such as the capillary-strength parameter) in a 
defensible manner. 
In contrast, the development of a defensible discrete fracture network model requires collecting a 
very large amount of geometric and hydrologic data. While part of the required geometric 
information can be obtained from fracture mapping, the description of the network remains 
incomplete and potentially biased towards fractures of a certain orientation and a certain size. 
D-16 No. 3: Water Seeping into Drifts October 2003
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Moreover, unsaturated hydrological parameters on the scale of individual fractures are required, 
along with conceptual models and simplifying assumptions regarding unsaturated flow within 
fractures and across fracture intersections. The databases required to develop a defensible 
discrete fracture network model are not available and are generally impracticable for site-specific 
simulations. 
As a result, discrete fracture network models need to be calibrated against flow or seepage data 
in a step very similar to that performed for a continuum model. This step is required to assure 
that key aspects of the system at the site of interest are captured and that potential biases from 
model assumptions and errors in parameter values are reduced or eliminated. 
Three-dimensional, calibrated discrete fracture network models are most likely capable of 
producing defensible seepage predictions consistent with those obtained with a calibrated and 
validated fracture continuum model. 
Discretization Issues D.4.2.5 
In a discrete fracture network model, an individual fracture is discretely represented in the 
numerical model by appropriately small computational grid blocks. This is often considered the 
defining feature of such a model. Note, however, the flow equations solved in and between grid 
blocks are essentially identical to those solved by a continuum model, i.e., the only fundamental 
difference between the two approaches lies in the discretization. 
In a numerical model, the grid blocks are computational elements needed to solve the governing 
equations. Continuum equations can be used if considered appropriate for a study on a given 
scale. Once the decision to use continuum equations is made, the domain is discretized for the 
numerical solution of these equations. Consequently, the size of the grid blocks does not 
necessarily need to be related to the size of a representative elementary volume. Specifically, 
fracture spacing in a classical double-porosity or dual-continuum model does not need to be 
smaller than the grid block size used to solve the continuum equations for the approach to be 
valid. As an analog, consider that the analytical solution to a flow problem provides results at an 
infinitely high resolution despite the finite size of the representative elementary volume 
underlying the governing equations. 
In a discrete fracture network model, flow within the fracture plane is governed by continuum 
equations. Consequently, it is standard practice to discretize each fracture plane into elements 
that are usually much smaller than the average fracture spacing. As outlined in Section D.4.1.4, 
if in-plane flow is considered an important process (as is the case for flow diversion and seepage 
into drifts), a continuum model is an appropriate conceptualization. Discretizing in-plane flow 
described by continuum equations using relatively small elements is thus reasonable and does 
not produce a conceptual or computational problem even if fracture spacing were relatively 
large. 
The decision whether continuum equations and associated effective parameter values are 
appropriate to solve a given flow problem is independent from its discretization. However, it is 
noted that conclusions regarding discrete flow behavior on the scale of the average fracture 
October 2003 D-17 No. 3: Water Seeping into Drifts
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spacing or of a computational grid block should not be made based on models such as the 
continuum seepage models developed to support TSPA. 
D.4.3 Summary 
A calibrated, three-dimensional, heterogeneous fracture continuum model has been shown to be 
appropriate for simulating average seepage rates into waste emplacement drift sections that are 
the approximate length of a waste package. 
A calibrated, there-dimensional discrete fracture network model has been evaluated as an 
alternative to the continuum approach. 
It was demonstrated for a two-dimensional setting that both modeling approaches yield 
consistent results for the seepage problems at the waste emplacement drift at Yucca Mountain. 
The parsimony of the continuum model, its computational efficiency, and its support by 
available field data are considered advantages that warrant use for seepage studies at Yucca 
Mountain. Most importantly, the continuum model is validated against field data in the middle 
nonlithophysal zone and lower lithophysal zone and is well integrated into the comprehensive 
data analysis and modeling approach for studying the performance of the unsaturated zone at 
Yucca Mountain. 
D.5 REFERENCES 
Birkholzer, J.; Li, G.; Tsang, C-F.; and Tsang, Y. 1999. Modeling Studies and Analysis of 
Seepage into Drifts at Yucca Mountain. Journal of Contaminant Hydrology, 38, (1-3), 
349-384. New York, New York: Elsevier. TIC: 244160. 
BSC (Bechtel SAIC Company) 2001. In Situ Field Testing of Processes. ANL-NBS-HS- 
000005 REV 01. Las Vegas, Nevada: Bechtel SAIC Company. ACC: MOL.20020108.0351. 
BSC 2003a. Seepage Calibration Model and Seepage Testing Data. MDL-NBS-HS-000004 
REV 02. Las Vegas, Nevada: Bechtel SAIC Company. ACC: DOC.20030408.0004. 
BSC 2003b. Abstraction of Drift Seepage. MDL-NBS-HS-000019 REV 00. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: DOC.20030826.0001. 
Cacas, M.C.; Ledoux, E.; De Marsily, G.; Tillie, B.; Barbreau, A.; Durand, E.; Feuga, B.; and 
Peaudecerf, P. 1990. Modeling Fracture Flow with a Stochastic Discrete Fracture Network: 
Calibration and Validation. 1. The Flow Model. Water Resources Research, 26, (3), 479-489. 
[Washington, D.C.]: American Geophysical Union. TIC: 222351. 
Dverstorp, B. and Andersson, J. 1989. Application of the Discrete Fracture Network Concept 
with Field Data: Possibilities of Model Calibration and Validation. Water Resources Research, 
25, (3), 540-550. [Washington, D.C.]: American Geophysical Union. TIC: 254736. 
Finsterle, S. 2000. Using the Continuum Approach to Model Unsaturated Flow in Fractured 
Rock. Water Resources Research, 36, (8), 2055-2066. Washington, D.C.: American 
Geophysical Union. TIC: 248769. 
October 2003 D-18 No. 3: Water Seeping into Drifts
Revision 2 
Jackson, C.P.; Hoch, A.R.; and Todman, S. 2000. Self-Consistency of a Heterogeneous 
Continuum Porous Medium Representation of a Fractured Medium. Water Resources 
Research, 36, (1), 189-202. Washington, D.C.: American Geophysical Union. TIC: 247466. 
Liu, H.H.; Bodvarsson, G.S.; and Finsterle, S. 2002. A Note on Unsaturated Flow in 
Two-Dimensional Fracture Networks. Water Resources Research, 38, (9), 15-1 to 15-9. 
Washington, D.C.: American Geophysical Union. TIC: 253307. 
Mongano, G.S.; Singleton, W.L.; Moyer, T.C.; Beason, S.C.; Eatman, G.L.W.; Albin, A.L.; and 
Lung, R.C. 1999. Geology of the ECRB Cross Drift  Exploratory Studies Facility, Yucca 
Mountain Project, Yucca Mountain, Nevada. [Deliverable SPG42GM3]. Denver, Colorado: 
U.S. Geological Survey. ACC: MOL.20000324.0614. 
Nitao, J.J. 1996. The NUFT Code for Modeling Nonisothermal, Multiphase, Multicomponent 
Flow and Transport in Porous Media. Eos, 74, (43), 3. Washington, D.C.: American 
Geophysical Union. TIC: 226135. 
