Seismic reflection and seismic refraction surveying in ...
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JUN 1 2 1997
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EN 136
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Seismic Reflection andSeismic Refraction Surveyingin Northeastern Illinois
Paul c. ^
ILUNOIS
SURVEY
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ENVIRONMt
Department
ILLINOIS ST
Heigold
GEOLOGIC' LIBRAE
ENTAL GEO
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LOGY 136
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3VEY
ILLINOIS STATE GEOLOGICAL SURVEY
3 3051 00005 4738
Seismic Reflection andSeismic Refraction Surveying
in Northeastern Illinois
Paul C. Heigold
ILLINOIS GEOLOGICAL
SURVEY LIBRARY
ENVIRONMENTAL GEOLOGY 136
ILLINOIS STATE GEOLOGICAL SURVEYMorris W. Leighton, Chief
Natural Resources Building
615 East Peabody Drive
Champaign, Illinois 61820
Acknowledgment
Funding for this study was provided by the Department of Energy and Natural Resources(Contract ENR-5).
Printed by authority of the State of Illinois/1990/750
CONTENTS
Abstract v
Preface vi
Part I Seismic Reflection Profiling
Introduction 3
Geologic Setting 3Field Techniques and Instrumentation 6
Data Processing 7
Interpretation 9
Dauberman Road Seismic Reflection Line 1
1
Fermilab Seismic Reflection Line 21
Bristol Seismic Reflection Line 22Lily Lake Seismic Reflection Line 23
Conclusions 24References 25Appendixes 26A Recording Parameters and Processing Sequence of DaubermanRoad Seismic Reflection Line 26
B Recording Parameters and Processing Sequence of Fermilab
Seismic Reflection Line 27C Recording Parameters and Processing Sequence of Bristol
Seismic Reflection Line 29D Recording Parameters and Processing Sequence of Lily
Lake Seismic Reflection Line 30
Figures
1 Location of seismic reflection lines 2
2 Stratigraphic column of bedrock units in Northern Illinois 43 Regional geologic setting 64 Drift thickness map of the study area 7
5 Geologic map of the study area 8
6 Location of key drillholes used to constrain interpretation of seismic reflection sections 9
7 Stratigraphic column and interval velocities from test hole SSC-1 1
8 Stratigraphic column and interval velocities from test hole SSC-2 1
2
9 Stratigraphic column and interval velocities from test hole SSC-3 13
1 Synthetic seismogram constructed from sonic and density logs 1
4
1
1
Interval velocities from deep hole in Du Page County 15
1
2
Dauberman Road seismic reflection sections 1
6
1
3
Fermilab seismic reflection sections 1
8
1
4
Bristol seismic reflection sections 1
9
15 Lily Lake seismic reflection section 20
Part II Seismic Refraction Profiling
Introduction 33Seismic Refraction Method 34Equipment 35Field Procedures 35Processing of Seismic Refraction Data 36Results 36Summary 37References 39Appendix A Results of Seismic Refraction Profiling 40
Figures
1 Index map-location of seismic refraction profiles 332 Shot and geophone arrays used with FRAC and SIPT programs 353 Bedrock topography map of study area 38
Table1 Cable length and geophone intervals for estimated depth to bedrock in the study area 34
Abstract
As part of the Illinois State Geological Survey's comprehensive investigations to locate the most
suitable site for construction of the proposed Superconducting Super Collider, approximately 17
miles of high resolution seismic reflection profiling and approximately 80 miles of seismic refrac-
tion profiling were performed.
Seismic reflection profiling was used to define the stratigraphy and structural geology of the
proposed SSC site. The primary target of this profiling was the dolomite of the Ordovician Galena
and Platteville Groups, since the tunnel that would have housed the proposed SSC would have
been located in these rocks. In addition, the seismic reflection profiling provides a view of con-
tinuous sections of rocks to considerable depths, and thus, detailed information about the rocks of
northeastern Illinois unavailable from discrete drill holes.
Seismic refraction profiling was used to examine the geologic framework of near-surface deposits
at the proposed SSC site to aid in the construction of the SSC tunnel and the location of its atten-
dant vertical service shafts. The kinds of information provided by this profiling-depth to bedrock
(drift thickness) and lithology of both the drift and the bedrock surface-are relevant in many other
areas: for example, in other types of construction, evaluation of groundwater, aggregates
(crushed stone), and sand and gravel resources, and location of waste disposal sites.
Preface
The seismic exploration, conducted as part of the Illinois State Geological Survey's comprehen-
sive investigation to locate the most suitable site for the construction of the Superconducting
Super Collider, was carried out in two parts. The first part consisted of approximately 17 miles of
high-resolution seismic reflection profiling. The results of this profiling, together with information
gathered from available discrete drill holes, were used to define the stratigraphy and structural
geology of the site proposed for the SSC. The primary target of the seismic reflection profiling
was the dolomite of the Ordovician Galena and Platteville Groups, since the tunnel housing the
proposed SSC would have been located in these strata. The second part consisted of ap-
proximately 80 miles of seismic refraction profiling to examine the depth and configuration of the
bedrock surface, and the velocities of both the bedrock surface and the superjacent glacial drift
from which inferences can be made about the nature of these rocks. These kinds of information
were relevant not only to the construction of the SSC tunnel, but also to the location of its atten-
dant vertical service shafts.
