HEAT VARIATIONS CAUSED BY GROUNDWATER FLOW 
IN GROWTH FAULTS OF THE SOUTH TEXAS 
GULF COAST BASIN 

APPROVED: 

©December 1985 by Daniel Bodner, Austin, Texas 
Al 1 rights reserved. No part of this Thesis may be reproduced in any rorm or by any means without permission In writing rrom the Author. 
Printed in the United States of America 
HEAT VARIATIONS CAUSED BY GROUNDWATER FLOW 

IN GROWTH FAULTS OF THE SOUTH TEXAS 
GULF COAST BASIN 

by 
DANIEL PAUL BODNER, A.B. 
THESIS 
Presented to the Faculty of the Graduate School of 
The University of Texas At Austin 
in Partial Fulfillment 
of the Requirements 
for the Degree of 

MASTER OF ARTS 
THE UNIVERSITY OF TEXAS AT AUSTIN 
December, 1985 
ACKNOWLEDGEMENTS 
The pages of this volume represent the largest single project I have ever undertaken. Throughout its duration, I have had the unfailing support and counsel of my advisor, who is also my friend, Jack Sharp. am grateful to him. 
I also thank my committee members, Dr. Lynton S. Land and Dr. William E. Galloway, for sharing their advice and knowledge, and for their valuable contributions to the editing process. Lynton is also gratefully acknowledged for providing the original idea which grew into this thesis, and which proved to be rewarding and stimulating. 
The research stimulated not only myself, but also the Texas Mining and Mineral Resource Research Institute of the Department of the Interior, whom I thank for providing one of the most tangible rewards, the support of my research. 
Technical support was provided by the Bureau of Economic Geology, who supplied the well logs and computer facilites used in obtaining and processing my temperature data. I especially acknowledge Graham Fogg for his advice and time, which was always given freely. 
iv 
Md colleague Paul Blanchard has been very helpful tn sharing tdeas, references, and computer frustrattons. lmmessurab1e moral support has been generoulsy provided by my friends, who have made my tenure at the University of Texas a very enjoyable one. 
Finally, I owe a gratitude of a much grander scale to my parents, and also to my brother and the rest of my family, who have provided me with the tools to make of my self what I choose, and who have always loved and supported me, and whom I love and support tn return. 
v 

Abstract 

Zones of above average subsurface temperatures have been noted in certain areas of the Gulf Coast basin. Their cause has often been cred1ted to geopressure. wh1ch presumably traps heat because of higher poros1ty and consequently lower thermal conductivity. I determined the temperature distribution in a portion of South Texas by collecting and analyztng over 1600 bottom-hole temperature measurements. The analysts 1ncluded correcting the temperatures w1th the Kehle correction scheme; construct1ng 1sothermal surfaces by both 1nterpolat1ng and extrapolat1ng the data. and Kr1g1ng the result. Temperature profiles were plotted for twelve subregions of the study area. The greatest temperature anoma11es are assoc1ated w1th the Tert1ary wncox growth fault zone, and the s1mple presence of geopressure is insufficient to account for the temperature anomaly. 
Numerical modeling indicates that growth faults act as zones for concentrated vertical flow. The upwelling of deep bas1na1 flu1ds advects heat and causes the high temperatures observed in the growth fault zone. The model, by Sm1th (1983), 1s two-d1mens1onal, f1n1te element, steady state, and couples heat and flu1d transport. It 1nd1cates that the source of these flu1ds 1s deep, perhaps over 20,000 feet (6096 m) below the surface. The modeling results also suggest that an unidentified region of high thermal and hydraulic conduct1v1ty could exist coastward of the Wilcox faults at a depth of about 1 s.000­20,000 feet (4572-6096m). 
Vi 
TABLE OF CONTENTS 

ACKNOWLEDGEMENTS iv ABSTRACT vi LIST OF FIGURES xi INTRODUCTION PART 1 4 I I Background 4 
1.1.1 The Study Area 4 
t. 1.2 Regional Geology 4 
1. 1.3 ThermaI History 6 
1.1.4 Generalized Flow Systems 6 Meteoric Zone 9 Compactional/Overpressured Zone 9 Thermobaric Zone 11 1 2 Data ColJectjon and Preparation 13 
1.2. 1 Temperature Correct ions 14 
1.2.2 Creating the Computer Ftle 15 
1.2.3 Manipulating the File 16 
1.3 Observed Thermal Patterns 17 
1 .4 Groundwater Flow 44 
1.4. 1 Evidence for Vertically Moving Fluids 45 
1.4.2 Regional Trends 48 1 5 Summary 48 
vii 
PART 2 50 
2. 1 Model Specjfjcatjons 51 2 2 Features of the Model 53 
2.2. 1 Equations of Heat and Fluid Flow 53 
2.2.2 Bounddary Conditions, Assumptions, and Limitations 59 Basal Boundary 59 Surface Boundary 60 Lateral Bondary 60 Flux Nodes 60 Mathematical Assumptions 61 Chemistry 61 Assessing Thermal Conductivity 62 Limitations of Scale 63 2 3 Design 65 
2.3.1 Calibration 65 
2.3.2 The Mesh 66 
2.3.3 The Code Maps 67 Porosity Field 67 Thermal Conductivity 67 Permeability 68 
2.4 Results 69 
2.4.1 Simulation One -Conduction Dominated 70 Flux Nodes 70 Permeability Codes 72 Porosity Code 73 
vt11 
Therma1 Conductivity Code 74 
2.4.2 Simulation One-Results 75 F1uid Flux 75 F 1 u id Pressure 76 Temperature 78 The Flow Regime 80 
2.4.3 Simulation Two -Concentrated Flow 84 Flux Nodes 84 Permeability Codes 84 Porosity & Thermal Conductivity Codes 87 
2.4.4 Simulation Two -Results 88 Fluid Pressure 88 Temperature 91 The Flow Regime 91 
2.4.5 Simulation Three -Mixed Conditions 91 
2.4.6 Simulation Three -Results 95 F 1 u id Pressure 95 Temperature 95 The Flow Regime 102 
2.5 Qjscussjon 102 
2.5.1 Implications of the Model 102 CONCLUSIONS 110 APPENDIX A -THE DATA 113 APPENDIX B -THE KEHLE TEMPERATURE CORRECTION SCHEME 138 APPENDIX C -CALCULATING ISOTHERMS 139 ix 
APPENDIX D -KRIGING The Varjogram Variogram Computer Program The Search Window The UTM Coordinate System Variogram Program GAMM8 Plotting Program NEWPLOT The Kriging Program NEWUKB APPENDIX · E -CPS 1 Posting Data Contouring Isometric Projection APPENDIX F -FLOW VELOCITY REFERENCES VITA 
141 142 145 145 
148 148 
151 
155 
160 
161 
162 163 VECTOR FIELDS 164 181 188 
x 

LIST OF FIGURES 

1. 1 Study area. 5 1.2 Type cross section. 7 1.3 Heat flow after rifting. 8 1.4 Generalized hydrogeologic model of a sedimentary basin. 10 1.5 Generalized fluid pressure vs. depth in Gulf Coast. 12 1.6a 2oo·F isotherm -3D isometric. 18 1.6b 2oo·F isotherm -contour map. 19 1.6c Well locations for 2oo·F isotherm. 20 1.6d Standard Deviation of contoured 2oo·F isotherm. 21 1.7a 25o·F isotherm -3D isometric. 22 1.7b 25o•f isotherm -contour map. 23 1.7c Well locations for 2so·F isotherm. 24 1.7d Standard Deviation of contoured 2so·F isotherm. 25 1.8a 3oo·F isotherm -3D isometric. 26 1.8b 3oo·F isotherm -contour map. 27 1.8c Well locations for 3oo·F isotherm. 28 1.8d Standard DeviatIon of contoured 3oo·F isotherm. 29 1.9a 35o•F isotherm -3D isometric. 30 1.9b 3so·F isotherm -contour map. 31 1.9c Well locations for 3so·F isotherm. 32 1.9d Standard Deviation of contoured 35o·F isotherm. 33 
1. 1Oa 40o·F isotherm -30 isometric. 34 
1. 1Ob 400.F isotherm -contour map. 35 
1.1 Oc We111ocations for 40o•F isotherm. 36 xt 
1.1 Od Standard Deviation of contoured 4oo·F isotherm. 
1. 11 Study area with subareas, Wilcox growth faults, and location of type section shown. 39 
1.12 Temperature/depth profile for subarea 1. 	40 
1.13 Temperature/depth profile for subarea 2. 	40 
1.14 Temperature/depth profile for subarea 3. 	40 
1.15 Temperature/depth profile for subarea 4. 	40 
1.16 Temperature/depth profile for subarea 5. 	41 
1.17 Temperature/depth profile for subarea 6. 	41 
1.18 Temperature/depth profile for subarea 7. 	41 
1.19 Temperature/depth profile for subarea 8. 	41 
1.20 Temperature/depth profile for subarea 9. 	42 
1.21 Temperature/depth profile for subarea 10. 	42 
1.22 Temperature/depth profile for subarea 11. 	42 
1.23 Temperature/depth profile for subarea 12. 	42 
1.24 	South Texas showing subareas where temperature data were collected and their corresponding geothermal gradients, generated by linear regression. 43 
2.1 	Study area showing location of type section 52 
2.2 	The finite element mesh (40x). 58 
2.3 	The finite element mesh (true scale). 64 
2.4 	Fluid flux assigned to the basement nodes of the mesh for Simulation One. 71 
2.5 	Horizontal permeability field for Simulation one. 72 
2.6 	Vertical permeability field for Simulation one. 73 
xii 

2.7 Porosity field for Simulation one. 74 
2.8 Thermal conductivity field for Simulation One. 75 
2.9 Model-generated hydraulic head for Simulation One. 77 
2.10 Pressure profiles for Simulation One. 79 
2.11 Modeled isotherms for Simulation One. 81 
2.12 Modeled Temperature profiles of area 7. 82 
2.13 Modeled Temperature profiles of area 3. 82 
2.14 Modeled Temperature proflles of area 9. 82 
2.15 Modeled Temperature profiles of area 12. 82 
2.16 Flow velocity vectors for Simulation One. 83 
2.17 Fluid flux assigned to the basement nodes of the mesh for Simulation Two. 85 
2.18 Horizontal permeability field for Simulation Two. 86 
2.19 Vertical permeability field for Simulation Two. 87 
2.20 Thermal conductivity field for Simulation Two. 88 
2.21 Model-generated hydraulic head for Simulation Two. 89 
2.22 Pressure profiles for Simulation Two 90 
2.23 Modeled isotherms for Simulation Two 92 
2.24 Modeled Temperature profiles of area 7. 93 
2.25 Modeled Temperature profiles of area 3. 93 
2.26 Modeled Temperature profiles of area 9. 93 
2.27 Modeled Temperature profiles of area 12. 93 
2.28 Flow velocity vectors for Simulation Two 94 
2.29 Horizontal permeability field for Simulation Three. 96 
2.30 Vertical permeability field for Simulation Three. 96 
Xtii 
2.31 Porosity field for Simulation Three. 97 
2.32 Thermal conductivity field for Simulation Three. 97 
2.33 Model-generated hydraulic head for Simulation Two. 98 
2.34 Pressure profiles for Simulation Three. 99 
2.35 Modeled isotherms for Simulation Three 100 
2.36 Modeled Temperature profiles of area 7. 101 
2.37 Modeled Temperature profiles of area 3. 101 
2.38 Modeled Temperature profiles of area 9. 101 
2.39 Modeled Temperature profiles of area 12. 101 
2.40 Flow velocity vectors for Simulation Three. 103 01 Typical Variogram. 143 02 Kriging a block center using a variogram. 144 03 Constructing a nondirectional variogram 147 04 Constructing aa NW-SE directional variogram 147 05 Optaining C,CO, and A by construction 154 
x1v 




INTRODUCTION 
In the Gulf Coast Basin, as well as in most sedimentary basins, temperatures are unevenly distributed. The source of heat is the earth itself, which radiates heat from within in a relatively uniform fashion as a result of dispersed radioactive decay. There are many factors which cause uneven thermal patterns to emerge from this uniform heat source. These can be grouped into the following broad categories: heat transport by basinal fluids, heat transport through the solids, the presence of plutons or other heat sources or sinks, chemical reactions, and mass and energy exchanges across basina1 boundaries. Of these, conduction and transport of heat via the movement of ground water, which saturates the sediments of the basin, are perhaps the most important processes in the Gulf Coast. Water has a high specific heat (ie., it can absorb heat without greatly raising its temperature). Thus flowing ground water has the potential to transport a significant amount of heat. Conversely, the heat content itself influences groundwater movement by altering the fluid's hydraulic properties. Thus one process influences and is in tum tnfluenced by the other. These are said to be coupled. This thesis explores the importance of coupled ground water and heat transport in controlltng the deep bastnal thermal regime of the Gulf Coast Basin. 
Knowledge of groundwater movement tn the deep basin has practical consequences in both the energy and mineral industries, as well as tn academic inquiries into bastnal diagenesis. It ts, however, often difficult to observe groundwater movement, especially where rates are slow and/or tn the remote deep-basin. It is less difficult to measure temperatures at such points. The coupled flow phenomena provides a method by which groundwater movement tn the deep basin can be inferred from available temperature data. This is the approach of this research. 
The research required two distinct stages. The initial step was data collection and analysis. These are presented in Part I. Part I includes discussion of the data, their collection and preparation, descripttons of the thermal patterns that emerged from analysts of these data, and implications of these patterns for groundwater flow. After the completion of the first stage, tt was evident that too many factors were involved in the thermal regime of the basin to make any definitive conclusions possible from this largely empirical approach. However, the data were consistent and anomalous thermal trends were evident. Therefore, the second stage required computer modeling of the basin using the acquired thermal data. The details of the model, its results, and its implications are covered in Part 11. Finally, the analysis allows us to make some definite conclusions about heat flux and groundwater flow in the deep portions of the Gulf of Mexico Basin and to offer 
suggestions for further investigation. 
PART I 
1. 1 BACKGROUND 1 1 1 THE STUDY AREA 
The study was conducted on a regional scale, covertng a large portion of South Texas <Fig 1.1). The total area is over 17,000 square miles (44,030 km2) and includes all or part of the counties of Webb, Zapata, Jtm Hogg, Kleberg, Duval, Jtm Wells, Nueces, Lasalle, Mcf'tJllen, Live Oak, Refugio, San Patrtcto, Aransas, Bee,Atascosa, Karnes, Goltad, and Victoria. The area features low topographtc relief, _with greatest elevations of about 600 feet ( 183 m) to the west, dropptng gradually to sea level at the coast. The maximum depth Investigated Is 20,000 feet (6096 m), which is wholly within Tertiary sediments. 
1 1 2 REGIONAL GEOLOGY 
The onshore lower Tertiary Gulf Coast section is composed of several terrlgenous elastic wedges, which thicken down dip toward the Gulf of Mexico. The sediments prograded over and basinward of the rapidly subsiding Cretaceous Stuart City shelf margin, where 
4 

contemporaneous growth faulting ensued in bands along the shelf edge. As sedimentation and subsidence continued, the shelf edge prograded seaward, establishing other growth fault zones (Fig 1.2). The major growth fault zones have been named after large sediment packages associated with them. The three major ones are the Wilcox, Vicksburg and Frio growth fault trends as shown on the cross section in Fig 1.2 wh1ch also fdentiffes other major elastic groups. 
1I1 3 THERMAL. HISTORY 
Potentia11y dominant heat sources are recent tectonic events, 
which can cause high basement heat fluxes, and volcanic activity, which 
causes localized heat-source variations. 
The most recent tectonic event involving the Gulf Coast was 
the late Triassic/early Jurassic rifting episode. This event probably 
featured typical rift-level heat fluxes. Figure 1.3 (Boyden and others, 
1980) indicates a return to background heat-flux levels by Cretaceous 
time. Therefore, ·normal" levels of heat flux have presumably prevailed 
since the Cretaceous. While local Cretaceous and Tertiary volcanic 
activity may have perturbed this pattern, their effects were minimal. 
1 1 .4 GENERAL IZED FLOW SVSTEtt5 Generalized groundwater flow through Gulf Coast sediments 
· can be conceptualized as occurring in three distinct zones closely correlated wfth depth. Flow in each of these zones ts contro11ed by different mechanisms. The three, from sha11owest to deepest, are the 
Group 7 Group 3 Group9 Group 12 
A 
Vertical Exaggeration 40 
a 1s Mi 
o 15 Km 
A 
Figure 1.2: Generalized cross section of south Texas Gulf Coast. Grey pattern shows the sandier units;-the rest of the section being predominantly argillaceous (modified.from W.,E. Galloway, written communication). Also indicated are isotherms and the top of the geopressure Transition zone as determined by drilling mud weights. Heavy outline indicates position of finite element grid used in modeling (Part 2). 
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AGE IN M.Y. 
Figure 1.3: Generalized plot of mean heat flow versus time after a rifting event. Stippled boxes indicate various heat flow data (redrawn from Royden and others., 1980) 
meteoric, compactional/overpressured and thermobar1c zones. These are shown for a generaltzed sedimentary basin in Figure 1.4 from Galloway and Hobday ( 1983). 
Meteoric Zone. Groundwater flow 1n the meteoric zone ts contro11ed by the elevat1on of the water table (1.e., ground water moves from areas of high hydrau11c potential, usua11y under topographic highs, to areas where the potential is low, usually at rivers and streams). It has been demonstrated by Back ( 1966) for the Atlant1c Coastal Plain and also by Smith and others ( 1982) for the Oakville aquifer of Texas that most ground water discharges to rivers. This is contrary to the common misconception that meteoric water flows only down dip towards the coast, a condition that occurs primarily near the coast where there is little topographic relief and in deeper, more inactive portions of the meteoric zone. For these cases, discharge is by diffuse, upward, cross­formational flow in the vicinity of the shoreline and is not concentrated near rivers and streams. The term meteoric implies water of an atmospheric origin, but connate water may also enter the meteoric system. 
CompacttonaJ/oyerpressured zone The compactional/overpressured system lies below the meteoric one. Here groundwater movements are not significantly influenced by surficial conditions, but rather are controlled by excess pore-fluid pressure gradients. Excess pressures are partially caused by the weight of the accumulated overlying sediments which causes this zone to compress or compact. As the sediment grains come closer together, the intergranular 

SUBSIDENCE 
Figure 1.4: Generalized hydrogeologic model of a sedimentary basin (redrawn from Galloway and Hobday, 1983). 
spaces become smaller and the pore fluid is expelled concommitantly. If permeability is not sufficiently high, as is the case in Gulf Coast clays and shales, the fluid becomes trapped for a time. Higher porosities may thus be maintained in the sediment, kept open by trapped pore fluids which are also subjected to greater than normal pressures. This circumstance is variously known as overpressuring, excess pressuring, or geopressuring and represents a compactional disequilibrium. Eventually, the trapped fluids will bleed off, the sediments will compact, and equilibrium will be reestablished, unless the pressuring processes are continued (Gibson, 1956; Magara, 1976; Sharp, 1976; Sharp and Domenico, 1976; and Keith and Rimstidt, 1985). Other mechanisms have been proposed as contributing to excess pressuring, including aquathermal pressuring (Barker, 1972), mineral phase transformations such as clay dehydration(Burst, 1969; Weaver & Beck, 1971; Bruce, 1984), and hydrocarbon maturation (Hedberg, 1980). 
f1Jch of the Gulf Coast Basin is overpressured. The hachured line in Figure 1.2 indicates the top of overpressure derived from mud weights. Figure 1.5 shows generalized plots of fluid pressure versus depth for the Gulf Coast, depicting inflection points where pressure deviates from the normal hydrostatic condition. The sediments beneath these points are considered to be overpressured, although discontinuous zones of lesser overpressures may exist above this depth. 
Therroobaric Zone. The thermobaric regime is transitional with the compactional regime and encompasses the deepest parts of the basin. This regime is defined as the zone where the temperatures and pressures 
PRESSURE 
PSI (x 1000) 
0 3 6 9 12

o------.....;i.,_____...1.,______..._______...___....,...o 

Figure 1.5: Generalized variation of fluid pressure versus depth in the Gulf Coast. 
are great enough to cause low-grade metamorphfsm. The subsequent release of metamorphic fluids is presumed to be the major hydro1ogic process. Rocks above and/or below the Louann Salt may currently be producing water in addition to large quantities of carbon dioxide as the result of metamorphfc reactions. The importance of these fluids on the hydrology of the rest of the basin is unknown because direct sampling of this portion of the basin has not yet been accomplished. 
1.2 DATA COLLECTION AND PREPARATION 
The data collected for thfs research consists of over 1600 bottom-hole temperatures (BHTs) from over 725 separate we11s (see pocket map for locations). The BHT readings where taken off of well headers, ie., the first page of an electric log. The headers also list other information about the well including the Company that dri11ed it,the depths of each run, the land owner, sometimes the elevation of the well head, and its location. The Jogs listed in Appendix A are a11 from the files of the Bureau of Economic Geology (BEG), but are in the public domain and may be purchased from the appropriate we111ibraries. To co11ect them, all Jogs held by BEG for wells withfn the study area were examined. Of those, all that were readable, that included the we11 head elevation, and that had BHTs above 11o·F were recorded. It should be noted that data for shallow measurements below 11o·F were not recorded, though such measurements did exist on many logs. It was later apparent that this information would have been quite useful, but time constraints ruled out their aquisition. Any additional research should include adding shallow measurements to the data base. 
1.2 1 TEMPERATURE CORRECT IONS 
A bottom-hole temperature is a temperature reading taken at the bottom of a well. In the case of deep oil wells, such as those used in this study, a logging tool equipped with a thermometer is lowered periodically as the hole is deepened. Thus several runs, each with a separate BHT reading, are commonly available from a deep well. 
When a well is logged, the bottom-hole temperature is just one of many different types of measurements taken. Many different measuring instruments are usually lowered into the ho1e strung together in a pipe-like bundle known as a sonde. When Jogging, dri11ing operations must be halted, and the sondes are lowered into the hole without removing the dri11ing mud. There are many sources of error that are introduced when taking the bottom-hole temperature, mostly linked to temperature equilibration problems. When drilling, the drilling mud which fi11s the hole and surrounds the drill stem is circulated to remove the drilling debris and to keep the drill bit cool. As a consequence, the rocks surrounding the ho1e are a1so cooled. When Jogging, mud circulation is halted, but the time elapsed between halted circulation and temperature measurement is usually not enough for the bottom-hole temperature to reequilibrate with the actual temperature of the rock at that depth. Of course, it would be useful to record thfs elapsed time so that some estimate of the degree of equilibration could be made,-but 
IS 

unfortunately this is seldom included on the well log. It is clear, however, that some sort of correction is needed for the BHT reading. 
The correction scheme adopted for these data is that of Kehle ( 1971 ), an empirical correction determined by comparing equilibrium and we11-log bottom-hole temperatures from 602 selected West Texas and Louisiana wells. The apparent temperature from well-log BHTs was subtracted from the temperature obtained using equilibrium BHTs and the difference was plotted as a function of depth. A polynomial was fitted to these data using a least square error criterion, resulting in the correction curve shown in Appendix B. 
122 CREATING THE COMPUTER FILE 
In order to use the data in computer applications, a computer data file was created. The file was first loaded with well identification numbers and corresponding location coordinates. This was done using a digitizing tablet and BEG software. The wen maps were placed on the digitizing tablet, and the well positions were recorded by manually positioning a cursor over the selected wells. An arbitrary numbering system was used to keep track of each well, and a notebook was used to record all the corresponding log information. When all the wells were digitized, the elevation, temperature, and depth readings recorded in the notebook were free-formatted into the file from a terminal, one computer Hne per well. The completed f11e contained over 725 lines, each line containing one we11's identification number, location coordinates, multiple BHT and depth readings, and its elevation. ­
1 2 3 MANIPULATING THE FILE 
Once the raw data was entered into the file, a program was written to calculate the Kehle temperature corrections for each paired BHT and depth reading. The program created a new file which contained the corrected temperatures in a formatted form. Appendix B shows the correction scheme. 
In order to produce isothermal surfaces, the depth data had to be converted to a depth relative to sea-level, and interpolated or extrapolated to arbitrarily chosen temperatures. I choose so·F increments from 2oo·F to 40o·F. A program was written to produce files for each isothermal surface from the main data file. Since the thermal trends which were being investigated were assumed to vary with depth, tt was essential to limit the amount of tnterpolatton or extrapolation to a fairly narrow temperature range. The program thus requires the user to specify a temperature range limit. If a well has no BHT values w1thtn the specifled temperature range of that isotherm, then that well is disregarded. If there is a value within the range, than the depth to the isotherm is either interpolated between it and the next closest temperature/depth pair that the isotherm value straddles, or, if there are no other values, the data is extrapolated to the isotherm. The range was set at 3o•F for the 200,250, and 3oo·F isotherms, and was so·F for the 350 and 40o•F isotherms, for which data are more scarce. Appendix C shows the FORTRAN program used to create the isothermal data files. 
Data scatter had to be eliminated to contour isotherms. This 
was accomplished by the geostatistical technique of kriging. The kriging process smooths the data by analyzing the variation in the data and weighting each data point accordingly. The technique also provides a determination of the accuracy of the contoured surface by supplying standard deviations at gridded intervals. Appendix Dprovides extensive information on the procedures for kriging. 
Finally, to produce contour maps and three-dimensional drawings, Radian Corporation's CPS 1graphics subroutines were employed. Appendix E briefly covers the use of CPS 1, which is sophisticated and cumbersome. Large amounts of computer and personal time were consumed before the figures presented in this chapter were successfully produced. The temperature profiles and 1inear regressions were executed in the statistics package SPSS. 
1.3 OBSERVED THERMAL PATTERNS 
The following series of twenty illustrations (Figs. 1.6-1.10, a through d) depicts the temperature patterns that were resolved from the data. These patterns are viewed from the perspective of five isotherms (200, 250, 300, 350, 400 •F). Four illustrations are shown for each isotherm: a, a three-dimensional representation of the surface; b, the corresponding contour map; c, the selected data; and d, a contour map of the standard deviations for the isothermal surface. With each succeeding temperature increment the depths increase, as one would expect. Also increasing with temperature is the prominence of athermal 

18 , 

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Figure 1.Sa: Isotherm from.corrected and Kriged-BHT data with study area projected above. 

Figure 1.6b: Contoured 200"F isotherm within the study area. 
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Figure 1.6c: Well locations for the 200°F isotherm. 

Figure 1.6d: Standard Deviation of contoured 200"F isotherm (computed by Kriging). 

Figure 1.7a: Isotherm from corrected and Kriged BHT data with study area projected above. 

Figure 1.7b: Contoured 2so·F isotherm within the study area. 
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Figure 1.7c: Well locations for the 250°F isotherm. Figure 1.7d: Standard Deviation of contoured 250°F isotherm (computed by Kriging). 


Figure 1.Ba: Isotherm fram corrected and Kriged BHT data with study area projectedabove. 

Figure 1.8b: Contoured 3oo·F isotherm within the study area. 
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Figure 1.8c: Well locations for the 300°F isotherm. 

Figure 1.8d: Standard Deviation of contoured 300"F isotherm (computed by Kriging). 

Figure 1.9a: Isotherm from corrected and Kriged BHT data with study area projected above. 

Figure 1.9b: Contoured 350°F isotherm within the study area. 
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Figure 1.9c: Well locations for the 350°F isotherm. 

Figure 1.9d: Standard Deviation of contoured 350°F isotherm (computed by Kriging). 
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Figure 1.10a: Isotherm from corrected and Kriged BHT data with study arecfprojected above. 