NRC (U.S. Nuclear Regulatory Commission) 2002. Integrated Issue Resolution Status Report. 
NUREG-1762. Washington, D.C.: U.S. Nuclear Regulatory Commission, Office of Nuclear 
Materials Safety and Safeguards. TIC: 253064. 
Oreskes, N.; Shrader-Frechette, K.; and Belitz, K. 1994. Verification, Validation, and 
Confirmation of Numerical Models in the Earth Sciences. Science, 263, (5147), 641-646. 
Washington, D.C.: American Association for the Advancement of Science. TIC: 248958. 
Reamer, C.W. 2001. U.S. Nuclear Regulatory Commission/U.S. Department of Energy 
Technical Exchange and Management Meeting on Total System Performance Assessment and 
Integration (August 6 through 10, 2001). Letter from C.W. Reamer (NRC) to S. Brocoum 
(DOE/YMSCO), August 23, 2001, with enclosure. ACC: MOL.20011029.0281. 
Richards, L.A. 1931. Capillary Conduction of Liquids Through Porous Mediums. Physics, 1, 
318-333. New York, New York: American Physical Society. TIC: 225383. 
Schlueter, J.R. 2003. Staff Review of Information Addressing Radionuclide Transport (RT) 
Agreement 3.06 and Structural Deformation and Seismicity (SDS) Agreement 3.02, Status Partly 
Received. Letter from J.R. Schlueter (NRC) to J.D. Ziegler (DOE/ORD), February 14, 2003, 
0220036149, with attachment. ACC: MOL.20030909.0374. 
van Genuchten, M.T. 1980. A Closed-Form Equation for Predicting the Hydraulic 
Conductivity of Unsaturated Soils. Soil Science Society of America Journal, 44, (5), 892-898. 
Madison, Wisconsin: Soil Science Society of America. TIC: 217327. 
Ziegler, J.D. 2002. Transmittal of Information Addressing Key Technical Issue (KTI) 
Agreement Items Radionuclide Transport (RT) 3.06 and Structural Deformation and Seismicity 
(SDS) 3.02. Letter from J.D. Ziegler (DOE/YMSCO) to J.R. Schlueter (NRC), June 27, 2002, 
OL&RC:TCG-1316, 0628023167, with attachment. ACC: MOL.20020819.0283. 
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APPENDIX E 
ALCOVE 8NICHE 3 PRETEST PREDICTIONS 
(RESPONSE TO RT 3.06 AIN-1 AND SDS 3.02 AIN-1) 
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Note Regarding the Status of Supporting Technical Information 
This document was prepared using the most current information available at the time of its development. This 
Technical Basis Document and its appendices providing Key Technical Issue Agreement responses that were 
prepared using preliminary or draft information reflect the status of the Yucca Mountain Projects scientific 
and design bases at the time of submittal. In some cases this involved the use of draft Analysis and Model 
Reports (AMRs) and other draft references whose contents may change with time. Information that evolves 
through subsequent revisions of the AMRs and other references will be reflected in the License Application 
(LA) as the approved analyses of record at the time of LA submittal. Consequently, the Project will not 
routinely update either this Technical Basis Document or its Key Technical Issue Agreement appendices to 
reflect changes in the supporting references prior to submittal of the LA. 
No. 3: Water Seeping into Drifts October 2003
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APPENDIX E 
ALCOVE 8NICHE 3 PRETEST PREDICTIONS 
(RESPONSE TO RT 3.06 AIN-1 AND SDS 3.02 AIN-1) 
This appendix provides responses for Key Technical Issue (KTI) agreements Radionuclide 
Transport (RT) 3.06 additional information needed (AIN)-1 and Structural Deformation and 
Seismicity (SDS) 3.02 AIN-1. These KTI agreements relate to the documentation of pretest 
predictions for the Alcove 8Niche 3 (also referred to as Niche 3107) tests. 
E.1 KEY TECHNICAL ISSUE AGREEMENTS 
E.1.1 RT 3.06 AIN-1 and SDS 3.02 AIN-1 
Agreement SDS 3.02 was reached during the U.S. Nuclear Regulatory Commission (NRC)/U.S. 
Department of Energy (DOE) Technical Exchange and Management Meeting on Structural 
Deformation and Seismicity held October 11 to 12, 2000, in Las Vegas, Nevada (Schlueter 
2000). The agreement was reached during the course of this meeting in the discussion of SDS 
Subissue 3, Fracturing and Structural Framework. 
Agreement RT 3.06 was reached during the NRC/DOE Technical Exchange and Management 
Meeting on Radionuclide Transport held December 5 to 7, 2000, in Berkeley, California 
(Reamer and Williams 2000). During the course of this meeting, RT Subissue 3, Radionuclide 
Transport through Fractured Rock, was discussed and agreement RT 3.06 was reached. 
Both agreements read as follows: 
RT 3.06 and SDS 3.02 
The NRC needs DOE to document the pre-test predictions for the 
Alcove 8-Niche 3 work. DOE responded that pre-test predictions for 
Alcove 8-Niche 3 work will be provided to NRC via letter report (Brocoum to 
Greeves) by mid-January 2001. 
In response to these agreements, the DOE provided on March 12, 2001, the pretest predictions 
for the Alcove 8Niche 3 tests (Brocoum 2001). NRC staff subsequently provided review 
comments on the DOE initial response and identified three AINs resulting in RT 3.06 AIN-1 and 
SDS 3.02 AIN-1 (Reamer 2002). 
Both AINs request the following: 
RT 3.06 AIN-1 and SDS 3.02 AIN-1 
1) Provide the pretest predictions for the Phase II tests (flow and transport) for the 
Line-Release (Fault) Test and the Large Plot Test 
2) Provide clarification of whether the tracer transport results for the small plot 
tests discussed in the pretest prediction report, and the pretest predictions in 
No. 3: Water Seeping into Drifts October 2003 E-1
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Attachment II, are the pretest predictions for the Small Plot Test or the Line 
Release (Fault) Test or both 
3) Provide clarification on the specific test objectives of the Line Release (Fault) 
Test 
An initial response to these was provided to the NRC (Ziegler 2002), which satisfied items 2 and 
3 of the above NRC request. The only remaining AIN is pretest predictions for the 
Alcove 8-Niche 3 Phase II testing (Schlueter 2003). 
E.1.2 Related Key Technical Issue Agreements 
KTI agreements RT 3.06 and SDS 3.02 are related to agreements RT 3.05, SDS 3.01 and 
Unsaturated and Saturated Flow Under Isothermal Conditions (USFIC) 6.03. The NRC 
requested that the DOE address eight additional comments in its response to RT 3.05, SDS 3.01, 
and USFIC 6.03 (Schlueter 2003). However, as pointed out earlier, the DOE and the NRC 
agreed that the pretest predictions for the Phase II tests at Alcove 8Niche 3 constitute the final 
piece of information needed to fully address RT 3.06 and SDS 3.02. 