The information gathered from the seismic exploration, although particularly relevant to the
proposed SSC, was beneficial for all of northeastern Illinois. The seismic reflection profiling
provided information applicable to the overall understanding of the stratigraphic and structural
relationships in northeastern Illinois. The seismic refraction profiling provided data that were usedto improve existing maps of depth to bedrock and bedrock geology, which are used in construc-
tion, evaluation of groundwater, aggregate (crushed stone), and sand and gravel resources, andlocation of waste disposal sites in this part of Illinois.
VI
I Seismic Reflection Profiling
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Figure 1 Location of seismic reflection lines.
Introduction
The Illinois State Geological Survey's comprehensive investigations to locate the most suitable
site for the construction of the Superconducting Super Collider (SSC), a proton accelerator, in-
cluded approximately 17 miles of high-resolution seismic reflection profiling at four discrete loca-
tions around the proposed ring (fig. 1). Since it was proposed that the SSC be place in a 10-foot
diameter tunnel in dolomites of the Ordovician Galena and Platteville Groups underlying the site,
these strata were the primary target of the seismic reflection profiling (fig. 2). In addition to infor-
mation on Ordovician strata, seismic reflection sections generated at three of the locations con-
tain information about sediments as old as Late Cambrian (Mt. Simon); a section generated at a
fourth location contains information about Precambrian-age rocks (fig. 2).
Two of the locations where seismic reflection profiling was done, along Dauberman Road in T38
and 39N, R6E, Kane County and near the Fermi National Accelerator Laboratory in T39N, R9E,
Du Page County (fig. 1), were chosen because experimental chambers associated with the SSC
were to be sited there. The other two locations, near the town of Bristol in T39N, R7E, Kendall
County, and near the town of Lily Lake in T40 and 41 N, R7E, Kane County (fig. 1), were chosen
to investigate the possibility of faulting. At the Bristol location, small-scale faulting was suspected
from the results of previous test drilling and geologic mapping in the area. At the Lily Lake loca-
tion, large-scale basement faulting had been suggested by McGinnis (1966), on the basis of main-
ly gravity and magnetic data.
The high-resolution seismic reflection data, gathered by Walker Geophysical Company of Essex,
Iowa, proved to be a viable way to address specific stratigraphic and geological structure
problems associated with the proposed location of the SSC, and also a way to obtain information
about the rocks of northeastern Illinois, unavailable from discrete drill holes.
Geologic Setting
The geologic setting of the area in northeastern Illinois where the high-resolution seismic reflec-
tion work was done has been discussed at length in previous geological-geotechnical studies for
siting the SSC in Illinois (Kempton et al. 1985; Vaiden et al. 1988). Geologic aspects from these
studies pertinent to the acquisition, reduction, and interpretation of the seismic reflection data are
discussed briefly in this report.
The study area is located on the Kankakee Arch, a broad positive structure that separates the
Michigan and Illinois Basins and connects the Wisconsin Arch to the Cincinnati and Findlay Ar-
ches (fig. 3). In the study area the Kankakee Arch plunges gently to the southeast.
Along the four seismic reflection lines, the elevation of the earth's surface varies from about 650
feet to just beyond 1 ,000 feet above mean sea level. Glacial drift, ranging in thickness from 25 to
more than 200 feet (fig. 4) overlies the Paleozoic bedrock surface (fig. 5). At some places the
bedrock surface is dissected by valleys that commonly contain thick, coarse-grained sediments
that serve as excellent conduits for shallow groundwater supplies. The presence of these valleys
and the contained groundwater were important factors to be considered in the location and con-
struction of the proposed SSC tunnel and attendant structures.
Bedrock in the study area consists of Cambrian, Ordovician, and Silurian strata that have a com-
bined thickness of approximately 4,000 feet (fig. 2). The oldest sedimentary rocks in the area
belong to the Mt. Simon Sandstone (Upper Cambrian). This poorly sorted, coarse-grained
sandstone, which ranges in thickness from 1 ,400 to 2,600 feet in northeastern Illinois, rests un-
conformably on Precambrian basement. Other major unconformities occur at the bases of the An-
cell Group (Ordovician) and the Silurian, and the bedrock surface (fig. 2). The Upper Ordovician
and Silurian formations in northeastern Illinois dip gently eastward into the Michigan Basin, but
the Cambrian and older Ordovician formations dip gently and thicken southward toward the Il-
linois Basin (Buschbach 1964). The bedrock surface of the study area (fig. 5) comprises Silurian
carbonates and shales and minor amounts of dolomite of the Maquoketa Group (Upper Or-
dovician).
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Figure 3 Regional geologic setting.
Field Techniques and Instrumentation
Field parameters for the high-resolution seismic reflection profiling were chosen on the basis of
calculation, experience, and testing. Since detailed structural and stratigraphic information was re-
quired for the construction of the proposed SSC tunnel, close-source and receiver spacing, high
common depth- point (CDP) fold, and a fast sample rate for wide-band recording were necessary
to obtain good quality data in noisy suburban areas. One line crossed an interstate highway, and
all lines ran along heavily traveled roads. The actual field parameters used are summarized in ap-
pendixes A, B, C, and D.