Figure 1.10b: Contoured 400°F isotherm within the study area. 
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" 
Figure 1.10c: Well locations for the 400'F isotherm. Figure 1.10d: Standard Deviation of contoured 400°F isotherm (computed by Kriging) . 

ridge trending SW subparallel to the coast. This ridge corresponds to the Wilcox growth fault zone shown in Fig 1.11. It indicates that high temperatures occur shallower near the fault zone than in the surrounding areas and that this effect begins at. about 10,000 feet (3048m) and becomes more pronounced at increasing depths. 
The isothermal surfaces are informative but they obscure the actual data points. Another way to observe the thermal trends is via a series of charts plotting depth versus temperature for the actual corrected BHT measurements. For this purpose, the study area was divided into 12 subareas, shown in figure 1.11. The subareas were drawn to correspond to the Wi Icox growth fault trend (subareas 1 through 5), the Vicksburg/Frio growth fault trend (subareas 10, 11 and 12), and the remaining outlying areas. These temperature profiles appear in numeric order from figure 1.12 to 1.23. On this plot, the slope of a line corresponds to a thermal gradient. The steeper the slope, the lower the gradient. The dashed line on each plot Indicates what is generally considered the normal earth gradient of 1.64·FI100 Ft (30 •c/km) The+ signs indicate individual corrected BHT measurements. The solid line is a linear regression for the data. The correlation coef1cients among the regressions were all above .90. Fig. 1.24 summarizes all the regression lines and also tabulates the gradients represented by each regression line for each subarea. Not surprisingly, the Wilcox growth fault zone is characterized by the highest gradients, which far exceed normal _ gradients. Fairly high gradients are also found in the Vicksburg/Frio 

0 
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Figure 1.12 
GR OUP THREE 
50 100 150 200 250 TEMPIRATUllE DIG C 
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50 150 250 350 450 TEMPERATURE DEG F 
Figure 1.14 
GROUP T\til'.l 
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Figure 1.13 
GROUP FOUR
.
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50 150 250 350 450 TEMPERATURE DEG F 
Figure 1.15 
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Figure 1.16 
GROUP SEVEN 
50 100 150 200 250 TEMPERATURE DEG C 
/ 1.&4'Ft 100 FT 
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Figure 1.18 
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50 150 250 350 TEMPERATURE DEG F Figure 1.20  450  
50  '.;R OUP EL EVEN 100 150 200 TEMPERATURE DEG C  250  
/1.64 · F~100 FT  

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Figure 1.23 

11-ERMAL GRADIENTS Group °F/100ft °C/lun 
1  2.44  44.6  
2  2.52  46.1  
3  2.88  52.3  
"  3.08  58.3  
5  2.98  54.7  
6  1.80  32.9  
7  1.88  3".4'  
8  1.97  36.0  
9  2.oa  38.1  
10  2.06  37.7  
11  2.18  39.9  
12  2.38  43.5  

0 
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REGRESSION LINES FROM DATA GROUPS 
\ 1.64°F/100 FT 
\/ 

9  
\  
\  
\  
\  
\  
50  150  250  350  450  
TEMPERATURE  DEG  f  
Figure 1.24: s·outh Texas showing subareas where temperature data were collected and their corresponding geothermal gradients, generated by linear regression. 


' -· ·· .. . . -. -. ­

fault zone. The summary of regression lines also reveals a trend of higher gradients toward the southwest. 
1.4 GROUNDWATER FLOW 
One of the most frequently fnvoked scenarios to explafn anomalously high temperatures in the Gulf Coast was ffrst descrfbed by Lewis and Rose ( 1970) who called on overpressurfng as a major contrfbuting factor. The correlatton between overpressurfng and abrupt 1ncreases 1n thermal gradients fs hard to deny. On the temperature profi Jes of f fgures 1.12 through 1.23 the departure of the data trend from the normal gradient (dashed line) corresponds closely with the top of geopressuring indicated by the hachured Iine fn figure 1.2 (derived from mud weights). The Lewfs and Rose model attributes this to decreased thermal conductivity of the overpressured zone (i.e., the ability of this zone to conduct heat is diminished), giving it insulatfng properties relative to the surrounding sediments. The decreased conductivity results from the higher porosity and consequent water content of these overpressured sediments. Water has a lower thermal conductivity than mineral grains. 
This scenario 1s not completely consistent with the known configuration of the basin and the temperature data. Since overpressuring largely results from a compactional disequil1br1um, its presence correlates to the presence of extensive marine shale bodies whose low permeab111ty causes the dtsequ11tbrium. According to the scenario, these same areas should exhibit a temperature build up because 

of their insulating characteristics, and the more extensive the shales are, the larger the thermal insulating effect should be. But, in fact, the marine shales are more extensive on either side of the Wilcox fault zone than in the zone itself, which features significant sand accumulation (see Fig. 1.2). Yet the thermal anomaly is greatest within the growth fault zone and declines sharply on either side. Increased thermal gradients are also noted in the other major growth-faulted regions, the Vicksburg and Frio zones, where marine shales are least prevalent. One must therefore conclude that simple thermal conductivity variation is not sufficient to explain the observed patterns. Furthermore, the presence of the growth faults is clearly associated with the development of high-temperature anomalies within geopressure, so that flutd movement along the faults is an attractive mechanism for heat transfer. For reasons stated in section 1.1.3, isolated regions of high basement heat flux were ruled out as a possi lbe factor. 
1.4.1 EVIDENCE FOR VERTICALLY tDVING FLUIDS 
There is much circumstantial evidence that fluids move upward along growth faults. Galloway ( 1984) and Smith and others ( 1982) described evidence in Uranium deposits in the Oakville Sandstone (Miocene) for pulses of deep-basinal fluids from adjoining growth faults. Similar findings from temperature and salinity data were reported by '1..lmme and Ferrel ( 1979) for growth faults in Louisiana, and by Kingston ( 1985) for Oakville associated growth faults. Furthermore, the occurences of oil often suggests involvement of faults in migration. 
Philippi ( 1965) discusses chemical evidence from shallow oil fields indicating its similarity to deep-dispersed oil, again suggesting vertical migration of fluids. 
Petrographers have been confounded by the abundance of cements in Gulf Coast sediments, which imply that large volumes of water have been flushed through the system. Oxygen isotopes suggest that the fluids responsible for this cementation were from high temperature regions, as is also suggested by the presence of sphalerite 
(K. l. Milliken, personal communication, 1985), and sphene and laumontite (Boles, 1980; Richman and others, 1980) in minor cements. Again, the evidence points toward fluids upwelling from great depths. 
Therefore it is not unreasonable that growth faults could act as conduits for upwelling fluids. The result of fluid movement of this type would be transport of heat from the compactional or thermobaric zones toward the surface. This could cause a thermal ridge like the one associated with the Wilcox growth faults. If so, the temperatures observed in this zone suggest that flow is occurring at depths even greater than 20,000 feet (6096 m), steadily diminishing to 10,000 feet (3048 m). This is indicated by the initial prominence and steady dissipation of the thermal ridge through this depth range. 
A similar, albeit more subdued pattern ts evident tn the temperature prof iies from the Vicksburg/Frio fault trend. The above­average gradients occur at greater depths because the geopressure system ts likewise deeper. The lithology tn the Vicksburg/Frio trend ts more complex than in the Wilcox trend, and tts flow regime may therefore 1nvolve more than the s1mple vertical flow proposed for the Wilcox growth faults. For example, free convection has been proposed for the extensive normally pressured sand packages 1n the Frio (Blanchard and Sharp, 1985; Bodner and others, 1985). Free convection would cause temperatures to exceed normal values at the top of the convection ce11, while causing below normal temperatures at 1ts base. Hence the low temperatures near the top of geopressuring which are indicated in the temperature prof Hes 1.21-1.23 may result from the lower portion of a convection cell. The mechanism of the moving boundary effect (Sharp and Domenico, 1976) could also be invoked. When sediment accumlations are sufficiently rapid, deposited material remains cool relative to 1ts burial depth unitl it can thermally e·quilibrate. The low temperatues near the top of geopressuring could be explained in this way. Without the sha11ow temperature data, possible flow mechanisms in this region are conjectural. 
It should be noted that free-convection may also be occuring on a regional scale in the basin. Petrologists and sedimentary geochemists have estimated that large volumes of water are needed to account for the volume of cements in the basin ( Bjorlykke, 1983; Wood and Hewett, 1982; Land and Dutton, 1979; Sibley and Blatt, 1976). The flow volumes indicated are so large that the recirculation of bastnal fluids ts the only reasonable means by which they can be supp11ed. Convection ce11s might integrate growth faults in their circulation, which presumably would be 
confined to the compactional system since flu1ds could not freely convect downward across the geopressure transition. 
142 REGIONAL TRENDS 
An interesting trend is observable in figure 1.24. The summary of regression lines from each subarea shows a strong relationship between geothermal gradient and prox1mity to the Mexican border. The further southwest the subarea 1s located, the h1gher 1ts geothermal gradient tends to be. Th1s 1s observed 1n regressions 11nes 1-5, 6-7,and 10-12. The explanation for this phenomena is unknown. Apossible cause is increased heat flux across the basement towards the southwest. Why such a variation in heat flux should occur is unkown. Other possib11ities include a systematic regional gradation of lithology. Such a gradation seems unlikely because the trend is perpendicular to the progradation of facies and 1s therefore correlated to the location of depos1t1on, and not the type of depos1t1on. If reg1onal free convect1on 1s somehow integrated into the flow pattern of the major fault trends, one might speculate that the regional variations in the three-dimensional shape of the bas1n m1ght affect large scale convection cells, which could intum produce regional variations in geothermal gradients. 
1.5 SUMMARY 
Data collected for this research consists of bottom-hole temperatures from 750 wells. It ts clear that a h1gh-temperature ridge exists in the overpressured portion of the Wilcox growth fault zone. The anomaly begins to emerge at 10,000 feet (3048 m) and becomes more pronounced at increasing depths. Although high porosities associated with geopressures have been linked to lower thermal conductivities and higher geothermal gradients, this mechanism alone does not explain why the temperatures and gradients are highest in the fault zones, and lower in adjacent areas with similar geopressures. Instead, the fault zones themselves seem to be important, serving as conduits for vertical flow. The Wilcox faults correspond to greater temperatures than do the Vicksburg/Frio faults, perhaps due to the greater geopressuring in the Wilcox faults or other differences in their configuration and location. In addition, thermal gradients increase to the southwest for unknown reasons. The increase may be linked to increasing basement heat flux, but is not understood. Free convection may also be integrated into the flow pattern of the faults on a regional or local scale. The gradients in the Frio/Vicksburg trend, for example, ma~ in part be caused by a shallow, local convection cell. The regional variation of thermal gradients may likewise by tied to a changing configuration of regional convection cells. 
The evidence presented in thts section is empirical. Although ft presents a clear indication that vertical fluid movement in growth fault zones might be occurring, such an approach falls short of quantifying the flow. Variables such as thermal conductivy, hydraulic permeability, porosity, and the interplay between the meteoric, ­geopressured, and thermobaric zones, must be considered, and can be treated better by a quantitative model. 
PART 2-THE MODEL 
The temperature data discussed in the previous section support the hypothesis that vertical fluid movement is concentrated along fault-zones in the Gulf Coast Basin. However, because of the many different influences on heat distribution within the basin, it is difficult to distill empirically from these thermal patterns a definitive model of the deep-basinal flow -regime. In order to account for the many complicating factors in an integrated and realistic manner, a computer model is used to analyze the relative importance of certain factors vis-a-vis the others. This approach is termed a sensitivity analysis. In the case of observed thermal patterns, a model can, for example, help determine whether or not the concentrated vertical movement of fluids is an essential condition for producing the known temperature field. 
-
I have adopted a computer model for this purpose. This chapter is devoted to the modeling phase of research, and encompasses all its aspects, from the design of the program itself, to its 
so 
implementation, and the subsequent conclusions. For clarity, the computer code which performs the modeling operations shall henceforth be referred to as the program, and the design of the mesh and its various parameters to which the program is applied shall be termed the 
model. 
2.1 MODEL SPECIFICATIONS 
The overall goal of modeling was to determine the role of the groundwater flow regime in determining the basin's thermal regime. Using temperature distribution as the primary data, a model was implimented to inversely solve for fluid flow. A two-dimensional program by Smith (1984) was obtained for the study. It features coupled heat/fluid flow at steady-state conditions and calculates densities and viscosities as temperature and pressure dependent variables. 
Since the model was two-dimensional, only cross-sections could be modeled. For this purpose, a detailed cross-section compiled from well-logs by W. E. Galloway (written communication, 1985) was chosen as the type section. This particular section was one of the best avai I able and also traversed the study area from which the thermal data was collected. Fig. 2.1 shows its location in the study area and Fig. 1.2 shows a modified version of the cross-section. A second cross-sect ion by WesseIman ( 1983) which traverses a nearby area was also used as a cross reference. This cross-section also showed temperature data, which generally agreed with my data, but were 

derived from fewer points and were not statistically treated. The cross-section also provided pressure data, which also correlated well with pressure data taken from mud-weights. These data consist of contours of the geopressure transition zone and were used to position the top of the geopressure zone on the cross-section. 
2.2 FEATURES OF THE MODEL 
The first part of the following discussion covers the mathematical basis of the modeling program including its underlying assumptions. The mathematics are covered in greater detail by Smith ( 1984). A second sect ion deaIs with the boundary conditions and assumptions. 
2.2.1 EQUATIONS OF HEAT AND FLUID FLOW 
The building blocks of aNJ computer model are the equations on which it operates. Smith's model uses two general equations, one describing fluid flow, and the other heat flow. The fluid flow equation can be further subdivided into two parts, one for describing the driving forces for flow, and the other to state the conservation of mass at steady-state conditions. The former is of the form: 
-t11pog [ ahj az ] pr qi= -+pr -where pr= --1 (1) 
J1 axj axj po ­
where q1is the spec1fic discharge 1n the coordinate d1rect1on 1; klJ is the 
intrinsic permeability tensor of the porous medium,µ is the dynamic 
viscosity of the f1utd, gts the gravitational constant, /J ts the hydraulic head,p0 is a reference density of water, and Pr is a relative density of water derived from p0 and Pr· the nodal density of the fluid. Taken together, the permeability tensor, density, gravitational constant, and viscosity terms form the hydraulic conductivity K. The equation can be seen as a version of Darcy's law (f K*I where /,the hydraulic gradient, is reduced to two components, the pressure head plus the elevation head. The elevation head is modified in this case by the relative density term which adjusts for buoyancy affects. 
The flow equation must be combined with a continuity equation. The continuity equation is simply the mathematical statement that fluid mass is conserved, ie., in any given portion of the modeled area, the amount of fluid flowing in is equal to the amount flowing out. This equation is of the form: 
a a 
-[prqic] + -[prqz] = 0 (2) 
ax az 
fl utd cont1 nuttv equation The equation is set equal to zero to specify steady-state conditions. One equation is obtained from the two by substituting the expression for q from (1) into equation (2), this step being omitted here for clarity. 
The heat transport equation is composed of three basic terms, set equal to zero (steady-state). The equation is= 
a [ BT 8T]
-(n:A>0er + ( 1-n) :AIO<s ) -+ (n:A>ar + ( I -n) :A>a5 ) ­
ax ax az 
(x .arecti•• heat condldion and dispersion tn the solid-fluid composite) 
a [ 8T 8T]
+ -(n:AZ><r + (1-n):AzxS) -+ (n~r + (1 -n):AzzS) ­
az ax az 
(1 .anctt11 heat conduction and dtspersion 1 n the solid-flutd composite) 
8T 8T ] -pfCr qx -+ qz -=O (3)
[ 
ax az 
(ldYection of heat 'tt'ith fluid) 
where T is temperature, c, is the specific heat of the fluid, n is the pcrosity, Ar is the conduction-dispersion tensor for fluid, As is the 
heat conduction tensor for solid. The assigned longitudinal and horizontal thermal disperslvities were too and to meters respectively. The first two terms of the equation account for thermal conc:tuction and dispersion in the saturated medium. The third term accounts for the advectlon of heat with the fluid. 
For the above series of equations, viscosity and density are 
-
both figured as functions or temperature and pressure. For density, an Iterative proceedure Is used. based on equations given by Keenan and others. (1978). The basic equation which is solved for density pis: 
p=pRT [ 1 + pO + p2( Ba.) i-1 (4) ap 
where p is pressure. R is the gas constant. T is temperature on the Kelvin scale. T: is 1 ooon and Q is defined as: 1 a to Q=(-i---i-c> L(t:-t:1J)J-2 [LAjJ(p-p1J)i-J + e-Ep LAjjpl-9] (5) 
~· ~· ~ 
where T:c =1000/Tcrllical and T:aJ=T:c (if j=1) or =2.5 (If j>1) and PaJ= 
0.634 (if j= 1) or = 1.0 (if j> 1 ) . .A;J are coerricients whieh are 
tabulated in the appendix of Keenan and others ( 1978). 
Viscosity is determined from a set of equations presented by Watson and others (1980). The domain of validity for the equations is given by (O< Temp (Deg C) <900) for (O< Pres (MPa) <300). The viscosity equation is: 
p=Jlo(T)exp [ p• {L LaiJ X1YJ}] (6) 
where J.l is viscosity. T is temperature on the Kelvin Scale; pM = plpr where p is the denisty. Pr is a reference density; X=TM-t where T"=T/Tr· Tr being a reference temperature; Y=p"-1; a11 are 
coefficients tabulated in Watson and others (I 980); and J.lo is given by the equation: 
po(T) 3 a1c 
(7)
-= .fP [L(-)] -1 
I0-6Pa.s 1c=0 T* 
where C\ are coefficients which are also tabulated in the reference. The two dimensional model features anisotropic permeabi I ity, and temperature/pressure dependent density and viscosity. It employs the Galerkin finite-element method using linear basis functions applied to triangular elements. The reader is referred to the the works of Wang and Anderson (1982) and Pinder and Gray ( 1977) for a complete development of this method. For more about the application of finite­elements in heat transport problems see Mercer and others ( 1975), Andrews and Anderson ( 1979) and Li ( 1980). To use the model, a finite-element mesh is designed to conform to the area being studied. The mesh is a series of polygons, each being an element. At the corners of ·each polygon are nodes. Fig. 
2.2 shows the mesh used for this study. The following procedure was used to couple the heat and fluid flow equations: A purely conductive thermal regime Is Initially assumed and the temperature rlelel Is calculated by the heat transport equation (3), setting the advectlve term to zero. Appropriate viscosities and densities at the initial temperatures and pressures are then calculated for each element. These are entered Into the f lulcJ-flow equation ( 1 )+(2) to obtain a set of heads at the nodal points. The specific discharge q is then calculated ror each node (1). These are plugged back into the advective term of the heat-flow equation (3). and the whole equation is then 


MESH 
21. 81 43. 6J fi5. 44 87. 26 109. 07 130. 89 152. 70 174. 51 196. J3 21!. 14 239.H 281. 77 283. 59 METERS • 1 O' 
recalculated, entering into an iterative sequence. The iterations are halted when the maximum change in nodal temperatures is less than a given tolerance. The tolerance was set at .s·c. 
2.2.2 BOUNDARY CONDITIONS.ASSUMPTIONS AND LIMITATIONS 
The basic boundaries of the model are the four sides of the mesh, representing the bottom, surf ace, northwest and southeast edges of the cross section. 
Basal Boundary. The basal boundary is treated by the program as impermeable with a fixed heat flux value across it. It was assumed that the temperature perturbations of the basin are not the result of any basal heat source or si~. such as a pluton or a tectonic feature. Thus the basal heat flux was treated as uniform across the width of the mesh. The value used was 60 mW/sq m, which is a typical value for stable continental interiors (Reiter 1982, Epp and others, 1970, Smith, written communication, 1985). The Cretaceous boundary was taken as the basement of the basin, and although it is not impermeable, its permeability is probably very low. Note that the northwestern portion of the mesh slopes abruptly downward from shallow depths. This is intended to correspond with the position of the ancestral cretaceous shelf edges of the Stuart City and Sligo reefs. Further southeast, the boundary of the mesh is drawn horizontal at a constant depth of about 19,000 feet (5790 m). The actual depth to the Cretaceous here is not accurately known, but is perhaps as deep as 40,000 feet ( 12200 m). However, it was impractical to include greater depths in the model because of the lack of well control and temperature data. 
Surface Boundary. The upper boundary of the mesh is a constant head boundary with a fixed temperature at 2o·c. Because the temperature is fixed, the model can not account for any local heating at the water table due to upwelling fluids nor can it account for possible thermal springs. Since the meteoric system is not the prime focus of this investigation, these limitations are inconsequential. 
Lateral (Vertical) Boundaries. The sides of the mesh are treated as impermeable (no flow) and are also thermally nonconc:luctive. This is a somewhat unrealistic configuration. The mesh does not extend to the outcrop of many of the lower formations, nor does it go far offshore. Fluid and heat transfer could occur across both boundaries in nature. To resolve this problem, fluid flux terms were added to selected nodes on each of these boundaries. 
Flux Nodes. Several flux nodes were assigned to the lateral boundaries. Two on the northwest boundary near the outcrop belt of the Wilcox formation were assigned a combined flux of -0.00014 Kg/s, which is about 1 /2 ml per hour. The negative sign signifies injection of fluid. On the other side of the mesh were placed three constant flux nodes which withdrew fluid at the equal but opposite rate of +0.00014 Kg/ms. This arrangement simulated the passage of fluid into the section from outcrop, and also from the section into the Gulf. These fluxes proved to be rather unimportant in their effect on the pressure and temperature fields, and consequently their assigned values could be varied considerably without appreciable influence. Aside from the two negative flux nodes on the outcrop side of the mesh, other recharge of the meteoric zone was ignored. 

Because the model is steady-state and noncompacting, flux nodes were needed to simulate compaction-driven fluid in the geopressured zone. The model was first designed without such nodes and the result was a complete absence of geopressuring. Several distributions of these flux nodes were tried, and it was determined that fluxes assigned just to the basal nodes worked best. 
Mathematical Assumptions. As mentioned above, the program calculates appropriate densities and viscosities as functions of both temperature and pressure (equations 4 -7). The subroutines which handle these calculations are equipped to treat pure water in fluid, steam, or supercritical phases. However, multiphase flow is not allowed. In addition, the f luid is required to be in thermal equilibrium with the medium at all times. Thermal conductivity of the rock is assumed to be constant, although in reality is varies slightly as a function of temperature. Thermal conductivity of water is treated as a function of temperature. Porosity is also assumed to be nontransient. 
Chemistry. Chemical processes are extremely difficult to couple with groundwater models because of the oomerous calculations which even simple chemical models require. Including such calculations in an iterative sequence across an entire mesh would result in urmanageable computation times. As a result, both density and fluid flow calculations are somewhat handicapped. Fluid samples collected from Tertiary formations in the Gulf (Fisher 1982, Land, personal communication, 1985) indicate that the salinity (ppm) of formation waters is signif icanlly correlated to its in-situ density. The modeling program assumes only pure water. In an attempt to circumvent the problem, a reference density corresponding to a 50,000 ppm solution at standard state ( 1.053 gm/cm2) was substituted for the reference density of pure water in one test run. This had no affect on the modeled temperatures, and only a subtle affect on the modeled pressures, mainly in the meteoric zone. In the modeling program, the meteroic zone can not be assigned a separate reference density from the geopressured section. Likewise, viscosity and density subroutines were writen for pure water only. Hence, high ppm pore fluids could not be realistically considered in the study. Additionally, clay dehydration reactions may contribute a significant quantity of fluid at particular horizons. Some simulation runs of the model were conducted using assigned fluid flux nodes in areas of critical temperatures and pressures to simulate such fluid release, but this failed to produce correct temperatures or heads (simulating the process in this way did not take into account the heats of reaction). 
Assessing Thermal CoocJuctiyitu. The model requires the assignment of both a thermal conductivity and porosity field. The thermal conductivity is assigned to the solid portion of each element, and the porosity is therefore used to determine the fraction of the element that is assigned the thermal conductivity of fresh water at the appropriate temperature and pressure. Ulfortunately, there has been very little research into the thermal conductivities of the solid portion of rocks. Instead, there have been studies which list thermal conductivities for typical rock-types. These values are given without regard to porosity, water content, or pressure. Pressure is important because an important factor in the thermal conductivity of the solid matrix is the nature of the grain to grain contacts, which may vary as a function of pressure. Of course, the mineral composition of the sediment grains is also quite important because different minerals have widely different conductivities. Therefore, the thermal conductivity of the solid matrix should be dependant upon rock type. Because of the lack of research in this field, the only guide to thermal conductivities at present are the values for typical rock types. The porosity field modifies these values. 
Limitations of Scale. The mesh and all the output related to the mesh have been printed at a vertical exaggeration of forty. At true scale, the actual cross section represented by the mesh is very wide relative to its depth as shown in Fig. 2.3. Since the parameters in the design of the model are assigned on a per element basis, and the width of each element is at least several kilometers, many details of the cross section were omitted. A finer mesh could have been used to increase resolution, but this would have caused longer run times and an increased complexity in the set up and calibratton of the model. Of course, an important consideration in the design of the mesh was the quality of the data. 

