Dike Propagation Near Drifts Rev 00, ICN 00

ANL-WIS-MD-000015

April 2000

1. PURPOSE 
The purpose of this Analysis and Model Report (AMR) supporting the Site 
Recommendation/License Application (SR/LA) for the Yucca Mountain Project is the 
development of elementary analyses of the interactions of a hypothetical dike with a repository 
drift (i.e., tunnel) and with the drift contents at the proposed Yucca Mountain repository. This 
effort is intended to support the analysis of disruptive events for Total System Performance 
Assessment (TSPA). This purpose is documented in the development plan Coordinate Modeling 
of Dike Propagation Near Drifts Consequences for TSPA-SR/LA (CRWMS M&O 2000a). 
These analyses are intended to provide reasonable bounds for a number of expected effects 
1. Temperature changes to the waste package from exposure to magma 
2. The gas flow available to degrade waste containers during the intrusion 
3. Movement of the waste package as it is displaced by the gas and magma from 
the intruding dike (the number of packages damaged) 
4. Movement of the backfill 
5. The nature of the mechanics of the dike/drift interaction. 
These analyses serve two objectives: to provide preliminary analyses needed to support 
evaluation of the consequences of an intrusive event and to provide a basis for addressing some 
of the concerns of the Nuclear Regulatory Commission (NRC) expressed in the Igneous Activity 
Issue Resolution Status Report (IRSR) (Reamer 1999). 
The estimates of the number of waste packages at risk and the circumstances of that risk are 
functional inputs for two technical products: Igneous Consequence Modeling for TSPA-SR 
(CRWMS M&O 2000b) and Number of Waste Packages Hit by Igneous Intrusion (CRWMS 
M&O 2000c). 
2. QUALITY ASSURANCE 
This document was prepared in accordance with AP-3.10Q, Analyses and Models, and the 
development plan Coordinate Modeling of Dike Propagation Near Drifts (CRWMS M&O 
1999b), which was, in turn, prepared in accordance with AP-2.13Q, Technical Product 
Development Planning. A Technical Change Request (T2000-0040) was approved in accordance 
with AP-3.4Q, Level 3 Change Control. The development of this technical document has been 
evaluated (CRWMS M&O 1999a) in accordance with QAP-2-0, Conduct of Activities, and has 
been determined to be subject to the requirements of the Quality Assurance Requirements and 
Description (DOE (U.S. Department of Energy) 2000). 
All inputs to this document are listed in the Document Input Reference System (DIRS) for this 
report, in accordance with AP-3.15Q, Managing Technical Product Inputs. Accepted data as

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 8 
identified in the DIRS sheets are identified in accordance with AP-SIII.2Q, Qualification of 
Unqualified Data and the Documentation of Rationale for Accepted Data. The conclusions 
presented in this AMR do not affect the repository design permanent items as discussed in QAP- 
2-3, Classification of Permanent Items. 
In addition to the procedures cited above, the following procedures are applicable to this 
document: AP-2.14Q, Review of Technical Products, AP-3.14Q, Transmittal of Input, AP-6.1Q, 
Controlled Documents, and AP-17.1Q, Record Source Responsibilities for Inclusionary Records. 
3. COMPUTER SOFTWARE AND MODEL USAGE 
No software subject to the requirements of the AP-SI.1Q, Software Management was used in the 
preparation of this document. The commercial application software Microsoft Word (Office97) 
and PowerPoint (Office 97) were used to generate text and to construct figures and flow charts. 
The software was appropriate for the applications. Two sets of analyses, labeled as the first and 
second conceptual models, are identified and executed to establish the basis for PA analyses of 
the response of waste packages to an igneous intrusion. 
4. INPUTS 
The inputs to this document were analyses and ranges of data published in the technical 
literature. 
4.1 PARAMETERS 
Specific parameters used are listed here in Table 1, Table 2, Table 3, and in Section 6.3.1 under 
Current Stress State, Section 6.3.2 under Design Description and Section 6.3.4 under Gas Flow. 
Table 1. Input Parameters and Current QA Status 
Definition Symbol Value References Input Status 
Radius of the drift a ~2.75 m DTN: SN9908T0872799.004 Accepted 
Thermal conductivity 
of solid basalt K 
21.76 J/(kg sec C) 
0.0052 cal/(g sec C) 
Hodgman et al. 1955, p. 2251, 
Table Heat Conductivity Accepted 
Fusion temperature 
of magma 
Tf 1046-1169 C 
CRWMS M&O 2000d, Sec. 
6.2.3 
Technical 
Product Output 
Density of magma . 24842663 kg/m3 CRWMS M&O 
2000d, Sec. 6.2.4 
Technical 
Product Output 
Waste container skirt None ~.225 m CRWMS M&O 1999b Accepted 
Container separation None ~.10 m DTN: SN9908T0872799.004 Accepted 
Mass of Waste 
Package M 42.3 metric tons CRWMS M&O 2000e, p. II-2 Technical 
Product Output 
Drip shield perimeter None ~6.5 m DTN: SN9908T0872799.004 Accepted 
Notes: Data tracking number (DTN) 
Quality assurance (QA)

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 9 
Table 2. List of Exsolved Gases 
Species Mole Fraction References Input Status 
H2O 73.16 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
H2 1.17 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
CO2 14.28 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
CO 0.57 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
SO2 9.45 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
S2 0.37 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
HCl 0.49 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
HF 0.06 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
H2S 0.74 
CRWMS M&O 2000d 
ANL-MGR-GS-000002 
Technical Product 
Output 
Table 3. Properties of Exsolved Gases 
Species 
Critical 
Temperature 
K 
Critical 
Pressure 
Atm 
Molecular 
Wt. References 
Input 
Status 
H2O 647.14 217.7 18.01 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f 
Accepted 
H2 32.97 12.76 2 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f Accepted 
CO2 304.14 72.78 44.01 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f 
Accepted 
CO 132.91 34.53 28.01 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f 
Accepted 
SO2 430.8 77.8 64.06 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f 
Accepted 
S2 1314 204.28 64.12 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f 
Accepted 
HCl 324.7 82 36.46 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f Accepted 
HF 461 63.95 20.01 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f 
Accepted 
H2S 373.2 88.23 34.08 
Lide and Frederikse 1997 
p. 4-37f, p. 6-50f 
Accepted

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 10 
Reference information was obtained from the Technical Information Center and the Technical 
Data Management System, which is a controlled source. Sources are cited in the text where 
applicable and in Section 8, References. 
.
4.2 CRITERIA 
These analyses are investigatory and intended to provide estimates of the sizes of the effects of 
dike propagation. No criteria applicable to these analyses have been identified. 
4.3 CODES AND STANDARDS 
No codes or standards were used in these analyses. 
5. ASSUMPTIONS 
Assumptions are described here in general terms and are discussed in more detail in the sections 
in which they are used. 
5.1 GAS FLOW 
As real gas is supplied to the drift by the dike or vent: 
 There is isothermal flow down the drift (no axial temperature gradient). 
 Adiabatic expansion is ignored. 
 Heat carried into the rock (the porous media) by the gas is ignored. 
 There are no chemical interactions of the gases with the rock. 
 The components of the engineered barrier system (EBS), including backfill, are 
irrelevant to the flow. 
BasisGases exsolved from magma are real gases that obey the real gas law and satisfy the 
theorem of corresponding states as discussed (Pirson 1977). 
Confirmation StatusThese assumptions are shown to be conservative as a result of the analysis 
and do not need to be confirmed. 
Use in the AnalysisThese assumptions are used in Section 6.3.4 in the computation of gas flow.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 11 
5.2 SOLIDIFICATION OF MAGMA 
Estimates and calculations of the phase change behavior occur as discussed in Jaeger (1964), 
Kreith and Romie (1955), Soward (1980), Stewartson and Waechter (1976), Riley et al. (1974), 
and Pedroso and Domoto (1973). Drift wall temperature is assumed to be ~ 600C. Latent heat 
of fusion (L) and the specific heat (C) are assumed to be 100 cal/gm (upper limit) and ~ 0.3, 
respectively (from Jaeger 1964). 
BasisThe literature provides a reasonable basis for magmatic properties for this analysis and 
data specific to Yucca Mountain has been provided (CRWMS M&O 2000d). 
Confirmation StatusThe assumptions are taken from the literature and represent typical or best 
available information and do not need to be confirmed. 
Use in the AnalysisThe cited analyses and estimates are used in Section 6.3.5 and referenced in 
Section 8.1. 
5.3 CONTAINER 
A container of ~ 42.3 metric tons (CRWMS M&O 2000e, p. II-2) will be a representative 
package moved by the pressure pulse. 
BasisDesign information is taken from the current design as indicated by the citations. 
Confirmation StatusThe description of the waste package is obtained from design data and is 
confirmed in those citations. 
Use in the AnalysisThe design information is used in Section 6.3.3. 
6. ANALYSIS 
6.1 INTRODUCTION 
A long-standing problem in understanding the nature of possible volcanic disruption of a 
repository has been the physical details of how a dike interacts with a repository drift (and with a 
set of drifts) (Barr et al. 1993, p. 141). This problem of a dike interacting with a repository drift 
is not amenable to direct simulationdirect calculation of the interactions. Simulation would 
have allowed systematic examination of the most important processes. Rather, the problem is 
attacked piecemeal by examining end members or limiting cases of processes which can be 
modeled, and by interpretation, in terms of the Yucca Mountain site, of geologic observations of 
relic cinder cones and active volcanic systems believed to be analogous. End members (or 
bounding cases) are chosen by analysts because they provide an expeditious way to identify and 
explore physically possible dike/drift interactions for the consequences of the interactions. Some 
interactions can be rejected on the basis of negligible consequence and those needing more 
careful examination can be identified.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 12 
The results are often simplified because the fundamental driving processes producing the 
intrusion, extrusion and the volcano are not well-formulated at present. The interpretations are 
used to produce plausibility arguments about the interaction of the intrusive dike with a 
repository; and, however well argued, are the matters of contention between the Project and the 
NRC (Reamer 1999). 
This AMR is intended to provide a better focus on identifying the detailed problems, why they 
might be important, and how they are related. The AMR is also intended to provide simple 
estimates for some of the effects, based only on analyses and interpretations already provided in 
the literature. 
6.2 BASIC ISSUES 
This AMR addresses and attempts to provide context for several end member cases of the dike 
propagation problem, and to provide a framework for the dike/repository interaction problem as 
a whole. Because, in the absence of simulation, modeling decisions are made based on 
plausibility arguments constructed around their interpretations of analogue data and reasoned 
speculations, part of that context is presented in the form of a decision tree. 
The decision tree, Figure 1 (p. 39), presents where those decisions of what is plausible 
(represented by yes or no choices) are made, and how they are interrelated. A simple 
decision tree allows identification of the modeling choices made to reach surface release. The 
tree entries which receive the most interest are the final components, namely the formation of the 
ash plume, and its distribution and deposition. However, getting to the releases requires an 
assembly of components describing the details of the interactions. Some of those details are 
indicated on the tree as ovals, referred to as conditionals. These represent some of the 
supporting work which is required in order to make decisions about how the dike might 
reasonably be expected to interact with a drift. The topics of this AMR are analyses that feed 
these decisions. For a general discussion of dike development and properties refer to 
Characterize Eruptive Processes at Yucca Mountain, Nevada ANL-MGR-GS-000002 (CRWMS 
M&O 2000d). 
Interaction of a dike with a drift, based on velocity of propagation of the dike, is first a 
mechanical interaction and later, when connecting pathways are established, a thermal and fluid 
flow interaction. In order to provide an overall perspective of the interaction of a dike and a 
drift, it is necessary to discuss when and how current interpretations fit together. 
6.3 ANALYSES 
There are two basic conceptual models of how a dike and drift might interact. The first presumes 
that a drift is a relatively insignificant heterogeneity in the rock, which is intersected and 
otherwise provides no interaction with the dike as it propagates to the surface. Essentially, the 
forces driving propagation of the dike are so large that the drift is only a minor perturbation. The 
result is a planar (slab-like) intersection of the dike and driftthe idealized interpretation. The 
dike-repository interactions are then (1) direct physical entrainment of waste in the dike and 
(2) flow of gas and magma, or gas and fragments, down the drift to interact with waste 
containers and waste. These two kinds of interactions involving an idealized intersection of drift