R 8 E R 9 E
100
R 4 E R 5 E
-1 50- contour interval 50 feet;
datum is mean sea level
.25- contour of 25 feet also shown 18 km.
Figure 4 Drift thickness map of the study area.
The recording instrument was a Texas Instrument DFSV. Single hydrophone receivers (Mark
Products P-44 1 Hz) were placed in shot holes about 1 feet below the water table, generally 1
to 25 feet below the ground surface. The energy source used on three of the lines (DaubermanRoad, Bristol, and Fermilab) was a downhole air gun (Bolt Model DHSS 550) equipped with a
chamber, 10 in.3
, operated at a nominal pressure of 1 ,800 lbs/in.2
. The optimum locations for
firing the air gun were at the top of the water table or a few feet deeper. On the fourth seismic
reflection line (Lily Lake), where information about Precambrian rocks was required, the energy
source was 0.33 to 1 .00 lbs. of dynamite.
Data Processing
Data processing sequences began with an amplitude spectrum analysis. Since frequencies morethan 400 Hz were at least -40dB, the data were resampled from 0.5 to 1 .0 milliseconds. Record
length was 1 .0 second, but on all lines except the Lily Lake line only 0.5 or 0.6 second wereprocessed. On the Lily Lake line, 1 .0 second was processed. Initial stacking velocities were
derived from available sonic logs. Subsequent stacking velocities were obtained from velocity
analysis of the seismic data. The seismic sections were not migrated. Additional information on
the data processing is given in appendixes A, B, C, and D.
PENNSYLVANIAN (shale, sandstone, limestone)
DEVONIAN (shale, sandstone, limestone)
SILURIAN (undiff.; dolomite)
ORDOVICIAN
T-] Maquoketa (shale)
2H Galena (dolomite)
10 mi
20 km
Figure 5 Geologic map of the study area.
E:::::i Platteville (dolomite)
Ijjjjjiij Ancell (sandstone)
fjgijgijj Prairie du Chien (sandstone and dolomite)
1 CAMBRIAN (undiff.; sandstone and dolomite)
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D 1985 Test Hole
A 1986 Test Hole
4t 8 in. Test Hole, 1986
Figure 6 Location of key drillholes used to constrain interpretation of seismic reflection sections.
Interpretation
A considerable amount of geologic information is available for the region in which these seismic
reflection lines were run. This information includes reports on local and regional studies con-
ducted by the ISGS, graduate student theses, logs and samples of water wells and engineering
borings in the ISGS files, and records of subsurface drilling and sampling programs conducted for
water resource studies of northeastern Illinois (Kempton et al. 1985; Vaiden et al. 1988). Studies
by Buschbach (1964), Willman (1973), Willman and Kolata (1978), Willman et al. (1975), Willman
and Frye (1970), Willman (1971), Horberg (1950), Kolata and Graese (1983), Lineback (1979),
Piskin and Bergstrom (1967, 1975), and Willman et al. (1967) were particularly useful in inter-
pretation of the seismic reflection sections.
Three 8-inch diameter holes near the Dauberman Road and Fermilab seismic reflection line were
included in the test drilling and coring program conducted for siting the SSC in Illinois (fig. 6). The8-inch diameter was chosen to accommodate sondes used in downhole geophysical logging.
Sonic and density logs were particularly important to the interpretation of the seismic reflection
sections. Sonic logs from the three 8-inch holes were used to calculate interval velocities (figs. 7,
Depth
(ft)
Elevation
above MSLVelocity (ft/sec)
(ft) 10000i
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Clay, poor samplesGravel, coarse (1??-140 ft)
Dolomite, argillaceous, gray blue; shale, dolomitic (140-180 ft)
Shale, dark olive gray (180-279 ft)
Dolomite, pale yellow brown, fine to medium grained
(279-510 ft)
Dolomite, light brown, fine grained (510-611 ft), bluish
(510-530 ft), grayer (535-611 ft)
Sandstone, fine to medium-grained (611-684 ft)
Sandstone, fine to medium grained, rounded; chert (684-940 ft); cemented sand;
shale partings (684 ft, 888-896 ft)
Chert, white; sandstone, white, cemented; dolomite, pink; shale, gray; (940-955 ft)
Kress Mbr L Chert, oolitic, gray; siltstone, brown, red; shale tan, brown, gray green (955-985 ft)
994 TD
-144Eminence Fm Dolomite, light pinkish tan, sandy (985-994 ft)
Figure 7 Stratigraphic column and interval velocities from test hole SSC-1
.
10
8, and 9). The sonic and density logs run in test hole SSC-2 near the Fermilab line were used to
construct a synthetic seismogram (fig. 10).
All the large-diameter test holes bottomed out just below the base of the Ancell Group. Holes
SSC-1 and SSC-3, near the Dauberman Road line, bottomed out in the Eminence Formation
(Upper Cambrian) and Oneota Formation (Lower Ordovician), respectively; SSC-2, near the Fer-
milab line, bottomed out in the Shakopee Formation (figs. 7, 8, and 9). Because proposed ex-
perimental chambers were to be located along Dauberman Road and near Fermilab, the large
diameter holes were drilled only to depths necessary to provide information about the tunnel andthe experimental chambers.