E.2 RELEVANCE TO REPOSITORY PERFORMANCE 
These KTI agreements relate to the DOE providing documentation of pretest predictions for the 
Alcove 8Niche 3 work. 
During the October 2000 SDS Technical Exchange (Schlueter 2000), Subissue 3, Fracturing and 
Structural Framework, was discussed. The NRC expressed concerns about (1) the role of 
mineralized fractures in the unsaturated zone, (2) the technical basis for fracture-related 
parameters used in process models, and (3) tests to calibrate seepage models (Schlueter 2003). 
Agreement SDS 3.02 was reached with the intent to fracture-inform the pretest predictions for 
the Alcove 8Niche 3 tests (Schlueter 2003). 
During the December, 2000, RT Technical Exchange (Reamer and Williams 2000), the DOE 
presentation for Subissue 3, Radionuclide Transport Through Fractured Rock, included a 
discussion of acceptance Criterion 2a. During that discussion, it was noted that the breakthrough 
curves had been developed for reactive (sorbing), nonreactive (nonsorbing), and colloidal tracers 
from field tests. The NRC was concerned that the modeling approach of transport through 
fractured rock was less established than in porous media. While recognizing the Alcove 1 test 
provided data for developing breakthrough curves for nonsorbing tracer transport through 
fractured tuff, the NRC requested pretest predictions of the Alcove 8Niche 3 tests, a meso-scale 
field test, as a means to enhance confidence in the understanding of the flow and transport 
processes, particularly for nonsorbing and moderately sorbing tracers (Reamer and Williams 
2000; Schlueter 2003). 
Agreement RT 3.06 and SDS 3.02 are relevant to the repository performance because results and 
data from the hydrological tests at Alcove 8Niche 3 are relied upon for building confidence in 
the understanding of flow and transport processes through fractured rock and for validation of 
unsaturated zone process models supporting total system performance assessment. Specifically, 
matrix diffusion and seepage, as investigated in the Alcove 8Niche 3 test, are two important 
October 2003 E-2 No. 3: Water Seeping into Drifts
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processes by which to determine the performance of the unsaturated zone of Yucca Mountain as 
a natural barrier. Note, however, that the tests do not provide results that directly support the 
development or abstraction of unsaturated zone process models for total system performance 
assessment. 
E.3 RESPONSE 
The Alcove 8Niche 3 tests are aimed at evaluating unsaturated zone flow, seepage response, 
and matrix diffusion processes. Alcove 8 (located in the Enhanced Characterization of the 
Repository Block Cross-Drift) has been excavated for liquid releases through a fault (fault tests) 
and through a network of fractures (large-plot tests). Niche 3 (located in the main drift of the 
Exploratory Studies Facility (ESF), approximately 20 m below Alcove 8) serves as the site for 
monitoring wetting-front migration, seepage of water originating at Alcove 8, and tracer 
concentration in seeping water. Both fault testing and large-plot testing were originally planned 
to include two phases, each phase involving water release with and without tracers. Phase I 
corresponds to experimental conditions characterized by positive water pressure head (2 cm) at 
the infiltration sites (at the fault or the large plot). For Phase I testing, which is still in progress, 
the fault or fracture network is saturated near the infiltration plots. For Phase II testing, much 
smaller infiltration rates (i.e., more negative water pressure heads) will be used. 
The original Phase I predictions for flow, seepage, and transport were provided in a previous 
transmittal (Brocoum 2001; Ziegler 2002). The original test plan called for performing the 
Phase I flow testing, then tracer transport testing in the fault, followed by the same types of 
testing using the large plot. Phase I flow and tracer testing was completed in the fault, and 
Phase I flow testing was performed using the large plot. Phase I tracer transport testing using the 
large plot was delayed pending revisions in the test plan and pretest predictions. 
This appendix develops new pretest predictions for the final part of the flow testing component 
of the Phase I large-plot tests (which defines the initial hydrologic conditions for subsequent 
transport testing) and for the Phase I tracer testing part. As described in Section E.4, the 
predictive model has been refined from the original pretest predictions (Brocoum 2001) by 
calibrating to available Phase I large-plot flow test data, and incorporating modified test 
conditions (a detailed discussion of changes in test design is given in Section E.4.2.1). In 
addition, this appendix develops pretest predictions for the Phase II flow and tracer transport 
large-plot tests based on this updated model. 
The DOE no longer has plans for Phase II fault testing because the large plot tests are expected 
to better characterize water flow and tracer transport in a fracture network. Accordingly, the 
pretest prediction for Phase II of the fault tests is not provided in this appendix. 
The information in this report is responsive to NRCs AIN requests RT 3.06 AIN-1 and 
SDS 3.02 AIN-1. The report contains the information that the DOE considers necessary for 
NRC review for closure of these agreements. 
October 2003 E-3 No. 3: Water Seeping into Drifts
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E.4 BASIS FOR THE RESPONSE 
E.4.1 Test Objectives and Test Settings 
The information for this section is based on In Situ Field Testing of Processes (BSC 2003a, 
Section 6.12). The major objectives of Alcove 8Niche 3 tests include: 
 Quantification of meso-scale (approximately 20 m) infiltration and seepage processes in 
the unsaturated zone of Yucca Mountain 
 Estimation of relations between relative permeability and water potential for unsaturated 
flow in fractured rock 
 Evaluation of the importance of matrix diffusion in the unsaturated zone transport 
processes. 
Figure E-1a shows the location of the test site within the ESF main drift and the Enhanced 
Characterization of the Repository Block Cross-Drift. Figure E-1b shows a three-dimensional 
representation of the test area, including several slanted (near-vertical) boreholes. Alcove 8 is 
located within the Topopah Spring upper lithophysal (Tptpul) zone. Alcove 8 begins at 
Cross-Drift station 7+98.236 (BSC 2003a, Section 6.12). An elevation of about 1,094.0 m above 
mean sea level (amsl) is calculated for station 7+98.236. The elevation at station 0+00 of Alcove 
8 is approximately 0.5 m above station 7+98.236 or about 1,094.5 m (0.15 m) amsl based on 
Alcove 8 design drawings (BSC 2003a, Section 6.12). Niche 3 is located in the Topopah Spring 
middle nonlithophysal (Tptpmn) zone . The crown of Niche 3 is approximately 2 to 3 m lower 
than the 1,076.7 m amsl crown elevation of the ESF at station 31+07. The location of the 
Tptpul-Tptpmn contact is approximately 1,080 m amsl, based on GFM3.1 data (BSC 2003a, 
Section 6.12). 
A distinctive feature of the test bed in Alcove 8 is a near-vertical fault that cuts across the floor 
(Figure E-2). It is open on the ceiling of Niche 3 and appears to be closed along the floor of 
Alcove 8. To facilitate ponded releases of water, a trench approximately 5 cm wide and 
approximately 5 cm deep was etched along this fault for the fault tests. 
Niche 3 is approximately 4 m wide and extends to approximately 14 m from the centerline in the 
ESF main drift. The distance from the ceiling to the floor of the niche gradually drops from 
3.25 m at the opening to 2.5 m toward the midpoint of the niche. Three 9.0-m-long, 0.0762-m 
diameter horizontal boreholes were drilled approximately 0.5 m above the ceiling, parallel with 
the long axis of the niche. Additionally, there are seven 6.0-m-long, 0.0762-m diameter 
boreholes drilled inside radially outward from the side walls of the niche (Figure E-3). The fault 
is visible along the ceiling of Niche 3. 