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 13 
and dike, are pursued in Sections 6.3.3 Shock Interaction, 6.3.4 Gas Flow, and 6.3.5 Magma 
FlowThermal Environment. Since energy dissipation has been ignored, the idealization would 
be expected to produce stronger effects in the drift than would really occur. 
The second conceptual model presumes that the dike, which propagates by means of a selfgenerated 
crack, (Spence and Turcotte 1985; Turcotte et al. 1987) interacts strongly with the 
stress-altered region (which forms around the drift) and with the void space in a drift. It is 
currently thought that dikes are emplaced normal to least principal stress as measured regionally 
in the near-surface (Tsunakawa 1983; Delaney et al. 1986). For this conceptual model, the 
thermo-mechanical state of the mountain (and repository) is important. This is the case because 
the dike is interacting with a stress field which is evolving and therefore the stress-state is not 
fixed in time. That is, when the drift is driven, the surrounding rock first tries to relax into the 
drift. When waste is added, the waste heat causes thermal expansion which puts the rock around 
the drift into compression. This compression relaxes as the repository cools. These stress 
alterations are large enough so that the least principal stress (currently NNW-SSE) is rotated to 
vertical (Hardy and Bauer 1992); a circumstance which could alter how a propagating dike 
behaves as it encounters the stress-altered zone (perhaps producing a sill rather than a dike). 
After several thousand years, as the mountain cools, the least principal stress rotates back to its 
original direction. 
Of these conceptual models, the more complete description from current literature is the second 
(Watanabe 1999), which will be pursued in this analysis in Sections 6.3.1 Thermal-mechanical 
Evolution of the Repository and Mountain and 6.3.2 Interaction with the Drift. This second, 
physically more complete conceptual model functions to establish the constraints and 
qualitatively estimate the bounds that apply to the detailed interactions analyzed for the simple 
idealized model. Performance Assessment (PA) uses the first conceptual model as stated in 
Igneous Consequence Modeling for the TSPA-SR, ANL-WIS-MD-000017 (CRWMS M&O 
2000b). PA also uses the second complex model to provide constraints on the first model. 
The expected dike-repository interactions are (1) propagation of the dike into and across the 
drifts as described by the intersection of the dike crack with the drift in an evolving stress field, 
(2) flow of gas and magma, or gas and fragments, down the drift to interact with waste 
containers and waste, and (3) direct physical entrainment of waste in the dike. 
The specific problem of waste entrainment has been treated in detail elsewhere (Wilson et al. 
1994; CRWMS M&O 2000b (ANL-WIS-MD-000017)); CRWMS M&O 2000f (ANL-WIS-MD- 
000005) and will not be further examined. 
The analyses are laid out as indicated in the decision tree in Figure 1, where (1) rhombuses 
enclose questions, (2) rectangles enclose the analyses implied by the answers, and (3) ovals are 
conditionals referring to supporting information.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 14 
6.3.1 Thermal-Mechanical Evolution of the Repository and Mountain 
Analysis of the interaction of a dike with the repository requires identification of the time of 
occurrence and specification of the design of the repository. The initial interaction of a 
propagating dike with the repository is a mechanical process involving the interception of the 
crack propagating ahead of the dike with the void space of the drifts and the stress-relieved zone 
around the drifts (Brady and Brown 1985, p. 192f). After the initial interaction, the interaction 
becomes a fluid flow and thermal process. The expected direction of dike emplacement is 
controlled by the stress state and is generally normal to the least principal stress (Pollard 1987). 
Because the mechanical stress state of the mountain is changing as an effect of repository heat, 
the time dependence of the changes needs to be recognized explicitly. Accordingly, future time 
is separated into the thermal period, when the mountain is heated enough for the least principal 
stress to have rotated to vertical at the repository horizon, and the post-thermal period when the 
stress has returned approximately to its present orientation. This separation is honored in Figure 
1, the decision tree, with the first branching. 
Current Stress StateAccording to hydraulic fracturing stress measurements at and around 
Yucca Mountain, it appears that the least principal stress direction is horizontal about N60W as 
derived from the following references: 
 N60WN65W (Stock et al. 1985) 
 N51WN52W (Warren and Smith 1985) 
 N68W (Warren and Smith 1985) 
 N55WN60W (Frizzell and Zoback 1987). 
The minimum horizontal stresses measured were 2.6 to 3.1 MPa (Warren and Smith 1985) at 
330 m and 4.2 to 5.4 MPa (Stock et al. 1985; Stock and Healy 1988) at 295, 418, and 646 m. 
Vertical stresses were 6.1, 8.4, and 12.9 MPa, respectively. The experimental determinations 
included measurements at Yucca Mountain wells (Stock et al. 1985), at G-Tunnel (Warren and 
Smith 1985; Smith et al. 1981), and at Hampel Wash (Frizzell and Zoback 1987) nearby on the 
Nevada Test Site. 
Expected Changes to the Stress StateCalculations of the stress state at the drifts (Hardy and 
Bauer 1992) were performed for design considerations, to address drift stability. Their 
calculations were based on the thermal loading of 57 kW/acre and an earlier layout design 
(Hardy and Bauer 1991, p. 5-15, p. 5-16). The analysis indicates that the three principal stresses 
increase, with the horizontal components exceeding the vertical component within a few decades 
of closure. The details of the time-dependent change of stresses around emplacement drifts and 
the main access drift differ somewhat, but both drift analyses lead to the conclusion that the least 
principal stress quickly becomes vertical. Analyses performed for the NRC (Mack et al. 1989) 
show similar results. Horizontal stresses at the drift alter from 36 MPa to 1520 MPa. Based 
on this work (Hardy and Bauer 1992) it appears that, at the repository level, the vertical least 
principal stress will persist for the order of 2000 years (Figures 2 and 3, (p. 40)). The largest 
principal stress (the vertical component) is initially at about 7 MPa and the least principal stress 
is about 3.5 MPa (Note that the ordinate scales of the figures differ by about a factor of two.). 
Because of the drift alignment used, the axial stress indicated in the figures is along the