Velocity and density information useful in interpreting the portions of the seismic reflection sec-
tions deeper than the base of the Ancell came from sonic and density logs. These logs were run
in 1986 in a deep hole that penetrated basement in Section 9, T39N, R9E, in Du Page County,
just a few miles from the north end of the Fermilab seismic reflection line (fig. 1 1). As mentioned
above, the Dauberman Road, Bristol, and Fermilab sections provided information about the rock
to the depth of the Mt. Simon Formation (Upper Cambrian), whereas the Lily Lake section
provided information to the depth of Precambrian rocks.
On the seismic reflection sections shown in this report (figs. 12, 13, 14, and 15), several reflec-
tions were associated with geologic interfaces where large acoustic impedance contrasts are
known to exist. The strength, coherence, and continuity of these reflections can vary appreciably
for several reasons, many of which are geologically significant. However, given the proximity of
the seismic reflection lines in this study, enough of these reflections can be consistently traced
across these sections to interpret confidently the salient stratigraphic and structural nature of the
geologic formations.
Dauberman Road Seismic Reflection Line
The seismic reflection line along Dauberman Road in T38 and 39, R6E, Kane County, Illinois
(figs. 1 and 1 2) was shot from north to south in three segments, D1 , D2, and D3; their lengths
were 1 .47, 1 .82, and 4.68 miles, respectively. Because parts of the segments overlapped, the
total line was approximately 7.5 miles long.
Field parameters and the processing sequence for each segment of the Dauberman Road line
are given in appendix A. Although the record length for each segment was 1 .0 second, only 0.5
second was processed for the segments D1 and D2, and only 0.6 second was processed for seg-
ment D3. These section lengths were adequate given the purpose of this line, which was to ex-
amine the Ordovician strata in which the experimental chambers were to be constructed. Thesesections do not contain information about the lower Mt. Simon Formation (Upper Cambrian) or
subjacent Precambrian rocks.
Topographic elevation of the earth's surface along the Dauberman Road line, although somewhatirregular, generally decreases from a high of approximately 840 feet above mean sea level near
the north end of segment D1 to a low of approximately 700 feet above sea level near the south
end of segment D3.
The glacial drift along this line varies in thickness from more than 100 feet to as much as 200 feet
(Piskin and Bergstrom 1975). Test holes SSC-1 and SSC-3 near the north and south ends of this
line showed glacial drift thicknesses of 140 and 133 feet, respectively. Greater drift thicknesses
may be associated with bedrock valleys, which are common in northeastern Illinois.
The bedrock surface along this line is, for the most part, composed of rocks of the MaquoketaGroup (Upper Ordovician) and Silurian outliers (Willman et al. 1967); therefore, shales and car-
bonates can be expected at the bedrock surface. Test holes SSC-1 and SSC-3 encountered Ma-quoketa dolomite, probably the Ft. Atkinson, at the bedrock surface (Vaiden et al. 1988).
On the Dauberman Road sections, reflections have been identified at the following geologic inter-
faces, in descending order: bedrock surface, top of the Galena Group (Middle to Upper Or-
dovician), top of the Ancell Group (Middle Ordovician), base of the Ancell Group, top of the
11
Depth
(ft)
Elevation
above MSL(ft)
Velocity (ft/sec)
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Clay, gray, coarse, sandy silty, with sand seams (0-46 ft, 52-68 ft)
Sand, coarse gravel (46-52 ft)
Clay, brown, sandy silty, with sand and gravel (68-81 ft)
Dolomite (81-210 ft), light gray brown, fine grained, speckledblack (90-115 ft) glauconitic (170-180 ft); clay present (gray
and blue green), browner near base (160-210 ft), particularly
(190-210 ft)
Dolomite, light medium gray to blue gray, fine grained, argillaceous
(210-250 ft)
Dolomite, dark olive brown gray, very argillaceous; shale, similar
color, dolomitic (250-295 ft)
Shale, dark olive gray, dolomitic (295-365 ft)
Dolomite, pale yellow brown, fine grained; shale partings,
blue green common, black brown partings less common(365-570 ft)
Dolomite, pale yellow brown, some shale partings, blue
green; chert, white (570-686 ft)
Sand, fine to medium grained; rounded dolomite, some rare (686-897 ft)
Dolomite, light brown, fine grained; shale, blue green (897-920 ft)
Dolomite, light brown, fine grained; chert, white; pyrite rare (920-1000 ft)
Sand, fine to medium grained, rounded, floating grains, some cementedwith calcite (1000-1035 ft)
Dolomite, light brown; chert, white (rare to common); sand present in
some horizons (1035-1080 ft)
1080 TD
Figure 8 Stratigraphic column and interval velocities from test hole SSC-2.