October 2003 E-4 No. 3: Water Seeping into Drifts
Source: BSC 2003a, Figure 6.12.1-2. 
NOTE: ECRB = Enhanced Characterization of the Repository Block. 
Figure E-1. Schematic Illustration of the Test Bed for the Alcove 8Niche 3 Tests 
No. 3: Water Seeping into Drifts E-5 
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October 2003
Revision 2 
Source: BSC 2003a, Figure 6.12.1-3. 
Figure E-2. Schematic Illustration of the Infiltration Zones along the Floor of Alcove 8 
October 2003 E-6 No. 3: Water Seeping into Drifts
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Source: BSC 2003a, Figure 6.12.1-4. 
Figure E-3. Schematic Illustration of the Monitoring Boreholes in Niche 3 
There are three distinct components to the flow investigation: (1) controlled release of water 
(with and without tracers) into infiltration plots at Alcove 8, (2) borehole monitoring for changes 
in saturation and water potential, and (3) collection of seepage from the ceiling of Niche 3. The 
key features of techniques used in this field investigation are presented below. 
Water was released in Alcove 8, first along the fault (fault test), and then from a larger plot into 
fractured rock (large-plot test). The layout for the two tests is shown in Figure E-2. For the fault 
test, water was released along a 5.15 m long section of fault visible along the floor of Alcove 8. 
This section of fault was partitioned into four subsections, each serving as a separate release 
zone. In the ongoing large-plot test, water is ponded in a 3 m by 4 m section adjacent to the 
fault. This large plot is divided into twelve square compartments (1 m by 1m). In both these 
tests, water was ponded to a head of approximately 0.02 m. 
In nine monitoring boreholes (i.e., 1 to 7, 9, and 10 in Figure E-3), changes in saturation are 
measured continuously with electrical resistivity probes located at 0.25 m intervals along the 
length of each borehole during the entire field investigation. Water-potential measurements were 
made with psychrometers along the single borehole (i.e., 8 in Figure E-3). 
The psychrometers and electrical resistivity probes were housed in borehole sensor trays 
installed along the length of each monitoring borehole. The borehole sensor trays were 
fabricated from 0.10 m outside diameter PVC pipes, 3.0 m in section length. Each pipe section 
was cut lengthwise to produce a 0.075-m-wide curved tray. The borehole sensor tray housing 
permitted immediate contact between electrical resistivity probes and the borehole wall. The 
psychrometers were installed inside small cavities (0.005 m in diameter) perforated through the 
borehole sensor tray wall to measure water potentials of the rock. 
E-7 No. 3: Water Seeping into Drifts October 2003
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An automated water-collection system was designed to capture seepage from the niche ceiling. 
With this system, water dripping from the niche ceiling is collected in plastic trays and diverted 
to collection bottles. These bottles have been installed with pressure transducers to periodically 
measure the collected amount of seepage water. 
Both fault tests and large-plot tests were planned to include two phases involving water release 
with and without tracers. Phase I corresponds to an experimental condition characterized by 
positive water pressure head (2 cm) at the infiltration plots. In this case, the fault or fracture 
network is saturated (at least near the infiltration plots). Phase II corresponds to an experimental 
condition characterized by much smaller infiltration rates (or more negative water pressure 
heads) than Phase I. Although useful data on the infiltration and transportation properties of the 
fault were acquired during Phase I, Phase II of the fault tests is no longer planned because the 
large plot tests are expected to better characterize flow and transport behavior in the fracture 
network at Alcove 8Niche 3. More detailed discussions of fault-test results (Phase I) and model 
analyses of the test results are given in UZ Flow Models and Submodels (BSC 2003b, 
Section 7.6) and In Situ Field Testing of Processes (BSC 2003a, Section 6.12). 
E.4.2 Large-Plot Test and Modeling 
Information for this section is based on the following data: 
 DTNs: LB0306A8N3LIQR.001, Fault Infiltration Test from Alcove 8 to Niche 3 
(9/18/200210/16/2002), and LB0308A8N3SEEP.001, Seepage rate data for 
Alcove 8-Niche 3 large plot tests (Phase I) 
 DTN: LB0308A8N3TRTM.001, Water front travel-time data for Alcove 8Niche 3 
large plot tests (Phase I) 
 Data to be submitted, Model calibration using seepage rate data from Alcove 8Niche 3 
large-plot tests (Phase I) 
 Data to be submitted, Model prediction for Alcove 8Niche 3 large-plot tests (Phase I 
and Phase II). 
Experimental Results and Analysis E.4.2.1 
The large-plot tests involve the release of water (without and with tracers) under both ponded 
(Phase I) and nonponded (Phase II) conditions in a 3- by 4-m plot referred to in this document as 
the large plot (Figure E-4). The early data from Phase I were used to calibrate a model for 
predicting the future test results. Details of the site, the experimental setup, and monitoring for 
the large-plot test are the same as in the previous section (Section E.4.1) with the following 
additions. Ponded release of water to the 3- by 4-m section along the floor of Alcove 8 began on 
August 20, 2002. The infiltration zone was divided into 12 sections each 1 by 1 m (Figure E-4). 
Observations from this phase of testing include the seepage rates measured at Niche 3.
October 2003 E-8 No. 3: Water Seeping into Drifts
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Source: BSC 2003a, Figure 6.12.4-1. 
Figure E-4. Schematic Illustration of the Infiltration Zones along the Floor of Alcove 8 Large-Plot Test 
October 2003 
with the Numbers Identifying the 12 Infiltration Subplots 
Infiltration was initiated in the large plot on the floor of Alcove 8 by maintaining an 
approximately 2-cm head of ponded water (for Phase I). The amount of water necessary to 
maintain the 2 cm of ponding was recorded and thus the infiltration rates (liters per day) over 
time were also known for all plots (1 to 12 in Figure E-4). Infiltration rates were remotely 
monitored for each individual plot (1 to 12) in the large plot. The resulting infiltration rates may 
be found in Figure E-5. The plot numbers correspond to those in Figure E-4. Note that 
infiltration rate was both temporally and spatially variable despite diligent maintenance of the 
pond head. It is possible that infiltration capacity could presumably decrease over time (as 
observed in most plots) caused by redistribution of particles in the infiltration plot on the 
Alcove 8 floor. Other possibilities for the change in infiltration could be related to unstable flow 
processes and boundary conditions. Peak infiltration rates ranged from approximately 24 to 
120 L/day. 
All seepage into Niche 3 from the infiltrating water from the 3- by 4-m large-plot area in 
Alcove 8 was collected in trays that covered an area approximately 5.3 by 4.3 m of the Niche 3 
ceiling. The overall geometry of Niche 3 and its ceiling roughness lead to an intricate 
partitioning of the seepage area, as shown in Figure E-6. The collection tray units do not have 
the same surface area, but this is not necessary as long as the contributing areas and total seepage 
volume are known. 