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Generally, most of the loss of detai I was forfeited in the shallow meteoric portions of the basin. The deeper areas are apparently simpler lithologically although there are fewer well-logs available to document this fact. Because of scale, faults were treated as zones rather than as discrete discontiruities, and these zones thus reflect an averaged behavior. Modeled fluid velocities may therefore be less than the actual velocities that may exist in discrete portions of the fault zone. Likewise, much of the anisotropy caused by the small scale interlayering of muds and sands was averaged by assigning anisotropic permeabilies to the grid elements. 
2.3 DESIGN 
2.3.1 CALIBRATION 
Calibrating adjusts the model to accurately simulate the actual system. It involves repeatedly ruming the model, checking the output, making revisions, and then reruming it. In an ideally calibrated model, all of the independent variables are known. The model is adjusted so that these are all accurately reproduced by the model, and the dependent variables are then computed. Such ideal cases are rarely realized. 
The primary calibration tool for this investigation was the temperature data. Other constraints were the stratigraphy and the top of geopressure plus a general knowledge of the shape of the pressure­versus-depth profile. In addition were crude estimates on the magnitude of overall vertical flow from the deep basin (section 2.'1.2). 
The modeling procedure was as follows: 1) Four fields were assigned for vertical and horizontal intrinsic permeability, thermal conductivity, and porosity. For each field a code map was constructed where each element is represented by a coded number which is assigned a value for the particular parameter. 2) Flow rates were assigned to constant flux nodes, keeping the total flux as low as possible. 3) These parameters were then run with the program. 
The output from the model includes plotted isotherms and 
hydraulic heads. The isothermal plot was superimposed on the 
isothermal plots compiled from temperature data and aNJ discrepancies 
were noted. The same was done for the head plot. Adjustments were 
made to the various design aspects on a priority of permeability fields 
first, then if necessary flow rates, followed by conductivities and 
finally porosities. Initially, several parameters were adjusted between 
each run. As the model came closer to meeting the calibration critera, 
only one or two changes were made per run. 
2.3.2 THE MESH 
The mesh (Fig 2.2) corresponds to a cross-sectional width of 176 miles (283 km) and a depth of 20,000 ft (6096 meters). In this program, four-sided polygons are each divided into two triangular elements. All rows and columns of nodes are continuous. A general rule 
. in designing the elements ts to avoid any elements with obtuse angles. For mathematical reasons, obtuse angles will lead to erroneous values and convergence problems. Convergence problems may also result from extreme differences in assigned parameter values in adjacent elements. As a further consideration, to compensate for some of the scale problems mentioned earlier, nodes were concentrated in areas of greatest interest, such as in the growth fault zones. 
2 3 3 THE CODE MAPS 
Porositu Fjeld The data used to code for porosity was mostly taken from Loucks and others ( 1979), Bonham ( 1980) and Fyfe and others ( 1978). In general, porosity was treated as a function of depth, ranging from 35~ at the surface to 5~ at the greatest depths. Additionally, this decline with depth was suspended in the geopressured transition zone. Changes made to the porosity field proved to have very little effect on the modeling results. Porosity is only used in the conduction terms of the heat transfer equation (3), and its low sensitivity seems to indicate that saturated porosity is perhaps not as significant a factor in basinal thermal patterns as has been suggested by Lewis and Rose ( 1970). 
Thermal Conductivitu The thermal conductivity values were assigned using as a guide a table from Reiter and Tovar ( 1982) which lists thermal conductivities for various rock types. The conductivities were assigned to the mesh according to the rock types shown on the type-section. Somewhat lower conductivities were found to be necessary for the deep marine shales than the values listed in the table for shales, but this is justifiable in that much of the marine shale occurring under geopressures has been found to be more like a ·dense 
clay· than Hthified rock (Weaver & Beck, 1971 ). The values chosen were consequently intermediate between shale and clay. Additionally, the deepest marine shales were assigned higher conductivities because they are presumably more dense and consequently more conductive. 
Perroeabiltty. The data presented tn Loucks and others ( 1979) was used for permeabiltty values. This data conststed mostly of whole core analysis plotted against depth. A major draw-back with thts type of measurement is that it tgnores large scale permeabilities created by faults and fractures. These are perhaps more tmportant in determining hydrologtc characteristics of a large area. Additionally, permeabiltty is not only a functton of depth but also of rock type, pressure and chemical reactions. The whole core analyses are relative to atmospheric pressure. Nonetheless, the range of values for each depth was quite great, which provided room for adjustments in the calibration process. Permeability was the most sensitive of the input parameters. 
A matter of some speculation ts the contribution to permeability made by hydraulic fracturing, also known as mircofracturing. According to Fyfe and others ( 1978), microfractures are theorized to originate in flaws, which grow when pore-fluid pressure exceeds the least principal stress by an amount equal to the tensile strength of the rock. The stresses on rock can be resolved into three vectors, one for each dimension, x,y, and z. These are called the principal stresses, the smallest of which is called the least principal stress. In undeformed rock these stresses are usually compressional. Pore pressures tend to oppose compresstonal stresses equally tn all directions by forcing pore spaces open. When pore pressures exceed the least compressional force by an amount greater than the matrix can tolerate (the tensile strength), the rock ruptures, causing a fracture. Fracturing will occur in the direction perpendicular to the least principal stress. In a compacting basin the least principal stress is usually horizontal, whfle the greatest principal stress, resulting from the weight of sediments above, is vertical. Microfractures are usually oriented vertically (Jaeger & Cook, 1979). Stronger rocks are more susceptible because they tend to have greater stress differentials (the difference between least and greatest principal stresses). The strongest rocks should be those in the deeper basin, owing to their degree of consolidation. On the other hand, stress differentials decrease with depth. How these opposing factors control the occurence of hydrofacturing is currently unstudied, but faulted areas may be particularly susceptible owing to an abundance of suitably oriented flaws. 
2.4 RESULTS 
The investigation was broken down into three simulations, each testing a basic type of flow regime. The first considered the affects of evenly dispersed advection while the second concentrated the advecting fluids along faults. The third was a special case of the second, adding a speculative region of high thermal and hydrau1ic conductivity in order to more closely meet the constraints. 
Several criteria were employed to calibrate the model. They were fluid flux, fluid pressure, and temperature. The degree to which model output matches the calibrating critera is a measure of how well the design of the model depicts the actual system. The same criteria where used for each simulation, and the following discussion systematically compares them to the model's output. The implications of the results are covered in the discussion section 2.5. 
2.4.1 SltuLATION ONE -CONDUCTION DOMINATED 
The object of this simulation was to test the hypothesis that thermal patterns are basically controlled by the movement of dispersed (as opposed to fault-concentrated) compactional fluids coupled with geopressure-dominated thermaI conductivities. 
Flux Nodes. Fluid flux nodes were needed to simulate the release of compaction fluids, thus establishing a geopressured zone. These fluxes were evenly distributed across the base of the section. Because fluid fluxes must be assigned to nodes, which are point sources, the basal elements were given artificially high horizontal permeabilities. If this were not done, all nodes, being separated by several kilometers, would produce high pressure plumes. By assigning high horizontal permeabilities to the basal elements, a permeable avenue was created which permitted the simulation of a diffuse upward flow that would be typical of a hydraulically homogeneous compacting basin. Fig. 2.4 shows the flux distribution along the basal boundary. During calibration, very low fluxes were initially assigned. After 
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permeabiHties and thermal conductiv1ties were_optimized, remaining calibration discrepancies were addressed by conservatively incrementing the fluxes. This procedure was repeated until a "best fit" was obtained. The overall average was 8.91x1 o-s kg/s for each meter across the section; the total flux for the entire section being 3.2 x 1Q-3 kg/s. 
Perroeabi1itu Codes Figs. 2.5 through 2.8 show the coded mesh for horizontal and vertical permeability, porosity and thermal conductivity. The permeability fields were kept simple by assuming faults to have no influence. The geopressured zone was assigned the lowest permeabilities, with a rapid increase in permeability at the transition to normal pressures. The southeastern or right portion of the mesh corresponds to the sands of the Frio Formation and consequently higher permeabilities. 
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Porosity Code. The porosity mesh was also simply designed. Porosity decreases from a maximum of 357' at the surface to 57' at 20,000 feet (6096 m). Porosity is held constant at 217' across the pressure transition to geopressuring. Fig. 2.7 shows the coding for the porosity mesh. 

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Thermal Conductivity Code. The Thermal Conductivity mesh is comparatively complex (Fig. 2.8), particularly in the portions above the top of geopressure, because the lithology 1s most variable there. Sandy units typically have higher conductivities than clays and shales (Reiter and Tovar, 1982). Thus, higher conductivity units were assigned in the Frio formation on the right portion of the mesh. The lowest conductivities were assigned to the shallow geopressured section because the least consolidated thickly bedded clays were presumed to occur there. The more unconsolidated the sediments are, the more poorly they conduct heat. An Isolated high conductivity unit was placed In the deep geopressured Wilcox to correspond with a large sand body which is indicated on the type-section. 

Figure 2.8 
2 42 SIMJLAT!ON ONE-RESULTS 
Fluid Flux As mentioned above, the average fluid flux assigned across the geopressured section was 8.91x10-8kg/ms for each meter across the section. An estimate for comparison was provided by Lynton Land (personnel communication, 1985). The estimate is based on the chloride concentration of Gulf Coast rivers and streams whose watersheds do not drain Pennsylvannian or Permian evaporites. Possible sources of chloride in surface waters are aerosols (mostly in the form of rain), halite from evapor1tes, and discharge of deep-basinal brines. The average value for river-borne chloride was 8 grams of chloride per square meter of land surface per year. Of this, only 1.2 grams can be accounted for by aerosols. The 6.8 gram deficit which remains is assumed to be due to the contribution from deep-basinal discharge. 
Figuring the flux assigned in the model provides 2.81 kg or about 2.8 liters per square meter per year, thts implies a chloride concentration in the upwelling deep-basinal fluids of 243 parts per thousand. This is well within the realm of halite saturation which is about 400 parts per thousand at 1 oo·c, and is also very similar to concentrations reported from brines in the Edwards Formation of the basin. This estimate thus provides an indication that the flux rates chosen are quite reasonable. 
On the other hand, a volumetric calculation yields a very different result. Using the same 2.8 kg/ms flow rate, an estimate of the initial height of a one meter square column of compacting sediment needed to produce this flow rate was obtained. Assuming a period of 40 million years and an initial porosity of 35", a column of sediment 320,000 meters high would have to be compacted to 0% porosity to maintain this flow rate. Since the depth of the basin is probably no more than 13,000 meters, the flow rate appears from this calculation to be more than an order a magnitude too high, indicating that.simple compaction is inadequate to account for the postulated flow rate. Bruce ( 1984) claims that the smectite-illite clay transition can supply as much as three times more fluid than compaction in the depth range of 7000-11000 feet (2134-3353 m). However, this is only for a 5X volume reduction from 14%to 9" porosity. Though potentially important, the transition alone does not account for all the fluid needed, nor does is account for fluids sourced from depths greater than 11000 feet (3353m). 
Fluid pressure Fig. 2.9 shows the pressure contours generated by the model. The contours are meters of excess hydraulic head relative 
METERS OF EXCESS HEAD-Trial 1 

to the highest topographic elevation of the section. The contour interval is 200 meters. Since the contours are excess heads, they mark the geopressured zone. The flrst several contours should therefore correspond to the top of geopressuring as indicated by the hatchured line in the cross section of Fig. 1.2. Fig. 2.1 O shows pressure profiles taken along four transects of the section indicated on Fig. 2.9. Here the agreement with other data (shown on the figure) is not good. The pressures modeled at each of the four transects are within reason but are generally low compared to the generalized pressure trends, which are taken from Neogene deposits of South Texas (1 ine 1) and recent to Miocene in Louisiana Cline 2). But missing from the modeled pressures is the characteristic shape of the pressure profile, namely the inflection in the line caused by the transition from increasing pressure gradients at shallow geopressures to a constant pressure gradient at continued depths. The profiles are instead relatively linear, with little variation in the pressure gradient. The pressures therefore can not be considered well calibrated. 
Temperature Fig. 2.11 shows the isotherms produced by the model (dotted lines) superimposed on those from the BHT data (solid line). The gray shaded areas are the error ranges for the BHT data. These were taken from the contoured variances (from Kriging) shown in Figs. 1.6-1. I Od. The match of the 2oo·c isotherm is quite good, but discrepancies increase at higher temperatures, and are especially large between the 3so·c and 4oo·c isotherms. The largest discrepancies 

PRESSURE 
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Figure 2.10: Pressure profiles for Simulation One. Dashed lines show modeled pressure profiles keyed in Figure 2.9. Solid lines 1 & 2 show generalized profiles for Gulf Coast. 
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occur at the Wilcox growth fault zone, where modeled temperatures are much lower than the data indicate. 
Four temperature profiles where constructed from selected transects of Flg. 2.11 and these where superimposed on the temperature profiles from the correspond1ng subareas presented in F1gs. 1.18, 1.14, 1.20, and 1.23. The advantage of th1s comparison 1s the ability to view the actual BHT measurements 1n conjunct1on with the modeled temperatures. F1gs. 2.12 through 2.15 show these prof11es. Once aga1n, the matches are generally poor. In all but the group n1ne area, in fact, modeled temperature gradients are below average, whereas the data show that grad1ents in all areas are above average. 
The Flow Regime. Fig. 2.16 is of the fluid velocity vector field. The arrows in the figure are vectors, meaning that their length is proportional to the fluid veloc1ty at the point of the arrow's origin, and the direction of the arrow indicates the flow direct ion. The direction is corrected to account for the vertical exaggeration of the figure. The vectors are placed at element centers. Since many of the flow rates are extremely low, they appear only as the head of the arrow. Wide differences may still exist between these velocities, though not apparent from the figure. Appendix F Hsts the flow rates for each element. Readily apparent from the figure is the break from geopressured to meteroic regimes. The meterioc system is characterized by much h1gher flow rates as well as more variable, topograph1cally controlled directions. 
MODELED ISOTHERMS-Trial 1 

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' 84 

2.4.3 SltuLAIION TWO -CONCENTRATED FLOW 
Flux Nodes. The second simulation employed areas of concentrated vertical flow to model the basin. The same overall flux used in the first simulation was maintained in Simulation Two, but it was redistributed in such a way as to concentrate most of the flux along the Wilcox growth-fault zone. Fig. 2.17 shows this distribution. 
Permeabi1ilU Codes. Figs. 2.18 and 2.19 show the permeability codes. These are much more complex than in the previous simulation. Relatively high horizontal permeabilities were assigned to the basal row of elements to avoid pressure plumes around each node, but these values were much lower than those used previously in order to avoid widely dispersed fluxes across the basement.(Fig. 2.4). Elsewhere, horizontal permeability was decreased with depth, and in response to the new flux conditions, the horizontal permeability field was refined in the upper geopressured section. Specifically, values were increased in order to disperse the concentrated flux below the pressure transition, a condltion necessary to calibrate the isotherms. The justification for this alteration is that although vertical permeability in the marine shales is certainly very restricted, horizontal permeability can increase near the top of geopressure because of high porosity and a relatively unconsolidated, laminar structure. 


Horizontal 
Permeability 

m2 
07.00x 10-13 
D2.00 x 10-14 
(I s.oo x 10-16 
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Figure 2.18 
The vertical permeability mesh has a different configuration. Its values were assigned as a function of depth except where vertical conduits for flow were hypothesized. Two portions were modeled as such, the deeper parts of the Wi Jcox growth faults, and the geopressured portion of faults in the Catahoula Fm. 
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Porosity & Thermal Conductivity Codes. The porosity field is unchanged from the f1rst stmulatton (Ftg 2.7). Slight modificattoos were made to the thermal-conductivity mesh (Ftg 2.20). The cooducttve sand body to the deep basin was removed, and the elements of least conductivity were redistributed, addtng more in the Wilcox growth-fault zone. These ref1nements were needed to calibrate the model given the new fluid flux conditions, be1ng careful to keep values wtthtn ranges supported by the available data. 

F1gure 2.20 
2.4.4 SIMJLATION TWO-RESULTS. 
Fluid Pressure Fig. 2.21 shows the pressure contours for Simulation Two. Unlike the previous simulation, a plume indicative of concentrated upwelling is apparent in this figure. The .pressure vs. depth profiles derived from this diagram and given in Fig. 2.22 show much better agreement with the two other data sources shown. Line B from the growth fault zone shows near perfect agreement with Dickinson's data, reproducing the characteristic inflection point. The fact that the actual top of geopressure (indicated by the first deviation away from the hydrostatic line) does not match is not significant because Dickinson's data is from a different location, and the depth to the top of geopressuring is variable across the basin. Line D, 
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Figure 2.22: Pressure profiles for Simulation Two. Dashed lines show modeled pressure-profiles keyed in Figure 2.21 . Solid lines 1 & 2 show generalized profiles for Gulf Coast. · 
corresponding to the Frio Formation, shows lower overpressures, as would be expected in an area of higher sand content and permeability. 
Temperature The temperature contours modeled in Simulation Two are shown in Fig. 2.23. The match with the data is better here as well. The modeled isotherms stay within the error margins in most places. Some discrepancies appear along the 350 and 40o•c isotherms just southeast (right) of the Wilcox growth-fault zone, where temperatures are once aga1n somewhat cool relative to the data. This trend is also evident in the temperature-vs.-depth profiles of Figs. 2.24 through 2.27, where the modeled temperatures fall consistently below the general trend indicated by the BHT measurements. No manner of fluid flux could lessen these decrepancies without disrupting the rest of the cross-section. 
The Flow Regime. Fig. 2.28 differs Httle in appearance from Fig. 2.16. In each, the direction and magnitude of fluid movement appear quite similar. However, as previously menttoned, the flow rates are so low in the geopressured zone that differences within thts zone do not show on the diagram. Appendix F lists the velocities from this figure. The highest values for the meteoric zone are on the order of 1 o-a m/s. In the geopressured zone where fluids are concentrated, velocities are about t 0-11 mis, and drop off elsewhere in the geopressured zone to as low as 10-14 mis. 
2.4.5 Slt1JLAIION THREE -MIXED CONDITIONS 
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Simulation Three evolved from Simulation Two after 
successive refinements. The suite of code maps are shown in figs. 2.29 through 2.32. Porosity and fluid fluxes are essentia11y unchanged and the permeabilities are also very similar, excepting the addition of a speculative zone of high thermal and hydraulic conductivity located southeast (right) of the Wi 1cox growth-faults, which was added to simulate the isotherms more closely than in Simulation Two. The differences in the code maps between Simulation Two and Three are centered around the addition of this body. In conjunction, the depth of influence of the Carrizo-associated fault was decreased as indicated in Fig. 2.30. 
2 4.6 SltuLATION THREE -RESULTS 
Fluid Pressure. The fluid pressures are quite similar in this simulation to those from Simulation Two as illustrated in Fig. 2.33. The pressure profiles <Fig. 2.34) are consequently also quite similar and agree we11 with the available data. 
Temperature. Simulation Three produced temperature isotherms which correspond very closely to the data, as seen in Fig. 2.35. The major discrepancies which appeared in Fig. 2.23 from Simulation Two were largely eliminated in this simulation. An even better indication of the success of this simulation are the Temperature-vs.­Depth profiles in Figs. 2.36 through 2.39. The correlation of the model to the data is nearly perfect for all four profiles. 

Figure 2.29 

Figure 2.30 

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The FJow Regime Once again, the fluid velocity vector plot <Fig. 2.40) is nearly identical to the other simu1attons, and is especially similar to simulation two, as would be expected, since conditions governing the basic flow regime were essentially unchanged between simulations Two and Three. Appendix F lists the velocities for each element. 
2.5 DISCUSSION 
As a result of the three simulations, I conclude that dispersed advection coupled with geopressure-dominated conduction ts an inappropriate mode1 for the Gulf Coast Basin of South Texas. Simulation One tested this hypothesis and failed to simulate either the basina1 temperatures or the pressure data. Markedly better results were obtained in Simulation Two where concentrated f1ow was introduced in the growth-faulted zone associated with the Wilcox Group. The third simulation evolved from refinements to Simulation Two and achieved a close match to the calibrating criteria. The major adjustment was the addition of a hypothetical area of high thermal and hydraulfc conductivity placed just coastward of the Wilcox growth faults. 
2.5. 1 IMPLICATIONS OF THE tDOEL Although the digital model cannot provide a unique solution, the simulations do provide insights into the operative geological processes. 
The flux of fluids were all assigned along the basal boundary at a depth of 20,000 feet (6096 m) because the sensitivity analysts showed 
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that this was the best placement of the flux nodes. Compacttonal fluids should be supplied diffusely throughout most of the section, predominantly by consolidating clays and shales, which are abundant above as well as below the basal boundary. The model, however, implies that most compactional fluids are from sediments below the basal boundary at 20,000 feet (6096 m), contradicting a study by Magara ( 1976) which places the maximum cumulative volume of expulsed fluids at about 11,000 feet (3353 m). (Magara calculated this assuming fluid release resulting only from the steady consolidation of a typical Gulf Coast sediment-pile.) Furthermore, not only were the fluxes sourced from the basal boundary, but in Simulations Two and Three, the fluxes were also concentrated along the boundary under the growth faults, implying that not only are the fluids supplied from great depths, but that they have been focussed at these depths. 
The treatment of fault permeabil1tes opens other avenues of speculation. The deepest portion of the Wilcox growth fault zone was assigned higher vertical permeability ( 1.0 x 10-18 m2) than the surrounding rock. At intermediate depths still within geopressure, the higher permeabilities were discontinued. In a test simulation without this termination, fluids escaped the geopressured zone, leaving a large temperature plume penetrating the meteoric zone, with little geopressuring left at depth. The configuration presented thus supports 
the premise that faults leak fluid, but do not do so along their entire 
length. How faults might become sealed at intermediate depths ts open 
to speculation. Perhaps the shales become more consolidated and more brittle at depth, healing the faults more easily at intermediate depths, but leaving the faults open further below. There might also be greater fault movement in the deep basin. Finally, there is an unassessed potential for hydraulic fracturing. The fault zone may be particularly susceptible to mtcrofracturing because of the existing faults and associated structural flaws. Furthermore, since the occurrence of mtcrofracturing is dependent on high fluid pressure, suitable conditions may exist at greater depths. In short, it is not difficult to formulate several ways in which the configuration of the growth fault zone modeled in Simulation Two and Three might be produced in nature. 
Shallower faults in the Catahoula Formation were modeled in a similar way, with higher permeabilities terminated just below the top of geopressure. Uranium deposits in the meteoric portions of these faults, similar to those studied by Galloway ( 1982), indicate that pulses of fluid have periodically moved up these faults. Therefore, probably during periods of fault movement, higher permeability did extend up through the top of geopressure. This was apparently a temporary situation. The faults may have become plugged near the geopressure boundary, as configured. Causes could be rapid cementation or the fast healing of poorly consolidated sediments, especially aided by high differential stresses at these shallow depths. W. E. Galloway (personal communication, 1985) states that there ts little indication, at least at shallow depths, of extensive plugging due to cementation. 
The most puzzling aspect of Simulation Three is the speculation of a zone of high hydrau11c and thermal conductiviy. Despite 
that fact that the temperature contours most closely linked to this hypothesis also exhibit the largest standard deviations, comparison with the data points plotted on the temperature-vs-depth profiles argue persuasively that the temperature trends are real and that Simulation Three offers a posstlbe solution to the temperature distribution. This region, if it exists, could best be explained by the presence of salt diapirs, the salt itself being virtually impermeable but of high thermal conductivity, while the diapirism can lead to overlying faulting and good vertical permeability. S. Seni and W. Mullican (personal communication, 
1985) confirm that salt is present in this portion of the basin at the depths corresponding to the hypothetical zone. This salt may be in the form of salt pillows at various stages of maturity, and perhaps also diapiric structures. Several shallower salt structures in the form of salt domes have been identified in the region, including the Moca Dome, the Palangana Dome, and the Gyp Hill Dome, although W. E. Galloway (personal communication, 1985) suggests that the overall presence of salt in this region may not be very extensive. 
Thus far, we have assumed that the model ts useful tn providing insights into the processes within the study area. However, unknowns preclude a unique solution. One of these is the problem of fluid flux. The estimate using chloride concentrations shows that the fluxes modeled are reasonable for present day conditions. However, these values are not volumetrically possible if they have been maintained over the history of the basin. They are in fact, more than an order of magnitude too large for this. Other flow estimates have been made based on various observations such as the volume of cementation in the basin (Land, 1984, Table 2). These estimates have consistently been above flow rates that are volumetrically reasonable. ~simulation adds one more high estimate to the pile. 
A host of alternatives can be invoked to explain this discrepancy. One possibility is that the temperature data are seriously skewed. This is unlikely because the data base is large and the consistency of the data is good. Recall from Part One that the correlation coefficients for the thermal profiles were all above 90~. The steady-state assumption of the model is another possible contributing source of error. The flow rates may indeed be correct, but are transient, and have not persisted for a significant geologic period of time. Finally, error may have been introduced in the method employed to simulate compactional fluid flux. In reality, the volume of fluid moving out of the basin as a result of consolidation must be about equal to the volume loss of the consolidating sediments. Since the model does not compact, this inverse relationship does not occur. It is not know how significant this limitation is, but for the purpose of this investigation it was assumed to be insignificant. 
If the flow rates are correct, then perhaps there are other sources for the fluids besides compaction. A source from outside the modeled portion of the basin or from the Cretaceous sediments cannot not be ruled out, nor can the possible occurrence of some type of free convection, in which fluids flow in recirculating cells. Because f!uids recirculate, much more flow can be generated for a given volume of fluid. 
Convection ce11s might occur on a sma11 scale, such as with1n a local sediment package or sand-body, or they might also exist on a much grander scale, where faults function as the vertical portion of the ce11, and horizontal bedding planes and cross-bedding flow function to complete the cycle. Descending legs of the ce11s may be located off­shore and also northwest of the cross section, in the sha11ower Cretaceous. 
A 11mitation of the model is the inability to account for the dependence of fluid density on dissolved chemical species. The model uses pure water as the fluid. But the deep-basina1 brines may be more dense than pure water and would therefore require greater fluxes or other forces to concentrate them into upwe11ing plumes. However, tf fluids released by consolidating clays are fresher than these brines, (Kharaka and others, 1980; Price, 1976; Russe11, 1971 ), then these fluids would also be less dense than the brines. Consequently, upon release, if mixing were 11mited, these fluids would be buoyed upw_ard, creating upwelling plumes of fluids where conditions were appropriate, and requiring less fluid flux from below to drive the flow. In this way, a sufficient upward flow could be sustained to account for the temperature distribution while requiring sma11er overa11 fluid fluxes. Such an explanation would unfortunately unbalance the chloride concentration calculation. 
Clearly, much work remains in deciphering the hydraulic and thermal regimes of the Gulf Coast Basin. This research has hopefully provided a spring-board for further research and insight into the complex 
nature of this system. 
CONCLUSIONS 
Having compiled and assembled sufficient data to characterize the thermal distributions in a portion of the Tertiary rocks of the South Texas Gulf Coast Basin, it is evident that regional-scale processes are at work modifying the heat flux above the Cretaceous boundary. The most prominent feature of the temperature distributions is an arc­shaped region of high temperatures which correspond to the growth fault zone of the Wilcox Group. The anomaly begins to emerge at 10,000 feet (3048m) and becomes increasingly pronounced toward 20,000 feet (6096m), beyond which depth there are no data. Although high porosities associated with geopressures have been linked to lower thermal conductivities and higher geothermal gradients, this mechanism does not explain why the temperatures and gradients are highest in the faults zones, and lower in adjacent areas with similar geopress~res. Instead, the fault zones themselves seem to be important, perhaps serving as conduits for vertical flow. The configuration of the thermal 
t t 0 
I ti 
ridge implies upwelling from below the 20,000 foot (6096m) extent of data. 
This largely empirical method of deciphering the cause for the observed temperatures is limited because of the complexity of the problem. It is complex because many factors can influence temperature, including the nature of the heat source, thermal properties of the sediments, the thermal properties of the fluids which saturate the sediments, the hydraulic properties of the entire system through which the fluids move and advect heat, and the chemical behavior and interaction of the sediments and the fluids. Numeric modeling provides a way of accounting for these factors in a coordinated and quantitative way. 
The modeling effort provided additional support for the hypothesis that upwelling fluids are the major cause of the thermal anomaly in the Wilcox trend. For example, it was determined that the optimum placement of flux nodes was along the basal boundary of the model, with the flux concentrated along the Wilcox fault zone. This configuration supports the initial inference that upwelling occurs from below 20,000 feet (6096m), implying in addition, that the flow is focussed at these depths. Permeabilities configured for the model allow flow pathways along the growth fault zone, but only within the deeper portions of the zone. The model calls for a sealing of the fault zone at intermediate depths nearing the top of geopressure. Speculative plugging mechanisms include cementation, differential healing of _faults, differential fault movement and displacement, and depth constrained 
microfacturing. A puzzling aspect of the model is the call for a zone of high hydraulic and thermal conductivity coastward of the deep Wllcox growth faults. This region, if it exists, could be explained by the presence of salt diapirs, the salt itself being virtually impermeable but of high thermal conductivity, while diapirism can lead to faulting and good vert i ca1permeabi Ii ty. 
The model leaves unsolved a problem common to numerous other studies involving fluid movement in the basin. Namely, that the fluid fluxes called for are beyond what can be supplied from compactional processes alone. Studies of dissolution and cementation call for fluxes that are even greater. For this reason, the occurrence of free convection has been suggested. It may occur on both a local and regional scale. Regionally, growth faults may be integrated into the circulation of convection cells, a circulation which would presumably be confined to the compactional system since fluids could not freely convect downward across the geopressure transition. 
There is clearly much work still needed to decipher the hydraulic and thermal regimes of the Gulf Coast Basin. This research has hopefully provided a spring-board for further research and insight into the complex nature of this system. 
APPENDIX A -DATA 
This appendix contains first a complete listing of the names of the well-data base, followed by the file of all the data which is associated with each well. They can be cross referenced using the well number. 
113 