12
Depth
(ft)
Elevation
above MSL(ft)
Velocity (ft/sec)
100-
200-
300fiT^-
400-
500-
600-
700-
800-
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Clay, brown gray, sandy, silty (0-42 ft)
Sand, gravel, fine to coarse (42-128 ft)
Clay, brown gray, sandy (128-133 ft)
Dolomite, very argillaceous; shale, dolomitic, gray
brown (133-170 ft)
Shale, dolomitic, brown to olive brown (170-219 ft)
Dolomite, pale yellow brown, fine to medium grained
(219-435 ft) ; blue green, gray shale partings, calcareous
(275-400 ft)
Dolomite, light brown (435-544 ft), occasionally bluish,
dark brown (435-460 ft, 475-510 ft) fine grained
Sandstone, fine to medium grained, rounded (544-630 ft)
Sandstone, fine to medium grained, rounded; chert (630 851 ft)
Shale partings, light gray (765-815 ft), green blue (830-851 ft)
Dolomite, deep pink brown, fine grained, thin horizons (835-851 ft)
Dolomite, light pink-gray-brown, fine to medium grained; chert, white,
rare (851-903 ft); glauconite (895-903 ft)
Figure 9 Stratigraphic column and interval velocities from test hole SSC-3.
13
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ZERO-PHRSE5- 8-310-320 HZ
ZERO-PHRSE5- 8-270-280 HZ
ZERO-PHRSE5- 8-230-240 HZ
ZERO-PHRSE5- 8-190-200 HZ
Figure 10 Synthetic seismogram constructed from sonic and density logs.
Franconia Formation (Upper Cambrian), and top of the Lombard Member of the Eau Claire For-
mation (figs. 1 and 12). No discernible reflections were below 0.4 second. This two-way travel
time would correspond to a reflection emanating from a surface below the top of the Mt. SimonFormation (Upper Cambrian). The absence of reflections below 0.4 second possibly was due to a
lack of energy provided by the air-gun energy source or, more likely, it was the result of an ab-
sence of appreciable vertical impedance contrasts in the Mt. Simon.
The shallow reflection corresponding to the drift-bedrock contact can be traced intermittently
across sections D1 , D2, and D3. The quality of this reflection is dependent not only on the lithol-
ogy of the bedrock surface (carbonates and elastics), but also on the amount of weathering on
this surface. Between shot points 355 on section D1 and shot point 105 on section D2 (figs. 1 and
14
Velocity (ft/sec)
10000I
741
500
0-
-500-
-1000-
</>
o
-1500
-2000 -
-2500 -
-3000 -
-3500 -1
20000I
— Ground surface— Silurian
Maquoketa
Galena
Platteville
Glenwood-St. Peter
Potosi
Franconia
Ironton
Galesville
Eau Claire
— Mt. Simon
— Precambrian
Figure 1 1 Interval velocities from deep hole in Du Page County.
15
1 COca>
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Eo
y
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CO
CDoc
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ca
-O
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re
J--4
Willi-MM-mtA hiMmmmm
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co5
a> !_
(001
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77
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vmvtvwKi-MBER.ftM.k^KWi^^^^rjiow'3H f w-toc
»
CO
cCO oc
CDOc
oa) cCO CO
< LL
<0
c "OCU o CO1_ o .oU> o c FCD c oO < LL _J
'ewa>v>
_ro
|
CO
CD
3O)LL
rs
Murstproperty
?90 260 270 260 250
Maquoketa
Galena
Ancell
Shakopee
Franconia
Lombard
Bristol No. 1
Sec. ?<e ?3e j?b ?ia aee 19B iee pb i6B isb hb
Maquoketa
Galena
Ancell
Shakopee
Franconia
Lombard
Bristol No. 3
Figure 1 4 Bristol seismic reflection sections.
12) was evidence of a channel cut into the bedrock, although this evidence was disturbed bymuting associated with undershooting where the line crossed the East-West Tollway.
The reflection associated with the Maquoketa-Galena contact was consistently the strongest,
most coherent, and most continuous of all reflections on sections D1 , D2, and D3. This was aresult of the sharp contrast between the relatively low acoustic impedance Maquoketa elastics
that rest on the relatively high acoustic impedance Galena carbonates. The Maquoketa-Galenacontact and Platteville-Ancell Group contact were the two most important targets for the SSCproject, because the SSC tunnel was to be constructed in the Galena and Platteville Groups. Thereflection associated with the Platteville-Ancell contact could be followed easily across sectionsD1
,D2, and D3 even though it had reverse polarity from, and less strength than, the reflection at
the Maquoketa-Galena contact because of a downward decrease in acoustic impedance with lesscontrast than at the Maquoketa-Galena surface.
19
CO _ nj
* 8en J3o E
to c o oes < a. _i
oCL
OECO
"<Dco
CD^.ro
w
3
20
Examination of sections D1 , D2, and D3 (fig. 12) indicate that the combined thicknesses of the
Galena and Platteville Groups do not vary appreciably along the entire length of the DaubermanRoad line. This fact is corroborated by the combined thicknesses (332 and 325 feet, respectively)
of these groups in test holes SSC-1 and SSC-3 near the ends of this line. A southern component
of dip appears to be on the rocks comprising of these groups along the Dauberman Road line.
The dip is corroborated by the elevations of the tops (562 and 469 feet above mean sea level,
respectively) and bottoms (230 and 144 feet above mean sea level, respectively) of these Groups
in test holes SSC-1 and SSC-3. Some of the decrease in elevation of the rocks of the Galena and
Platteville Groups between the north and south ends of the Dauberman Road line is the result of
a small normal fault, downthrown to the south between shot points 840 and 850 on section D2(figs. 1 and 12).