E-9 No. 3: Water Seeping into Drifts
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NOTE: Plot numbers correspond to those in Figure E-4. 
Figure E-5. Infiltration Rates for Each Plot in the Large-Plots Test in Alcove 8 from 9/16/02 to 3/16/03 
October 2003 E-10 No. 3: Water Seeping into Drifts
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Figure E-6. Diagram of the Trays Collecting Seepage from the Ceiling of Niche 3 
Seepage water from each of these trays was separately collected and stored in containers, each 
connected to a pressure transducer (Setra C204, 0 to 25 psi range) used to remotely monitor 
seepage rate and volume. Using this system, the seepage rates were measured for each container 
related to each collection tray. 
The seepage measured over time from each tray for the period of September 16, 2002, to 
March 16, 2003, may be seen in Figure E-7. While the arrival time (initial breakthrough) of the 
seepage wetting front occurred at a relatively consistent time at all trays (approximately 
30 days), the peak seepage rate and timing of the occurrence of those peaks were variable. This 
large variability in seepage response was consistently observed in the large-plot studies. 
In addition to the data provided by the large-plot test, a full periphery geologic map of Niche 3 
has been prepared by the U.S. Geological Survey (DTN: GS030108314224.001) and related to 
the position of the capture zones listed in Figure E-6. No direct relationship could be observed 
between the seepage in the trays and fracture presence or characteristics. This may be partially 
due to the limited nature of the fracture data. 
October 2003 E-11 No. 3: Water Seeping into Drifts
Revision 2 
NOTE: Tray numbers correspond to those in Figure E-5. 
Figure E-7. Seepage Rates for Each Tray Collected from Niche 3 in the Large-Plots Test from 9/16/02 
E.4.2.2 
October 2003 E-12 
to 3/16/03 
Model Development 
A numerical model was developed to simulate and understand results from the large-plot tests 
(Phase I). The seepage and infiltration-rate data were used to calibrate the model to obtain the 
site-specific rock properties. The calibrated model was then used to predict results for the 
subsequent tests. 
A three-dimensional numerical grid was constructed for modeling the large-plot tests 
(Figure E-8). The top of the grid corresponds to the floor of Alcove 8, where infiltration 
occurred. The 12 infiltration plots and the projected outline boundary of Niche 3 ceiling (under 
which seepage trays were installed) are also shown on the top of the grid in Figure E-8. Small 
grid sizes were used above the niche ceiling and near the interface between model layers tsw33 
No. 3: Water Seeping into Drifts
Revision 2 
(corresponding to lithostratigraphic zone Tptpul) and tsw34 (corresponding to lithostratigraphic 
zone Tptpmn) to capture diverted water flow around the niche and rock property transition at the 
interface between model layers. The dips of the contact between tsw33 and tsw34 are ignored 
because flow in fractures is expected to occur mainly in the vertical direction. For simplicity, the 
niche ceiling was approximated as a flat surface. To capture the transient flow and transport 
behavior, the multiple interacting continua model (Pruess and Narasimhan 1985), which is well 
suited to simulate steep pressure and concentration gradients at the interface between the 
fractures and matrix continua, was used. In the numerical grid shown in Figure E-8, each 
gridblock includes a fracture element and five matrix elements. 
NOTE: MINC = multiple interacting continua. 
Figure E-8. Three-Dimensional Numerical Grids for the Large-Plot Tests 
To handle the spatial variabilities observed from both the infiltration rates applied in Alcove 8 
and the resultant seepage rates observed in Niche 3 (Section E.4.2.1), heterogeneous distributions 
of fracture properties within a given model layer were considered in the three-dimensional 
model. Within a model layer, fractured rock is divided into a number of vertical columns within 
zones below the infiltration plots (for tsw33) or above the ceiling of Niche 3 (for tsw34). 
Therefore, there are two sets of vertical columns that are located in tsw33 and tsw34, 
respectively. Each column corresponds to an infiltration plot (in tsw33) or one (or a combination 
of adjacent two) seepage tray (in tsw34). Table E-1 gives the relationship between identification 
number of seepage trays and the vertical column number. The rest of the rock was considered to 
have homogeneous property distributions within each model layer. The homogeneous property 
distributions were also generally used for each column. 
E-13 No. 3: Water Seeping into Drifts October 2003
Seepage Tray 
Table E-1. Relation between Seepage-Tray Identification Number and the Vertical Column Number 
U4-B2 
U4-B3 
U4-B4 
U3-B2 
U3-B3 
U3-B4 
U4-B1 
U1-B5 
U1-B4 
(U1-B3) + 1/4(U1-B1) 
1/4(U1-B1) 
1/2(U1-B1) 
Previous fracture-network modeling demonstrated that unsaturated flow paths within a fracture 
network are generally vertical (as a result of gravity-dominated flow behavior) (Liu et al. 2002), 
supporting the use of the column-based heterogeneous distributions. Use of these vertical 
columns may be able to approximately capture flow behavior associated with these flow paths. 
Another consideration for using the simple column-based approach is data limitation. As in any 
field test in the area of subsurface hydrology, limited data are available for characterizing 
detailed flow paths between Alcove 8 and Niche 3. A simple model of heterogeneity generally 
involves a relatively small number of parameters that need to be calibrated. The usefulness and 
limitations of this approach will be investigated by comparing prediction results with future test 
observations. 
Similar to the fault tests (Section E.4.1), considerable temporal variability in the infiltration rate 
occurred during the large-plot tests, although a constant water-pressure head (2 cm) was applied 
at the infiltration plot (Section E.4.2.1). This may result from in-filled materials within the 
fractures just below the infiltration plots (BSC 2003b, Section 7.6). In other words, the effective 
permeability of fractures just below the plot changed with time, although fracture properties may 
not change for zones away from the infiltration plots. Based on these considerations, infiltration 
rates (that are both spatially and temporally variable) at Alcove 8, rather than the pressure head, 
were used as the boundary condition at the large infiltration plot. The side boundary corresponds 
to zero-flow conditions (in the direction perpendicular to the simulation domain). The niche wall 
boundary was modeled by a zero-capillary-pressure condition, representing capillary barrier 
effects. The bottom boundary corresponds to free drainage conditions. As previously noted, 
Flint (1998, p. 44, Table 7) reported that under ambient conditions, matrix saturation is 0.72 for 
tsw33 and 0.85 for tsw34. Because of the disturbance of nearby fault tests, the actual matrix 
saturations are expected to be higher than these values. In the model, a value of 1.0 averaged 
with the saturation value reported by Flint (1998, p. 44, Table 7) was used as the initial matrix 
saturation value for each model layer. Because of this approximation, a larger degree of 
uncertainty is expected to exist for initial conditions assigned in the model. Other initial 
conditions assumed for the rock mass within the model domain are that the rock is solute-free 
and has a small water saturation (0.0105) in fractures. 