Township Well 
Range No. I IS 21E 26 11S 21E 1 27 I IS 21E 3 28 11S21E9 29 I IS 21E 1 30 I IS 21E 1 31 Cunningham I IS 21E 1 32 11S 22E 3 33 11S 22E 1 34 12S 21E 35 9S 17E 1 36 9S 17E 2 37 9S 17E 3 38 9S 17E 2 39 9S 17E 2 40 9S 18E 7 41 9S 19E 7 42 9S 19E 43 9S 19E 44 9S 19E 7 45 9S 19E 8 46 9S 19E 47 9S 19E 48 9S 19E 6 49 9S 19E 8 50 19S 20E 51 19S 20E 52 19S 20E 53 19S 20E 5 54 19S 20E 8 55 19S 20E 1 56 19S 20E 7 57 19S 20E 7 58 19S 20E 8 59 19S 20E 7 60 19S 20E 5 61 19S 20E 1 62 19S 20E 2 63 19S 20E 8 64 19S 20E 3 65 19S 20E 7 66 !OS 17E 9 67 !OS 17E 7 68 !OS 18E 9 69 !OS 18E 7 70 !OS 18E 6 71 10S 18E 72 
Well Name 
Harkins.•B-1 Fimbel Assoc O&G el a1,• 1van Dohlen Hewitt,• t Baker Plymoulh,• 1 Thompson Hewitt.• t Hall Assic O&G el al, • 1 
Texas O&G,• 1 ·A· Richter Texas O&G.• t Earp Shell,• t-A Bego Plymouth,• t Thompson Slandard,• 1 Rzeppa Standard,•! Moczygemba Mortimer el al,• 1 Dzuik Coastal Slates.• t Kowalik Standard,• t Pollok Standard,• 1 Pace 
Tex Easl. Trans .••! Garbe Tex East. Trans .•• 1 Mugge Tex Easl. Trans.,•2 Voelkel Tex East. Trans .• • 1 Woskow Standard,•! Tipton Mustang,• 1 Vanta Occidental,• 1 OslerIoh el al. Hunt Est..• t Schuenemann 
• 1Flenniken Southland.• t Responder Ranger,• t Clark Tidewater.• t Musselman Hamon,• 1 Roeder Hanson et al .• • 1 Altman Southland,• t Gips McCulloch,• 1 Franke Mo05anlo et al.,• 1 Green Monsanto el al,• t Kolodzeg Monsanto el al.,• 1 Estrella Tidewater.• 1 Korth Harper-Smith,•2 Gips Hamon & Ehman,• t Kleberg Murphy Baxter,• 1 Hilgarlner Untex,• 1 Warwas McCulloch,• 1 Hurst el al. Della Am, • 1 Sahm General Crude,• t Gunewald General Crude.• 1 McDowell Atlantic Ref.,• I Pullin el al. General Crude,• 1 Wessendorff Bruns,• t Tips 
Township Well Range No. Well Neme 
IOS 18E 3 73 Harrison,• 1 Hysaw el al. 
10S 18E 5 74 Hunt,• 1 Huckman 
IOS 19E 9 75 Shell,•1-R Atkinson 1OS t9E 8 76 Hunt,• I Zavesky IOS 19E 2 77 Argo.• I-A Dittmer Est IOS 19E 5 78 Cities,• I Slanchos "A" IOS 19E 6 79 Cilies,• t-A Janssen IOS 19E 5 80 Cilies,• 1-A Pargmann IOS 19E I 81 Kirk & Neeb,• 1 Mueller Est. !OS 19E 1 82 Cilies,• t-A Gaus !OS 19E 7 83 Nat. Explor. Co.,•1 Effenberger 10S 20E 8 84 Continental,•42 Pettus 1OS 20E 6 85 Lone Star.• 1 Jank 10S 20E 3 86 Gelly,• 11 Nordheim !OS 20E 3 87 Southland,•! Fuhrken 9S 13E 4 88 Continental,• t Taylor & Brow 9S 13E 7 89 Corthay Land,• 1 Brite 9S 14E 1 90 Exxon,• t Heinen 9S 14E 3 91 Sorelle & Sorelle,• 1 Heinen 9S 14E 7 92 Smith,• 1 Westland 9S 16E 6 93 Seaboard,•2 Gabrysch 9S 16E 2 94 Coloma,•2 Dzuik 9S 16E 95 Seaboard-Hamon,•! Szalwinski 9S 16E 8 96 Viking,• 1 Clark 9S 16E 97 Renwar et at.,• t Franklin 10S 15E 6 98 Burnwe11.• 1 Pfiel 1OS 15E 7 99 Harkins.• 1 Zunker 1OS 1SE 4 100 Continental,• 1 Slienle !OS 16E 101 Filon.•1 Slurcken 1OS 16E 8 102 Hundt,• t -Hardt 11S 13E 9 103 Dougherly,•t Henry 11 S I SE 1 104 Steward,• t Mcilvaine el al I IS !SE 8 105 Buzzini,• t Seale 12S 13E 8 106 Continental,• 1 Horton 12S 13E 6 107 Tenneco,•! Jamber 12S 14£4 108 Chiles,•! Morril 12S 14E 8 109 Tex Easl.Trans.•t-A Atkinson 12S !SE 4 110 Glasscock,•1 Terrel 12S !SE 7 111 Tenneco,•! Schulz 12S 16E 2 112 Pickens,•! Meyer 12S 16E 8 113 Vreeland,• 1Probst 12S 16E 8 114 Burns,•! Slidde 12S 16E I 115 Shell,•2 Turner 12S 16E I 116 Shell,• I <Nerby 125 16E 7 117 Texas O&G.• 1-c Smith 12S 16E I 118 Shell,• I Leppard 12S 16E I 119 Shell,• I Currer 12S 16E 2 120 Shell,•2 O'Neal 
Township Well Township Wall 
Benge No. Well Neme Benge No. Well Name 12S 16E I 121 Shell,• 1 Turner 14S 15E 3 169 Venus,• 1 Schreiner 12S 16E 8 122 Shell,• I Braune 145 ISE 9 170 Mesa.• I Johnson 12S !IE I 123 Pan Amer,•! Franklin 14S 1SE 1 171 Coastal Sl., • 1 Lukas et al 125 12E 6 124 Colo Oil,• I Roark 14S 1SE 5 172 Atlantic Rich,•2 Richter 125 12E 1 125 Humble.•B-1 Gubbels 14S 15E 1 173 Hanover.• I Fair 125 I 2E 126 5upron, • 1 Henry 14S 15E5 174 Hamon-Carl,•! Kalzfey 9S 9E 127 Magnolia,• I McKinley 14S 15E 5 175 Hamon-Carl,• I Ybaney 95 12E 9 128 Skelly,• I Winkler 145 1SE 6 176 Argo,• 1 Bras I au I OS 9E 5 129 Pan Amer.• 1 Oppenheimer 14S 15E 6 177 Hughes,• I-AW Townsite 10s 1IE 4 130 Gulf,• 1 Reese 145 15E 6 178 Crow-Muslow, • 1 Smith 13S 14E 3 131 Standard,• 1 Calliham 14S 16E 3 179 Pam Amer,• 1 Scogin 13S 14E 1 132 Standard,• 1 Isaacks I 4S 16E 4 180 Hughes-Hughes,•2 Kendall 13S 15E 7 133 Kilroy,•2 McClelland 14S 16E 161 Hanson,•1 Perkins 13S 16E 9 134 Western Nat.,• 1 Harris 145 16E 8 162 Atlanlic,•1 Riser 
13S 16E6 135 Carri,•! Smith 14S 16E 7 163 Atlantic.• I Baker 135 16E 2 136 Peel,• 1 Goebel 14S 16E 6 184 Brown,• 1 Hayes 13S 16E 2 137 Coloma,• I-A Dove 14S 16E 7 165 Smith,•! Cravens 13S 16E 1 138 Hanson el al,• 1 Maguglin 14S 16E 9 185 Abercrombie,• I West el al 13S 16E 6 139 Coastal St,• 1 Morrison 14S 16E 8 187 Pan Am,•1 Randall 13S 16E 1 140 Texas Ol.G,•1 Maguglin 145 16E 3 188 Gulf, •1 Lee 13S 16E 1 141 Sinclair,•3 Dilworth 14S 16E 4 189 Kilroy,•1-A Crocker 13S 16E 9 142 Shoreline.• I Bartlett 155 13E 7 190 Argo,• I-A Edrington Est 13S 16E 4 143 Texas O&G.• 10 McClelland !SS 13E 9 191 Appell.•! Atkinson 13S 16E 8 144 Love el al,• I McMurray 155 13E 5 192 Steward-~igley,• 1 Rhode 13S 16E 6 145 Jones et a1.• 1 Martin 1SS 13E I 193 Mobil,• 1 Wheeler 135 16E 146 Newman,• 1 Edwards 1SS 13E 5 194 Southland el al,• 1 Coron 13S 16E 9 147 Huisache,• 1 Allen 1SS 13E S 195 Peet,• 1 Rhode 135 16E 7 148 Texas Ol.G,•1-A Dunn 15S 14E 6 196 Allanlic,• 1 El Paso Hal 13S 16E 7 149 Continental.• 1 McKinney 1SS 14E 5 197 Hamon,• 1 Dougherrly 13S 16E 4 150 Neumin,• 1 Hinton et al 155 14E 7 198 Coastal Sl, • 1 Lehmberg 135 16E 7 151 Nat. Explo,• 1 McKinney et al 1S5 14E 2 199 Hurl MPS et al,• I Riser 145 14E 8 152 Meeker,• 1 Lebman 155 14E 4 200 Arco.Rhode 5ecl.18 145 14E 9 153 Kilroy.• I Hays-Ezzell 1S5 14E 9 201 Rutherford,•4-A Baker 145 14E 4 154 Texam,• 1 Hays-Ezzell 15S 14E 4 202 Atlantic Rich,•3 Rhodes 145 14E 1 155 Kilroy,•! Herring I SS 14E 6 203 Aninoil. • I Ausa el al 14S 14E I 156 Kilroy,•2 Herring 15S 14E 8 204 Rulherfor,•2-A Baker el al 14S 14E 9 157 Kilroy,•2 Hays-Ezzell I SS 14E 1 205 Davis,•2 Lyne 14S 14E 6 156 Tenneco,• 1 Stephens 1SS14E2 206 Kilroy,•1Petlitetal 14S 1SE 7 159 Getty,• 1 Christenson !SS 14E 1 207 Davis,•3 Lyons 14S 15E 1 160 Pen Oreille,•3 Nelson Tr 15S 15E 2 208 Hanson-Hurl,• 1 Sparkman 14S 15E 7 161 Limes.• 1 Houdmann ISS 15E 4 209 Sohio,•A-2 Slick 14S 15E 6 162 Hanson,• 1 Prosen 15S 15E 6 210 Huber-Manco,•1 Tullis 14S 1SE 6 163 LaGloria,• 1 Bush I SS I SE S 211 Standard,• 1 Burns ­14S 15E 8 164 Kilroy,•! Beirwith 15S 15E 2 212 Stanolind,•1 Sparkman 14S 1SE 9 165 Atlantic Rich,• 12 Lyne 1SS 1SE S 213 Tidewater.• 1 Burns 14S 15E 6 166 So Petro,• I West 15S 1SE 8 214 Placid,• I Patterson 14S 15E 9 167 Warren,• 1 Whitley-Johnson 1SS !SE 8 21S Tenneco,•1 Jones 14S 15E 3 166 Inter. Amer .••2 Herring 1SS !SE 6 216 Cities,•! Bailey 
t t 6 
Township Well Range No.  Well Name  Township Well Range No.  Well Name  
I SS I SE 2  217 Allan lie Ref.• t Burns  11 S 20E 9  265 Callie Land.• 1 Gantt  
15S 15E 9  218 Cilies,• 1-B Hendrick  11 S 20E 9  266 Relco,• t Ganll  
I SS I SE 4  219 Coastal SL,• t Ferrell  12S 17E 3  267 Shell.• I Alvarado el al  
1SS 1SE 2  220 Coastal SL.,•2-A Lennox  125 I 7E 3  268 5hell,• t Ford  
!SS !SE 4  221 Hunt Sands.• I Dolan  t25 17E 7  269 Mosbacker-Cenlury. • I L ylle  
I SS 15E 2  222 McMoran,• t Burns  12S 17E 9  270 South Tex,•t Mckinley  
!SS !SE 9  223 Hamill,• I McClure  12S 17E 3  271 Shell,• 1 Tomasek el al  
15S 15E 9  224 Monsanto,• 1 McCullough  12S 17E 3  272 Shell,• t O'Neal  
!SS ISE 3  22S Austral,• I Lyne  125 17E 7  273 Gasoline,•C-1 Holzmark  
15S 15E 6  226 Hilliard,• I Bailey  125 18E 8  274 Atlantic Rich,•2 Dougherty Est  
1SS I SE 9  227 Katz,•c-1 Slick  I 2S 18E 7  275 Coastal St,• t-A Scott  
15S 15E 4  228 Constantin, • 1 Dolan  125 IBE 2  276 Harris,•2 West Tutela-Hall  
ISS ISE 4  229 Atlantic Ref,•2 Lyne  12S 18E 5  277 Skelly.•2 Hill  
15S 15E 3  230 SRG,• 1 Lyne  125 18E I  278 Hughes et at,•2 McKinney  
I SS I 6E 2  231 Lone Star.• t Walson  125 18E I  279 Tex 0~G,•1-A McKinney  
15S 16E 4  232 Tidewater, }-A Hall Est  125 18E 2  280 Ellsworth-Stapp,• t McKinney  
!SS 16E 4  237 Highland,• I Cocker  125 18E 6  281 Skelly,• I Zook  