The next reflection on sections D1 , D2, and D3, in order of increasing two-way travel time, cor-
responds to the unconformity at the base of the Ancell Group (fig. 2). In the study area, the St.
Peter Sandstone may rest unconformably on rocks as young as the Shakopee Dolomite of the
Prairie du Chien Group (Lower Ordovician) and as old as the Franconia Sandstone Formation
(Upper Cambrian) (Buschbach 1964). Test holes SSC-1 and SSC-3 at the north and south ends
of the Dauberman Road line encountered the Eminence Dolomite (Lower Cambrian) and the
Oneota Dolomite, respectively, below the St. Peter. The quality of the reflection emanating from
this unconformity is inconsistent. In some places, the reflection is strong and coherent, indicating
a sharply defined surface where the St. Peter, resting on unweathered carbonates, provides a
sizeable acoustic impedance contrast. In other places, where the reflection becomes weak and in-
coherent, the St. Peter may be resting on rubble and/or formations with similar acoustic proper-
ties.
Along the Dauberman Road line, the exact location where rocks of the Prairie du Chien Group ter-
minate on the subjacent Eminence Formation is difficult to determine. However, the northerly dip-
ping reflection at shot point 1350 on section D3 (figs. 1 and 12), which apparently corresponds to
the top of the Oneota Formation, together with cycle terminations farther north at shot points 1050
and 920, are indicative of the northernmost extent of the Prairie du Chien Group. Due to the un-
conformity at its base, the thickness of the Ancell Group in the study area varies. This is also the
case along the Dauberman Road line.
Below the sub-St. Peter unconformity were several significant reflections in Cambrian strata. Near0.220 second at the north end of section D1 (figs. 1 and 12) is a reflection corresponding to the
contact between the Potosi Dolomite and the Franconian Sandstone. This reflection, which ex-
hibits negative polarity, can be followed to the south well into section D3 (fig. 12), where it be-
comes discontinuous. At approximately 0.295 second at the north end of section D1 is a strong
reflection that corresponds to the top of the Lombard Dolomite Member of the Eau Claire Forma-
tion. This reflection could be followed easily on most of sections D1 , D2, and D3, although it
diminished in strength near the south end of the section D3 (fig. 1 2). The top of the Lombardalong the Dauberman Road line dips slightly to the south.
In addition to the previously mentioned small normal fault near shot point 850 in section D2 (figs.
1 and 12), a second small normal fault that cuts strata older than the St. Peter appears to be near
shot point 610 on section D3 (figs. 1 and 12). The only other structure of significance along the
Dauberman Road line occurs between shot point 55 and 155 on Section D2 near the East-WestTollway (figs. 1 and 12), where strata older than the St. Peter appear to have been downwarpedsignificantly prior to deposition of the St. Peter.
Fermilab Seismic Reflection Line
The seismic reflection line at Fermilab in T39N R9E, Du Page County, Illinois (figs. 1 and 13) wasshot from north to south in three segments, NAL-1 , NAL-2, and NAL-3; lengths were 0.64, 0.43,
and 2.08 miles, respectively. Because some segments overlapped, the total length of the line wasapproximately 3.1 miles.
21
Field parameters and the processing sequence for each segment of the Fermilab line are given in
appendix B. Although the recorded length for each segment was 1 .0 second, only 0.5 secondwas processed for segments NAL-1 and NAL-2 and only 0.6 second for segment NAL-3 (fig. 13).
Like section 1 of the Dauberman Road seismic reflection line, the recorded lengths of the Fer-
milab sections were adequate for the intended purpose of this line, which was to examine the Or-
dovician strata in which the SSC experimental chambers were to be constructed. Like the Dauber-man Road sections, the Fermilab sections do not contain information about the lower Mt. Simonand Precambrian rocks.
Surface elevations along the Fermilab seismic reflection line range from 730 to 750 feet abovemean sea level with no discernible trend. Glacial drift thickness varies from 50 to 100 feet (Piskin
and Bergstrom 1975). The bedrock surface is composed entirely of Silurian age-rocks (Willman et
al. 1975; fig. 5).
The general quality of the seismic reflection data along the Fermilab line is fair. The quality is
poor where noise levels from large pumps and compressors in the experimental area of Fermilab
adversely affected the data. Reflections from the bedrock surface generally are inconsistent anddifficult to follow. Test hole SSC-2 (fig. 6) near the south end of the Fermilab line shows that
Silurian dolomite rests directly on Maquoketa Dolomite, and gradually changes to shale at the
base of the Maquoketa. With no sharp lithologic break between the Silurian and Ordovician strata
and a gradual decrease in seismic velocity through the transition from dolomite to shale within the
Maquoketa (fig. 8), a strong reflection is not possible from the top of or within the MaquoketaGroup. The reflection corresponding to the Maquoketa-Galena contact, although generally weak,
can be followed across sections NAL-1 , NAL-2, and NAL-3 (fig. 13). The reflection from the top of
the Ancell Group is, for the most part, coherent and consistent. On the basis of information col-
lected from test hole SSC-2, the Fermilab section NAL-3 shows St. Peter resting on Shakopee at
the south end of the Fermilab line. The tops of the Franconia, Proviso, and Lombard Dolomite are
easy to follow for a short distance, but farther to the south, although strong and coherent for short
distances, they become discontinuous and difficult to follow. On section NAL-1 a noteworthy
reflection emanates from the contact between the Galesville Sandstone Formation and the
Proviso Siltstone Member of the Eau Claire Formation (the top of the Eau Claire). The upper part
of the Proviso can be dolomitic (Buschbach 1964). This would be the case along section NAL-1,
where a strong acoustic impedance contrast suggests a clastic-carbonate interface between the
Galesville Sandstone and the Proviso Siltstone Member.