No. 3: Water Seeping into Drifts 
1
2
3
4
5
6
7
8
9 
10 
11 
12 
E-14 October 2003 
Vertical Column 
Revision 2
Revision 2 
Model Calibration E.4.2.3 
Model calibration is needed to develop site-specific rock properties before a meaningful 
prediction of future test results can be made. Model calibration was performed using the inverse 
modeling code iTOUGH2 V4.0 (LBNL 1999a). The observed spatial distribution of the seepage 
rate on the ceiling of Niche 3 was explicitly considered. In addition to the observed total seepage 
rate as a function of time, the seepage rates from individual intersections between the niche 
ceiling and the vertical columns in tsw34 (Table E-1) were matched in the model calibration 
procedure. Note that Columns 1 to 9 in tsw34 correspond to individual seepage trays. In this 
case, the seepage rates used in model calibration for a column are the same as those observed 
from the corresponding tray. The situation is more complicated for Columns 10 to 12. Seepage 
rates (as a function of time) for Column 10 were taken as a summation of seepage rates from 
Tray U1-B3 and a quarter of the seepage rates from Tray U1-B1. Seepage rates for Columns 11 
and 12 were taken as one-quarter and one-half of seepage rates from Tray U1-B1, respectively. 
Model calibration adjusts rock properties such that modeling results match field observations. 
For model layer tsw33, calibrated rock properties are fracture permeabilities and van Genuchten 
alphas for vertical columns (corresponding to individual infiltration plots) and for the rest of rock 
mass. An initial guess of fracture permeability for a column was determined by the largest 
infiltration rate (for time greater than 1 day) at the infiltration plot under water pressure head of 
2 cm. The largest infiltration rate (per unit area) is considered to be the saturated hydraulic 
conductivity for the column. A scale factor was used to calibrate all these fracture permeability 
values for the columns in tsw33 such that calibrated fracture permeability for a vertical column is 
equal to its initial guess, multiplied by the calibrated scale factor. This way the effects of 
observed spatial variability of infiltration rate were approximately captured by the model 
calibration. (Note that a vertical column in tsw33 has a uniform property distribution.) For 
model layer tsw34, calibrated rock properties are again fracture permeabilities and 
van Genuchten alphas for vertical columns (corresponding to seepage trays) and for the rest of 
rock mass. While most vertical columns have uniform distributions in this model layer, 
Columns 1, 6, 11, and 12 were further divided into two parts, upper and lower. The upper and 
lower parts have different rock properties for each of the columns mentioned above in order to 
consider rock-damage effects on rock properties near the niche ceiling. The lower parts 
correspond to rock between the niche ceiling and 0.4 m above the ceiling. Fracture porosity 
calibrated from the fault tests and matrix properties used in fault-test modeling studies are used 
here. These properties were not varied during model calibration. 
Experimental observations from boreholes about 1 m above the niche ceiling indicate that 
water-front transport times from the infiltration plots to the niche ceiling are fairly uniform 
(about 30 days) (DTN: LB0308A8N3TRTM.001). Simulated water transport time is related to 
initial matrix saturation because of matrix imbibition process. Considering the large degree of 
uncertainty in initial matrix saturation values used in the model, water transport time data were 
used as soft data only. To do so, zero vertical water flux along the columns at locations about 
0.4 m above the ceiling were treated as observed data for a period of 0 to 20 days. Use of these 
data is equivalent to making sure that water transport times are generally larger than 20 days in 
the model. Since the major purpose of model calibration is to develop a calibrated model for 
predicting future test results, and considering that a large degree of uncertainty exists about the 
October 2003 E-15 No. 3: Water Seeping into Drifts
initial conditions of the model, relatively high weights were given to the seepage rate data at later 
stage of the Phase I test (time greater than 90 days). Table E-2 lists calibrated rock properties. 
Note that the calibration step discussed in this section is an integral part of developing a sound 
model for predicting future tests to be conducted at Alcove 8CNiche 3. The model is developed 
using only data from the time before the prediction period. This modeldeveloped based on 
prior informationis then used for pretest predictions of future experiments, as discussed in the 
next section. 
Model Layer 
tsw33 
tsw34 
Column 1 0.9926  10.13 
Column 2 0.1685  10.12 
Column 3 0.2959  10.13 
Column 4 0.3146  10.13 
Column 5 0.5569  10.13 
Column 6 0.1845  10.13 
0.2453  10.3 
Column 7 0.1314  10.13 
Column 8 0.6757  10.13 
Column 9 0.2470  10.13 
Column 10 0.9786  10.13 
Column 11 0.1864  10.12 
Column 12 0.3332  10.13 
0.1190  10.11 Rest rock mass 0.4787  10.3 
0.225  10.11 Column 1 (upper) 0.5677  10.3 
0.704  10.12 Column 2 0.1480  10.2 
0.448  10.14 Column 3 0.1152  10.2 
0.171  10.13 Column 4 0.3857  10.2 
0.304  10.14 Column 5 0.8647  10.3 
0.149  10.13 Column 6 (upper) 0.2932  10.3 
0.434  10.11 Column 7 0.1891  10.2 
0.614  10.13 Column 8 0.3208  10.2 
0.104  10.13 Column 9 0.5316  10.2 
0.616  10.14 Column 10 0.9825  10.3 
Column 11 (upper) 0.189  10.14 0.3107  10.3 
Column 12 (upper) 0.143  10.13 0.2424  10.3 
0.495  10.12 Rest rock mass 0.7399  10.3 
Column 1 (lower) 0.5012  10.12* 0.1275  10.2 
Column 6 (lower) 0.5012  10.12* 0.2052  10.2 
Column 11 (lower) 0.5012  10.12* 0.2360  10.2 
Column 12 (lower) 0.5012  10.12* 0.1721  10.2 
NOTE: *These properties are not varied during model calibration. 
Table E-2. Calibrated Rock Properties 
Van Genuchten  Permeability Van Genuchten m 
0.608* 
0.608* 
Porosity 
0.066* 
0.010* 
No. 3: Water Seeping into Drifts E-16 
Revision 2 
October 2003
Test Phase 
Model Prediction E.4.2.4 
This section documents predictions of future Alcove 8Niche 3 test results. Associated 
uncertainties in the model prediction are presented in Section E.4.2.5. 
After about 210 days of ponded release of water to 12 infiltration plots, the test condition was 
changed on March 24, 2003, such that water is released to Plots 2 and 12 only. These two plots 
have the largest infiltration rates at the late stage of the ponded water release. Seepage responses 
to this focused-infiltration condition are expected to provide information regarding connectivity 
of flow paths between infiltration plots and individual seepage trays. Then the original test 
condition (ponded release of water to 12 infiltration plots) will be restored. After approximately 
steady-state infiltration and seepage processes are reestablished, different tracers are 
simultaneously introduced into the infiltrating water applied at different infiltration plots. 
Table E-3 gives the information regarding tracers to be used. Phase II tests (corresponding to 
50 percent of the infiltration rate observed at the end of Phase I) will start once the multiple 
tracer tests are completed. Again, after approximately steady-state infiltration and seepage 
processes are established for the reduced infiltration rate, a tracer (pentafluorobenzoic acid, with 
molecular diffusion coefficient of 7.6  10-10 m2/s) will be introduced into infiltrating water at all 
12 infiltration plots. Total mass and the concentration in infiltrating water at infiltration plots are 
5 g and 25 mg/l, respectively, for this tracer. In all the tracer tests, tracer concentrations as a 
function of time will be observed at Niche 3. 