15S 16E 3 234 Hanson-McCormick,• I Johnson 12S 18E 2 282 Fly,•2 Ray ISS 16E 8 23S Auslral,•t-A Hinnant 12S 18E I 283 Hughes et al.•3 McKinney 15S 16E 6 236 Anschutz,• I Parker 125 I 8E 6 284 Hanson el al.• 1 Harris ISS 16E 3 237 Daniet,• t Peter et al 12S 19E 3 285 Haring el al.• 1 Ray 11 S 17E 238 MGF,• 1 Zuniga 125 19E 8 286 Coastal St,• I Farish I IS I 7E 239 Apache et al ,B-1 Tips 12S 19E 4 287 Miller,• I Farish 11S 17E 5 240 Shell,•1 Ruhmann 12S 19E 4 288 Tidewater,•! Kidd llSl7E6 241 Spartan,•tTips 125 I 9E 7 289 El Paso et al.• 1 Hardison 11S 18E 5 242 Union,•2 Burnell Spielhagen 125 19E 4 290 Kissinger,•! Kidd I Is 18E 7 243 Union,•84 Ray 125 19E 8 291 Coastal St.• I Farish I IS 18E 7 244 Union,N Pettus Ray7 125 19E 1 292 Coastal SL,•3 McCord 11 S 18E 9 24S Cox-Hering,• t Copeland 12S I 9E 6 293 Coastal St.• 1 McCord 11 S 18E 3 246 Southland,• t Mueller 12S 19E 6 294 Coastal St,•4 McCord 11 S 19E 4 247 Miller-fox,• t Lott 12S 19E2 295 Forest.•! FirstVNllBank I IS 19E 7 248 Amerada,•3 McFadden 12S 19E 3 296 Forest,• I Ray I IS 19E 7 249 Tex East Prod,•! Hall I 2S I 9E 4 297 Magnolia,•2 Irby 11 S 19E 1 250 Haring-Alcoa,• 1 Powell et al 135 I 7E 3 298 Chorchran Zoch,• 1 Lippard 11 S I 9E I 2S I Samedan,• I Berckenhoff 13S I 7E 6 299 Carl,• 1 Gillette 11S 19E 7 252 Amerada,•3 McFadden 135 17E 6 300 Carle,•ITurnbow IIS 19E 4 2S3 Miller-fox,• 1 Loll 13S 17E I 301 Hughes el at,• I Pouloit "A· 115 19E 8 254 Viking,•! Ray Est 135 17E 2 302 Tex Co.,• 1 Ragsdale 11 S I 9E 7 255 Brown,• 1 Pereira 13S I 7E I 303 Hughes et al.• 1 Macdon el al 115 19E 7 256 Coastal St,• 1 McKinney 135 17E I 304 Vikingetat,•t Williams IIS 19E 5 257 Fly.• 1 Key Estate I 3S 17E 3 305 Ci lies,•B-1 Beck 11 S 20E 6 258 Abel &Bancroft.•2 Neese 13S 17E 1 306 N Central et al,• 1 Bomar 11 S 20E 6 259 Abel ~ Bancroft,•2 Ramsey 13S 17E 2 307 Hamon,• I Ragsdale ­I IS 20E 1 260 McCormack,•25 Albrecht 13S 17E 8 308 Argo,• I Huegler 11 S 20E 4 261 Coastal St.• 1 Ussery I 3S I 7E 8 309 Colorado,• 1 Choate 11 S 20E 6 262 Humble,• 1 Neese 13S 17E 5 310 Colorado,•! Tindal 11 S 20E 6 263 Normanly. • 1 Nesse 13S 18E 2 311 Carri-Leahy,• I Littlejohn llS 20E 4 264 General Crude,• I Pettus I 3S I 8E 4 312 Tidewater.• 1 Taylor 
Township Well Township Well 
Range No. Well Name Range No. Well Name 13S 18E 1 313 Coastal.• 1 Scott 16S24E8 361 Amerada.St Tr 191 41 1 13S 18E 3 314 Dougherly el al.• 1 Johnson 16S 24E 2 362 Phillips.• I Pano 13S 18E 8 315 Sunray 0-x.• 1 May 16S 24E 4 363 Chevron.St Tr 125 •1 I3S 18E 8 316 Tamarack.• I Humberson 16S 24£ 1 369 Getty.SL Tr 94 41 1 
13S 18E 3 317 Texaco.•1 Litllejohn 16S 24E I 370 Getty.St Tr 119•1 13S 18E 4 318 Tidewaler,41 1 Taylor 16S24E6 371 Getty.SL Tr 118, 41 1 13S 18E 4 319 Tidewater.•! Aloes I3S 9E 5 372 Gulf,• 1 Naylor g. Jones 13S 18E 9 320 Mitchell el al,•B-1 Robertson 13S 11E 6 373 Exxon,41 13 Dilworth 13S 18E 2 321 Dougherly.• 2 Perez 13S 12E 9 374 Slandard,41 1 Henry 13S 18E 4 322 White Shield,41 1 Marlin 13S 12E 7 375 Pan Am,• 1 McClaugherly I3S I8E 4 323 McCormick.• 1 Littlejohn I 4S 9E 6 376 Phillips,• 1 La Salle 13S 18E 4 324 McCormick,• 1 Kearns 14S 9E 3 377 Pan Am.• 1 Foerster 14S 17E 3 325 Shenandoah.• 1 Good 14S IOE 1 378 Texas 0 g. G.C-1 Washburn 14S 17E 2 326 Pend Oreille,• 1 Womack 14S 1OE 3 379 Sulton.So Tex Syn 41 1 14S 17E 7 327 Humble,•B-9 Thompson I4S 1OE I 380 Pam Am.• t-A Alamo NU Bank I6S I7E 9 328 Max Pray.41 3 Banker 14S I IE 6 381 Amerada,•! Grines 16S 20E 8 329 Morgan,•3 Dodson Van Way 15S I IE 4 382 Phillips,• I-A Nueces 16S 20E 8 330 Morgan,• t Johnson 1SS I2E 6 383 Ridley Wheeler.41 1 Rives I3S 21 E 9 331 Pure Oile.41 1-6 O'Brien 15S 12E 7 384 Tex Co. 41 1 Atkinson 14S 22E 8 332 Kelly-Brock,41 1 Snyder 16S 9E 9 385 Smyth,41 1 Withers I4S 24E 7 333 Cities.•0-1 Tatton 16S !OE 3 386 Texaco.• 1 Canaies 15S 21E 6 334 Cilies,41 1-A Rooke 16S 10E 8 387 Gulf,41 1 Friedrichs 1SS 22E 9 335 4-B Trust,• I Rooke 16S 11 E 1 388 Mid Century,• 1 Hubbend 15S 23E 8 336 Sunray el al,41 1 Hartman 16S 12E 9 389 Allanlic,41 1 Hagist 15S 23E 7 337 Storm.St. Tr. 41 53,41 1 I6S 12E 8 390 Marion.• 1 Heirs 15S 23E 3 338 Conlenenlal,41 34 SL Charles 16S 12E 6 391 Rutherford,41 1 Pursch 15S 23E7 339 Prairie.St Tr 12 41 1 16S 12E I 392 Cox,• I Atkinson 16S 21 E 5 340 Superior,41 27 Welder 16S 12E 9 393 Atlantic Rich,41 44 F~ler 16S 21E 9 341 Smith,41 1 Cage et al I6S 12E 9 394 Arco.•2 Haoisl 16S 21E 8 342 Atlantic Rich,41 1 File 17S SE S 39S Burns Corp,41 1148 Matrix 16S 22E 7 343 Cities,• I Elzner I 7S 7E 1 396 Southwest Petro.• 1 Olmitos 16S 22E 7 344 Fox,• I Wendland I7S 7E 8 397 Mobil,•s Callaghan 16S 22E 7 345 Fox.• I Netek 17S 7E 3 398 Haynes-UT.• 1 Olmitos 16S 22E 8 346 Texaco,41 3 Ritchie 17S 7E 8 399 Southern Un,•4 Williams el al 16S 22E 1 347 Gloria.•A-1 Welder I8S SE 8 400 Lamar Hunt.• 1 Benavides 16S 22E 6 348 Hurl,41 1 Ritchie 18S SE 3 401 Lamar Hunt,41 1 Hachar 16S 22E 9 349 Cherryville,p Sweatt 18S SE 3 402 MGF. 41 2-C Hachar 16S 23E 7 350 Hamon,• 1 Banker Morl 18S 6E 7 403 Mobil,41 1 Gretchen et al 16S 23E 2 351 Cities.St Tr 86 41 1 18S 7E 7 404 Gulf,• 1 Hirsch 16S 23E 8 352 Hunl Trusl,41 65-1 Banker M 1BS 7E 5 405 Sunray Mid,• 1 Lincoln I6S 23E I 353 Aluminum Co.St Tr 84 •2 18S 8E 8 406 Hunt,• 1 Walker 16S 23E 6 354 Shenandoah.St Tr 120 •1 17S 9E 9 407 Dougherty el al,41 1 Nicholson I6S 23E 5 355 Amerada,• t Bankers Mort 17S 9E 6 408 Appell,41 1 Adami 16S 23E 9 356 Graham.el al, Bible •2 17S IOE 5 409 Rowe,•! Hendrickson 16S 23E 6 357 Midwest.St Tr 122,41 1 17S 1OE 1 410 Blair-Vreeland,• 1 Harison 16S 23E 9 358 Amer Petrofina,41 1 Ray el al 17S I IE 9 411 Mobil,41 9 DCRC Sec 80 ­16S 23E 359 Slate Tract 128•1 17S 11E 9 412 Magnolia.41 79 DCRC 16S 24E 6 360 Getty-Mission.St Tr 125•1 17S 11 E 7 413 Marine.• 1 Hahl Weiderkehr 
Township Well 
Range No. Well Name I 7S 11 E 6 414 Horizon.• I Lundell 364 17S 12E 415 Atlantic Rich,• 1 Arco et al 17S 12E 1 416 Texaco.Hugo Slate •1 17S 12E 1 417 Argo,• I Gorman 175 12E 6 41B Ramada.Welder Heirs 2-217 1BS 9E 5 419 McDermott,• A-1 Mclean 1BS 9E 7 420 The Tex Co.•B-1 Moos 18S 9E B 421 Conoco,•2 Hughes est 1BS 12E S 422 5hell,A-3 Weatherby 18S 12E 5 423 Shell,•2 Lloyd 18S 12E S 424 5hell,• 1-B Hubberd 18S 12E 6 425 Shell,• I-A Weatherby 185 12E 6 426 Shell,•2 Weatherby IBS 12E 6 427 Shell,• I Hubberd I BS I 2E 6 42B Socony Mobil.• 1 Weatherby 18S 12E 5 429 Shell.• I Penwell I BS 12E S 430 Shell,• 1-B Hubberd 18S 12E 6 431 Shell,•3Wenecke 
195 SE 4 432 Lamar Hunt.• I Reuthinger 19S SE 3 433 General Crude,• I Ruethinger 195 SE 3 434 General Crude.• 1 Killam-Hurd 19S 7E 9 435 Mobil,B-1 Garza 195 7E 8 436 North Cent.• 1 Webb Co Sehl 19S BE B 437 Delange et al,• I Walker 195 8E 1 438 Forest.• 1 Russel-Winch I 9S BE 5 439 Good Hope.• 1 Carr 20S 6E 2 440 Ginther el al.• 1-A Kill am 20S 6E 6 441 Ginther et al,• I Killam 20S 7E 4 442 Ginther el al.• I Benavides 205 7 E 3 443 Ginther el a1.• 1 Benavides 205 8E 7 444 Bright-Schiff,• 1-24 Atlantic 205 BE 9 445 Good Hope,41 3 Frost Nll Bank 17S 13E 6 446 Pan Am, 41 1-E Farmers Life 17S 13E 6 447 El Paso,•t-B Yates 175 13E S 448 Davis,• 1 Bravo Land 175 13E 3 449 Texas Crude,•! Farmers Life 17S 13E 1 4SO El Paso, 41 2-B Farmers 17515E7 451 Kidd,41 1 Trejo 1B5 13E 3 4S2 Cherryville,• I Reyes 185 15E 2 453 Esunas et al,41 1 Hawkins 1B5 1SE 6 4S4 Howell.• 1 Moos 17S 19E 9 455 Northern Pump,• t Ocker 175 20E 7 4S6 Sinclair.• 1 Doney Jr 175 20E S 457 Renwar,• I Peeks 175 20E 4 4S8 Union,• 1 Parker 17S 20E 7 4S9 Hamon,•B-1 Odem 175 20E 1 460 Trans Cont,• 1 Taft Morrow 175 20E 6 461 Diamond Sham,• 1 Cleo Pianta 
Township Well Range No. Well Name 175 20E B 462 Southern Min,• 1 Griffith 185 1BE 6 463 Southern Min,• t Slone et al 
185 IBE 2 464 Bell el a1.• 1 Franks Est 185 18E 8 465 Hughes et al,41 4 Shulze 1B5 IBE 4 466 Amer Petrofina,•! Kaiser 1BS I BE I 46 7 Gillring, •2 Dix 1BS 1BE 6 468 Dominion,• 1 Charba 18S 19E B 469 Chicago el al,41 1 Lewis 1BS 20E 4 470 Barnsdall.• 1 Merrill 18S 20E 2 471 Gulf,• I Mcgregor 195 9E S 472 5undance.• 1 Frost 195 9E 3 473 Foresl,41 4 Winch-State I 9S I OE 4 47 4 Houston.• 1 Billings 19S IOE 5 475 Rowe,• I Peal Est 195 11E 9 476 Eason,• I Peters Est 195 11 E 9 477 Eason-Harper,• 1-160 Peters 195 12E 1 47B Aluminum,• 1 Hoffman el al 195 12E 1 479 Maguire,• I Braslau 20S IOE B 480 Mobil.41 1 Dinn 20S 1OE 5 481 Hamon,• t Leal 205 IOE 6 482 Morgan,41 3-B Richardson 205 IOE 4 483 Shell,41 1 Benavides 205 I IE B 484 Argo,•A-21 Bennett 20S 11 E 3 48S Amerada,• t Gruy 195 14E S 486 Aluminum.• 1 Oliveira 195 15E 1 487 Delta Gulf,• I Kalinec 20S I 3E 7 488 Hiawatha,•B-1 205 13E 9 489 Morris et al,• I Southland 195 18E 9 490 Hawley,• I Treybig 19S 1BE 3 491 •3 Ingram 19S 18E S 492 <Ntline,• 1 Hoepfner 195 19E 6 493 Atlantic Ref,• I Womack 19S 20E S 494 Midwest,• I Walton 19S 20E 4 495 Hamon,• I Hoepfner 19S 20E S 496 Southern Un,• 1 Bevly 19S 20E 2 497 Hoover,• I Baker 19S 20E 6 498 Sabine,• 1 Doughty 19S 20E 3 499 Fisher-Davidson,• I Klosterman 19S 20E 6 500 lnexco,• 1 Bevly I 9S 20£ 501 Coastal St,• t Cudding Airport 195 20E 9 S02 Anderman et al,41 1 Ocker 19S 20E 3 503 May,• t Merritt 205 17E 1 S04 Champlin, 41 127 Wardner 20S 20E 3 505 Texaco,•5s Loby 20S 20E 7 506 Humble,•39 King Reh 215 SE 507 Gulf,•A-2 Marlin 215 6E S 50B Chevron,• I Marlin 215 7E 9 509 Gulf,•A-10 BMT 
Township Well Township Well Range No. Well Name Range No. Well Name 
21S 7E 9 510 Gulf.•A-11 BMT 225 16E 8 558 Sun,• 1 Wright 
21S 7E 9 511 Gulf,•A-2 BMT 22S 16E 6 559 Sun.•21 Canales 
21 S 7E S12 Northern Natural.• I BMT 21 S I 7E 9 560 Morgan,• 1 Hill 
21SBE9 513 TexEast.•1 BrunieEst 21 S I 7E I 561 Southern Min,• t Werneck 
21 S 8E 8 S14 Skelly.•6 Martin 21S 17E 9 562 Exxon,•A-34 King Reh 
21 S BE 1 515 Gulf,• 1 Villarreal 21 S 17E 6 563 Meeker Haas,• 1 Burris 
22S SE 4 516 Consol O&G et a1.•2 Zachry 21 S 17E 7 564 Meeker Haas.• 1 Conner 
22S 6E 9 517 Chevron,• 1 Briones 21S 17E 3 565 Hurnble.•ME-1 Bornegos 
22S 6E 7 S18 Tex O&G.•4 Hein 21S 18E 7 566 Lone Star.•1 Muil 
22S 6E I 519 Moore et al. •G-1 Hubbard 21S 18E 3 567 Fly,•1 Fisher 
22S 6E S 520 Good Hope,•2 Bruni Reh 21Sl8E5 568 Sun.•1Dietz 
22S 6E B 521 Chevron.• 1 McCann 21 S 19E 9 569 Mokeen,• t May 
22S 6E 7 522 HNG,• 1 Hein Est 215 19E 1 570 Exxon.• 15 King Reh Madero 
22S 6E 6 523 Tex O&G,•E-1 BMT 21S 19E 9 571 Mokeen,•t Salazar 
22S 6E 7 524 El Pason.• I Hein Trust 21519E9 573 Vikingeta1.•1Muil 
22S 7E 3 525 Gulf,•A-11 BMT 21S 20E 3 574 Exxon,•303 Alazon 
22S 7E 2 526 Good Hope,•9 BMT 21S 20E 5 575 Exxon.•308 Alazon 
22S 7E 2 527 Good Hope,• t Saldivar 21S 20£ 3 576 Exxon,•306 Alazon 
225 7E 3 528 Gulf,•A-16 BMT 21S 20E 5 577 Humble.•245 Alazon 
22S 7E 3 529 Gulf,•A-4 BMT 21S 20£ 9 578 Hurnble.•267 Alazon 
225 7E 8 530 Gas Prod,• 1 Bartera 21S 20E 5 579 Humble, •266 Alazon 
22S 7E 2 531 Mobil,• I Bonugli 22S 17E 3 580 Humble,•31 King Reh Canelo 
225 8E 3 532 Coasta1.• 1 Martin et al 22S 18E 7 581 ArkansConroe.•1 Kaufer 
22S 8E 7 533 Superior.• 1 McGrath 22S I8E 4 582 Exxon,•6 Rincon 
215 9E S 534 Pauley.• 1 Laurel Fee 22S 18E 7 583 Arkanxax McKeen.• 1 Womack 
21S 9E 535 Hughes et al ,• I-A Laurel 22S 18E I 584 Hill el a1.• 1 Brookshire 
215 I OE 4 536 McCulloch,• 1 Cuellar et al 22S 18E 6 585 Cities.• 1 Poteet 
21S 10£ 2 537 Brown,•! Benavides 22S 18E 9 586 Hurnble,•4 Rincon 
215 10E 5 538 Getty,•1 Benavides 225 18E 4 587 Exxon,•5 Rincon 
22S 9E 2 539 Coastal St.• t Puig 22S 19E 8 588 Humble,•B-23 East 
22S 9E 3 540 Atlantic Ref.• 1 Puig 22S 19E 8 589 Sun,• I Laguna Olmos 
22S 9E 4 541 Pickens.• t Brunie 22S 19E 4 590 Forest,• 1 Alvarado 
225 9E 4 542 Hamon.• t Ramirez 225 19E 9 591 Davis Chiles.• 1 Koch 
22S 9E 9 543 Atlantic Ref.• A-I Hinnant 225 19E B 592 Hurnble,•B-25 East 
225 9E 2 544 Atlantic Ref,• 1 Garcia 22S 19E 6 593 Carre et al.St Tr 70•1 
22S 9E B 545 Mosbacher,• 1 Fulbright 22S 19£ 3 594 Cilies,• 1 Yaklin 
225 9E 7 546 Austral, •2 Mclean 22S 19E 5 595 Cosden.• I Hubert 
225 9E 7 547 Atlantic Ref,•3 Mclean 22S 19E 7 596 Carril Hawn.St Tr 68•1 
225 9E 7 548 Atlantic Ref,• 1 Stroman 22S 19E 2 597 Pan Am.Cayo Del Grullo 84 • 1 
22S 9E 7 549 Atlantic Rich,•2 Stroman 22S 19E 3 598 McMormick,• t King Rnch 
225 9E 7 550 Austa1.• 1 Mclean 22S 19E 4 599 Arkansas,• 1 Huff 
22S 12E 551 Lone Star.• 1 Miller 22S 19E 2 600 Morgan,• I Matilda Limp 
215 14E 4 552 Jocelyn-varn. • 1 Palacios 22S 19E 9 601 Tex O&G.•1-6 Martin 
21 S I 6E B 553 Sun,• 117 Canales 20S 21E 6 602 King Ranch G-38 
22S 13E 1 554 Harkins.• 1 Leal 20S 21 E 2 603 Marion • I Heirs 
22S 13E 7 555 Tex. Co.•1 Denman 20S 21E 1 604 Mobil •B-9 Chapman 
22S 16E 5 556 Mobil.B-3 Blucher 20S22E 1 605 Humble. ST Tr 173•1 
225 16E 557 Sun.•9 Sullivan 205 22E 6 606 McMoran. ST Tr 171 • 1 
Township Well Township Well Renge No. Well Nnme Renge No. Well Neme 
20S 22E 2 607 Hill, • 1 Richardson 17S 24E 2 655 Skelly, • 1 Schnitz 205 22E 8 608 Am Petrofina, St Tr 169 •2 21 s 22E 2 656 Slnrd, • 1 Dunn Mccampbell 19S 21 E 1 609 Nor Am. • 1 Vision 21S 22E 9 657 Humbel.St Tr 196 •1 195 21E 4 610 Socony Mobil,•1 R~sel 21S21E6 658 Shell.SL Tr206•1 I 9S 21 E 9 611 Morgan Ent, • I Zdansky 21S 21E 8 659 Samedan et al.St Tr 6•1 19S 21E 4 612 Getty, •1 Bevly 2 IS 22E 2 660 Cherryvill,Sl Tr 978-S • 1 19S 21E 9 613 Clinton.Sims 1-VTrust 21 S 22E 2 661 Sun,• 1 Dunn-McCampbell 19S 21E 7 614 Davis,•1 Gwynn 21S 22E 4 662 Sun,•3-A Dunn-McCampbell 19S 21E 3 615 Nor Am. •1 Peterson Prop 21S 22E 6 663 Humble,•3 King Ranch et al 19S 21E 2 616 Hamon, •1 Pulliam 16S 25E 4 664 Hanson.SL Tr 129•1 19S21E2 617 Hamon,•1Sikora 16S 25E 3 665 Sunray, St Tr 96•1 19S 21E 7 618 Heard BOK, Guaranty Nal1 Bk 16S 25E 4 666 Getty, SL Tr 142 •1 19S22E4 619 Mitrchell etal. •1 Nugent 16S 25E 3 667 St Tr 77•1 19S 22E 4 620 Atlantic Ref, • 1 Pearse 16S 25E 4 668 St Tr 143•1 19S 22E 8 621 Coastal St.• 1 Dunn et al 16S 25E 9 669 Exxon.Nine Mi Pt. • 12 19S 22E 2 622 Anadarko.SL Tr 181 •1 16S 25E 3 670 Getty, St Tr 95•1 19S 22E 2 623 Cities, St Tr 96 •2 16S 25E 9 671 Phillips.St Tr 163 • 1 19S 22E 9 624 Marion, • 1 Peterson 15S 25E 4 672 Union,41 15 Tallon 19S22E I 625 Cherryville. St Tr81 •1 15S 25E 4 673 Union,• 16 Tatton 19S 22E 3 626 Stale Tr11cl 88, • 1 15S 25E 6 674 Conlinentat,•46 St Charles 19S 22E 4 627 McMoran. StTr 37•1 12S 25E 5 6 75 Tenneo.• 1 Schultz 19S 22E 3 628 McMor11n, ST Tr 97 •2 9S 21 E 4 6 76 Hanson, • 1 Gips est 19S 22 629 McMoran, St Tr 97•1 9S 21E 4 678 Skelly• 1 Menn 19S 22E 4 630 Coastal St, St Tr 83•1 9S 21E 5 679 Texaco,•2 Broughton 17S21E6 631 Phillips, •IFJinn 9S 21 E 3 680 Musselman.• I Danysh 17S 21 E 7 632 G11l11xy. • 1 Moore 9S21E5 681 Texaco,•1 Feller 17S 21E 7 633 Houston Natrt.• 1 Campbell 9S 21 E 9 682 Lone Star, • I Gips 17S 21 E 7 634 Galaxy. • I Ci lies 9S 21 E 6 683 Brazos,• 1 Sievers 17S 21 E 8 635 Marathon. •2 Kellog 9S 21 E 9 684 Atlantic,• 1 Kerlick 17S 21 E I 636 Hiawatha,• 1 Green esl 9S 21 E 5 685 Houchins •2 17S 22E 7 637 Am Petrofina,• 1 Green Est 9S 21 E I 686 Austral.• 1 Schroeter 17S22E I 638 TerOti.G,Ray "b" •1-A 9S 21 E 2 687 Monsanto El Al.• 1 Boldt 17S 22E 9 639 Republic Natrl. • 1 Floerke 9S 21 E 2 688 <a.iintana. • 1 Jochen 175 22f 4 640 Lawbar, Hunt Dugal •2 9S 21 E 6 689 Hamilton,• 1 Harter 17S 22E I 641 Hamon.•3 Harvey 9S 2 IE 5 690 Monsanto,•3 Kulawik 17S 22E 9 642 Slark • 1 9S 21 E 1 691 Mosbacher,• 1 Spies 17S 23E 1 643 Pennzoil,• 1 Grant 1OS 21 E 1 692 Normandy.• I Fromme 17S 23E 9 644 Midwest, •3 McCampbell I OS 21 E 5 693 Cummings el al.• 1 Urban 175 23E 3 645 Pan Am.• I Banker's Mort IOS 21E 7 694 Houston,•! Fromme 17S 23E 4 646 Hamon Sinclair. • 1 Guettler 1OS 21 E 5 695 Burns,• 1 Norrel 17S 23E 5 647 Getty,•! Mccampbell 11 OS 21 E 3 696 Lone Start.• 1 Dohlmann 17S 23E 8 648 McCampbell • 1-A IOS 2 IE 2 697 Mitchell,• I Dohlman 17S 23E I 649 Bass.,Atlantic-Porterfield I OS 21 E 3 698 Lone Star.• I Haynes 17S 23E 2 650 Tenneco,• 1 Barry Est IOS 21E 3 699 Humble, 412 McMillan 17S 24E 9 651 Mobil.St Tr 284•1 I OS 21 E 6 700 Kirkwood.• t Hoff 17S 24E 9 652 Mobil, SL Tr 310•1 7S 16E 3 701 Sohio,• 1 Southern 17S 24E 9 653 Getty.St Tr 275•1 8S 13E 6 702 Petro Tex. • 1 Garcia 17S 24E 9 654 Tamarack, SL Tr 274 • 1 9S 12E 9 703 Skelly • 1 Winkler · 
Township Well Township Well Range No. Well Nnme Range No. Well Neme IOS IOE 3 704 Slanolind,• I Garcia 165 14E 1 752 Skelly,Weil •A. • 1 
IOS I IE 4 705 Gulf,• I Morris Reese 16S 14E 2 753 Milchell,• 1 Brookshire ISS 7E 2 706 Shell,• I Martin 16S 14E 1 754 Tenneco.• 1 Patterson ISS 7E 6 707 W Artesia Trans. • 1 Koehne 16S 14E6 755 Kilroy, elal,•1 Pesmore 
ISS BE 8 708 Flamingo Vent.et al. • 1 Coquat 165 14E 3 756 Hamon.• 1 Hefner 16S SE I 709 Slampede,•3 Burkholder 16S 14E 3 757 Energy Soures.• 1 Hinnant 16S SE 3 710 Stampede.•6 Dawson 165 14E 2 758 Sanchez-O'Brien,• 1 Jones 16S SE 6 711 Mengden,•1 Carr 16S 16E 3 759 Humble, McCelin • 12 16S 6E 5 712 Mengden.• I Schletze 16S 16E 1 760 Tex O&G,Hinnant •5 17S 6E 6 713 Royal O&G, • 1 Dellano el al 16S 16E 2 761 Hughes g. Hughes.Wilson• I 16S 7E I 714 General Crude.• 1 Miller 165 16E 7 762 Tidewater/Skelly,NoSH-22 14S 7E I 715 Bass,•1 Johnson 14S8E5 716 Stanolind,•1 Cooke 14S8E I 717 Sullons,•1 Hillje 14S BE 4 718 Pan Am.•C-1 Cooke 7S 18E 8 719 Sun,•1 Patton BS 17E 6 720 Morgan.• 1 Pawelek BS 19E 8 721 Geochem Sur,• I Tam Jr BS 19E 3 722 Wiatrek • I es 21E 4 723 Shell,•! Brown BS 21E 6 724 Superior.•! Blackwell BS 21E I 725 Gulf,• I Mueller BS 21 E 7 726 Commonwealth,• 1 Richards as 2 IE 9 121 Shell. • 1 Roehl BS 21 E 7 728 Howell.• I Gansow es 2 IE 7 729 Am Petrofina,• I Boldt BS 21 E 5 730 Highland,• 1 Wood Jr es 21 E 4 731 Esperanza.• 1 Gohmerl es 21 E 5 732 Atlantic,• 1 Smith BS 21 E 9 733 Shell,• 1 Roehl 
16S 13E 9 734 Harkins.Ragsdale Sec 120• 1 16S 13E 7 735 Siegfried,•! Lowe 16S 13E 8 736 MobiI.Labbe Rnch 413 • 1 16S 13E 9 737 Inland Ocian.• 1 Roos 16S 13E 7 738 Pelro-Lewis• 1 Bindewald 16S 13E 6 739 Sunray.• 1 Amer Nat Ins 16S 13E 6 740 Texaco,• 1 Hughes 16S 13E 6 741 Sun Ox,•4 Stella Penn 165 13E 4 742 Harkins.• 1-112 Murphy est 16S 13E 1 743 Atlantic• 1Rhodes 54 16S 13E 5 744 Texaco.•27 Gouyer 16S 14E 1 745 Kilroy el al,• 1 Dunn 16S 14E 3 746 Allantic,•1 Glasscock 16S 14E 9 747 • 1 Eubanks 16S 14E 3 7 48 Centura. • 1 Roos 16S 14E 9 749 Auslral,• 1 Baker 16S 14E 3 750 Argo.• I Dearman 16S 14E 3 751 Allantic,•4 Baker 
Temperature and Elevation Corrected Data-Base 
Each line represents one well. The well numbers are approximately sequential in the order that the file was created. However, some editing of the data was done after numbers were assigned (due to duplicate entries, lack of elevation data, etc.), so certain well numbers are skipped. 
112  UTti COORQINAIES  QEPTUITEtie e61 RS....  
26  3177667.0  646361.1 9219  236  0  0  0  0  0  0  0  0  0  0  
27  3176623.0  655861 .1 9164  250 10900  304  0  0  0  0  0  0  0  0  
26  3176547.0  649312 .5 666 7  246  0  0  0  0  0  0  0  0  0  0  
30  3176406.6  656315.2 9334  244 9965  291  0  0  0  0  0  0  0  0  
31  3177516.5  655821.0 9265  240 10206  264  0  0  0  0  0  0  0  0  
32  3177551 .0  656539.1 6606  241 10296  266  0  0  0  0  0  0  0  0  
33  3176462.4  660931 .6 6619  242 12316  323  0  0  0  0  0  0  0  0  
34  3161243.9  669796.6 6635  241 13100  347 13925  369  0  0  0  0  0  0  
35  3166752.7  647216.9 11243  290 6769  223  0  0  0  0  0  0  0  0  
36  3205702.1  604327.8 10620  268  0  0  0  0  0  0  0  0  0  0  
36  3204547.3  599632.4 11101  262  0  0  0  0  0  0  0  0  0  0  
40  3204069.3  602225.9 10740  261  0  0  0  0  0  0  0  0  0  0  
42  3196193.7  632631.9 9900  237 13687  329  0  0  0  0  0  0  0  0  
43  3199494.9  631792 .8 9355  240 11655  283 13652  326  0  0  0  0  0  0  
44  3200374.2  633968.9 6016  252 14147  350  0  0  0  0  0  0  0  0  
45  3197336.1  630425. 1 9090  226  0  0  0  0  0  0  0  0  0  0  
47  3202246.5  625171 .6 13033  292  0  0  0  0  0  0  0  0  0  0  
49  3201216.0  633440.2 16174  383 16816  344 18178  370  0  0  0  0  0  0  
50  3196612.0  626772.3 12912  316 15594  316 17919  404 20673  432  0  0  0  0  
51  3206560.0  646006.2 9812  241  0  0  0  0  0  0  0  0  0  0  
53  3200137.4  f>411620 .6 9153  215 10150  269  0  0  0  0  0  0  0  0  
54  3202902.3  638338.7 6460  230  0  0  0  0  0  0  0  0  0  0  
56  3205227.2  64271 1.2 9672  249  0  0  0  0  0  0  0  0  0  0  
57  3195754.0  644462.9 9631  233 11609  267 12171  333  0  0  0  0  0  0  
56  3196039.0  643095.9 9759  243  0  0  0  0  0  0  0  0  0  0  
59  3195259.6  640472.3 9716  226 11659  316 12259  330  0  0  0  0  0  0  
60  3199015.1  644453.5 9690  242 12179  333  0  0  0  0  0  0  0  0  
61  3200900.9  641396 .9 8864  228 9829  259  0  0  0  0  0  0  0  0  
62  3206257.7  64460 t. 1 9732  240  0  0  0  0  0  0  0  0  0  0  
63  3204194.4  640225.0 9009  233  0  0  0  0  0  0  0  0  0  0  
64  3196453.2  640635.1 9547  241 10216  264  0  0  0  0  0  0  0  0  
65  3206978.0  636547.3 13474  307 15441  337 16183  373  0  0  0  0  0  0  
66  3196629.7  645602.6 9966  246 11635  312  0  0  0  0  0  0  0  0  
67  3180931 .9  599445.4 8039  200  0  0  0  0  0  0  0  0  0  0  
68  3161523.3  609050 .6 14794  329 15606  362  0  0  0  0  0  0  0  0  
69  3182473.4  609980.3 10722  259 14480  333 15798  383  0  0  0  0  0  0  
70  3164590.0  620736.3 6162  217 9167  246 9442  254 10794  300  0  0  0  0  
71  3168217.7  619105.3 9844  252  0  0  0  0  0  0  0  0  0  0  
72  3167690.2  616602.4 6753  227  0  0  0  0  0  0  0  0  0  0  

~~ ~MCOORDINATES PEPTHnEMP PAIRS.... 
31 591.5 610511. 1 6459 227 0 0 0 0 0 0 0 0 0 0 
74 3165179.6 616367.4 13631 306 0 0 0 0 0 0 0 0 0 0 
75 3161062.5 625726.2 15716 367 17923 414 19207 436 21463 452 0 0 0 0 
76 31B4466.2 625905.5 940B 239 10369 272 12745 339 0 0 0 0 0 O 
n 3191196.2 626647.3 6600 220 9713 247 o o o o o o o o 
7B 31B9997.6 630154.0 B990 242 10540 295 0 0 0 0 0 0 0 0 
79 3169773.5 630656.1 9202 252 10051 270 11370 304 0 0 0 0 0 0 
BO 31B7643.6 628903.3 9254 245 9B26 266 12119 319 0 0 0 0 0 0 
61 3194513.7 631962.6 9374 241 0 0 0 0 0 0 0 0 0 0 
62 3190196.6 631319.5 12247 337 0 0 0 0 0 0 0 0 0 0 
63 3161402.0 632873.0 6616 252 6969 252 9961 262 0 0 0 0 0 0 
B4 31B2122.0. 640803. 1 7326 204 0 0 0 0 0 0 0 0 0 0 
65 3169659.4 643255.6 9756 249 11109 305 13152 352 13643 364 0 0 0 0 
B6 3193157.0 635451 .B 9651 249 10985 267 11626 313 0 0 0 0 0 0 
67 3192759.7 636619.5 9914 242 11697 321 0 0 0 0 0 0 0 0 
BB 32009B2.4 550461. 1 6735 175 7006 254 0 0 0 0 0 0 0 0 
69 3197379.5 560162.6 6102 213 0 0 0 0 0 0 0 0 0 0 
90 3202721.4 563464.5 6936 188 7569 206 7B30 21B 0 0 0 0 0 0 
91 3205672.o 5626n.9 6494 161 6802 166 6656 211 o o o o o o 
92 3194224.2 571601 .3 9130 226 0 0 0 0 0 0 0 0 0 0 
93 3199639.5 595163.4 8050 207 8591 220 9401 231 10146 244 10327 246 10592 272 94 3203800.3 593409 .5 11013 262 0 0 0 0 0 0 0 0 0 0 95 3207720.9 596926.9 9931 253 10342 256 10881 258 11304 265 11445 267 0 0 96 3194420.6 592163.3 10762 256 0 0 0 0 0 0 0 0 0 0 97 3197870.6 592808.0 10680 257 10835 262 11120 269 0 0 0 0 0 0 96 3166303.6 564694.1 10566 240 10942 247 0 0 0 0 0 0 0 0 99 3163972.1 582632.2 10810 272 0 0 0 0 0 100 3186090.6 574043.6 10111 242 11279 273 0 0 0 0 0 0 0 0 101 3181242.4 589766.0 11756 282 0 0 0 0 0 0 0 0 0 0 102 3163125.1 591614.5 7631 206 0 0 0 0 0 0 0 0 0 0 103 3170111.2 549018.3 10137 243 0 0 0 0 0 0 0 0 0 0 104 3175592.3 549018.3 12014 297 0 0 0 0 0 0 0 0 0 0 105 3167266.9 578808.7 7761 208 0 0 0 0 0 0 0 0 0 0 106 3156696.1 552911.5 11816 249 0 0 0 0 0 0 0 0 0 0 107 3159136.0 558521.0 6319 195 0 0 0 0 0 0 0 0 0 0 106 3159735.2 561906.111038 263 0 0 0 0 0 0 0 0 0 0 109 3153183.4 568374.0 7399 212 12543 282 12841 282 0 0 0 0 0 0 110 3158882.0 573225.8 7506 187 0 0 0 0 0 0 0 0 0 0 111 3158060.6 581614.3 8233 218 13134 317 13704 343 0 0 0 0 0 0 112 3164896.0 590526.4 8235 217 0 0 0 0 0 0 0 0 0 0 113 3153733.0 589302.1 6925 206 0 0 0 0 0 0 0 0 0 0 114 3156703.9 591134.66966 206 0 0 0 0 0 0 0 0 0 0 115 3163381.9 593201.1 13843 334 0 0 0 0 0 0 0 0 0 0 116 3164141.1 595761.1 15211 359 0 0 0 0 0 0 0 0 0 0 117 3154198.0 593224.3 7426 210 0 0 0 0 0 0 0 0 0 0 116 3163657.7 593603.9 13844 346 0 0 0 0 0 0 0 0 0 0 119 3163139.1 594417.5 13895 353 0 0 0 0 0 0 0 0 0 0 120 3165319.5 596256.3 13697 329 0 0 0 0 0 0 0 0 0 0 
I~ 121  UTM COORDINATES DEPTHl!~MP f61~.... 3163369.9 593195.3 14110 3 5 0 0 0  0  0  0  0  0  0  0  
122  3155095.9  500172.7 6988  212  0  0  0  0  0  0  0  0  0  0  
123  3163061.6  533221.1 10385  234 13960  303 15097  322 16601  336  0  0  0  0  
124  3158748.1  547124.7 10844  262  0  0  0  0  0  0  0  0  0  0  
125  3163773.5  546354.6 7346  207 6793  213 9669  243 10306  254 10623  261  0  
126  3153383.6  539984.7 10272  262  0  0  0  0  0  0  0  0  0  0  
127  3199115.0  501743.1 9612  246 11020  236 11434  251  0  0  0  0  
128  3195146.6  537211.5 9839  208 14594  299 15061  312  0  0  0  0  0  0  
129  3166466.9  506119.5 9242  231  0  0  0  0  0  0  0  0  0  0  
130  3185210.9  524491 .0 7572  218 8657  246  0  0  0  0  0  0  0  0  
131  3150797.6  563501.2 7314  201 11510  277 11951  271 12024  271 12194  301  
12361  303  
132  3152597.5  569174.7 7284  196 12247  263 12395  301 12573  313 13610  362  0  
133  3139142.1  584843.4 7978  228 8281  232  0  0  0  0  0  0  0  0  
134  3139950.6  566502 .0 6296  211 6575  224  0  0  0  0  0  0  0  0  
135  3141647.2  590931 .0 9008  230  0  0  0  0  0  0  0  0  0  0  
136  3149363.6  593391 . 1 6542  229  0  0  0  0  0  0  0  0  0  0  
137  3148839.7  593392.7 7309  216  0  0  0  0  0  0  0  0  0  0  
136  3150260.4  596291.4 8459  216 10163  246 11144  267  0  0  0  0  0  0  
139  3140528.1  592661 .1 7929  234 9001  240 9392  239  0  0  0  0  0  0  
140  3146666 .6  597314.0 6262  249 6699  255  0  0  0  0  0  0  0  0  
141  3151050.5  596367.0 7448  217  0  0  0  0  0  0  0  0  0  0  
142  3140647.0  567636.9 8412  226  0  0  0  0  0  0  0  0  0  0  
144  3140132.1  590538.2 7803  227 8793  240  0  0  0  0  0  0  0  0  
145  3140662.2  591664.4 7499  212 9040  241  0  0  0  0  0  0  0  0  
146  3144243.1  597229.4 9631  249 10042  292  0  0  0  0  0  0  0  0  
147  3142527.6  569652.9 6905  258  0  0  0  0  0  0  0  0  0  0  
148  3143046.2  595494.0 10649  312 11607  341 13828  348 14610  358  0  0  0  0  
149  3141000.7  597411.9 9743  249 11363  267 13194  332 13616  339  0  0  0  0  
150  3146522.4  587726.6 7623  223  0  0  0  0  0  0  0  0  0  0  
151  3140643.5  596295.0 10367  262 11200  326  0  0  0  0  0  0  0  0  
152  3126331.7  567243.4 7115  206  0  0  0  0  0  0  0  0  0  0  
153  3126140.0  564643.3 6195  225  0  0  0  0  0  0  0  0  0  0  
154  3133455.6  562901.7 7220  212 8224  209 10264  257 13228  342 14763  363  0  
155  3135647.5  572647.9 6200  222  0  0  0  0  0  0  0  0  0  0  
156  3135385.8  572160.2 8163  220  0  0  0  0  0  0  0  0  0  0  
157  3126109.9  564656.3 6166  237  0  0  0  0  0  0  0  0  0  0  
158  3132043.2  572473.2 8313  226  0  0  0  0  0  0  0  0  0  0  
159  3126626.1  564014.6 6606  197 10231  297 11172  310  0  0  0  0  0  0  
160  3134992.5  582259.4 8337  222 11732  291 12730  330  0  0  0  0  0  0  
161  3126567.4  563341.1  6157  237 10619  270 12241  336 13701  356  0  0  0  0  
162  3130907.2  582591.9 7774  215 9165  269 9679  291  0  0  0  0  0  0  
163  3127711.7  576983.7 7535  209 6904  264 9107  266 9750  261  0  0  0  0  
164  3128471.0  580992.5 7584  247 8114  288  0  0  0  0  0  0  0  0  
165  3127715.6  576345 .6 7225  214 9209  269 9710  277  0  0  0  0  0  0  
166  3130874.3  584591 .0 7530  223 8035  230 9232  266  0  0  0  0  0  0  
167  3126963.2  577456.3 7294  197 6222  233 6706  240  0  0  0  0  0  0  
168  3134164.2  575061. 7 7793  222  0  0  0  0  0  0  0  0  0  0  
169  3136248.2  576938.3 6935  206 8383  227  0  0  0  0  0  0  0  0  