Along the Fermilab line most of the rocks show a slight southern component of dip. The thickness
of the Galena-Platteville Groups, 221 feet in test hole SSC-2 near the south end of segment NAL-
3, remains almost constant.
Between shot points 150 and 160 on section NAL-1 (figs. 1 and 13), the reflections associated
with the Prairie du Chien Group and the Franconia Formation exhibit evidence of a small reverse
fault upthrown on the north. Faulting cannot be traced into the overlying Ancell Group, nor can it
be traced into the Franconia Formation for a significant distance. Deeper reflections exhibit
evidence of upwarping in the lower strata south of the fault, indicative of a different, but neverthe-
less, consistent reaction to lateral compressive stresses.
Bristol Seismic Refraction Line
The Bristol seismic reflection line in T37N, R7E, Kendall County, Illinois (figs. 1 and 14) was shot
in a north-south direction in two segments, BR-1 and BR-3. The segments are 0.96 and 0.60 mile
long, respectively, for a total of 1 .56 miles.
Field parameters and the processing sequence for each segment of the Bristol line are given in
appendix C. The recorded length for each segment was 1 .0 second, but only 0.5 second wasprocessed for segment BR-1 and only 0.6 second for segment BR-3. The Bristol line was used to
examine the continuity of the Galena-Platteville rocks in this area. Small-scale faulting in the
Galena-Platteville was suspected on the basis of drilling and sampling in nearby test holes. Like
the Dauberman Road and Fermilab seismic sections, the Bristol sections only provided informa-
22
tion about strata as deep as the upper part ot the Mt. Simon. Although the same datum and sub-
weathering velocity were used in processing the data of seismic sections BR-1 and BR-3 (fig. 14),
a correction factor of 0.071 second was added to the datum correction of section BR-1 . Thus
reflections indicated on the BR-1 section will have two-way travel times, apparently 0.071 second
greater than their counterparts in section BR-3.
Topographic relief on the earth's surface is small along the Bristol line, ranging from just over 660
feet to just below 650 feet above mean sea level. The thickness of the glacial drift along the Bris-
tol line varies between 25 and 100 feet (Piskin and Bergstrom 1975). The bedrock surface is com-
posed of carbonates of the Maquoketa Group at the north end of segment BR-1 and shales andcarbonates of the Maquoketa Group elsewhere on this line (Willman et al. 1967) (fig. 5).
At a two-way travel time of approximately 0.190 second on seismic reflection section BR-1 (fig.
14), a reflection is interpreted as the top of the Maquoketa. This reflection becomes morecoherent and continuous on section BR-3 (fig. 14) to the south where rocks of the MaquoketaGroup form the bedrock surface. Between this reflection and the strong reflection associated with
the top of the Galena (at about 0.220 second on section BR-1), short, discontinuous reflections,
likely associated with the Ft. Atkinson Limestone (Maquoketa Group), can be seen. The reflection
associated with the top of the Ancell Group is of lesser quality, but continuous and traceable. Thereflection associated with the top of the Ancell Group occurs at about 0.250 second on section
BR-1 . At about 0.290 second on BR-1 is a reflection corresponding to the top of the Prairie du
Chien Group (Ordovician). Rocks as young as the Shakopee Dolomite may form the surface of
the unconformity at the top of this group (Buschbach 1964). Other notable reflections on BR-1 are
associated with the tops of the Franconia Sandstone (0.330 second) and the Lombard Dolomite
Member of the Eau Claire Formation (0.410 second). The reflection seen at about 0.330 second
on the section BR-3 may correspond with the top of the Proviso Siltstone Member of the EauClaire.
All reflections noted above generally are parallel, which is indicative of little or no thickening of
strata along this short line. Evidence of a slight southern component of dip is on much of the
strata along the Bristol line, but no evidence of faulting exists along the line.
Lily Lake Seismic Reflection Line
The Lily Lake seismic reflection line in T40 and 41 N, R7E, Kane County, Illinois was shot in a
north-south direction along Highway 47 through the town of Lily Lake (figs. 1 and 15). The line
was approximately 4.22 miles long.
Field parameters and the processing sequence for this line are given in appendix D. Significant
changes made on the Lily Lake line included dynamite (0.33 to 1 .00 lb.) as the energy source and
a recorded length of 2.0 seconds. Processing length was 1 .0 second, enough time to include infor-
mation about Precambrian rocks. This line was shot to examine the shallow Ordovician targets as-
sociated with the construction of the SSC tunnel and to determine the presence or absence of
large-scale basement faulting in this region, which had been suggested by McGinnis (1966)
primarily on the basis of interpretations of potential field data. The 1 .0-second length of the seis-
mic reflection section LL-1 (fig. 1 5) was adequate for both purposes.