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 15 
maximum principal horizontal stress. Figures 2 and 3 show that the least principal stress 
(horizontal at ~N60W) increases to exceed the vertical stress component and does so for about 
2000 years. The increases of the stress components at the main access drift are due to thermal 
expansion of the rock around the emplacement drifts. 
Although the calculations cited (Hardy and Bauer 1992) are directed at the level of the 
emplacement drifts, much more rock will be involved. This rotation of least principal stress can 
be expected to extend several hundred meters below and out from the repository horizon (the 
region affected by repository heat)(Mack et al. 1989). Figure 4 (p. 41) presents a diagram that 
shows the extent of influence. The region of alteration in which the least principal stress has 
been rotated is time dependent and eventually returns to its approximate horizontal orientation. 
Possible Effects of Stress RotationRotation of least principal stress from horizontal to vertical 
changes the stress field through which the dike and its leading crack must penetrate. If, as the 
literature indicates (Spence and Turcotte 1985; Turcotte et al. 1987, Stock et al. 1985), the dike 
will deflect to be normal to least principal stress, then the direction of dike propagation would be 
expected to be deviated. Figure 5 (p. 42) illustrates the changing stress state and the possibility 
of deviating the path of the dike from vertical, including possible sill formation. In Figure 5, Vo 
is the initial vertical principal stress, H0 is the larger horizontal principal stress and h0 is the least 
principal stress. These stresses are altered by the addition of thermally derived stresses from 
repository heat, (TS). For simplicity, Figure 5 (as modified from Anderson 1963) shows the 
addition to be linear with multiplying factors of a and b compared to the effect on h0 (see Figures 
2 and 3 for a better estimate of growth and relaxation). At some point the line for h0 crosses that 
for V0 and the least principal stress is then vertical. Accordingly, it is then possible for the 
direction of dike to deviate from the vertical and for a sill to develop (see the analysis of 
Anderson 1963, pp. 5053). This circumstance persists until cooling of the mountain allows 
rotation of the least principal stress back to horizontal. 
Since the Yucca Mountain block has bounding faults (e.g., Solitario Canyon, Bow Ridge), in 
addition to sill formation, a possible consequence is deflection or redirection of the dike 
propagation to these fault zones (Wilson et al. 1994, v. 1, pp. 224). These faults, which strike 
mostly north-south, have a strike that is only about 30 degrees from the direction of regional least 
principal stress. Because the way in which the thermal stress from the repository will affect 
these near-by fault zones is unknown, deviation of the magma flow up the fault zones to the 
surface is a possible alternative consequence to sill formation. 
As a result of these arguments on the changing stress state of Yucca Mountain, the decision tree 
of Figure 1 distinguishes the thermal period from the post-thermal period. There are additional, 
more detailed, effects on the drifts during the thermal period (Mack et al. 1989) which affect the 
actual dike/drift interaction, but which are not discussed because they are germane to other issues 
(e.g., closure of water-bearing fractures leading to the drift). 
Alternative InterpretationsThe Igneous Activity Issue Resolution Status Report (IRSR) 
(Reamer 1999, p. 52f) considers the details of stress around and at Yucca Mountain on two 
scales, the regional scale involving the tectonic setting and extension (Reamer 1999, p. 43f), and 
the local scale (Reamer 1999, p. 52). These issues arise in Probability Criterion 5, the

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 16 
probability of occurrence of igneous activity. The discussions under that Criterion are related to 
structural control of an intrusion and the ability of an existing fault to influence the propagation 
of a dike. An argument is presented for dike emplacement perpendicular to the least principal 
stress and parallel to the principal horizontal stress (Reamer 1999, p. 52). 
The time-dependent alteration of the local stress-state around Yucca Mountain (and possible 
effects on dike injection), due to repository heat, does not appear in the models discussed in the 
IRSR. 
6.3.2 Interaction with the Drift 
It appears that dikes propagate by fluid-induced fracturing of the confining rock (Lister and Kerr 
1991; Lister 1990a, 1990b; Spence and Turcotte 1985). A dike is preceded by a crack generated 
by the magma fluid pressure (Figure 4). The driving mechanism for the crack leading the dike is 
the buoyancy of the magma column relative to the adjacent rock column (due to the density 
difference) (Lister and Kerr 1991; Lister 1990a, 1990b; Pollard 1987; Spence et al. 1987; Spence 
and Turcotte 1985; Watanabe et al. 1999). Advance of the dike depends on the local differences 
between the buoyancy and the viscous pressure loss and the elastic stress in the rock. The total 
effective buoyancy, P, in the crack drives the fluid flow up the crack and propagates the crack in 
a manner which can be represented by equation 1. 
P = (.f - .r )gh + pe + pv 
(Eq. 1) 
where
.f = fluid density 
.r = rock density 
g = acceleration of gravity 
h = height of the dike 
pe = elastic (non-hydrostatic) pressure exerted by crack walls 
pv = viscous pressure loss 
(Lister 1990b, p. 265). 
With insightful analyses of the fluid mechanics of viscous fluids, interpretations of emplacement 
of many dikes and sills, and a few data on dike injection velocities (Lister and Kerr 1991; Aoki 
et al. 1999), various authors have established the general behavior of dike propagation and sill 
formation (Lister and Kerr 1991; Lister 1990a, 1990b; Pollard 1987; Spence et al. 1987; Spence 
and Turcotte 1985, 1990; Watanabe et al. 1999). (Equation 1 is a simple representation for these 
more complicated analyses.) These analyses derive (and depend on) the interpretations that 
dikes propagate by means such that the rate is in the range of a few meters per second to 1  107 
m/sec (Lister 1990a; Aoki et al. 1999). Once a dike has reached the surface, flow velocities, now 
less impeded, can be larger.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 17 
Two of these interpretations will affect the analyses of the following sections: there is a fluidfilled 
leading crack, and the plane of the dike tends to be normal to least principal stress. 
Fracture/Fracture InteractionThe buoyancy-driven magma fracture eventually interacts with 
the drift. The drift consists of a void spacethe original opening with waste packages, drip 
shield and backfilland the stress-relieved region around the opening. This stress-relieved 
region develops as country rock relaxes into the openings. Classically, the stress-relieved region 
extends out to about 3 drift diameters (Brady and Brown 1985, p. 192f; Jaeger and Cook 1979). 
Because the thermal output of the repository has significantly altered the local stress conditions 
(Hardy and Bauer 1991; Mack et al. 1989), the extent of stress-relief depends on when, in 
repository history, the dike intrusion is presumed to occur. During the thermal period (Figure 1, 
left branch), there is no stress-relief, rather the drift is experiencing compression (Mack et al. 
1989). Stress relief appears as strain adjustment, that is, concentric and radial fractures develop 
around the drift, accompanied by stoping (chimneying) in the drift. This fracture/fracture 
interaction is intended to provide input for each of two decisions on parallel branches on the right 
hand side of the tree. 
To establish how the dike fracture might be expected to interact with the drift, consider the case 
of no stress-relief, so that the interaction can be approximated as a linear crack (the dike crack) 
encountering a penny-shaped crack (the drift). This approach is extremely conservative 
because the drift does not provide a stress concentration comparable to that of a crack, and as 
will be developed, the dike can not resume propagation simply by expanding a penny-shaped 
crack. Further propagation of the dike across the drift is delayed until part of the drift has filled 
with magma and pressurized sufficiently to initiate hydraulic fracturing (conditions for hydraulic 
fracturing are discussed in part in Reamer 1999, p. 78f). The driving source for fluid fracturing 
of the rock is the magma fluid pressure in the dike (and the crack). For a steady-state linear 
crack, this pressure is related to material properties and the least principal stress as: 
Pl - s = ( 2E./pL(1 - 2))1/2 
(Eq. 2) 
(Daneshy 1978, p. 33). 
If the linear crack intersects the drift normal to the drift axis, the drift is treated as a pennyshaped 
crack. The pressure necessary to propagate the penny-shaped crack is given by 
PD - s = (pE./2R(1 - 2))1/2 
(Eq. 3) 
(Daneshy 1978, p. 33)

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 18 
where
Pl = pressure (linear crack) 
PD = pressure (penny-shaped crack) 
L = length of a 2-D linear crack 
R = radius of the penny-shaped crack 
E = Youngs modulus for the rock 
 = Poissons ratio 
. = effective fracture surface energy 
s = in situ least principal stress 
The ratio of the minimum driving pressures is a measure of how easily the linear crack interacts 
with the penny-shaped crack and is
Pl - s ~0.45(PD - s ) 
(Eq. 4) 
where L = 2R in equation 2. 
So, a linear crack, being propagated at minimum driving pressure, has only 45 percent of the 
pressure required to drive a penny-shaped crack (Daneshy 1978). So even for interaction with a 
planar segment of the drift, the dike is not able to continue propagation across the drift by 
converting a linear crack into a penny-shaped crack. To continue propagation, a mechanism is 
required for loading the drift so it can fail along a structural zone of weakness by restart of a 
linear crack. A possible mechanism is loading of the drift, that is, filling the drift with sufficient 
magma to initiate hydraulic fracturing. Loading of the drift sufficient to initiate fracturing is 
discussed in the IRSR (Reamer 1999, p. 78f). As a result, if the drift is subsequently loaded, the 
linear crack resumes along a line of weakness, probably along a rib (drift wall). While the 
section of the drift is filling (which will reinitiate hydraulic fracturing), the crack leading the dike 
is advancing vertically in the pillars between adjacent drifts. Local delay at the drift could mean 
that the flow of magma is diverted preferentially to the region between drifts. In the current 
design, the diameter of an emplacement drift is ~5 m (DTN: SN9908T0872799.004) and drift 
centers are 81 m apart (CRWMS M&O 2000g), so the length of the dike (for a dike normal to the 
drift axis) is about six percent of the drift spacing. This suggests the possibility that a dike may 
tend to divert around a drift, leaving it locally filled with magma. The time to fill a section of 
drift can be estimated from the void space assumed for a length of the drift to be filled, the 
dimensions of the dike and the flow velocity in the dike (greater than the dike propagation 
velocity). The dike propagation velocity then allows an estimate of how far the dike has 
advanced before a linear fracture resumes advancement from the drift. 
Local Stress StateThe discussion of the thermo-mechanical evolution of the mountain (Section 
6.3.1) argues for a long delay (~2000 years) (Hardy and Bauer 1992) for thermo-mechanical 
stress relief to occur around repository openings. Stress-relief, when it occurs, is expressed in 
generation of fractures and rockfall and possibly as creep into the drift. In classical rock 
mechanics (Brady and Brown 1985, p. 192f; Jaeger and Cook 1979), an opening (drift) develops