ID 170  UTM COORDINATES DEPTH/TEMP PAIRS.... 3126374.3 577534.6 7217 211 9566 271  0  0  0  0  0  0  0  0  
171  3136935.1  583853.4 8307  224  0  0  0  0  0  0  0  0  0  0  
172  3131543.1  579425.5 7721  213 9201  236  0  0  0  0  0  0  0  0  
173  3134555.8  583263.9 7854  219  0  0  0  0  0  0  0  0  0  0  
174  3130316.9  561065.9 7613  223 6350  247 9010  253 9692  269  0  0  0  0  
175  3130020.6  580610.7 7602  226 9236  265  0  0  0  0  0  0  0  0  
176  3132026.0  563671.4 7610  217 6235  237 6344  279 9334  301 9634  301  0  0  
177  3133526.1  585692.2 8158  231 8824  296 9261  262 9706  270  0  0  0  0  
176  3134036.6  565153.9 7750  227 9325  265  0  0  0  0  0  0  0  0  
179  3137327.9  568613.4 9170  272 9202  270  0  0  0  0  0  0  0  0  
160  3132667.3  565669.9 6467  223 9625  261  0  0  0  0  0  0  0  0  
181  3130928. 1  590828.1 8080  234 9882  291 10370  308  0  0  0  0  0  0  
162  3126101.7  592937.1 9263  240 9765  279 10733  271 10629  273  0  0  0  0  
183  3127521.1  594725.1  8885  232 10393  278 11654  293 12197  331  0  0  0  0  
164  3133351.5  597514.9 6552  236 9647  265  0  0  0  0  0  0  0  0  
185  3128191.4  594731.9 7770  213 8996  234 9933  291  0  0  0  0  0  0  
166  3129395.5  587907.4 7652  216 9002  260 9543  271 10201  262 10714  305  0  
187  3128738.2  591653.2 8686  246 9786  291 10800  309  0  0  0  0  0  0  
168  3134929.6  589626.6 6777  230 9925  273 10695  264 11472  297  0  0  0  0  
189  3131496.1  587395.5 6523  219 9803  25410153  292  0  0  0  0  0  0  
190  3113723.6  556600.1 6005  229  0  0  0  0  0  0  0  0  0  0  
191  3112932.6  552200.9 6120  220  0  0  0  0  0  0  0  0  0  0  
192  3116196.6  557027.6 7062  216  0  0  0  0  0  0  0  0  0  0  
193  3124752.3  560702.7 7665  214  0  0  0  0  0  0  0  0  0  0  
194  3116704.6  555693.2 7745  250  0  0  0  0  0  0  0  0  0  0  
195  3117076.0  558237.3 7321  203  0  0  0  0  0  0  0  0  0  0  
196  3116647.0  571197.3 7710  214 11072  303 11790  305 13100  364 14410  371  0  
197  3116046.5  566962.0 7100  207 7849  219  0  0  0  0  0  0  0  0  
196  3112544.2  572601 .3 7722  209 10621  310  0  0  0  0  0  0  0  0  
199  3122639.1  565364.9 7776  260 8253  259  0  0  0  0  0  0  0  0  
200  3116392.0  562039.4 7739  221 10924  297 13574  366  0  0  0  0  0  0  
201  311446.6  564566.5 6777  201 7759  217 8526  260 10067  298 10560  299 11059  
314  
202  3116097.3  562943.2 8020  226  0  0  0  0  0  0  0  0  0  0  
203  3116664.6  572762.6 10123  292  0  0  0  0  0  0  0  0  0  0  
204  3113610.9  565973.0 7487  201 8987  221 9966  294  0  0  0  0  0  0  
205  1.0  1.0 -513  -1  -513  -1  -513  -1  0  0  0  0  0  0  
206  3122999.8  568247.6 7234  229  0  0  0  0  0  0  0  0  0  0  
207  3122449.0  573169.4 7359  212 9976  297  0  0  0  0  0  0  0  0  
208  3122323.9  577891.4 6527  249 10234  295 11838  333  0  0  0  0  0  0  
209  3116540.6  576039.5 6653  230 10306  262 11014  299  0  0  0  0  0  0  
210  3118718.1  582834.9 8550  235 11045  291  0  0  0  0  0  0  0  0  
211  3117459.3  576224.5 6623  225 11165  298 12207  323 14093  379 14445  384  0  
212  3123077.4  577290.4 8669  227 9639  289 10269  303  0  0  0  0  0  0  
213  3119044.7  560694.2 6756  242 9609  260 10486  267 10966  294  0  0  0  0  
214  3113098.3  580689.5 8754  240 10389  282 11545  321 12620  341 13596  375  0  
215  3111570.4  561275.7 9775  256 10627  316 12483  330  0  0  0  0  0  0  
216  3119349.5  584905.3 8587  234 10053  258 11098  312  0  0  0  0  0  0  
217  3122556.9  580860.0 10206  293 11716  295 12394  304  0  0  0  0  0  0  

ID 218  YIM COORDINATES ~~PTHITEMP eAIRS .11 3111722.5 574469.8 9595 281 10737~323 12540  358  0  0  0  0  0  0  
219  3115964.5  576694.6 8665  230 10365  302 11865  337  0  0  0  0  0  0  
220  3123496.9  581489.9 7151  214 7624  222 11505  333  0  0  0  0  0  0  
221  3118823.7  575187.6 8491  231 11620  323  0  0  0  0  0  
222  3121734.6  581065.0 8607  253 11671  321 12867  334  0  0  0  0  0  0  
223  3112711.0  574611.6 8870  255 10311  306 10991  319  0  0  0  0  0  0  
224  3112013.4  574078.2 11293  333  0  0  0  0  0  0  0  0  0  0  
225  3120805.1  575099.4 8579  250 9182  256 9950  290  0  0  0  0  0  0  
226  3117684.2  584778.7 9771  236 12410  327 13692  372  0  0  0  0  0  0  
227  3114903.9  574101.7 8752  242 10290  300 10817  304 11825  332  0  0  0  0  
226  3117630.5  575632.1 8746  244 10442  299  0  0  0  0  0  0  0  0  
229  3119500.6  573849.1  8527  256 8830  252 9086  258 9628  276 10128  274 10236  
286  
230  3124110.9  57526 7 .3 7303  205 9160  247 9766  277  0  0  0  0  0  0  
231  3123191.6  590376.0 7691  219  0  0  0  0  0  0  0  0  0  0  
232  3120092.1  587298.4 7511  203 9589  266 10111  272 11212  295  0  0  0  0  
233  3118948.7  586626.7 7967  230 10676  317  0  0  0  0  0  0  0  0  
234  3123402.3  589783.5 7843  201 11283  318  0  0  0  0  0  0  0  0  
235  3114763.1  592816.7 8901  238 11587  313 12318  337 13031  340 13509  366  
14533  378  
236  3116634.8  595418. 1 7839  225 9751  252 12653 321 13629 353  0  0  0  0  
237  3122715.0  587481.6 7763  202 10618  312 11418  327  0  0  0  0  0  0  
238  3171969.5  606718.5 13391  332  0  0  0  0  0  0  0  0  0  0  
239  3174374.9  607268.1 8002  244 6186  254  0  0  0  0  0  0  0  0  
240  3172611.0  604669 .5 12915  284 13484  361  0  0  0  0  0  0  0  0  
241  3173029.5  609132.6 7610  226  0  0  0  0  0  0  0  0  0  0  
242  3174143.1  617140.3 9076  271  0  0  0  0  0  0  0  0  0  0  
243  3166825.1  618871.3 7663  226  0  0  0  0  0  0  0  0  0  0  
244  3167146.7  618689.3 8259  243 8587  266  0  0  0  0  0  0  0  0  
245  3167308.5  612416.8 7177  203  0  0  0  0  0  0  0  0  0  0  
246  3160316.9  610716.6 8668  270 13277  309  0  0  0  0  0  0  0  0  
247  3175205 .6  622980. I 6975  20 I  0  0  0  0  0  0  0  0  0  0  
248  3170599.3  633974.7 10739  250  0  0  0  0  0  0  0  0  0  0  
249  316935 1.5  632847 .8 7652  217  0  0  0  0  0  0  0  0  0  0  
250  3176634.3  633737.9 8917  236 10323  288  0  0  0  0  0  0  0  0  
251  3180798.7  632688.3 6805  223 9660  270 9975  278  0  0  0  0  0  0  
252  3169914.5  633003.9 8148  221 10739  250  0  0  0  0  0  0  0  0  
253  3175205.5  622974.0 6965  201  0  0  0  0  0  0  0  0  0  0  
254  3167344.2  626985.6 8939  249  0  0  0  0  0  0  0  0  0  0  
255  3170092.2  632257 .8 9017  270  0  0  0  0  0  0  0  0  0  0  
256  3169106.0  630694.4 9130  247  0  0  0  0  0  0  0  0  0  0  
257  3173858.0  628606.2 10161  300  0  0  0  0  0  0  0  0  0  0  
256  3174070.8  645232 .0 9452  269  0  0  0  0  0  0  0  0  0  0  
259  3175231.5  642990.5 6873  286  0  0  0  0  0  0  0  0  0  0  
260  3178118.2  643294.5 9033  239 10693  302  0  0  0  0  0  0  0  0  
261  3176470.3  636208.2 8430  233  0  0  0  0  0  0  0  0  0  0  
262  3174397.7  645093.0 7767  212 8823  274 9272  280 9575  282 9734  261 10244  
287  
263  3173657.1  645683.0 9766  269  0  0  0  0  0  0  0  0  0  0  

ID 264  UTM COORDINATES DEPTH/TEMP PAIRS.... 3172996.3 635746.5 7900 210 8898 252 10995  271  0  0  0  0  0  0  
265  3169615.1  638230.4 9546  275 10100  280  0  0  0  0  0  0  0  0  
266  3170331.7  638475.6 9651  271  0  0  0  0  0  0  0  0  0  0  
267  3164584.2  599783.3 14045  309 14917  343 15624  337 16537  414  0  0  0  0  
268  3165979.2  598945.9 15174  331 15817  406 15974  411  0  0  0  0  0  0  
269  3153496.8  606049.1 7651  212  0  0  0  0  0  0  0  0  0  0  
270  3153292.4  599331.1 7589  227  0  0  0  0  0  0  0  0  0  0  
271  3165384.7  598711.1 13040  348 13985  369 15047  386  0  0  0  0  0  0  
272  3164606.5  597945.9 13417  320 14531  340 15124  389 16033  396 16988  403  0  
273  3153563.1  609368.7 7904  220 9074  265  0  0  0  0  0  0  0  0  
274  1.0  1.0 -441  -1  -441  -1  0  0  0  0  0  0  0  0  
275  3153204.7  619891.6 9660  289  0  0  0  0  0  0  0  0  0  0  
276  3162256. 1  614381.5 8353  245 9601  268  0  0  0  0  0  0  0  0  
277  3158927.1  617502.5 7626  224 8318  267  0  0  0  0  0  0  0  0  
278  3163276.4  619033.7 8073  235 9851  292  0  0  0  0  0  0  0  0  
279  3165012.7  620634.6 7364  219 7680  228 10632  310  0  0  0  0  0  0  
280  3165146.8  617927. 1 8155  239 9750  295  0  0  0  0  0  0  0  0  
261  3158154.3  618385.4 7909  218 8172  249 8824  262  0  0  0  0  0  0  
285  3165434.3  623165.5 8911  216  0  0  0  0  0  0  0  0  0  0  
286  3155337.1  628236.7 6693  248 9903  280 10919  292 11236  309 11516  313  0  
287  3159214.2  626235.2 8268  243 9221  269 10170  292  0  0  0  0  0  0  
288  3159445.4  622395.5 8149  219 8995  258  0  0  0  0  0  0  0  0  
289  3155741.1  633657.9 8799  256 9961  287 10382  306 11305  323  0  0  0  0  
290  3159309.5  624574.9 9880  222  0  0  0  0  0  0  0  0  0  0  
291  3155331.2  628249.0 8692  246 9902  280 10918  292 11235  309 11515  313  0  
292  3162633.2  631803.3 11395  316  0  0  0  0  0  0  0  0  0  0  
294  3162079.2  632245.2 10127  292  0  0  0  0  0  0  0  0  0  0  
295  3163972.4  629366.8 9171  283 9421  279  0  0  0  0  0  0  0  0  
296  3164686.0  625562.1  8826  269  0  0  0  0  0  0  0  0  0  0  
297  3162060.2  637148.7 8995  234 9207  251 9788  263 10524  302  0  0  0  0  
298  3151711.8  599562.4 7510  232  0  0  0  0  0  0  0  0  0  0  
299  3146403.1  609538.8 9675  243 10299  262  0  0  0  0  0  0  0  0  
300  3144760.3  608714.5 9564  279 9934  287 10327  304  0  0  0  0  0  0  
301  3150460.9  606692.1  8585  239 10032  280 11617  313  0  0  0  0  0  0  
302  3150938.5  604476.7 6466  214 9612  279 10118  292  0  0  0  0  0  0  
303  3151036.1  606563.8 9090  24710634  26711218  26411703  325  0  0  0  0  
304  3149147.5  606043.2 8693  246  0  0  0  0  0  0  0  0  0  0  
305  3151091.1  601462.0 8646  224  0  0  0  0  0  0  0  0  0  0  
306  3143388.4  606169.0 8906  249 9762  277 10038  264  0  0  0  0  0  0  
307  3149545.3  602690.2 7427  202 8452  229  0  0  0  0  0  0  0  0  
308  3142234.9  604112.6 8403  245 9515  281 10026  283 10500  287  0  0  0  0  
309  3141070.7  602699.8 10004  256  0  0  0  0  0  0  0  0  0  0  
310  3144725.9  603263.5 9143  278  0  0  0  0  0  0  0  0  0  0  
311  3151293.6  614446.6 10161  267  0  0  0  0  0  0  0  0  0  0  
312  3146334.7  614007.7 9084  242 10827  293 11883  348  0  0  0  0  0  0  
313  3152090.5  620210.4 8187  227 9566  281 9984  294  0  0  0  0  0  0  
314  3151184.8  612954.5 8543  226 9607  293 10226  300 10610  309  0  0  0  0  
315  3141700.9  617941.9 9700  258 10310  290 10640  305 11162  3  
316  3143578.8  616068.0 6750  246 10440  295 10629  312  0  0  0  0  0  0  

\28 

~~7  UTti COORQl~H~ ~~~HIT~tiP Pt!IRS.... 31495742 6143 7.4 9<Y6 250 0 0 0  6  0  0  0  0  0  0  
316  3146363.1  613966.9 9065  242 10620  293 11679  346  0  0  0  0  0  0  
319  3146005.6  612376.6 9026  232 10093  274 10913  292 10959  293 11647  327  
11925  339  
320  3141573.4  610270 .0 9722  261 10704 300  0  0  0  0  0  0  0  0  
321  3149365.5  614797. 1 10 127  262 11497  331 11922  346  0  0  0  0  0  0  
322  3147293.8  61195b6.5 9936 264 10189 308  0  0  0  0  0  0  0  0  
323  3147226.9  610919.3 10116  268  0  0  0  0  0  0  0  0  0  0  
324  3146183.6  613554.2 10010  262  0  0  0  0  0  0  0  0  0  0  
325  3136184.7  600220.3 10129  262  0  0  0  0  0  0  0  0  0  0  
326  3138850.3  602307.3 103"46  262  0  0  0  0  0  0  0  0  0  0  
327  3127470.3  644451.6 5883  190  0  0  0  0  0  0  0  0  0  0  
328  3097920 .8  601046.0 7400  207  0  0  0  0  0  0  0  0  0  0  
329  3101577.1  642244.8 7650  194  0  0  0  0  0  0  0  0  0  0  
330  3101505 .4  641039.2 7924  198  0  0  0  0  0  0  0  0  0  0  
331  3139980.6  646027.4 11687  265 14274  353 16213  364  0  0  0  0  0  0  
332  3126250.5  665199.7 6961  210  0  0  0  0  0  0  0  0  0  0  
333  3127752.4  695443.6 6400  199 9078  206 9569  216  0  0  0  0  0  0  
334  3117404.9  657456.1  7971  201  0  0  0  0  0  0  0  0  0  0  
335  3113962.2  661286.5 8460  202  0  0  0  0  0  0  0  0  0  0  
336  3114345.1  676840.7 6031  198 8971  208  0  0  0  0  0  0  0  0  
337  3112958.6  661620.4 9000  219  0  0  0  0  0  0  0  0  0  0  
336  3123604.8  685364.9 8707  215 9792  226 11108  259 11937  240 12576  249 13109  
297  
339  3117032.9  693444.8 8666  214  0  0  0  0  0  0  0  0  0  0  
340  3107094.2  653176.5 6570  234 11466  279 13461  296 15457  326 16627  364  
17142  376  
341  3096326.5  650707. 1 6454  215  0  0  0  0  0  0  0  0  0  0  
342  3098431.1  653946.4 9391  240 11112  276  0  0  0  0  0  0  0  0  
343  3099146.7  667566.0 7716  194 9956  219  0  0  0  0  0  0  0  0  
344  3098610.6  670395.2 10167  230  0  0  0  0  0  0  0  0  0  0  
345  3098610.4  669979.6 9980  229  0  0  0  0  0  0  0  0  0  0  
346  3100108.7  664222.4 9321  225 9694  231  0  0  0  0  0  0  0  0  
347  3107454.3  669618.5 6989  210 9183  216  0  0  0  0  0  0  0  0  
3"46  3105751.1  668517 .5 7680  209 8757  215 8984  219  0  0  0  0  0  0  
349  3099900.5  662362.1  9193  215 9475  220  0  0  0  0  0  0  0  0  
350  3101154.7  661013.6 9135  215 11500  273 12140  263  0  0  0  0  0  0  
351  3108766.3  6 76948. 1 9232  206  0  0  0  0  0  0  0  0  0  0  
352  3102449.5  677759.4 9380  215 10485  250  0  0  0  0  0  0  0  0  
353  3109636.2  660320 .6 9644  222 9982  229  0  0  0  0  0  0  0  0  
354  3104569.3  679733.7 10009  211 10116  215 10328  251  0  0  0  0  0  0  
355  3103330.9  678266.4 9042  208 10251  221 11996  261  0  0  0  0  0  0  
356  3103137.0  673779.3 8411  222 9057  237 9469  241  0  0  0  0  0  0  
357  3104646.5  6814072 6807  211 9027  216 10666  260  0  0  0  0  0  0  
358  3100010.8  672988.7 9990  249  0  0  0  0  0  0  0  0  0  0  
359  3103696.2  661505.7 6752  225 10567  245  0  0  0  0  0  0  0  0  
360  3106562.6  694751.5 9060  204 9814  215  0  0  0  0  0  0  0  0  
361  3099161.6  691145.6 8422  201 9461  215 11021  237  0  0  0  0  0  0  
362  3111898.4  690465.5 8995  215 10878  246 12479  265  0  0  0  0  0  0  

ID 363  UTM COORDINATES DEPTH/TEMP PAIRS.... 3104760.6 664066.2 9034 206 12324 266  0  0  0  0  0  0  0  0  
364  3109754.5  695764.4 9069  210 11379  268  0  0  0  0  0  0  0  0  
365  1.0  1.0  -21  -1  -21  -1  0  0  0  0  0  0  0  0  
366  1.0  1.0  -21  -1  -21  -1  0  0  0  0  0  0  0  0  
367  1.0  1.0  -21  -1  -21  -1  0  0  0  0  0  0  0  0  
368  1.0  1.0  -21  -1  -21  -1  0  0  0  0  0  0  0  0  
369  1.0  1.0  -21  -1  -21  -1  0  0  0  0  0  0  0  0  
370  3108382.2  695037.9 9056  219 10447  256 10918  270  0  0  0  0  0  0  
371  3108569.9  696040 .8 9176  220 11808  268  0  0  0  0  0  0  0  0  
372  3144552.5  505813.6 7920  203 10578  242  0  0  0  0  0  0  0  0  
373  3144945.4  533340.2 11617  297 13326  324 14217  346  0  0  0  0  0  0  
374  3141493.9  537278.6 11125  255 11261  250  0  0  0  0  0  0  0  0  
375  3140475.1  547726.4 11733  303  0  0  0  0  0  0  0  0  0  0  
376  3132261.9  510950.0 9539  241 11586  271  0  0  0  0  0  0  0  0  
377  3134326.4  503469.9 6795  297 11210  304 12356  366 13220  341 16267  377  
17262  395  
378  3135182.6  522216.9 16572  326 16374 399 20124  424  0  0  0  0  0  0  
379  3138194.4  513461.3 10344  238  0  0  0  0  0  0  0  0  0  0  
381  3133944.6  532769. 1 13557  303 14561  362  0  0  0  0  0  0  0  0  
382  3119135.0  524606.3 7327  205 12273  281 14915  313 17372  343 20746  413  
23937  452  
383  3117932.8  546185.9 8156  227  0  0  0  0  0  0  0  0  0  0  
364  3113012.3  545421.5 7601  207  0  0  0  0  0  0  0  0  0  0  
385  3100124.8  500166.5 6130  198  0  0  0  0  0  0  0  0  0  0  
386  3107292.1  513950.2 7712  208 16626  342  0  0  0  0  0  0  0  0  
387  3100721.1  519468.4 9031  240 15136  368 15448  405  0  0  0  0  0  0  
386  3107094.8  533126.4 7703  197  0  0  0  0  0  0  0  0  0  0  
389  3101094.4  539628. 7 9049  217 9549  279  0  0  0  0  0  0  0  0  
390  3097179.5  542113.2 7522  217  0  0  0  0  0  0  0  0  0  0  
391  3103091.0  549024.6 8354  246 10406  302 10907  314 11385  327  0  0  0  0  
392  3107344.0  547252.9 8178  224 8994  241  0  0  0  0  0  0  0  0  
393  3099061.9  539422.0 7868  214 9870  290 10968  295  0  0  0  0  0  0  
394  3101425.7  540140.1 9572  280  0  0  0  0  0  0  0  0  0  0  
395  3088406.3  458107.4 7921  219  0  0  0  0  0  0  0  0  0  0  
396  3096639.9  464730 .0 8639  230 9023  232 9405  237  0  0  0  0  0  0  
397  3087825.8  463311.3 656 7  195  0  0  0  0  0  0  0  0  0  0  
396  3093120.7  492019.0 6770  196  0  0  0  0  0  0  0  0  0  0  
399  3084194.8  494285.1 7462  223  0  0  0  0  0  0  0  0  0  0  
400  3072431 .2  455681.2 12486  274 14279  369  0  0  0  0  0  0  0  0  
401  3081822.9  454480.3 11786  277 13555  330 14628  334  0  0  0  0  0  0  
402  3081615.2  454869.0 8465  232  0  0  0  0  0  0  0  0  0  0  
403  3071451.8  474529.7 6459  195 6837  201  0  0  0  0  0  0  0  0  
404  3072069.5  486303.7 7441  214  0  0  0  0  0  0  0  0  0  0  
405  3076104.9  487322.3 8248  212 9032  224  0  0  0  0  0  0  0  0  
406  3072280.9  492281 .6 9662  256 13300  322 14090  342 17360  403 18520  437  
20055  459  
407  3087274.1  500151.9 7144  206  0  0  0  0  0  0  0  0  0  0  
408  3090578.0  510169.8 7103  204  0  0  0  0  0  0  0  0  0  0  
409  3092037.4  517017. 1 6637  208  0  0  0  0  0  0  

ID 410  UTM COORDINATES DEPTH/TEMP PAIRS.... 3093296.4 520945.6 5777 204 0 0 0  0  0  0  0  0  0  0  
411  3085741.3  528048.9 7717  219 10467  298  0  0  0  0  0  0  0  0  
412  3084824.1  528273.5 7489  202 8959  251  0  0  0  0  0  0  0  0  
413  3085355.0  535497.7 7348  197 7510  206 9569  241 9700  248  0  0  0  0  
414  3091738.1  533730.9 8111  225 8655  258  0  0  0  0  0  0  0  0  
415  3096796.1  548057.4 8520  248 10065  297  0  0  0  0  0  0  0  0  
416  3093238.3  546260 .2 8485  221  0  0  0  0  0  0  0  0  0  0  
417  3095001.9  548141 .4 8857  269  0  0  0  0  0  0  0  0  0  0  
418  3091719.8  545661.1 6316  260  0  0  0  0  0  0  0  0  0  0  
419  3076905.3  507740.8 7125  199  0  0  0  0  0  0  0  0  0  0  
420  3070891.9  510284.1  7111  215 7395  219  0  0  0  0  0  0  0  0  
421  3071623.8  504621.8 6013  209 10515  287  0  0  0  0  0  0  0  0  
422  3077077.3  544607.7 8099  247 9655  260 13645  376  0  0  0  0  0  0  
423  3076493.1  542791 .5 7990  247 9694  298 13294  376  0  0  0  0  0  0  
424  3077622.3  544396.7 6411  250 10414  326 11061  337 12387  367  0  0  0  0  
425  3078001 .9  545787.6 8299  249 11147  317 11948  372 13400  401 14323  414  
15415  439  
426  3076316.6  546096.0 6466  252 9466  267  0  0  0  0  0  0  0  0  
427  3075906.6  545380.6 8442  244 8899  277 9447  295  0  0  0  0  0  0  
426  3075803.9  546482.4 6602  276 9065  281 9361  287  0  0  0  0  0  0  
429  3078026.8  542903.8 9119  230 11069  337 12349  368 12881  383 13274  383  0  
430  3077689.2  544390 .2 8425  250 10398  326 11045  337 12373  367  0  0  0  0  
431  3074181 .6  545835.3 7654  229 10020  306 14631  409  0  0  0  0  0  0  
432  3063536.9  453624.7 12536  288  0  0  0  0  0  0  0  0  0  0  
433  3064689.3  454767.7 8936  232  0  0  0  0  0  0  0  0  0  0  
434  3056498.9  455074.0 9152  225  0  0  0  0  0  0  0  0  0  0  
435  3057797.1  476666.1 9212  260  0  0  0  0  0  0  0  0  0  0  
436  3058535.3  482881.0 7650  232 8748  256  0  0  0  0  0  0  0  0  
437  3059710.4  492140 .5 7326  201  0  0  0  0  0  0  0  0  0  0  
438  3066942.8  499776.6 7486  216 9285  277 9832  291  0  0  0  0  0  0  
439  3064491 .4  494565.9 7428  207 10462  237 10467  266  0  0  0  0  0  0  
440  3052507.1  470702.0 7328  210 9070  245 10647  266 11608  277 13140  314  0  
441  3050633.5  472270.1 7379  214 10421  268 12412  308  0  0  0  0  0  0  
442  3049126.9  476948.7 7023  220  0  0  0  0  0  0  0  0  0  0  
443  3054017.5  477829 .2 7927  22 t  0  0  0  0  0  0  0  0  0  0  
444  3045008.0  499617.6 6783  216  0  0  0  0  0  0  0  0  0  0  
445  3044392.8  491212.7 7106  21 1 10517  303  0  0  0  0  0  0  0  0  
446  3089863.8  557919.5 7919  214 9469  275  0  0  0  0  0  0  0  0  
447  3092013.1  556644.8 8756  250 9487  296 9600  302  0  0  0  0  0  0  
448  3069345.3  5547332  9014  236 9668  302  0  0  0  0  0  0  0  0  
449  3096708.7  550364.2 877 1  228  0  0  0  0  0  0  0  0  0  0  
450  3092981 .1  559308. 7 8050  291 9005  287 9500  291 9636  292  0  0  0  0  
451  3087740.6  583209.5 6703  195  0  0  0  0  0  0  0  0  0  0  
452  3081731.3  551215.5 8355  250 9230  279 9993  305  0  0  0  0  0  0  
453  3080694.5  578229.0 6470  195  0  0  0  0  0  0  0  0  0  0  
454  3077197.1  584977.6 7116  212 7888  238  0  0  0  0  0  0  0  0  
455  3091223.5  629616.0 7646  199  0  0  0  0  0  0  0  0  0  0  
456  3085955.5  647405.4 9926  223  0  0  0  0  0  0  0  0  0  0  
457  3091378.5  639370.6 8958  210  0  0  0  0  0  0  0  0  0  0  