Phase I 
1
2
3
4
5
6
7 Phase II 
NOTE: *Zone 1 includes infiltration plots 1 and 2; zone 2 includes plots 3 to 9; zone 3 includes plots 10 to 12. 
Seepage rate data collected for the first 210 days (after the large-plot tests started) were used for 
model calibration (Section E.4.2.3). The calibrated model was used to predict test results after 
the first 210 days. Forward simulations using iTOUGH2 V4.0 (LBNL 1999a) were performed 
for predicting seepage rates. T2R3D V1.4 (LBNL 1999b) was used for simulating tracer 
transport. The dispersion process was ignored because it has an insignificant effect on overall 
solute transport behavior, as discussed in UZ Flow Models and Submodels (BSC 2003b, 
Section 7.6.3). Again, following Moridis et al. (2003, Table 1), the tortuosity factor for the tuff 
matrix are approximated by the corresponding matrix porosity. 
No. 3: Water Seeping into Drifts 
Tracer Name 
Table E-3. Tracers To Be Used in Phases I and II Tests 
2-6-Difluorobenzoic Acid 
Potassium Iodide 
2,5-Difluorobenzoic Acid 
Calcium Bromide 
2,4,5-Trifluorobenzoic 
Acid 
Potassium Fluoride 
Pentafluorobenzoic Acid 
Molecular 
Diffusion 
Coefficient 
(m2/s) 
1000 8.1  10-10 
1000 2.045  10-9 
500 8.1  10-10 
Applied 
Solution 
Volume 
(liters) 
500 2.080  10-9 
1000 7.9  10-10 
1000 1.475  10-9 
2000 7.6  10-10 
E-17 
1,2,3 
Tracer 
Concentration 
50 
10 
50 
500
(ppm) 
Infiltration 
Zone No* 
50 
50 
25 
Tracer Number 
1
1
2
2
3
3 
13.713 
55.49 18.020 
55.49 18.020 
24.945 80.18 
October 2003 
Infiltration 
Rate 
(l/d) 
Revision 2 
Duration of 
55.08 18.156 
55.08 18.156 
36.46 13.713 
36.46 
tests 
(days)
Revision 2 
Figure E-9 shows simulated total seepage rates for both Phases I and II. Figure E-10 presents the 
corresponding (simulated) seepage rates for different vertical rock columns corresponding to 
individual seepage trays (Table E-1). Figures E-11, E-12, and E-13 show predicted tracer 
breakthrough curves for different vertical rock columns for Phase I. Note that, in Phase I, a 
tracer is applied to several selected infiltration plots, but not all the plots (see Table E-3). The 
lack of any breakthrough curve for a particular tray is because there are not flow paths 
connecting the tray to infiltration plots where the corresponding tracer is applied. The 
corresponding seepage-flux-averaged breakthrough curve is also given in Figure E-14. The 
predicted breakthrough curves for Phase II tests are presented in Figures E-15 and E-16. 
NOTE: The observed seepage rate data used for model calibration are also shown here. 
Figure E-9. Simulated Total Seepage Rates for Both Phase I and Phase II 
E-18 No. 3: Water Seeping into Drifts October 2003
NOTE: The observed seepage rate data used for model calibration are also shown here. 
Figure E-10. Simulated Total Seepage Rates for Different Vertical Rock Columns Corresponding to 
Individual Seepage Trays 
No. 3: Water Seeping into Drifts 
Revision 2 
October 2003 E-19
Revision 2 
Figure E-11. Predicted Tracer Breakthrough Curves for Different Rock Columns for Phase I: Results for 
Tracers 1 and 2 
October 2003 E-20 No. 3: Water Seeping into Drifts
Revision 2 
Figure E-12. Predicted Tracer Breakthrough Curves for Different Rock Columns for Phase I: Results for 
Tracers 3 and 4 
October 2003 E-21 No. 3: Water Seeping into Drifts
Revision 2 
Figure E-13. Predicted Tracer Breakthrough Curves for Different Rock Columns for Phase I: Results for 
Tracers 5 and 6 
October 2003 E-22 No. 3: Water Seeping into Drifts
Revision 2 
Figure E-14. Predicted Seepage Flux-Averaged Tracer Breakthrough Curves for Phase I 
Figure E-15. Predicted Seepage Flux-Averaged Tracer Breakthrough Curve for Phase II 
October 2003 E-23 No. 3: Water Seeping into Drifts
Revision 2 
Figure E-16. Predicted Tracer Breakthrough Curves for Different Rock Columns for Phase II 
Model Uncertainty and Other Issues E.4.2.5 
It is important to note that the current pretest prediction is subject to a large degree of 
uncertainty. This section discusses the major uncertainties involved and how these uncertainties 
can be quantified and reduced in future testing and modeling activities. 
One major uncertainty is associated with water flow paths from the infiltration plots to the 
ceiling of the niche. Particularly, connectivity between water flow paths from each of the 
12 infiltration plots to individual infiltration trays is largely unknown. The consideration of 
spatial variabilities in both infiltration and seepage rates in the current model calibration cannot 
adequately capture the detailed flow patterns between Alcove 8 and Niche 3. However, the 
pattern and connectivity of flow largely determine future test results (especially at a scale 
characterized by individual seepage trays). While the flow paths from Alcove 8 to Niche 3 are 
October 2003 E-24 No. 3: Water Seeping into Drifts
Revision 2 
determined by the geometry of the fracture network, characterizing this fracture network and its 
hydraulic connectivity based on available fracture mapping data is difficult and leads to 
ambiguous interpretations, as is evident from the poor correlation between properties of mapped 
fractures on the ceiling of Niche 3 and the observed seepage rate distribution. This uncertainty 
regarding the flow paths can be investigated, using the future results of tracer tests that involve 
different tracers applied at different infiltration plots. Future calibration of the numerical model 
against the tracer test data will improve the characterization of the flowing fracture connectivity 
from the Alcove 8 infiltration plots to the ceiling and collection trays in Niche 3. 
The second major uncertainty is related to the potential enhancement of matrix diffusion. 
Analyses of the fault test results indicated that matrix diffusion is indeed an important process 
for retarding the tracer transport and that the fault-matrix interface area (or the effective matrix 
diffusion coefficient) needed to be increased to match the test results with the corresponding 
numerical model (BSC 2003b, Section 7.6). This potential enhancement of matrix diffusion is 
supported by some studies reported in the literature (BSC 2003b, Section 7.6). However, the 
physical mechanisms behind this potential enhancement are not totally clear at this stage. Also, 
whether the similar enhancement holds for fractured rock away from the fault zone is still an 
open question. If the enhancement of matrix diffusion is the case for nonfault fractured zones, 
the current prediction results likely underestimate tracer breakthrough times and overestimate 
peak concentration values. 