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 19 
radial and concentric fractures as strain relieves the stress, to some extent, for a distance of up to 
3 drift diameters. In Figure 1, this is illustrated in the right branches of the decision tree. 
The propagating crack from the intruding dike encounters the stress relieved zone and the 
associated fractures some distance away from the original location of the drift. Effectively, the 
propagating crack sees a fractured rock before it reaches the drift. 
There are two possible end members for the dike-drift interaction. In the first, the propagating 
crack encounters discontinuous concentric and radial fractures. From the work of Tsunakawa 
(1983), propagation of magma-filled cracks becomes impeded as the angle of intersection of the 
dike crack and the local fractures increases. Further, Tsunakawa establishes a requirement for 
minimum magmatic pressures (depending on angle) for assured propagation. 
For the second end member, the propagating crack intersects a radial fracture that persists to the 
drift. Such stress-relief radial fractures, while approximately parallel to the drift axis, are short 
and discontinuous and would not be expected to significantly rotate the injection direction of the 
dike. 
Fragmentation HistoryFragmentation is the complex process of exsolution of gas, formation 
of bubbles in the magma and solidification and disruption of the bubbles to form pyroclasts. For 
flow up an existing dike or up a conduit through the repository, fragmentation may occur below 
the repository depth. Figure 1, the organizing decision tree, has a pair of right-hand branches 
dependent on when in the course of propagating the dike that the fragmentation occurred below 
the repository. The issue is whether, in the course of formation, the magma propagating the dike 
fragmented below the repository level, or whether it propagated to the surface first and then a 
pressure relief wave moved back down the intrusion to allow fragmentation at the fragmentation 
depth. 
The first case is one of the two circumstances in which magma, as a liquid, is available to flow 
into the drift (the second is late stage degassed flow). In addition, the pressure at the drift level 
for the flow of ash and shards (with a density of perhaps 1000 kg/m3) can be less than that for a 
magma flow (with a density of 2556 kg/m3). [The value for magma density is taken from 
Characterize Eruptive Processes at Yucca Mountain, Nevada, ANL-MGR-GS-000002, CRWMS 
M&O 2000d, for 2 wt% water content.] There are two reasons for concern about whether 
fragmentation occurs during driving of the dike. The first is that magma has to be available at 
the drift in order to flow into the drift. The second is exsolution of gas and fragmentation into 
the drift. The drift is at ~0.1 MPa (atmospheric pressure) compared to ~7.5 MPa (~1100 psi) in a 
liquid magma flow and perhaps ~3.1 MPa in a fragmented flow. The fragmented flow, with a 
high gas content, is more likely to be susceptible to loss of pressure through fractures around the 
drift that are intercepted by the dike, with a reduction of flow of pyroclastics down the drift. The 
pressure, p, at the drift is calculated from p = .gh, where . = density of contents of the dike 
(magma or fragments), g = acceleration of gravity, and h is the distance to the surface. P is then 
the pressure at the drift necessary to support the dike.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 20 
Design Description of a DriftCurrent design of an emplacement drift includes the following 
components: ground support, invert, rails, waste packages, emplacement pallet, drip shield, and 
backfill, (A drain is a possibility but is not part of current design.). The dimensions are shown in 
Figure 6 (p. 43)(DTN: SN9908T0872799.004) and Figure 7 (p. 44) is a sketch of the general 
configuration. Waste containers have a skirt about 25 cm long at each end (CRWMS M&O 
1999b) and adjacent containers are separated by about 10 cm along the drift (DTN: 
SN9908T0872799.004). 
Alternative InterpretationsThe Igneous Activity Issue Resolution Status Report, in Section 
4.2.3.3.2 (Reamer 1999, p. 78f), develops requirements for hydraulic fracturing which is initiated 
from a loaded drift. That is, the drift is filled with magma and two orientations for reinitiation of 
hydraulic fracturing are considered. These directions are normal to the drift axis and along the 
drift axis (in present design, normal to least principal stress and normal to maximum horizontal 
principal stress, respectively). The details of the mechanical interaction of the crack leading the 
dike with the drift have not been considered. The analyses address how a dike may be 
propagated by hydraulic fracturing of the rock around a drift pressurized by magma. 
In present repository design, the drifts are oriented roughly along the current least principal 
horizontal stress. Since the most likely orientation of a dike is normal to the least principal stress 
(Reamer 1999, p. 52), an intersection of a dike with a drift along the axis of the drift is unlikely. 
Therefore, this possibility has not been considered in this AMR. 
6.3.3 Shock Interaction 
Intersection of dike and drift will result in a pressure pulse generated by the rapid exposure of the 
drift to the ~7.5 MPa (1100psi) pressure of the dike. This pressure pulse, which moves rapidly 
down the drift, interacting with the packages, drip shield and backfill. The backfill is displaced 
and compressed by the moving drip shield to close the openings above and around the waste 
packages and drip shield. The pressure pulse is followed by a flow of pyroclastics down the 
drift. This flow of pyroclastics reaches and reinforces (and may move) the blockage of jammed 
drip shield and backfill which was generated by the pressure pulse. 
Air in the drift is at ~0.1 MPa (atmospheric pressure) while the dike volatiles are about 7.5 MPa 
(~1100 psi) for a liquid magma dike and ~3.1 MPa for a fragmented flow producing the dike 
(pressures are derived for a dike which reaches the surface, with densities of the magma and 
pyroclastic flow are 2556 kg/m3 and 1000 kg/m3, respectively). A sudden connection means that 
leakage of gas and magma to relieve pressure through any fractures around the drift is precluded. 
The decision tree in Figure 1 shows two choices: either liquid magma reaches the drift with rapid 
exsolution and decompression or fragmented flow reaches the drift with a smaller 
decompression. The topic of this section is intended to allow a decision about the scope of the 
disruption. Figure 6 shows a number of drift components for the pressure pulse to interact with. 
It is expected that waste packages will be displaced and the drip shield, backfill and invert will 
be moved. Waste packages falling directly in the dike are not considered here, they are 
considered in Igneous Consequence Modeling for the TSPA-SR, ANL-WIS-MD-000017 
(CRWMS M&O 2000b).

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 21 
To estimate waste package movement, the pressure pulse is applied uniformly across the head 
(end cap) of the waste container. Figure 7 is a sketch of the pre-intrusion layout in the drift. The 
waste package slides along the emplacement pallet until the center of gravity of the waste 
package passes the emplacement pallet end (or the emplacement pallet otherwise collapses). 
Containers have an attached skirt about 25 cm long and are separated by 10 cm. When the first 
waste package moves down the drift more than 10 cm, skirts are in contact and crushed thereby 
moving the adjacent waste package. 
To estimate the velocity of a waste package it is necessary to have a mass for the waste package 
and a coefficient of friction. The container is taken to be a 21 assembly PWR container. The 
waste package mass is calculated to be ~ 42.3 metric tons (CRWMS M&O 2000e, p. II-2). The 
waste package rests on an emplacement pallet with its motion resisted by a coefficient of friction 
of 0.3 (The specific value will turn out to be unimportant because the driving pressure is so 
large.). The interaction is idealized in that the pressure pulse provides a constant acceleration 
until the shock wave reaches the end of the waste package. 
From Glasstone (1962, p. 121f) the shock wave velocity v in air is given by U = Co(1 + 
6P/(7Po))1/2, with Co = ambient speed of sound, P = overpressure, and Po = ambient pressure. For 
p = 7.5 MPa, the dike pressure, U ~ 8Co. The dynamic pressure q (= 5/2  p2/(7Po + P)) is ~17 
MPa (Glasstone 1962, p. 122). Since the incident shock wave is reflected from the waste 
package end cap, the overpressure is approximately twice the incident overpressure and the total 
driving pressure, P = P (overpressure) + q (dynamic pressure), is ~32 MPa. 
In this idealized case the force F , on the head of the waste package, is given as 
F = (A P -  M g) = M a 
(Eq.5) 
where
A = the cross-sectional area of the container (~2.19 m2) 
P = the total pressure 
 = the coefficient of friction (nominally 0.3) 
M = the mass of the waste package (represented by a 21 assembly PWR waste package of 
42.3 metric tons (CRWMS M&O 2000e, p. II-2) 
g = the acceleration of gravity (9.8 m/sec2) 
a = the acceleration of the waste package 
Integration gives the velocity v as

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 22 
v = t (A P -  M g)/M 
(Eq. 6) 
where t is the length of time the force is applied as the waste package slides down the 
emplacement pallet. The driving pressure accelerates the waste package until pressure has built 
up on the back end cap. The time for buildup (Glasstone 1962, p. 184), t = L/U + 4R/U (L = 
container length, R = container radius), is t ~ 3.27  10-3. Substitution of this value of t into 
equation 6 yields a velocity v ~ 5.4 m/sec. Details of shock buildup and decay (Glasstone 1962, 
p. 182f), which would reduce the driving pressure (perhaps by more than a factor of 2) and the 
velocity, have been ignored. 
For small velocities, the waste package would be expected to stop moving almost immediately 
on contacting the invert. (Based on a train derailment analogy, rail cars of 50100 tons each, stop 
fairly quickly in the track ballast even though derailment occurs typically at much higher 
speeds). 
On this basis, it appears that the first waste package will move until it drops off the emplacement 
pallet, presumably <2 m, when the center of gravity of the waste package passes the end. 
Collapse of the emplacement pallet, which would further reduce motion, is undetermined and is 
conservatively neglected. Since the waste package then stops quickly, its translation affects 
adjacent waste packages with much of the movement accommodated in crush of the skirts. The 
approximately 2 m of movement is accommodated by movement of 3 to possibly 4 waste 
packages. If the pulse is produced by a fragmented flow then the pressure and the velocity scale 
according to the equation for velocity, v, with the density of the flow (magma ~2556 kg/m3, 
fragmented flow <1000 kg/m3). (A diagram showing a final orientation of the disrupted waste 
packages appears in Figure 8 (p. 45)). 
The pressure pulse interacts with the other components of the drift as well. The interactions are 
not amenable to an idealized calculation and are treated qualitatively. As shown in Figure 7, the 
waste package sits on a emplacement pallet above a ballast invert and is covered by a drip shield 
loaded with backfill. If the drip shield functions as designed, diverting water from the packages, 
there are some few locations along a drift where the backfill is wetted by the drip. From Figure 
6, the load on top of the drip shield is <10 Pa. Accordingly, it is to be expected that the pressure 
pulse will displace the drip shield and both the backfill and invert material as well. The drip 
shield (Figure 6) has a circumference of about 6.5 m (DTN: SN9908T0872799.004) and it will 
be made in short lengths for emplacement. The pressure pulse can be expected to displace the 
drip shield upward and down the drift and to jam it into the void space above the backfill 
(snowplowing the backfill). From Figure 8, the drip shield and backfill associated with one 
waste package appear adequate to block the opening (~13 m2 per segment); however, since three 
waste packages (and possibly 4) are likely to be displaced by the pressure pulse, Figure 8 shows 
drip shields from three waste packages involved. Figure 8 portrays displacement of the ballast, 
its accumulation along the damaged waste packages, and upon close inspection, tries to include 
mechanical damage to the waste packages (everted heads and crumpled sidewalls). The extent 
of damage depends on both dike flow characteristics and the age, that is to say the strength of the 
affected waste packages. Splitting of welds and waste package blowout are possibilities that are 
not addressed. The first waste packages has been treated as a rigid, non-deformable body