ID 458  UTM COORDINATES DEPTH/TEMP PAI RS.... 3068934.9 63626 7 .3 8250 204 8907 215  0  0  0  0  0  0  0  0  
459  3085011.7  646035.2 9773  215 10303  221  0  0  0  0  0  0  0  0  
460  3097412.7  646726.6 9210  216 9543  241 10106  255  0  0  0  0  0  0  
461  3089382.0  643630.8 9666  211  0  0  0  0  0  0  0  0  0  0  
462  3088273.2  641650.6 6643  202 9267  223 9942  229  0  0  0  0  0  0  
463  3079223.7  621053.7 6454  214 6704  216  0  0  0  0  0  0  0  0  
464  3060015.6  616917.2 7065  196  0  0  0  0  0  0  0  0  0  0  
466  3078906.6  614409.8 7450  213  0  0  0  0  0  0  0  0  0  0  
467  3079312.2  621652.5 6416  219  0  0  0  0  0  0  0  0  0  0  
466  3078627.3  622840.1 8461  214  0  0  0  0  0  0  0  0  0  0  
469  3073116.3  626264. 7 8420  223  0  0  0  0  0  0  0  0  0  0  
470  3079016.5  637902.9 8018  217  0  0  0  0  0  0  0  0  0  0  
471  3062494.4  641351.2 6697  210  0  0  0  0  0  0  0  0  0  0  
472  3064407.6  508085 .3 7629  213  0  0  0  0  0  0  0  0  0  0  
473  3067547.0  501449.2 7610  216  0  0  0  0  0  0  0  0  0  0  
474  3060053.2  515116.6 7924  228 8995  257  0  0  0  0  0  0  0  0  
475  3061145.2  520206.0 6302  235 9309  291  0  0  0  0  0  0  0  0  
476  3056381 .0  527891.8 7507  248 10487  352  0  0  0  0  0  0  0  0  
477  3057931 .8  527454.3 7424  238 10521  339  0  0  0  0  0  0  0  0  
478  3069106.6  546437.1  6964  227 8136  241 9335  303  0  0  0  0  0  0  
479  3065921 .6  545596.9 7413  229  0  0  0  0  0  0  0  0  0  0  
480  3045527.6  520023.2 6743  220 10526  329 11036  347 11425  359 12741  394  0  
481  3046327.0  520060.6 11105  328 11275  349  0  0  0  0  0  0  0  0  
482  3047865.6  524347.2 8912  283 10316  302 11085  317 12285  349  0  0  0  0  
483  3050300.9  514701.3 9011  241 12600  352 14197  391 19126  479 21639  507  
22973  526  
484  3045329.0  532070.4 6986  207  0  0  0  0  0  0  0  0  0  0  
485  3054160.8  526869.7 7190  226 9641  254 10694  333  0  0  0  0  0  0  
486  3063936.3  569076.8 6906  216  0  0  0  0  0  0  0  0  0  0  
487  3066482.6  586230.5 8166  218  0  0  0  0  0  0  0  0  0  0  
486  3045654.1  559059. 1 EM75  206  0  0  0  0  0  0  0  0  0  0  
489  3046499.4  551449.2 5579  197  0  0  0  0  0  0  0  0  0  0  
490  3059104.5  613624.1 7708  207  0  0  0  0  0  0  0  0  0  0  
491  3068423.9  614560.5 7464  197  0  0  0  0  0  0  0  0  0  0  
492  3064732.4  615753.6 7115  204  0  0  0  0  0  0  0  0  0  0  
493  3062056.3  634241 .4 6396  232 6921  265 9200  270 9432  261 9672  265 9926  
267  
494  3062652.9  643215 .2 6642  216 10120  251  0  0  0  0  0  0  0  0  
495  3064428.5  639537.3 8929  214 9218  226  0  0  0  0  0  0  0  0  
496  3063390.0  642228.5 8439  209 10486  247  0  0  0  0  0  0  0  0  
497  3069936.6  640095.0 9129  215  0  0  0  0  0  0  0  0  0  0  
496  3063199.2  647708.8 10246  240  0  0  0  0  0  0  0  0  0  0  
499  3066053.3  635314.7 6232  201  0  0  0  0  0  0  0  0  0  0  
500  3064705.7  645924.9 9593  237 9748  237  0  0  0  0  0  0  0  0  
501  3066391.1  646604.4 9079  206 9649  21110121  222  0  0  0  0  0  0  
502  3060604.9  639515.0 EM53  211  0  0  0  0  0  0  0  0  0  0  
503  3066052.4  639561 .3 6542  219  0  0  0  0  0  0  
504  3053739.6  607427.5 7560  195 8797  234 10756  265  0  0  0  0  0  0  
505  3052752.6  63EM16.3 10661  253  0  0  0  0  0  0  0  0  0  0  

ID UTM COORDINATES DEPIHqEMP ~AIRS.... 
~D 54  UTM COORDINATE~ PEPTH/TEMP PAIRS.... 3027643.6 5595 9.0 7541 197 0 0 0  0  0  0  0  0  0  0  
555  3015206.0  556413.1 7943  211  0  0  0  0  0  0  0  0  0  0  
556  3022447.0  591223.3 6072  210 10746  253  0  0  0  0  0  0  0  0  
557  3014739.6  595005.8 9266  215 101 to  250 12003  295  0  0  0  0  0  0  
556  3015401.4  594523.3 6456  207 12393  291  0  0  0  0  0  0  0  0  
559  3020855.9  595417.4 6180  206 11684  286  0  0  0  0  0  0  0  0  
560  3028796.6  601789. 1 9006  220  0  0  0  0  0  0  0  0  0  0  
561  3040646.3  609512.0 7941  198 8337  204 8321  203  0  0  0  0  0  0  
562  3026599.6  599466.3 8291  218 10766  260 11559  306 12167  322  0  0  0  0  
563  3034835.6  608742.8 8428  217  0  0  0  0  0  0  0  0  0  0  
564  3030665.5  607739.3 9133  228  0  0  0  0  0  0  0  0  0  0  
565  3039015.9  602419.4 7687  191 9480  220 11161  270  0  0  0  0  0  0  
566  3031665.4  622623.1 10149  221 12974  296 14929  334 15679  353  0  0  0  0  
567  3040088.2  612386.6 8306  204 9004  214 9304  216 9437  226  0  0  0  0  
568  3032906.6  619155.6 7951  194 8960  206 9519  215 9740  229  0  0  0  0  
569  3029458.7  625589.5 9240  202 9318  204 9683  211  0  0  0  0  0  0  
570  3037952.4  633160.4 10071  233 10437  240  0  0  0  0  0  0  0  0  
571  3030164.1  625251.0 8900  216 9592  226 10286  237  0  0  0  0  0  0  
572  3040552.9  632874.3 9373  218 10550  258  0  0  0  0  0  0  0  0  
573  3031743.5  624073.6 9987  225  0  0  0  0  0  0  0  0  0  0  
574  3041915.2  636254.5 9759  252  0  0  0  0  0  0  0  0  0  0  
575  3034804.6  643162.2 8674  218  0  0  0  0  0  0  0  0  0  0  
576  3039434.8  636067.0 9383  210 9513  219 10222  242 11947  284  0  0  0  0  
577  3035699.6  640076.1  9172  211  0  0  0  0  0  0  0  0  0  0  
576  3029529.5  636804.4 9646  211 9961  216 14954  319 15573  336  0  0  0  0  
579  3034200.3  640116.8 9451  215 9944  239 13602  311  0  0  0  0  0  0  
580  3026499.3  602746.6 8835  214  0  0  0  0  0  0  0  0  0  0  
581  3018812.1  622245.2 7875  188 8979  208 9480  209  0  0  0  0  0  0  
562  3016646.3  614019.4 10437  241  0  0  0  0  0  0  0  0  0  0  
583  3018703.6  621487.7 9548  209 9982  223 10479  229  0  0  0  0  0  0  
564  3026156.6  620003.7 9977  225  0  0  0  0  0  0  0  0  0  0  
585  3019463.5  623170.6 10147  231  0  0  0  0  0  0  0  0  0  0  
566  3017566.0  614667.5 10949  244  0  0  0  0  0  0  0  0  0  0  
567  3019417.4  614414.7 9933  236  0  0  0  0  0  0  0  0  0  0  
566  3015206.2  630837.1  9784  223 10370  246 10465  249 12249  266 14187  325  
14679  330  
569  3017979.3  630297.6 9537  232 10215  250 11235  272 11724  271  0  0  0  0  
590  3019929.8  625513.6 10254  230 10767  235 10871  242  0  0  0  0  0  0  
591  3019203.3  626678.7 9473  213 10364  224  0  0  0  0  0  0  0  0  
592  3014813.3  628936.2 9706  204 9910  227 11118  261  0  0  0  0  0  0  
593  3019345.9  635163.110455  232 10549  244 11167  266 11746  274 12506  266  
15060  325  
594  3026202.8  624308.4 9399  215 10014  221 10524  250 11031  254  0  0  0  0  
595  3020072.3  630976.8 9985  221 11495  269 12495  309  0  0  0  0  0  0  
596  3017363.4  63o4588 .0 10092  228 11361  245 11915  283 13239  9  
597  3028253.5  628643.8 8874  211 9337  215 10057  230  0  0  0  0  0  0  
598  3025116.9  625187.0 10284  224 11964  269  0  0  0  0  0  0  0  0  
599  3020222.1  623948.6 8776  199 9725  219  0  0  0  0  0  0 . 0  0  
600  3027423.2  627945.8 9060  216 9902  223 11360  261  0  0  0  0  0  0  

ID 601  UTM COORDI MATES DEPTH/TEMP PAIRS.... 3017173.6 625960.0 9960 297 0 0 0  0  0  0  0  0  0  0  
602  3050293.6  660422.0 8371  214  0  0  0  0  0  0  0  0  0  0  
603  3054946.6  654536.0 11413  224 12615  292 13562  306  0  0  0  0  0  0  
604  3055925.8  648013.1 10255  274 11551  295 12939  327  0  0  0  0  0  0  
605  3053177.7  670599.7 9364  220 10991  262  0  0  0  0  0  0  0  0  
606  3050016.4  669717. 7 9268  225 9514  239 10003  239 I 0430  254 10983  242  0  
607  3055031 .0  667756.4 6744  209 10014  241  0  0  0  0  0  0  0  0  
609  3046748.7  668079.4 9549  222 10256  234  0  0  0  0  0  0  0  0  
609  3066164.6  651360.6 9551  250 10473  242  0  0  0  0  0  0  0  0  
610  3060975.9  648091.9 10394  232 12444  293 14444  318 14933  332  0  0  0  0  
611  3059929.6  646653.6 10149  216 11579  271  0  0  0  0  0  0  0  0  
612  3061496.4  649804.6 10488  242 10900  240 11187  242 11355  246 13155  299  0  
613  3057679.4  650076.6 10300  216 11550  275  0  0  0  0  0  0  0  0  
614  3058452.0  658792 .8 9364  214 11155  258  0  0  0  0  0  0  0  0  
615  3066673.4  651612.0 9657  226 10569  257  0  0  0  0  0  0  0  0  
616  3068622.6  654373.7 9276  213 9601  218 9984  234  0  0  0  0  0  0  
617  3066951 .1  654237.9 9046  211 9936  223 11500  236  0  0  0  0  0  0  
618  3059296.2  658235.5 10399  232 12441  293 14437  318 14933  332  0  0  0  0  
619  3062506.3  662496.3 9'464  231  0  0  0  0  0  0  0  0  0  0  
620  3061824.7  662000.5 7466  202 6468  204 10452  247  0  0  0  0  0  0  
621  3059006.7  665444. I 9321  210 10966  260  0  0  0  0  0  0  0  0  
622  3069114.7  669836.9 9226  212  0  0  0  0  0  0  0  0  0  0  
623  3066113.9  671338.0 9434  226 10611  256 11971  276  0  0  0  0  0  0  
624  3058328.5  661653.3 9587  217 13836  277 14157  311 15176  319  0  0  0  0  
625  3066536.7  671341.4 9402  214 115'46  273  0  0  0  0  0  0  0  0  
626  3068698.0  674978.9 9169  222 10509  244  0  0  0  0  0  0  0  0  
627  3064370.6  672664.7 9329  220 10479  241 10672  267  0  0  0  0  0  0  
628  3067903.6  672628.7 8455  209 9674  233 10569  256  0  0  0  0  0  0  
629  3067630.3  672605.9 9599  223 10337  240 10691  260 11976  279  0  0  0  0  
630  3064459.3  675708.8 9010  216 9384  219  0  0  0  0  0  0  0  0  
631  3093173.6  654515.1 9158  216 9632  215 10139  255  0  0  0  0  0  0  
632  3087972.2  658373.6 10621  243 13431  306 14546  340  0  0  0  0  0  0  
633  3065171.2  656106.2 9624  213 10040  220  0  0  0  0  0  0  0  0  
634  3067945.5  659147 .6 10581  238 13584  320 14362  321  0  0  0  0  0  0  
635  3065909.6  655504.6 10251  241 12276  266  0  0  0  0  0  0  0  0  
636  3097035.2  657201.0 9695  216 10075  231  0  0  0  0  0  0  0  0  
637  3067520.3  671676.5 10107  222 14137  311  0  0  0  0  0  0  0  0  
638  3097258.4  671643.2 9680  230 10959  278  0  0  0  0  0  0  0  0  
639  3067656.6  663276.6 6611  194 9523  213 9954  206 10666  250 11217  256  0  
640  3089166.7  662271.4 10407  214 11902  268  0  0  0  0  0  0  0  0  
641  3096462.2  672025.0 9'460  226 9730  229 10913  262 11469  270 12434  291  0  
642  3087664.3  663849 .2 9906  222 10934  263 11683  261  0  0  0  0  0  0  
643  3096763.2  662031.2 6991  211 9944  221  0  0  0  0  0  0  0  0  
644  30890202  675917.2 9947  236 11260  271 12519  298  0  0  0  0  0  0  
645  3096932.6  6 75371.2 9472  217 9666  221 10972  26 7 11226  270  0  0  0  0  
646  3093209.4  672298.8 9970  230 10988  243 11479  269  0  0  0  0  0  0  
647  3091034.4  660265.4 10020  225 11960  266 13974  311  0  0  0  0  0  0  
648  3086701.6  677493.5 9949  226 11750  271 13528  302  0  0  0  0  0  0  
649  3094529.0  663166.0 9363  230 11216  272  0  0  0  0  0  0  0  0  

ID 650  UTM COORDINAT~S DEPTH/TEMP PAIRS.... 3094576.0 660231 .0 9617 225 12472 267  0  0  0  0  0  6  0  0  
651  3066514.9  666505.2 6679  205 9625  256 10635  270  0  0  0  0  0  0  
652  3065396.2  666302.6 6997  212 9575  231 11963  261  0  0  0  0  0  0  
653  3066332.2  667211.0 9060  209 13005  306  0  0  0  0  0  0  0  0  
654  3066243.6  666248.2 9160  220 10610  262  0  0  0  0  0  0  0  0  
655  3095951.5  666400.7 9107  216 12963  297  0  0  0  0  0  0  0  0  
656  3036665.0  666656.8 8987  225 10191  236  0  0  0  0  0  0  0  0  
657  3030631 .6  660720.0 10366  223 11461  266  0  0  0  0  0  0  0  0  
656  3022976.4  659607.9 8972  200 10474  230  0  0  0  0  0  0  0  0  
659  3016497.9  654034. 1 10266  216 10574  227 12505  276  0  0  0  0  0  0  
660  3025817.5  666633.0 9964  229 10346  215 11620  255 12419  283 13271  306  0  
661  3025933.0  665607.7 9043  209 10677  255 10969  262  0  0  0  0  0  0  
662  3020411.5  662645.3 6010  201 10803  257  0  0  0  0  0  0  0  0  
663  3035674.2  656590 .3 8417  204  0  0  0  0  0  0  0  0  0  0  
664  3105642.3  697633.0 9213  217 11962  272  0  0  0  0  0  0  0  0  
665  3109420.7  696966.0 8473  204 8909  214 9718  241 10469  254  0  0  0  0  
666  3104290.2  697267.4 9117  217 9346  219 11505  240 11966  245  0  0  0  0  
667  3111727.6  697650. 1 9080  226 11394  273  0  0  0  0  0  0  0  0  
666  3104251.9  696416. 1 9141  216 11999  261  0  0  0  0  0  0  0  0  
669  3101751.6  696196.4 9256  226 11790  261  0  0  0  0  0  0  0  0  
670  3109153.9  696332 .8 9155  220 11451  269  0  0  0  0  0  0  0  0  
671  3101971.4  696669. 7 6959  214 10062  227 10964  250 1 1790  258  0  0  0  0  
672  3120033.6  697571.1 11076  255  0  0  0  0  0  0  0  0  0  0  
673  3120011.5  697146.6 11091  244  0  0  0  0  0  0  0  0  0  0  
674  3120217.9  705136.7  -27  -1  0  0  0  0  0  0  0  0  0  0  
675  3157330.8  705361.9  -27  -1  0  0  0  0  0  0  0  0  0  0  
676  3203165.3  647473.2  -27  -1  0  0  0  0  0  0  0  0  0  0  
677  1.0  1.0 -27  -1  0  0  0  0  0  0  0  0  0  0  
676  3200627.9  646557.6 9772  245 10272  263 10706  266 11602  315  0  0  0  0  
679  3204234.5  653625 .6 9939  252 10112  254 12622  317  0  0  0  0  0  0  
660  3204910.3  646291 .0 9670  243  0  0  0  0  0  0  0  0  0  0  
661  3204002.8  651961 .4 9861  245 12243  333 12721  332  0  0  0  0  0  0  
662  3196016.2  648582.5 9813  255 10510  304 10858  312 12919  342  0  0  0  0  
663  3204015.0  656665.9 10162  26611717  313  0  0  0  0  0  0  0  0  
664  3197767.6  647963.1  9100  247 9371  24611079  306 12106  329  0  0  0  0  
665  3202699.3  651569 .2 9911  252 1 1096  300  0  0  0  0  0  0  0  0  
666  3207411.1  655930.0 9723  241 10026  244 10190  246 11747  314  0  0  0  0  
667  3207207.9  652427.6 10102  25611512  324  0  0  0  0  0  0  0  0  
666  3207273.9  653917.7 9903  262 10401  297  0  0  0  0  0  0  0  0  
669  3199965.7  654761.9 14606  369 15291  363  0  0  0  0  
690  3202304.6  651970 .6 10062  252 11762  326 12776  342  0  0  0  0  0  0  
691  3204706.6  655336.1  9703  24111213  31511714  330  0  0  0  0  0  0  
692  3191127.0  657457.3 6752  240  0  0  0  0  0  0  0  0  0  0  
693  3166066.4  653357.0 9144  244  0  0  0  0  0  0  0  0  0  0  
694  3161266.2  655539.5 9232  245 9373  261  0  0  0  0  0  0  0  0  
695  3169262.I  651566.9 8960  246  0  0  0  0  0  0  0  0  0  0  
696  3193565.6  649032.7 10164  254 11013  276 12401  313  0  0  0  0  0  0  
697  3190595.5  652129.1  9218  251 10718  316  0  0  0  0  0  0  0  0  
696  3193652.7  648765.3 9729  251 10251  256 11646  313 14037  356  0  0  0  0  

ID 699  UTM COORDINATES DEPTH/TEMP PAIRS.... 3192624.3 649090.0 10202 264 11329 307  0  0  0  0  0  0  0  0  
700  3166965.0  657551 . 7 8504  205 9253  223  0  0  0  0  0  0  0  0  
701  3231943.0  567236 .6 7126  197  0  0  0  0  0  0  0  0  0  0  
702  3213007.0  560232.7 8027  200  0  0  0  0  0  0  0  0  0  0  
703  3195033.5  537210.1  9639  206 14604  299 15057  312  0  0  0  0  0  0  
704  3191383.0  515670.8 6940  196  0  0  0  0  0  0  0  0  0  0  
705  3165204.0  524446.6 7572  216 6646  246  0  0  0  0  0  0  0  0  
706  3123907.1  461486.1 10764  261  0  0  0  0  0  0  0  0  0  0  
707  3119671.7  463646.3 6075  213  0  0  0  0  0  0  0  0  0  0  
708  3112902.5  494547.6 5609  214  0  0  0  0  0  0  0  0  0  0  
709  3110616.7  462051 .3 7356  206  0  0  0  0  0  0  0  0  0  0  
710  3107029.6  454494.3 6682  246  0  0  0  0  0  0  0  0  0  0  
711  3101707.1  459794.9 6955  209  0  0  0  0  0  0  0  0  0  0  
712  3103245.8  469115.4 6110  219  0  0  0  0  0  0  0  0  0  0  
713  3102059.6  474632.5 6237  219  0  0  0  0  0  0  0  0  0  0  
714  1.0  1.0 -476  -1  0  0  0  0  0  0  0  0  0  0  
715  3134935.6  466014.2 7242  196  0  0  0  0  0  0  0  0  0  0  
716  3132072.7  492722 .5 10049  235 10236  284 10446  284  0  0  0  0  0  0  
717  3135249.1  499432.1 10135  247  0  0  0  0  0  0  0  0  0  0  
718  3130637.3  490272.1 10114  240  0  0  0  0  0  0  0  0  0  0  
719  3224326.4  614266.5 7665  216 6190  217  0  0  0  0  0  0  0  0  
720  3216829.6  608870.2 9199  244 9759  240 10037  241 10840  267  0  0  0  0  
721  3210166.1  627926.9 6516  224  0  0  0  0  0  0  0  0  0  0  
722  3217890.2  622673.2 10853  254  0  0  0  0  0  0  0  0  0  0  
723  3215624.2  649304.7 15302  336 16334  376 17606  402  0  0  0  0  0  0  
724  3217049.5  658003.4 9650  255 11130  271 14358  332  0  0  0  0  0  0  
725  3219630.2  655621.5 13756  310 13952  309  0  0  0  0  0  0  0  0  
726  3209567.8  657716.0 9896  253 10314  257  0  0  0  0  0  0  0  0  
727  3211649.3  650013.1 13665  306 14355  324  0  0  0  0  0  0  0  0  
726  3209173.6  657324.5 10053  267  0  0  0  0  0  0  0  0  0  0  
729  3210365.7  655563.3 7226  221  0  0  0  0  0  0  0  0  0  0  
730  3213649.5  653510.7 13234  304 14063  319 14345  312  0  0  0  0  0  0  
731  3215745.3  646700.4 13610  332  0  0  0  0  0  0  0  0  0  0  
732  3216623.7  650998.6 9506  241 14084  326  0  0  0  0  0  0  0  0  
733  3211637.1  650013.3 14347  324  0  0  0  0  0  0  0  0  0  0  
734  3102095.4  549212.5 8527  248 10408  309  0  0  0  0  0  0  0  0  
735  3100349.4  559164.5 6179  221 6243  222 9465  191  0  0  0  0  0  0  
736  3099576.3  555084.5 8725  258 10161  308 10930  336 10997  343  0  0  0  0  
737  3101341.1  552016.6 9149  255 10364  292 11015  308  0  0  0  0  0  0  
738  3099209.4  559209 .3 8335  252 9565  294 9671  296 10395  344  0  0  0  0  
739  3103396.3  559734.3 6010  225 6231  259 9022  269 9566  263 10136  304  0  
740  3103869.9  560291.9 7648  236 10494  316  0  0  0  0  0  0  0  0  
741  3106076.7  557654.0 6402  230 10763  312  0  0  0  0  0  0  0  0  
142  3102412.6  550106.6 9360  303 10354  317  0  0  0  0  0  0  0  0  
743  3109557.9  560104.9 7632  256 9719  297 11370  343 13026  360  0  0  0  0  
744  3105136.1  556661.9 7478  224 7980  231 9850  257 10455  302 10779  302  0  
745  3110296.1  572947.9 6606  236 10946  310 11517  327  0  0  0  0  0  0  
746  3110611.1  563274.3 7624  225 10126  302  0  0  0  0  0  0  0  0  

rn  YIM ~RDINATES  DEPTHITtMP PAIRS....  
747  310149.1  563028.5 7968  249 9465  296 10431  319 10697  324 11804  357 12131  
365  
748  3108758.1  561683.8 7748  237 10161  262  0  0  0  0  0  0  0  0  
749  3098945.9  561583 .2 7998  238 8902  282 9421  296 10007  312 10339  322  0  
750  3107062.9  561683.8 7682  220  0  0  0  0  0  0  0  0  0  0  
751  3110880.7  563461 .4 7629  243 9035  262 I 0036  297 10533  314 11220  341  0  
752  3111118.6  572002.9 8829  264 11560  338 12507  341  0  0  0  0  0  0  
753  3106895.6  568136 .5 7982  220 11060  335  0  0  0  0  0  0  0  0  
754  3110462.0  582508.2 10280  262 12468  338 13804  368  0  0  0  0  0  0  
755  3110863.9  573907.3 6652  240 10899  319 11261  326  0  0  0  0  0  0  
756  3111006.0  575022.2 6982  216 8942  273 10918  315 12183  343  0  0  0  0  
757  3110873.8  576996.8 6552  250 12217  341  0  0  0  0  0  0  0  0  
758  3109922.9  581310. 7 9402  223 12043  339 12271  345 12992  356  0  0  0  0  
759  3106076.2  589397.5 6729  193  0  0  0  0  0  0  0  0  0  0  
760  3108444.9  598047 .B 6419  209  0  0  0  0  0  0  0  0  0  0  
761  3108935.3  594147 .8 6562  204  0  0  0  0  0  0  0  0  0  0  
762  3101966.7  594319.5 7007  221  0  0  0  0  0  0  0  0  0  0  

APPENDIX B-THE KEHLE TEMPERATURE CORRECTION SCHEME 

~As Published by ' 
32 
USGS in AAPG 1<,_e~le in AAPG
OF 
LL. 
28 
0 

Keb.l..e • Equ ations far
z 
z 24 
,,,~0"" Eq uilib rium Temperatures 
0 
t; 20 
w 
a:: 
g§ 16 

u 
w
3 12 
1­
<l 
a:: 
g: 8 
~ 
w 
1-4 

TE: TL+ lgO (7689X10-14 03 -3.888x10-9 02 + 3.619 x 10-50 ~0270245) 