Finally, uncertainties also exist in our conceptual understanding of the temporal variability of 
infiltration rates. As previously indicated, significant temporal variabilities of infiltration rates 
(for a given water pressure head at infiltration plots) have been observed from both fault tests 
and large-plot tests. These variabilities cannot be explained by the interplay between capillary 
pressure gradients and gravity effects. The current understanding is that they may result from 
fracture infilled materials (particles). These materials (particles) move around and can either 
open or plug pore spaces in fractures near infiltration plots, resulting in fluctuation and final 
reduction of infiltration rates. This mechanism is only approximately considered in the model by 
using observed infiltration rates as a boundary condition. However, a future disturbance at the 
infiltration plots (e.g., changes in applied infiltration rates and (or) water-pressure head) may 
activate particle movement again, further modifying the effective fracture permeability and its 
spatial distribution below the infiltration plots. This temporal modification of rock properties is 
difficult to capture in the model. It should be noted that, because of this issue, one of the planned 
test objectives regarding estimation of relations between relative permeability and water 
potential might be extremely difficult to achieve. 
E.4.3 Summary 
Alcove 8Niche 3 tests provide a unique opportunity to examine important flow and transport 
processes in the unsaturated zone of Yucca Mountain, including infiltration-seepage processes, 
matrix diffusion, and the character of flow and transport within a fault and fracture network. 
This appendix provides model-prediction results for Alcove 8Niche 3 large-plot tests 
(Section E.4.2), including a discussion of the major model uncertainties and how these 
uncertainties can be quantified and reduced in future testing and modeling activities 
(Section E.4.2.5). 
October 2003 E-25 No. 3: Water Seeping into Drifts
Revision 2 
E.5 REFERENCES 
E.5.1 Documents Cited 
Brocoum, S. 2001. Response to Radionuclide Transport Key Technical Issue Technical 
Exchange Subissue 3, Agreement 6; and Structural Deformation and Seismicity Key Technical 
Issue Technical Exchange Subissue 3, Agreement 2 with Concurrence CopyEnclosure not 
Included, March 12, 2001. Letter from S. Brocoum (DOE) to C. W. Reamer (NRC), March 12, 
2001. ACC: MOL.20030922.0008. 
BSC (Bechtel SAIC Company) 2003a. In Situ Field Testing of Processes. ANL-NBS-HS- 
000005 REV02B. Las Vegas, Nevada: Bechtel SAIC Company. ACC: MOL.20030915.0238. 
BSC 2003b. UZ Flow Models and Submodels. MDL-NBS-HS-000006 REV 01. Las Vegas, 
Nevada: Bechtel SAIC Company. ACC: DOC.20030818.0002. 
Flint, L.E. 1998. Characterization of Hydrogeologic Units Using Matrix Properties, Yucca 
Mountain, Nevada. Water-Resources Investigations Report 97-4243. Denver, Colorado: 
U.S. Geological Survey. ACC: MOL.19980429.0512. 
LBNL (Lawrence Berkeley National Laboratory) 1999a. 09/16/1999. Software Code: 
iTOUGH2. V4.0. SUN, DEC. 10003-4.0-00. 
LBNL 1999b. Software Code: T2R3D. V1.4. FORTRAN 77, SUN, DEC / ALPHA. 
10006-1.4-00. 
Liu, H.H.; Bodvarsson, G.S.; and Finsterle, S. 2002. A Note on Unsaturated Flow in 
Two-Dimensional Fracture Networks. Water Resources Research, 38, (9), 15-1 to 15-9. 
[Washington, D.C.]: American Geophysical Union. TIC: 253307. 
Moridis, G.J.; Hu, Q.; Wu, Y-S.; and Bodvarsson, G.S. 2003. Preliminary 3-D Site-Scale 
Studies of Radioactive Colloid Transport in the Unsaturated Zone at Yucca Mountain, Nevada. 
Journal of Contaminant Hydrology, 60, ([3-4]), 251-286. New York, New York: Elsevier. 
TIC: 253921. 
Pruess, K. and Narasimhan, T.N. 1985. A Practical Method for Modeling Fluid and Heat Flow 
in Fractured Porous Media. Society of Petroleum Engineers Journal, 25, (1), 14-26. 
Dallas, Texas: Society of Petroleum Engineers. TIC: 221917. 
Reamer, C.W. 2002. Radionuclide Transport Key Technical Issue Agreements. Letter from 
C.W. Reamer (NRC) to S. Brocoum (DOE), February 6, 2002, with attachments. 
ACC: MOL.20020920.0318. 
Reamer, C.W. and Williams, D.R. 2000. Summary Highlights of NRC/DOE Technical 
Exchange and Management Meeting on Radionuclide Transport. Meeting held December 5-7, 
2000, Berkeley, California. Washington, D.C.: U.S. Nuclear Regulatory Commission. 
ACC: MOL.20010117.0063. 
October 2003 E-26 No. 3: Water Seeping into Drifts
Revision 2 
Schlueter, J. 2000. U.S. Nuclear Regulatory Commission/U.S. Department of Energy Technical 
Exchange and Management Meeting on Structural Deformation and Seismicity (October 11-12, 
2000). Letter from J. Schlueter (NRC) to S. Brocoum (DOE), October 27, 2000, with 
enclosure. ACC: MOL.20010730.0232 
Schlueter, J. R. 2003. Staff Review of Information Addressing Radionuclide Transport (RT) 
Agreement 3.06 and Structural Deformation and Seismicity (SDS) Agreement 3.02, Status Partly 
Received. Letter from J.R. Schlueter (NRC) to J.D. Ziegler (DOE), February 14, 2003, with 
attachment. CCU #0220036149. ACC: MOL.20030909.0374. 
Ziegler, J.D. 2002. Transmittal of Information Addressing Key Technical Issue (KTI) 
Agreement Items Radionuclide Transport (RT) 3.06 and Structural Deformation and Seismicity 
(SDS) 3.02. Letter from J.D. Ziegler (DOE) to J.R. Schlueter (NRC), June 27, 2002, with 
attachments. ACC: MOL.20020819.0283. 
E.5.2 Data, Listed by Data Tracking Number 
Data to be submitted. Model calibration using seepage rate data from Alcove 8Niche 3 
large-plot tests (Phase I). Submittal date: TBD. 
Data to be submitted. Model prediction for Alcove 8Niche 3 large-plot tests (Phase I and 
Phase II). Submittal date: TBD. 
GS030108314224.001. Geotechnical Data for Alcove 8 (ECRB) and Niche 3 (ESF): Full 
Periphery Geologic Map (Drawing OA-46-356). Submittal date: 02/05/2003. 
LB0306A8N3LIQR.001. Fault Infiltration Test from Alcove 8 to Niche 3 (9/18/2002 
10/16/2002). Submittal date: 06/19/2003. 
LB0308A8N3SEEP.001. Seepage Rate Data for Alcove 8Niche 3 Large Plot Tests (Phase I). 
Submittal date: 09/23/2003. 
LB0308A8N3TRTM.001. Water Front Travel-Time Data for Alcove 8Niche 3 Large Plot 
Tests (Phase I). Submittal date: 09/23/2003. 
October 2003 E-27 No. 3: Water Seeping into Drifts
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E-28 No. 3: Water Seeping into Drifts 
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October 2003