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 23 
(except for the skirt), a conservative assessment since damage to the first waste package would 
reduce damage to waste packages further down the drift. Note that since failure of ground 
support and rockfall have not been considered here, progression of the plug of magma down the 
drift may be substantially overestimated. 
Alternative InterpretationsThe Igneous Activity Issue Resolution Status Report (IRSR) 
(Reamer 1999, Section 4.2.3.3.1 Flow Conditions, p. 77f) discusses response to the pressure 
pulse and possible shock wave and is based on scoping calculations done for the NRC. The 
study presumes that backfill is absent from the drifts and on intersection, the pressure in the dike 
will fall to atmospheric pressure. The dike will then decompress and magma will have a 
tendency to flow into the drifts. The IRSR argues that the capacity of a drift is so large 
compared to the expected dike width (0.52m, in their case) that, locally much of the flow is 
diverted to the drift. Because of the large pressure drop the IRSR authors anticipate an 
acceleration of magma into the drift at a much larger flow rate than is anticipated. The IRSR 
authors expect flow speeds for magma down the drift of the order of 100 m/s. The IRSR authors 
also believe that a shock wave will proceed down the drift, reaching the end in about 10 s (1000 
m in 10 s). 
For this AMR, the interaction of dike and drift starts with a pressure pulse generated by the rapid 
exposure of the drift to the ~7.5 MPa (1100 psi) pressure of the dike. A pressure pulse moves 
rapidly down the drift, interacting with the waste packages, drip shield and backfill. The backfill 
is displaced and compressed by the moving drip shield to close the openings above and around 
the waste packages and drip shield. The pressure pulse is followed by a flow of pyroclastics 
down the drift. This flow of pyroclastics reaches and reinforces the blockage generated by the 
pressure pulse. Repressurization of the drift to allow the flow from the dike as magma is not 
considered because the permeability of the formation is expected to be too high. An estimate is 
made of the number of waste packages experiencing physical damage. 
6.3.4 Gas Flow 
An issue, which appears in the branches of Figure 1, is that of failure of the waste container. 
One possible cause of failure is corrosion of the container by the aggressive gases exsolving 
from the magma intrusion or flowing in the dike or in the vent. This section attempts to estimate 
the gas flow down the drift under idealized circumstances, in order to estimate the size of a 
source term to allow a decision about whether corrosion is a possible problem (whether sufficient 
gas for corrosion is available). 
The idealization is that the gas flow is a steady-state flow of a real gas, as controlled by leakage 
through the drift wall, which persists for the duration of the eruption. More specifically (as listed 
in Section 5.1), it is assumed that 
1. Gas is supplied to the drift by the dike or vent. 
2. There is isothermal flow down the drift (no axial temperature gradient). 
3. Adiabatic expansion is ignored. 
4. Heat carried into the rock (the porous media) by the gas is ignored. 
5. There is no chemical interaction of the gases with the rock.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 24 
6. The components of the EBS are irrelevant to the flow. 
Assumptions 26 are those made explicitly for this calculation. They ignore dissipation of 
energy to the drift wall and the EBS and are intended to be conservative because more energy is 
retained in the flow. The analysis based on these assumptions overestimates the gas flow. 
These assumptions mean that the calculation is for steady-state flow down an empty drift. The 
volumetric flow rate is controlled only by how fast the gas can escape by leaking through the 
drift wall into the country rock, and real gas properties are assumed to be more important than 
heat transfer into the porous medium. 
The flow of a real gas through a porous medium is described by the Equations 7, 8, and 9 
2 . m(p) = 1 ) ( ) ( - k p c p f t p m . . / ) ( 
(Eq. 7) 
where m(p) is the pseudo-pressure defined as 
m(p) = 2 .p 
pm p z p
pdp 
) ( ) (  
, with 
) ( p  the pressure dependent viscosity and z(p) the correction to the ideal gas law, 
( . = 
RT 
M 
.. 
. 
.. 
. 
) ( p z 
p 
, where . = density, M = molecular wt, R = gas constant, T = temperature, 
p = pressure, and z(p) = correction for real gases). 
In the referenced paper, a steady-state solution is presented for flow through concentric 
cylinders, which can be adapted for the purpose here. The equation derived there for qsc , the 
radial mass flux (m3/sec) is given by 
q = 
w
o 
sc 
w o sc 
r
r 
Tp 
p m p m khT 
ln 
)] ( ) ( [ - p 
(Eq. 8) 
where
k = permeability (~1100 Darcys, LeCain 1997, p. 11f) 
h = length of drift presumed involved 
T = temperature (K) 
Tsc = reference temperature at standard conditions (300 K)

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 25 
px = pressure at the: outer boundary (x = 0), drift boundary (x = w), standard conditions 
(x = sc) 
rx = radius at the: outer boundary (x = 0), drift wall (x = w) 
For this problem the outer radius is allowed to become infinite and m(po) becomes zero, so the 
equation for q reduces to 
q = 
w sc 
w sc 
r Tp 
p m khT 
ln 
) ( p 
(Eq. 9) 
(Al-Hussainy et al. 1966). 
To utilize this work requires values for the pseudocritical temperature and pseudocritical 
pressure for the volcanic gases. Those values are developed from Table 4.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 26 
Table 4. Characteristics of Exsolved Gases and Their Pseudocritical Properties 
Species 
Mole 
Fraction 
Critical 
Temperature 
K 
Pseudo- Critical 
Temp 
K 
Critical 
Pressure 
atm 
Pseudo- 
Critical 
Pressure 
atm 
Molecular 
Wt. 
Average 
Molecular 
Wt. 
H2O 73.16 647.14 473.45 217.7 159.269 18.01 13.18 
H2 1.17 32.97 0. 3857 12.76 0.14929 2 0.0234 
CO2 14.28 304.14 43.43 72.78 10.39 44.01 6.2846 
CO 0.57 132.91 0.7576 34.53 0.19682 28.01 0.1597 
SO2 9.45 430.8 40.71 77.8 7. 3521 64.06 6.0537 
S2 0. 37 1314 4. 8618 204.28 0.7558 64.12 0.2372 
HCl 0.49 324.7 1.5910 82 0.4018 36.46 0.17865 
HF 0.06 461 0.2766 63.95 0.03837 20.01 0.0120 
H2S 0.74 373.2 2.76168 88.23 0.652876 34.08 0.2522 
Tpc = 568.22 Ppc = 179.21 
NOTE: Critical temperatures and critical pressures, p. 6-50f, and Molecular weights, 
p. 4-37f, Handbook of Chemistry and PhysicsLide and Frederikse 1997; 
Mole fractions from CRWMS M&O 2000d) 
In order to utilize the tables provided by Al-Hussainy and co-workers (their Table 1) for m(p) in 
terms of measured properties of real gases, a pseudo reduced pressure and a pseudo reduced 
temperature are extracted from Table 4, above. For P = PprPpc, with P = 75 atm (7.5 MPa) at the 
drift and, Ppr = 0.38, Ppc = 179.2 atm, and T = TprTpc, with T = 1100 0C (1373 K, magma 
temperature (CRWMS M&O 2000d), Tpc = 568.22 K, Tpr = 2.42. 
For a viscosity of 0.47 cp (linear extrapolation of table values for H20: Lide and Frederikse 1997, 
p. F43f), a pressure at the drift wall of 1100 psi (7.5MPa), m(p) is found to be 7.97 x 103 
(atm)2/cp. With these numbers, the values for q are presented in Table 5.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 27 
Table 5. Volumetric Flow Rates for Two Different Wall Lengths and 
Two Different Permeabilities of the Drift Wall 
h (length of drift 
involved) 
Air Permeability 
k = 1 Darcy 
Air Permeability 
k = 10 Darcy 
5. 5 m (1 container) ~2 m3/sec ~20 m3/sec 
1 km (~1 drift length) ~3.5 102 m3/sec ~3.5  103 m3/sec 
The volumetric flow rate for the entire drift at k = 10 Darcy implies an unreasonably high 
velocity for the gas at the effective dike face (location of intersection of dike and drift). The 
unreasonably high velocity suggests that in this approximation, gas flow is over estimated and 
that the model should include cooling of gas and heating of the country rock through which the 
gas is leaking. It appears that the volume of gas arriving at a container is not directly a limiting 
factor in corrosion. (For a discussion, definition of, and use of pseudo properties see Pirson 
1977, p. 341f). 
Alternative InterpretationsThe Igneous Activity Issue Resolution Status Report (IRSR) 
(Reamer 1999), in Section 4.2.3.3.1, discusses flow conditions and the possibility that 
decompression of the magma produces a shock wave and a vesicular flow. It may be inferred 
from the discussion in the cited section that the drift is expected to pressurize. 
For this AMR, Section 6.3.4 discusses the constraints on gas flow down the drift for flow 
controlled by leakage through the surrounding rock. While the intent is to establish whether 
sufficient gas is available for container corrosion, as a result it appears that pressurization 
sufficient to prevent fragmentation is expected to be unlikely. 
6.3.5 Magma FlowThermal Environment 
If the fragmentation depth is below the repository, then liquid magma can enter a drift either 
during the initial intersection of dike and drift, as an intermittent stage, or as a late stage, 
degassed flow. The first, initial intersection, is associated with the entire dike, and as the dike 
flow fragments below the repository, the unchilled portion can flow back to the dike from the 
drift because the dike pressure is reduced, leaving covered (or possibly partially covered) waste 
packages. The second, the intermittent stage, is related to formation of a vent and conduit, which 
reduces the population of exposed drifts, and can allow accumulation of fragments (ash) in the 
drift. The late stage is flow of degassed liquid magma into the drift. Magma flow is the 
presumption of one of the right hand branches of Figure 1, and is intended to support decisions 
about waste package failure and entrainment of contaminants. 
The magma flow is presumed to follow the decompression and gas flow into the drift, so the 
state of the drift and waste packages is that suggested in Figure 8. The first, and possibly second, 
waste packages should have experienced considerable damage to their heads (endcaps), with