0
60~-000~....L.--1_0,~0-0-0--1..~oo-_
00---'~-8~-,2-,~o-~.J._-,4-,0LOO~L--,6~,0LOO__J~,-s~.o-o_o--1~2_JO,OOO 
DEPTH 
138 

APPENDIX C-CALCULATING ISOTHERMS 
Program DBINTP 
This program creates a data file (OUTPUT) for an isothermal 
surface. The program interactively asks for the temperature of the 
isothermal surface and the temperature range(± ILIM) of eligable data. 
The program reads CORCT which is the filename of the temperature 
corrected data base. 
PROGRAH DBllTP(CORCT,OUTPUT,m,TAPES=CORCT,TAPE6= 
10UTPUT,TAPE7=m) 
DIMENSION ITEMP(9) 
DIMENSION IDEPTH(9) 

fC=O 
WRITE(7,5) 
FORMAT( 1X,'WHAT TEMP TO PLOT,WHAT LIMIT Of INTERPOLA 

1TION•) 
READ(7,*)INTEM,ILIM 
00 1001=1,1000 
READ(5,*,END=110) NUM,DUM1,DUM2,IDEPTH(1),ITEMP( 1), 

1IDEPTH(2) ,ITEMP(2) ,IDEPTH(3), 
1ITEMP(3),IDEPTH( 4),ITEMP( 4),IDEPTH( 5),ITEMP( 5) ,I DEPTH( 6 
1),ITEMP(6) 

00 30 K=1,6 
IF(ITEMP(K).EQ.INTEM) GOTO 50 
lf(ITEMP(K).LT.INTEM .AND. INTEM-ITEMP(K) .LE.ILIM 

1.AND. (ITEMP(K+ 1).GT.INTEM .OR. ITEHP(K+ 1).EQ.O)) GO TO 40 
IF(ITEMP(K).GT.INTEM .AND. ITEHP(K)-INTEM.LT.ILIM) GO 
1TO 70 

139 

140 
30 CONTINUE GOTO 100 40 IF(ITEMP(K+ 1).EQ.O)THEN 
ICRCD=I NTEM*I DEPTH( K) /ITEMP( K) 
ELSE 
ICRCD= (IDEPTH( K+ 1 )-IDEPTH( K)) *(I NTEM-ITEMP( K)) I 
1 (ITEMP(K+ 1 )-ITEMP(K) )+IDEPTH(K) END IF 50 WRITE(6,55) NUM,DUM1 ,DUM2,ICRCD NC=NC+ 1 
55 FORMAT(1X,15,2F13.1,16) 
60 GOTO 100 
70 ICRCD=I NTEM*I DEPTH( K) /ITEMP( K) GOTO 50 100 CONTINUE 110 WRITE(7,120)NC 120 FORMAT( 1X,'THE NUMBER OF ENTRIES IS',15) WRITE(6,130)NC 130 FORMAT( 1X,'C** THE NUMBER OF ENTRIES IS',15) STOP END 


APPENDIX D-KRIGING 
Aut/Jor's note: Before embarking on t/Je study of t/Jis appendix, you are /Jereby warned t/Jat t/Je Kriging process is rat/Jer involved and will not be learned in a day, nor probably even in a week. You will first need: A basic knowledge of FORTRAN, data that are digitized using a cartesian system reg. UT/1), access to t/Je programs covered /Jeretn(GAl1118B, NEWPL TB, NEWUKB, & /"IAPWB w/Jic/J are property of tile UT Bureau of Economic Geology, Contact t/Je Bureau's computer center) and familiarity wit/J t/Je computer on w/Jic/J you intend to run them. 
Kriging is a data smoothing technique which employs statistical methods to accomplish smoothing. The method can transform irregularly spaced or unevenly distributed data into regularly spaced points, each point being estimated from the actual data points surrounding it. A standard deviation at each of the estimated points is also calculated. The method was originally developed for estimating mineral recovery in mining operations, but has been applied to other geostatistical problems such as preparing data for contouring in cases where the reliability of the data is not absolute. In such cases, contouring the data without some way of first smoothing out the scatter can result in an impossibly 
141 
complex and unrealistic surface. Kriging allows one to average out the scatter while providing a measure of the reliability of the resulting estimated surface at each contoured point. In my work, the kriging technique has been employed to smooth bottom-hole temperature measurements for contouring subsurface isotherms. 
The kriging process involves several steps. A computer is essential for handling the multitude of calculations required. This appendix does not attempt to explicitly review all the calculations needed. Presented is a genera1 out I ine of the procedures, accompanied by instructions in the use of the various computer programs that I used to accomplish them. The programs were donated to the Bureau of Economic Geology of the U1iversity of Texas by Dr. Young C. Kim of the U"\iversity of Arizona College of Mines. 
THE VARIOGRAM 
Constructing a variogram is the first step in the kriging process. A variogram is a plot which graphically describes how the data varies on average at increasing distances away from any point within the data field. It can be thought of as a plot of the difference in value between some starting point and points increasing distances away from that starting point. A typical variogram is shown in figure 01 . The underlying assumption of the variogram, and hence the kriging process itself, is that the values of neighboring points influence each other. In other words, we expect the variogram to show the smallest differences at points closest to the starting point (represented on the variogram by the origin), with the differences becoming greater at increasing distances away from the starting point. Data that behaves in this manner is termed regionalized. As distance increases, the regionalized influence diminishes and variation increases until some plateau is reached where differences become purely random. 
VARIOGRAM 
,.x .. x-x 
X X 'X·X 
I 

x 
" 
x 
0 h 2h3h4h5h 
Distance (class interval =h 
Figure D1. A typical variogram where the x's are ?f(h)'s plotted at each multiple of h. 
The variogram is an integral part of the Kriging process. In essence the kriging program I used constructs a regularly spaced grid over the data field and then finds values for the center of each block in the grid. It determines the value of each block center by averaging the surrounding data points. This is not a simple average because the kriging process weights each surrounding datum separately. This weight is based on its distance from the block center. The program knows how to weight the data by referring to the variogram as shown in figure 02. In general, points closest to the block center receive greater weight than those farther away. In actuality, the kriging program cannot read the variogram directly. Instead, it must be given an equation of a curve which closely approximates the variogram. This curve is shown infigure 02 by the heavier line. The details of fitting a curve are supplied in the section on NEWPLOT. 
VARIOGRAM 
4
• 
1 
'. 
1f(h)






3/ "-·2 
• 

Distance 
Figure 02 shows how a variogram is used to krig a block center (left). The data points 1-4 around the block center are weighted according to the variogram (right). The weighting values are derived from the ?5's read off the variogram, which in turn are approximated by fitting a curve to the actual variogram. The weighted values are then averaged yielding a value for the block center. 
The variogram is constructed by surveying within a set distance 
around each data point, finding the average difference of the value 
between the point being surveyed and the points that occur within the set 
distance from it, and then averaging this result with those of all the 
other data points in the data field. This number is then plotted on the 
variogram, with the average difference plotted along the y axis and the distance surveyed plotted along the x axis. The process is then repeated for multiples of the original surveying distance. The distance used in the original survey is set arbitrarily and is termed the class interval Finding the optimum class interval is a trial and error process. The 
investigator guesses at the class interval until a proper looking variogram such as shown in figure 02 results. Note in the figure that the y axis is labeled gamma. Gamma is actually the standard deviation squared. The squaring eliminates the problem of dealing with both positive and negative variations. If this were not done, the average differences would be near zero as a result of the positive and negative variations cancelling each other. As one can now see, there is a staggering amount of calculation involved in finding all these averages for each data point, and then averaging these together. This technique would not be practical without the aid of a computer. 
The above method is stated in equation form as follows: 
N 
~h] =~ 2: [f(x1) -f(xj + h)]2 
2N j=1 
where N is the number of data points, ~ is the standard deviation squared, and h is the class interval. To construct the variogram, ~ is plotted against distances h and multiples of h. 
VARIOGRAM COMPUTER PROGRAM 
THE SEARCH WINDOW 
When calculating Cf at multiples of class interval h, it is possible to control the direction of search. In otherwords, one need not necessarily sweep 360 degrees around each data point. In fact, since every data point is used as a starting point of search for each class interval, the search angle, also termed the window, need only be 90 degrees to cover the whole data base in all directions as shown in figure 
03. By decreasing the window angle further and specifying a direction, such as N, NW, SE ect., a variogram showing behavior of the data in one direction is created (figure 04). This variogram can be compared to variograms resulting from different window orientations for the purpose of estimating anisotropy. The section Fitting A Curve contains some additional information on this. It is necessary to introduce the concept of the search window here since the following program requires that the window be specified. 
construct1ng a Nond1rect1on Var1ogram 

90• Windows Figure 03 schemat1cally show1ng sweeps of the data f1eld for h. 2h and 3h 1ntervals for a nond1rect1ona1 var1 ogram. 
CONSTRUCT ING A 
NW-SE DIRECTIONAL VARIOGRAM 

45• Windows 
F1gure 04 schemat1ca11y show1ng sweeps of the data field for h. 2h and 3h intervals for a d1rect1ona1 var1ogram. 
THE UTM COORDINATE SYSTEM 
. 
For all the programs used to analyize my data, a cartesian coordinate system is required as the means to locate the data points. The usual latitude and longitude will not work as these are not cartesian. Another mapping system was developed for this need and it is called the Universal Transverse tlercator system or UTtl for short. Unfortunately, there are some problems with UTM that can make it difficult to use. UTM does not account for earth curvature, and for a very large area, say the size of the state of Texas, this can be a problem, depending on how accurately the data need to be located. For my study this was not a problem. Another problem occurs at central meridians, which occur every six degrees of longitude, where the UTM system is discontinous. This is a concern only if the Bureau's printed UTM listings are used. This may be convenient for some applications, but if data cross over one of these meridians, a program which the Bureau cal ls LLTRANB shoo Id be used to get your UTM coordinates. 
VARIOGRAM PROGRAM GAMM8 
The following instructions apply to the use of the FORTRAN program GAMM8B which is the property of the Bureau of Economic Geology. This and other programs used in my thesis are not in the public domain and are not listed here for that reason. A knowledge of FORTRAN formating is assumed. 
To use this program, one must create an input deck. The input deck contains information which controls the various options of the program as well as suppling basic information about the data. The data are then placed after this initial information. When running the program, the input deck must be specified as the input file. For those not familiar with constructing an input deck: The term card in the listing below refers to the now seldom used computer punch cards. An entry I ine on a terminal display is the modern equivilant of a card. There are 80 columns to a card and each column corresponds to one character. An input deck should have the following form (Bold type indicates the usual selections): 
CARD COLUMN FORMAT SELECT ION DESCRIPTION 
Card 1 1-80 8A10 Run Name 
Card 2  3  11  1= Log Transform, O= no  
4  11  1 =Average variogram option:  
yes  
O=  "  ,,  •  
no  
5  11  1= Punch for NEWPLOT, O= no  
6  11  1= Moment center, O=~(h)  
7  11  1=Auto Scale, O= no  
8  11  2= divide by variance  
1= divide by mean square  
O=neither  
9  11  1-tape input, O= system  
10  11  No. of directions (max. 8)  
11-20  FlO.O  Class interval: 20 x  

class= max range 41-50 F10.0 Max vertical value to allow 
Card 3 	You will need one of these cards for each Direction 1-10 F10.0 Direction 
0. = E-W 45. =NE-SW 
90.= N-5 -45. =NW-SE 11-20 FlO.O Window in degrees 
Card 4 11 1,2, or 3 (specifies order of occurence of value being Kriged ondata line) 2 11 1 ,2, or 3 (specifies occur. of y coord. ie. Northing) 3 11 1,2 or 3 (specifies occur. of x coord. ie. Easting) 4 11 1 =flags definition of rectangular sub-area to confine variogram to follow: O=no sub-area defined 11-20 F10.0 Minimum Northing (y) 21-30 FlO.O Maximum Northing 31-40 F10.0 Minimum Easting (x) 41-50 FlO.O Maximum Easting 
Card 5 1-80 8A10 Format of input on system enclosed in (paren.) 
Card 6 1-80 8A10 Title of Variogram for output 
Card 7-+n 
Data.. . 
Each data point is represented by its own data card (7-+n). Three values are being read in from each of these. They are the Easting, Northing, 
l 5 l 
and the value to be kriged in that order. Other numbers may exist on the data line as well, but formatting should ensure that just the three numbers being used are read in. 
The output from the program is written to a file named OUTPUT and also to one named TAPES. OUTPUT includes information on the variogram(s) just run and a character built plot of the variogram which comes off the I ine pr inter and provides a good, if not pretty, var iogram plot. To get a copy of the results printed on an actual plotter, TAPES provides unformated plotting output. NEWPLOT, the next program described, will produce a ZETA plot file from the TAPES file, which in turn can be sent directly to a ZETA plotter for draft-quality plots. 
PLOTTING PROGRAM NEWPLOT 
Before ruming this program, output file TAPES discussed above must be modified. To run several variograms at once with GAMMSB, TAPES must contain plotting information for each variogram, each being separated by a blank card (I ine). For each plot, one card free-formated with the following data must be present: 
Variogram value at the top of the graph 
Var iogram value at the bottom of the graph 
Variogram value at the right of the graph 
Variogram value at the left of the graph 
Length of the x axis (distance) in inches 
Length of the y axis (~) in inches 

These values should be seperated by spaces but contained within one line 
and should be listed in order. Do not leave a blank card between this card 
and the TAPES group (plot). Each plot should have one of these cards at the top. Leave only one blank card between the end of one group and this top card for the following one. 
To then run NEWPLTB on the CDC (Control Data Dual Cyber) you will need to first execute the following command (this procedure as of May, 1985): 
LDSET ,PRESET=ZERO,LIB=ZETLIBF The computer than prompts you with: 
LOR> 
You then type: 
NEWPLTB,TAPES The program then generates a file called PLOTR, which can be sent to a ZETA plotter by issuing the command: 
DISPOSE PLOT=PLOTR,ID= id site where id site is some printing site identification number, eg. Taylor Hall is 44. 
Fitting A Curve. As mentioned in the section THE VARIOGRAM, and as shown in figure 02, you will need to fit a curve to the variogram. This curve will be the weighting curve that the kriging program will actually use. The kriging program presented in this appendix uses the so­called spherical model for this curve. To fit the curve, three characteristic measurements of the variogram plot must be estimated. These are the nugget value, Co: the C value: and the range, a. To read these values off the variogram, the variogram must first be plotted. 
The line-printed plot will do (this can be done on a terminal screen). Figure 05 illustrates the proceedure. Draw a straight line along the slope described by the first three for four points. Then draw another straight Iine across the points that indicate a plateau (its normal for this plateau to slope back down at the far end of the x axis.) This second line should be nearly horizontal and should pass through or near the highest ?5 values on the graph. If the shape of your variogram does not comply with this proceedure and does not resemble those shown in the various figures in this appendix, then the variogram needs to be redone chosing a different class interval. They-intercept of the first sloping line is the nugget value (Co) and can be thought of as an indication of the accuracy of the data. Ideally this intercept should intersect the origin, though it almost never does. They-intercept of the horizontal line is the sill value which 
is given as C • Co, C being the difference between the si II and the nugget values. The si II indicates the maximum variance of the data. The range 
(a) is calculated as 3/2 times the distance (measured off the x axis) from the origin of the intersection of the two lines which have been traced. 
VARIOGRAM 


Distance Figure 05. Optaining C, Co and a by construction. The sill is given by C + Co. 
These three values alone are used to describe the fitted curve. Record these for future use in the kriging program. NEWPLOTB can plot the fitted curve on the variogram by further adding the following cards to the end of each data group on TAPES: 
CARD 	COLUMN FORMAT DESCRIPTION 
Cardi Blank Card 2 Al Type a "JM 1n th1s column 
Card 3 	1-10 FlO.O Nugget value (Co) 11-20 FlO.O Sill value (C) 21-30 FlO.O Range (a) 
The Anisotropy Ratio. If several variograms have been run in 
different directions as discussed in previous sections, the anisotropy 
ratio can be calculated using the sill values. The ratio is given by the ratio of the maximum directional sill value to the minimum directional sill value. The anisotropy ratio is used by the kriging program. Since the program only allows integers for this ratio, if the ratio is less than 1.5, then the anisotropy should be ignored. 
THE KRIGING PROGRAM NEWUKB 
The goal of constructing a variogram is to obtain the nugget, sill and range values for the nondirectional variogram, and also the anisotropy ratio if it is not less than 1.5. These will now be used as part of the input deck of the kriging program. 
Kriging produces a rectangular grid of rows and columns. The centers of the blocks in this grid are the points for which the kriging program calculates values. One must therefore decide what size blocks to use. Considerations include how much resolution is desired, how many data points there are, and how much computer time can be dedicated to the procedure. In general, smaller blocks yield better resolution, but also require more computer time. However, a block will not be kriged with less than two points. If there are less than two points within the radius of search you specify, no value wi II be generated for that block. 
The theory of kriging has been covered in the previous sections detailing the construction of the variogram. The procedure for executing the kriging program NEWUKB follows the same form as the previous programs. Here is the form for the input deck= 
CARD COLUMN FORMAT SELECTION DESCRIPTION 

Card 1 	1-5 15 Starting Column 6-10 15 Ending Column 11-15 15 Starting Row 16-20 15 Ending Row 21-30 FlO.O Max. Northing (Row 1) 31-40 FlO.O Min. Easting (Col 1) 41-50 FlO.O Block Width-North direction 51-60 FlO.O Block Width-East direction 
Card 2  1-5  FS.O  Max. dist. from block for hole  
to be included in kriging.  This  
should be about half the  
distance across the data field.  
6-10  15  Max. no. of points to be used for  
each block ~50, usually 1 O is  
enough).  
11  11  Debug output ( 1 =yes, O=no)  
12  11  Lisl dr i II holes ( 1 =yes, O=no)  

Card 3 	Card three is for mining applications and is used for kriging mineral-grade. You should set everything except the anisotropy ratio equal to zero. The ratio should be set at one. Card four, however is identical and was originally intended for vein thickness. For thickness, substitute the value you want to krig, eg. hydraulic heads. You should select the appropriate settings for card four. Bear in mind that in the output, the kriged values wi 11 be printed under the heading "thickness". 
1-10 FlO.O Nugget Value (Co) 
11-20 FlO.O Si II Value (C) 
21-30 FlO.O Range (a) 
31-40 FtO.O Angle of anisotropy (0 if none) 

0. = E-W 45. =NE-SW 
90.= N-S -45. =NW-SE 41-50 FlO.O Anisotropy Ratio ( 1 if none) 
51-60 FlO.O Vertical anisotropy (for mining, set too for 20) 
Card 4 Same as Card 3. Use this card for you kriging values. 
Card 5 	Format Card for your data (bracketted by paren.). You must format for the following variables in order (use tab format if necessary): 
Well identification 
X coordinate (Easting) 
Y coord1nate CNorth1ng> 
zcoordtnate (supply a dummy var1able, 

blanks should work; however, if you have problems, you mtght have to supply zeros) 
Grade-thickness (another dummy) Thickness Value (thts ts the value you are krigtng) 
card 6-+n Your Data Cone data potnt per card). 
To then run NEWUKB on the CDC the following command needs to be executed (this procedure as of May, 1985): LDSET,PRESET=ZERO The computer than prompts with: LOR> You then type: 
NE\VUKB, datafile Where datafile is the name given to the input deck. The program then generates a file called OUTPUT, which contains the kriged grid, giving the kriged value for the block center under the column "thickness" and the 

158 

row and column for each block center. These block-centers can be 
displayed by using the following program MAPWB, which provides a crude line-printed map of the output. However, it will not handle more than approximately 30 blocks across. The output file can be used as input for a plotting package (eg. CPSl). 
MAPWB For a I ine-printed map of the kriged output used the output file in conjunction with the following cards: 
CARD COLLJ1N FORMAT DESCRIPTION 
Card 1 1-10 F10.0 North coord of upper edge (row 1) 11-20 F10.0 East coord of left edge (col 1) 21-25 F5.0 Block size y dimension 26-30 F5.0 Block size x dimension 31-35 15 Beginning col. no. of area to be mapped 36-40 15 Ending col. no. of area to be mapped 41-45 15 Beginning row. no. of area to be mapped 46-50 15 Ending row. no. of area tobe mapped 
Card 2  1-10  FlO.O  Scale parameter to make  
variable 1 an integer (usually 1)  
11-20  FlO.O  Scale parameter to make  
variable2 an integer (usually 1)  
21-30  FlO.O  Sea le parameter to make  
variable3 an integer (usually 1)  

Card 3 	Format Card for your data (bracketted by paren.). You must format for the following variables in order (use tab format if necessary): 
East coordinate (as produced by NEWUKB) North coordinate (as produced by 
NEWUKB) Variable 1 (thickness) var1able 2 (dummy> Variable 3 (dummy) 
Card 4-+ n Data (from output of NEWUKB) 
APPENDIX E-CPS 1 
The following files were used to execute the CPS I graphics subroutines on the Dual Cyber computer. The command file was used to submit the job batch, ie., run CPS I as a job on a queue independant of an interactive user. The command file is written in a command language which is specific to the operating system (called Taurus) on the CDC at the University of Texas. The verb files contain the commands (which they call verbs) to execute the CPS I subroutines. 
CPS I turned out to be computation intensive . . The contouring programs, for example, required an average of 300 seconds of central processing time. The isometric plots (3-D) took even longer. The boldface print indicates file names or variables that can be changed depending on the desired options and which files the user desires to be used for data input, etc... Because of the complexity of using CPS I, these files are presented without explanation. For descriptions of their construction and use, the reader is refered to a Taurus manual for the command files, and a CPS 1 manual for the verb files. 
160 
POSTING DATA 
COMMAND FI LE READPF 4170 T400L50 READPF 4170 POSTYRB RENitiME T 400L50 Tit.PE 1 RFL 220000 CPS 1 POSTYRB CPS 1TRN••PLOT. 
SKIPCC. EXIT. REVIEW L•Dit.V SAVEPF 4170 5682 DAY OUTPUT P400LSO=PLOT ZAP 
VERB FILE $VC .x>B= 1 $END WELL LOCATOIS FOR K400L50 $VC AOl=1,YMIN=3014056.1,YMAX=3237605.5)CMIN=450501.3)CMAX= 
718654.3, Xltc=1 .,Vltc=1. $END $VC PDEF=1,XSCL=23000,YSCL=23000,IOPT=O $END $VC POLY=1,NPC=27,ISMB=O,ISCL=1,IFHT=2 $END 
(20X,f20.1,T1 ,f20.1) 3014594. 7 451204. 7 3014007.3 675797.4 3055372.3 6 74940.5 
ect..... 
3112021.3 475036.1 
3112309.0 450669.6 
3014594.7 451204.7 

$VC FENC=1,NPC=27,IFMT=2,ISCL=1 $END 
( 20X,F20.1,T 1,F20.1) 3014594. 7 451204. 7 3014007.3 675797.4 3055372.3 6 74940.5 
ect.... 
3112021.3 475036.1 
3112309.0 450669.8 
3014594. 7 451204. 7 

$CD FILD=O $END 
$VC LGPT=1,ISM8=-6,SIZE=0.06,LUN=1 iMODE=2 $END 
$CD f 1LD=1,SIZP=0.06,1PSN=1,tcLS=5 ~END 

( 19X,2f 10.0,T1,11,T4,SA1) $VC NWPG= 1 $END $VC STOP= 1 $END 
CONTOURING 
COMMAND FILE READPF 5576 (RGCOIB IRG350 RENAME IRG350TAPE1 REWALLX RFL,250000 CPS 1 IRGCOIB CPS 1TRN,,PlTCNT. St::IPCC. EXIT. REVIEW,l=DAYCIT SAVEPf 5576 8908 DAYCIT,(350L50=PlTCNT,OUT(RGB=OUTPUT ZAP 
VERB FILE $VC "-18= 1 $END 1250L30 $VC AOl=1,XHIN=450501.3,XHAX=718654.3,YHIN=3014056.1,YHAX= 3237605.5, XI te=5000.,YI te=5000. $END $VC t1;RD=1,tCP=O,lfHT=2,LUN=1 $END ( 19X,2f 10.0,T56,F8.0) $'t'C STAT= 1 $END $VC PDEF=1,XSCL=23000.,VSCL=23000.,t'llDE=1 $END $VC POLY=1,NPC=27,ISHB=O,ISCL=1,IFHT=2 $END (20X,f20.1,T1 ,f20.1) 3014594. 7 451204. 7 3014007.3 6 75797 .4 3055372.3 6 74940.5 
ect... 
3112021.3 475036.1 
3112309.0 450669.8 
3014594. 7 451204. 7 

$VC FEtC=1,NPC=27,lfHT=2,ISCL=1 $END 
(20X,f20.1,T1 ,F20.1) 3014594. 7 451204. 7 3014007.3 6 75797 .4 3055372.3 6 74940.5 
ect... 
3112021.3 475036.1 
3112309.0 450669.8 
301 4594.7 451 204.7 

$CD FILD=O $END 
.	$VC CTYP= 1,NREF=0,BOLD=O,DIS1=4.,DIS2=2.,HSHR=O,LABR= 1,SIZE=.08 $END $VC ClV4= 1,ZIDA=1,CLHN=-5000.,DEL=-500.,tCV=30,ICRT=1 $END $VC STOP• 1 $END 
ISOMETRIC PROJECTION 
COMMAND FI LE READPF 5576 YRBISOC IRG350 RENAME KR6350 TAPE1 REWALLX RFL,371000 CPS 1YRBISOC CPS1TRN,,1350LSO SKIPCC EXIT REVIEW,L=DAYISO SAVEPF 5576 8908 MYISO,1350L50, OUTISO=OUTPUT ZAP 
VERB FILE $VC .xlB=1 $END LOOKllG •RTHEAST,,DEPTH TO 250 DEG f $VC AOl=1,YHIN=3014056.1,YHAX=3237605.5)CHIN=450501.3,XHAX=718654.3, XINC=8000.,YINC=8000. $END $VC t1;RD=1,IFMT=2,LUN=1,NCP=O,NZ=1,IANL=1 $END ( 18X,F10.0,Ft O.O,T56,F8.0) $VC STAT=1 $END $VC PDEF• 1,XSCL•SOOOO.,VSCL•SOOOO. $END $VC RFIT=1,NREF=1,ZIM=1,ITYP=1,ZIDB=O $END $VC ISOH=1,ZIDA=1,ZSCL=2500.,ZHIN=-20000.,ZHAX=1000., ISID=1,THET=65. $END $VC NWPG= 1 $END $'t'C STOP= 1 $END 
APPENDIX F -FLOW VELOCITY VECTOR FIELDS 

The flow velocity vectors are listed for each triangular element. They appear by column, each column taking three lines in this listing. The columns are listed in order, as they appear from the left to right side of the mesh. The vectors for each element are listed in order starting at the bottom or basement of the mesh, and working toward the top. There are twenty-two elements in each column, and the vectors of the top two elements are all that appear on the third line for each column. The columns can be distinquished by this partial line. 
164 

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SIMULATION THREE-Horizontal component  
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VITA 
Dan Bodner was born in Jersey City, New Jersey on the sunny morning of July 6, 1960. He spent most of his youth growing-up and schooling in the suburban town of Westfield, New Jersey. After graduating Westfield Senior High School in 1978, he attended Vassar College in Poughkeepsie, New York, where he received his AB. in geology in May of 1982. He spent the following year experimenting in various employment fields including computer programming/data processing, architecture, and consulting-geology. In September of 1983, Dan enrolled in the Master's program at the Univeristy of Texas at Austin, to study hydrogeology under the direction of Dr. John M. Sharp. Upon graduation from the program, he will begin work at Woodward-Clyde Geotechnical Consultants in the Walnut Creek, California office.