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 28 
eversion and cracking as strong possibilities, and may be collapsed and fractured along the sides; 
waste packages further down the drift are damaged to a lesser extent. 
Rapid flow of magma (presumed to be approximately at its liquidus) into the drift, as suggested 
by flow velocities in the dike, would fill the drift more rapidly than it, the magma, could chill, 
forming a plug in the void space around the waste packages as indicated in Figure 9 (p. 46). The 
plug space drawn in Figures 7, 8, and 9 is about 5.5 m (dia.)  11m (to ~22 m) (length) and if the 
cross-section of the drift and dike represents the source, would be expected to fill in minutes. 
The case of a continuing flow of magma, as considered in Reamer (1999), requires an exit to the 
surface from the drift, a circumstance that is not considered here. An exit would be possible only 
through paths occurring as a result of reestablishment of dike propagation or opening of existing 
bounding faults. Further, flow of magma, down an open drift to its end, would be expected to be 
rapid compared to the chilling (solidification) time for the magma. 
There are certain peculiarities of the waste package, which affect the magmacontainer 
interaction. The waste package, as a large, cool (relative to the magma) mass with high thermal 
conductivity and heat capacity, will rapidly chill the magma making initial contact, and as is 
observed for some objects in lava flows, will tend to form an insulating crust about the waste 
package. This crust is unstable (not necessarily well-bonded to the waste package). 
Correspondingly, cracks in the waste package will admit limited volumes of magma that will 
tend to chill and plug. Large cracks and tears might allow the void spaces in a waste package to 
fill with magma that chills. 
The interaction of waste package and magma is too non-specific and variable to be amenable to a 
direct calculation without a more detailed description of the part of the interaction to be modeled. 
As an approximation, the magma fills a cylindrical chamber (the drift) and solidifies to form a 
plug. Because, waste can only be dissolved or mobilized while the magma is liquid, what is of 
interest is how long liquid magma could be in contact with a waste package and its contents. 
Magma, which is presumed to be approximately at the liquidus temperature, as it solidifies 
(chills), releases the latent heat of fusion (e.g., Jaeger 1964, p. 451f) of the order of 3.348-4.185 
 105 J/kg (80100 cal/g). For the cylindrical plug in contact with the drift wall and ground 
support, the solidification surface gradually moves inward. 
This problem is a Stefan problem, a so-called moving boundary problem. There is substantial 
literature describing solidification of a spherical and a cylindrical molten mass (e.g., Soward 
1980; Stewartson and Waechter 1976; Riley et al. 1974; Pedroso and Domoto 1973; Kreith and 
Romie 1955), which has provided series solutions for the temperature history and for the time of 
final solidification. The particular problem of a magma plug of finite length is not among the 
solutions mentioned or among the problems tried. 
The problem for magma flow solidifying in an infinitely long cylindrical drift is described in 
Soward (1980), and the general approach to such problems is given in Carslaw and Jaeger (1959, 
p. 295f). The problem of actual interest, a finite plug imbedded in a medium, at a constant 
temperature at one end and cooling at the other and cooling along a cylindrical surface, has not

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 29 
been addressed. However, enough can be gleaned from the existing solutions to make 
preliminary assessments about the waste package environment. Several of the analyses (Kreith 
and Romie 1955; Riley et al. 1974) provide simple expressions for the time for solidification of a 
cylinder filled with chilling magma, in terms of the diameter of the drift, the drift wall 
temperature, and the physical properties of the magma. Riley et al. (1974, p. 1514) estimate a 
time to chill, tf, as 
tf = a2( + 1)/(4k) 
(Eq. 10) 
where
 = L/(C(Tf -Tw)) 
a = radius of the drift (~2.75m) 
k = thermal conductivity of solidbasalt at 21.76 J/(kg sec C) (0.0052 cal/(gm sec C) 
(Hodgman et al. 1955, p. 2251, Table Heat Conductivity) 
L = Latent heat of fusion (3.348-4.185 x 105 J/kg (80100 cal/gm) )(Jaeger 1964) 
C = Specific heat (~0.3) (Jaeger 1964) 
Tf = Fusion temperature of magma (~1100 C, selected as a representative value from the 
range reported in CRWMS M&O 2000d, also see Table 1) 
Tw = Drift wall temperature (~600 C) 
With these numbers, the time for solidification to reach the center of the magma filled drift is 
approximately 70 days. Estimates using other reference calculations suggest that to the order of 
accuracy of the expansions that the time is 70< tf < 82 days. These estimates depend on the drift 
wall temperature, which is a function of the thermal properties of the surrounding rock; 
increasing the drift wall temperature increases the length of time to chill. 
As an upper estimate of temperature, part of the waste package has seen Tf for most of the time 
for solidification. The actual temperature distribution for the chilling magma cylinder is given 
by Soward in series form (1980, p. 143f). 
Alternative InterpretationsThe Igneous Activity Issue Resolution Status Report, in Section 
4.2.4.3.1 (Reamer 1999, p. 83f), develops a heat transfer model in order to establish a 
temperature history for waste packages being enveloped in magma. They assume that the waste 
packages are located centrally in a convecting magma cylinder, the temperature is only a 
function of radius, the magma represents an infinite heat source, and the drift wall is 
approximately at the magma temperature for 20 days. Magma displaced by the waste package 
and waste package thermal properties are accounted for by treating the magma intrusion as a 
cylinder the diameter of the drift. The calculation allows for the possibility of a chilled rind of

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 30 
basalt forming on the drift wall and reducing the heat transfer coefficient. These assumptions 
lead to the conclusion that there is ample time to heat the waste packages to failure during a 
typical basaltic eruption. 
This AMR analyzes a magma plug, which has entered a drift from the intersecting dike, as an 
infinite cylinder of solidifying magma. The magma has filled the drift rapidly and there is no 
further flow along the drift axis (there is no exit for flow to continue). Details of the heat 
transfer, such as orientation and location of the waste package relative to the center of the drift, 
and the fact that a waste package is a large metal object with good thermal conductivity relative 
to the rock, are treated by replacing the waste package with magma. While these details are 
important to the actual temperature distribution in the waste package, they are relatively 
unimportant to the issue of waste package failure because the length of time the waste package is 
subject to heat soak is so long. The calculation is for the length of time it takes for the magma 
filled drift to solidify. This time represents the length of time that a typical waste package will 
be exposed to a temperature near the magma liquidus temperature (1100 0C). The time 
calculated for solidification for the magma around the embedded waste packages is long 
compared to the time estimated in the IRSR. 
The case of a continuing flow of magma, as considered in Reamer (1999) requires an exit to the 
surface from the drift, a circumstance that is not considered here. An exit would be possible only 
through paths occurring as a result of reestablishment of dike propagation or perhaps opening of 
existing bounding faults. Further, flow of magma, down an open drift to its end, would be 
expected to be rapid compared to the chilling (solidification) time for the magma. 
7. CONCLUSIONS 
The topics (end members) examined in this AMR are: (1) waste package temperature due to flow 
of magma down a blind drift, (2) steady-state gas flow down drift to interact with containers, (3) 
physical interaction of pressure pulse from the dike to displace waste packages and drift 
contents, and (4) qualitatively, the interaction of the self-generated crack leading the dike with 
the stress-altered region around the drift. 
Based on these analyses the following conclusions are physically possible and not excluded by 
data relevant to the mountain or to a repository.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 31 
1. The thermally altered stress state of the mountain may cause propagating dikes to 
deviate for the order of 2000 years (addresses the nature of the mechanics of the dike 
drift interaction). 
2. Disruption of waste packages caused by flow from the dike extends down the drift from 
the dike edge to 3 or possibly 4 waste packages (addresses movement of the waste 
packages as they are pushed down the drift). 
3. Magma flow down the drift is limited to a few waste package lengths (11 to 22 m) by 
plugging from the crumpled drip shield and displaced backfill (addresses disruption of 
the drip shield and backfill as they are pushed down the drift). 
4. The temperatures inside a magma plug (and approximately in embedded waste 
packages) are given by Soward (1980) with a solidification time of 70 to 82 days 
(addresses temperature changes to the waste package from exposure to magma). 
5. Gas flow down an idealized drift is about 3.5 1023.5  103 m3/sec, and suggests an 
isothermal model is inadequate and overestimates the flow rate (addresses the amount 
of gas available to degrade waste containers). 
Data and assumptions used in these analyses are derived from the published literature as 
indicated in Table 1. No corresponding qualified data (data acquired under the controls of 
current QA procedures) have been developed specifically for Yucca Mountain and vicinity. 
This document may be affected by technical product input information that requires 
confirmation. Any changes to the document or its conclusions that may occur as a result of 
completing the confirmation activities will be reflected in subsequent revisions. The status of the 
input information quality may be confirmed by review of the Document Input Reference System 
database. 
7.1 ALTERNATIVE INTERPRETATIONS 
In order to provide the basis for the PMR addressing the IRSR criteria, this section develops 
observations about the relevance of the analyses done in this AMR to the NRC  IRSR criteria, 
by comparison to the intent of the NRC  IRSR criteria and the analyses presented in the IRSR. 
The summary observation is that a more complete level of detail than is included in the IRSR is 
required to address the NRC  IRSR criteria. 
The NRC has developed the following acceptance criteria related to the Igneous Activity Key 
Technical Issue and the subissues of consequences (Reamer 1999, pp. 76 and 82). The first 
acceptance criterion related to the subissue of consequences is (Reamer 1999), Section 4.2.3.1. 
Acceptance Criterion: Estimate of the dose consequences of igneous activity on the 
proposed Yucca Mountain high-level radioactive waste repository will be acceptable 
provided that: The models adequately account for changes in magma ascent 
characteristics and magma/rock interactions brought about by repository 
construction.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 32 
The IRSR analysis assumes that an idealized interception of the drift by the dike has occurred. 
The analysis is qualitatively concerned about propagation of shock waves and pyroclastic flow 
down the drift. It explores quantitatively pressurization of the drift by magma and the conditions 
for re-establishment of dike propagation by hydraulic fracturing. 
This criterion contains several implicit questions which are only partly addressed by the IRSR 
interpretation of the physical processes. These questions are addressed in somewhat more detail 
by the following analyses (developed in Section 6.3): 
1. Stress state evolution around the repository 
2. Interaction of a linear crack with a penny-shaped crack 
3. Consequences of shock wave movement (pressure pulse) down a drift. 
These implicit questions concern how the stress state affects the assent of magma, both in 
direction and in the detailed interaction with the drifts, and the consequences of the intersection, 
including pressure pulse propagation down the drift. 
The questions are mixed, in the sense, that they actually involve both conceptual models 
introduced in Section 6.3, the simple idealized intersection model, and the stress-field dependent 
model. 
Analyses 1. and 2. involve the second conceptual modela model in which the stress state of the 
mountain and its evolution are important. Analysis 3. involves the idealized, first model, in 
which the stress state of the repository itself is ignored. The results of this AMR differ from 
those of the IRSR in part because of alternative interpretations of how much physical detail is 
required. 
The second acceptance criterion related to the subissue of consequences is Reamer 1999, Section 
4.2.4.1. 
Acceptance Criterion: Estimate of the dose consequences of igneous activity on the 
proposed Yucca Mountain high-level radioactive waste repository will be acceptable 
provided that: The models account for the interactions of basaltic magma with 
engineered barriers and waste forms. 
This IRSR analysis assumes that the waste packages are enveloped by a convecting magma flow 
which fills the drift. On this basis, the analysis tries to establish whether waste packages will see 
temperatures sufficiently high and persistent to compromise package integrity. 
This criterion contains several implicit questions which are addressed in part by the following 
analyses (developed in Section 6.3): 
1. Interaction of a linear crack with a penny-shaped crack 
2. Steady-state flow of a real gas down a drift 
3. Chilling of a magma plug enveloped within waste packages.

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 33 
These implicit questions relate to the details of dike propagation in a space with an already 
existing circular opening, the flow of corrosive gas down a drift (amount available), and the 
temperature history of waste packages that are enveloped by magma. 
As for the previous Criterion, the questions involve both conceptual models (Section 6.3), the 
simple idealized intersection model, and the stress-field dependent model. In this case, analysis 
1. depends on the second, stress-dependent conceptual model and analyses 2. and 3. on the first, 
simple idealized, conceptual model. The results of these analyses differ from those of the IRSR 
in part because of an alternative interpretation of how much physical detail is required. 
8. INPUTS AND REFERENCES 
8.1 DOCUMENTS CITED 
Al-Hussainy, R.; Ramey, H.J., Jr.; and Crawford, P.B. 1966. "The Flow of Real Gases through 
Porous Media." Journal of Petroleum Technology, 18, 624-636. Dallas, Texas: Society of 
Petroleum Engineers. TIC: 237975. 
Anderson, E.M. 1963. The Dynamics of Faulting, and Dyke Formation with Applications to 
Britain. London, United Kingdom: Oliver and Boyd. TIC: 246728. 
Aoki, Y.; Segall, P.; Kato, T.; Cervilli, P.; and Shimada, S. 1999. "Imaging Magma Transport 
During the 1997 Seismic Swarm Off the Izu Peninsula, Japan." Science, 286, (5441), 927-930. 
Washington, D.C.: American Association for the Advancement of Science. TIC: 246714. 
Barr, G.E.; Dunn, E.; Dockery, H.; Barnard, R.; Valentine, G.; and Crowe, B. 1993. Scenarios 
Constructed for Basaltic Igneous Activity at Yucca Mountain and Vicinity. SAND91-1653. 
Albuquerque, New Mexico: Sandia National Laboratories. ACC: NNA.19930811.0013. 
Brady, B.H.G. and Brown, E.T. 1985. Rock Mechanics for Underground Mining. London, 
United Kingdom: George Allen and Unwin. TIC: 226226. 
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 1999a. Conduct of Performance Assessment. Activity Evaluation, September 
30, 1999. Las Vegas, Nevada: CRWMS M&O. ACC: MOL.19991028.0092. 
CRWMS M&O 1999b. Enhanced Design Alternative (EDA) II Repository Estimated Waste 
Package Types and Quantities. Design Input Transmittal PA-WP-99184.T. Las Vegas, 
Nevada: CRWMS M&O. ACC: MOL.19990526.0188. 
CRWMS M&O 2000a. Coordinate Modeling of Dike Propagation Near Drifts Consequences 
for TSPA-SR/LA. TDP-WIS-MD-000027 REV 01. Las Vegas, Nevada: CRWMS M&O. ACC: 


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Hardy, M.P. and Bauer, S.J. 1992. "Invited Paper: Rock Mechanics Considerations in 
Designing a Nuclear Waste Repository in Hard Rock." Rock Mechanics, Proceedings of the 
33rd U.S. Symposium, Santa Fe, New Mexico, 3-5 June, 1992. Tillerson, J.R. and Wawersik, 
W.R., eds. Pages 1041-1050. Rotterdam, The Netherlands: A.A. Balkema. TIC: 239168. 
Hodgman, C.D.; Weast, R.C.; and Selby, S.M. eds. 1955. Handbook of Chemistry and Physics, 
A Ready-Reference Book of Chemical and Physical Data. 37th Edition. Cleveland, Ohio: 
Chemical Rubber Publishing Co. TIC: 247067. 
Jaeger, J.C. 1964. "Thermal Effects of Intrusions." Reviews of Geophysics, 2, (3), 443-466. 
Washington, D.C.: American Geophysical Union. TIC: 246686. 
Jaeger, J.C. and Cook, N.G.W. 1979. Fundamentals of Rock Mechanics. 3rd Edition. New 
York, New York: Chapman and Hall. TIC: 218325. 
Kreith, F. and Romie, F.E. 1955. "A Study of the Thermal Diffusion Equation with Boundary 
Conditions Corresponding to Solidification or Melting of Materials Initially at the Fusion 
Temperature." Proceedings of the Physical Society, Section B, 68, 277-291. London, United 
Kingdom: The Physical Society. TIC: 246910. 
LeCain, G.D. 1997. Air-Injection Testing in Vertical Boreholes in Welded and Nonwelded Tuff, 
Yucca Mountain, Nevada. Water-Resources Investigations Report 96-4262. Denver, Colorado: 
U.S. Geological Survey. ACC: MOL.19980310.0148. 
Lide, D.R. and Frederikse, H.P.R., eds. 1997. CRC Handbook of Chemistry and Physics. 78th 
Edition. Boca Raton, Florida: CRC Press. TIC: 243741. 
Lister, J.R. 1990a. "Buoyancy-Driven Fluid Fracture: Similarity Solutions for the Horizontal 
and Vertical Propagation of Fluid-Filled Cracks." Journal of Fluid Mechanics, 217, 213-239. 
Cambridge, United Kingdom: Cambridge University Press. TIC: 225065. 
Lister, J.R. 1990b. "Buoyancy-Driven Fluid Fracture: The Effects of Material Toughness and 
of Low-Viscosity Precursors." Journal of Fluid Mechanics, 210, 263-280. Cambridge, United 
Kingdom: Cambridge University Press. TIC: 246674. 
Lister, J.R. and Kerr, R.C. 1991. "Fluid-Mechanical Models of Crack Propagation and Their 
Application to Magma Transport in Dykes." Journal of Geophysical Research, 96, (B6), 10,049- 
10,077. Washington, D.C.: American Geophysical Union. TIC: 225066. 
Mack, M.G.; Brandshaug, T.; and Brady, B.H. 1989. Rock Mass Modification Around a Nuclear 
Waste Repository in Welded Tuff. NUREG/CR-5390. Washington, D.C.: U.S. Nuclear 
Regulatory Commission. TIC: 229166. 
Pedroso, R.I. and Domoto, G.A. 1973. "Inward Spherical Solidification - Solution by the 
Method of Strained Coordinates." International Journal of Heat and Mass Transfer, 16, 1037-

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1043. New York, New York: Pergamon Press. TIC: 246685. 
Pirson, S.J. 1977. Oil Reservoir Engineering. Huntington, New York: Robert E. Krieger 
Publishing. TIC: 246776. 
Pollard, D.D. 1987. "Elementary Fracture Mechanics Applied to the Structural Interpretation of 
Dykes." Mafic Dyke Swarms, A Collection of Papers Based on the Proceedings of an 
International Conference held at Erindale College, University of Toronto, Ontario, Canada, 
June 4 to 7, 1985. Halls, H.C. and Fahrig, W.F., eds. Special Paper 34, 5-24. St. John's, 
Newfoundland, Canada: Geological Association of Canada. TIC: 247071. 
Reamer, C.W. 1999. "Issue Resolution Status Report (Key Technical Issue: Igneous Activity, 
Revision 2)." Letter from C.W. Reamer (NRC) to Dr. S. Brocoum (DOE), July 16, 1999, with 
enclosure. ACC: MOL.19990810.0639. 
Riley, D.S.; Smith, F.T.; and Poots, G. 1974. "The Inward Solidification of Spheres and 
Circular Cylinders." International Journal of Heat and Mass Transfer, 17, 1507-1515. New 
York, New York: Pergamon Press. TIC: 246684. 
Smith, C.; Vollendorf, W.C.; and Warren, W.E. 1981. In-Situ Stress from Hydraulic Fracture 
Measurements in G Tunnel, Nevada Test Site. SAND80-1138. Albuquerque, New Mexico: 
Sandia National Laboratories. TIC: 207978. 
Soward, A.M. 1980. "A Unified Approach to Stefan's Problem for Spheres and Cylinders." 
Proceedings of the Royal Society of London, A 373, 131-147. London, United Kingdom: The 
Royal Society of London. TIC: 246671. 
Spence, D.A. and Turcotte, D.L. 1985. "Magma-Driven Propagation of Cracks." Journal of 
Geophysical Research, 90, (B1), 575-580. Washington, D.C.: American Geophysical Union. 
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Spence, D.A. and Turcotte, D.L. 1990. "Buoyancy-Driven Magma Fracture: A Mechanism for 
Ascent Through the Lithosphere and the Emplacement of Diamonds." Journal of Geophysical 
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246860. 
Spence, D.A.; Sharp, P.W.; and Turcotte, D.L. 1987. "Buoyancy-Driven Crack Propagation: A 
Mechanism for Magma Migration." Journal of Fluid Mechanics, 174, 135-153. Cambridge, 
United Kingdom: Cambridge University Press. TIC: 225149. 
Stewartson, K. and Waechter, R.T. 1976. "On Stefan's Problem for Spheres." Proceedings of 
the Royal Society of London, A 348, (1655), 415-426. London, United Kingdom: Royal Society 
of London. TIC: 246670. 
Stock, J.M. and Healy, J.H. 1988. "Stress Field at Yucca Mountain, Nevada." Chapter 6 of 
Geologic and Hydrologic Investigations of a Potential Nuclear Waste Disposal Site at Yucca



ANL-WIS-MD-000015 Rev 00 39 April 2000 
Figure 1. Decision Tree for Perspective 
View of Modeling 
Release in 
ash plume? 
Conduit forms 
through drift? 
Container 
failure? 
Contaminant 
entrainment? 
Drift size 
and growth, 
conduit 
erosion 
Drift 
entry by 
dike flow? 
Yes 
Yes 
Yes 
Yes No 
No 
No 
No 
Fracture/ 
fracture interaction 
with stress-relieved 
zone? 
Dike 
propagates 
to surface? 
Yes 
Yes No 
No 
Dike terminates 
Conduit 
forms between 
drifts and outside 
repository 
Shockwave 
disrupts DS, backfill 
and containers? 
No 
"Knife" cut 
of dike across 
drift? Yes No 
Dike 
compromises 
cotainers? 
Yes No
Yes 
Lateral 
entrainment to 
conduit between 
drifts? Yes No 
?? 
Release in 
ash plume Yes No 
Release in 
local deposition 
Mechanical failure 
(shock, abrasion/erosion 
of container/fuel pellet) 
Gas corrosion 
Elastic collision 
Inelastic collision 
(sticky particles) 
Respirables 
Plume 
deposition 
Fracture/ 
fracture interaction 
with stress-relieved 
zone? 
Dike 
propagates 
to surface? 
Yes 
No 
Release in 
ash plume 
Conduit forms 
through drift? 
Container 
failure? 
Contaminant 
entrainment? 
Stress interaction 
controls location; 
Conduit surge and 
growth 
Drift 
entry by 
dike flow? 
Yes 
Yes 
Yes 
Yes No 
No 
No 
No 
Yes 
Conduit 
forms between 
drifts and outside 
repository 
Gas flows 
down drift 
Mechanical 
and corrosion 
failures 
Fragmentation 
occurs below 
repository? 
Fragmentation 
occurs above 
repository; Magma 
reaches drifts 
No 
Yes 
No 
Dike terminates 
Shockwave 
disrupts DS, backfill 
and containers? 
No 
"Knife" cut 
of dike across 
drift? Yes No 
Dike 
compromises 
containers? 
Yes No
Yes 
Lateral 
entrainment to 
conduit between 
drifts? Yes No 
Release in 
ash plume 
?? 
3 
2 
4 
No 
release 
Conduit 
forms 
Yes No 
No 
release Release in 
ash plume 
4 
Yes 
No adverse 
interaction 
Dike reaches 
repository 
Encapsulated 
waste/containers 
Thermal 
period 
intrusion 
Dike 
propagates 
to surface? 
Thermal 
period 
stress 
rotation 
Sill forms 
below repository? 
Magma 
flow exits to 
surface along 
fault zone? 
Containers 
in magma, fail? 
Sill 
forms at 
repository 
Intrusion 
only 
Waste 
dissolved and 
entrained? 
Flow 
system 
alteration with 
aqueous 
transport 
Distributed/ 
mixed encapsulated 
waste 
Flow 
system 
alteration with 
aqueous 
transport 
Encapsulated 
waste 
1 
No 
No 
No Yes 
No 
No 
2 
Yes 
Yes 
Yes 
Yes 
Intrusion occurs 
during post-thermal 
period? No 
Dike 
deviated by 
repository? 
Dike 
intercepts repository 
~vertically? 
?? 
No Yes 
Dike exits 
via fault zones? 
(SCF,DHW) 
Yes 
Yes 
No 
No 
Thermal and 
gas effects 
Fracture/ 
fracture 
interaction 
Yes No 
2 3 
Lava 
flow 
SCF = Solitario Canyon Fault 
DHW= Drill Hole Wash 
DS = Drip Shield 
??= To be investigated

Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 40 
Figure 2. Thermo-Mechanical Response of the Stress StateMain Drift 
Figure 3. Thermo-Mechanical Response of the Stress State 
Vertical 
stress 
Horizontal 
stress 
Tuff Main Access Drift 
10
9
8
7
6
5
4
3
2 
10 100 1000 10000 
Years After Start of Waste Emplacement 
Stress (MPs) 
Axial stress 
Vertical 
stress 
Horizontal 
stress 
Emplacement Drift 
18 
10 100 1000 10000 
Years After Start of Waste Emplacement 
Stress (MPs) 
Axial stress 
16 
14 
12 
10
8
6
4
2
0

Figure 4. Generic Location of Transition from Horizontal to Vertical Least Principal Stress 
Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 41 N 
s3 
s2 
s1 
s1 
s2 
s3 
~ 1 m (Dike not to scale) 
Repository 
Ghost Dance 
fault 
Solitario Canyon 
fault 
Bow Ridge 
fault 
Dike 
Regional least principal 
(NNW/SSE) stress 
Vertical stress = 
Least horizontal stress 
Region of vertical 
least principal stress 
Propagating 
crack 
Magma 
s1, s2, s3 Principal stresses 
s Least principal stresses

Figure 5. Idealized Stress Trajectory for the Mountain. Principal Stresses: Vo = Initial Vertical, Ho = 
Larger Horizontal, and ho = Smaller Horizontal (Least Principal Stress), TS = Thermal 
Addition to Stress, TSm = Maximum Additional Stress 
H0 
h0 
H= H0 +aTS 
V= V0 +bTS 
h = h0 +TS 
TSm 
TS(Temperature) 
V0 
Increasing stress 
Initial 
Stress 
Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 42

Figure 6. Design Cross-Section 
0.606 
Sketch not to scale 
Springline 
0.5 
1.339 
1 2.75 
1.495 
0.396 
0.835 
26 deg 
1.231 
backfill 
invert 
NOTE: Sketch corresponding to In-Drift Data for Drift-Scale Models for TSPA-SR (Rev 01). 
Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 43 
DTN: SN9908T087279.004

Figure 7. Pre-Intrusion Layout 
5.5 m 
Backfill 
Drip 
shield 
Spacing between 
containers ~10 cm Pallet 
Invert 
Container 
Drip 
shield 
Backfill 
Skirt ~.25 m 
Dike Propagation Near Drifts 
ANL-WIS-MD-000015 Rev 00 April 2000 44 
Sketch Not to Scale 
DTN: SN990870872799.004 
CRWMS M&O 2000f

ANL-WIS-MD-000015 Rev 00 45 April 2000 
Figure 8. Post-Intrusion Disruption 
Jammed 
drip shields 
Displaced 
backfill 
Distorted 
drip shield 
Displaced 
invert 
Dike

ANL-WIS-MD-000015 Rev 00 46 April 2000 
Figure 9. Post-Dike Emplacement, 
Magma Plug Superimposed 
on Figure 8 
Dike 
Magma plug 
Jammed 
drip shield Distorted 
drip shield 
Displaced 
backfill 
Displaced 
invert