Surface elevations on the Lily Lake line range from just over 1 ,010 feet above mean sea level at
the northern end to about 880 feet above mean sea level near its southern end. The thickness of
the glacial drift under the Lily Lake line is approximately 200 feet (Piskin and Bergstrom 1975).
The bedrock surface along this line is composed entirely of rocks belonging to the MaquoketaGroup (Willman et al. 1967; fig. 5).
The quality of the seismic reflection data on the Lily Lake line generally is good. Near the top of
the LL-1 section (fig. 15), a strong reflection between 0.040 and 0.050 second likely correspondsto the Ft. Atkinson Limestone of the Maquoketa Group (Ordovician). In some places, the Ft. Atkin-
son Limestone appears to form the bedrock surface. Where it does not, a shallower reflection
above it appears to be associated with the bedrock surface, perhaps composed of youngerBrainard Formation shales. At 0.070 second is a strong reflection associated with the top of the
23
Galena. At 0.035 to 0.40 second below the top of the Galena reflection is a weaker but con-
tinuous reflection corresponding to the top of the Ancell Group. The parallelism of these latter tworeflections indicates the uniform thickness of the Galena-Platteville Group along LL-1 . A slight
southern component of dip is on rocks of the Galena-Platteville Group on the Lily Lake line. At
about 0.165 second at the southern end of section LL-1 , a strong reflection is associated with the
sub-St. Peter contact. This reflection likely emanates from the St. Peter resting on the Potosi
Dolomite, but a deep hole at St. Charles, Illinois, about ten miles east of the southern end of the
LL-1 line, encountered the Franconia Sandstone below the St. Peter (Buschbach 1964). Wherethe reflection from this surface is strong, the Potosi is likely present at the surface of the unconfor-
mity. Where the reflection is weak, the Franconia, which has less acoustic impedance than the
Potosi, is present, or perhaps the Potosi is present, but with a rubble zone between it and the
overlying St. Peter (Buschbach 1964). The very strong reflection at about 0.270 second cor-
responds to the top of the Lombard Dolomite. Along this line, the Lombard appears to be about
200 feet thick and flat lying. Below the Lombard reflection, the seismic section appears devoid of
continuous reflections down to 0.640 seconds. This void corresponds to the predominately clastic
rocks of the lower Eau Claire and Mt. Simon Formations. Occasionally, weak, short reflections
occur near the base of the Mt. Simon, probably because of weak bedding or zones of especially
dense cementation.
The basement surface, indicated by the strong reflection at about 0.640 second, also appearsrelatively flat lying along the Lily Lake line. Within the basement rocks no evidence of the large-
scale basement faulting suggested by McGinnis (1966) exists.
Conclusions
The high-resolution seismic reflection profiling at four discrete locations around the proposed
SSC ring proved to be viable in answering questions about the stratigraphy and structural geol-
ogy at those locations, as well as providing significant insight into the geologic history of north-
eastern Illinois. The seismic reflection profiling provided considerably more information than pre-
vious geological and geotechnical studies, which relied on drill holes and downhole logging.
With the exception of a few interpreted minor faults, carbonate rocks of the Galena and Platteville
Groups are relatively flat lying and uniform in thickness and lithology. This consistent stratigraphic
relationship was desirable along the Dauberman Road and Fermilab lines (figs. 1,12, and 13)
where the chambers of the proposed SSC were to be located.
The seismic reflection sections near Bristol (figs. 1 and 1 4) showed no evidence of faulting in the
rocks extending from the bedrock surface to the upper Cambrian. The results of previous test drill-
ing and geologic mapping suggested the possibility of small-scale faulting in the Bristol area.
The Lily Lake seismic reflection section (figs. 1 and 15), which showed a strong, continuous reflec-
tion at the basement surface and provided information about basement rocks, did not showevidence of large-scale basement faulting interpreted from potential field data by McGinnis
(1966).
A downwarping of strata below the St. Peter Sandstone (fig. 12) and a small reverse fault that
cuts strata from the top of the Prairie du Chien Group down to the top of the Franconia Sandstone(fig. 1 3), are indicative of a compressive event across the study area prior to the deposition of the
St. Peter.
A zone of small, parallel, high-angle normal faults that extend from the bedrock surface well into
the Cambrian strata (fig. 12) is indicative of a tensional event younger than the Silurian Ma-quoketa rocks comprising the bedrock surface.
The seismic reflection sections were particularly useful in examining the deeper rocks of the study
area because of the paucity of deep drill holes. The nature of the unconformable surface at the
base of the Ancell Group can be observed on sections from all four seismic reflection lines (figs.
12, 13, 14, and 15). The basement surface on the Lily Lake seismic section (fig. 15) yields a
reflection as strong and continuous as anywhere else in the state.
24
References
Buschbach, T. C, 1964, Cambrian and Ordovician strata of northeastern Illinois: Illinois State
Geological Survey, Report of Investigations 218, 90 p.
Horberg, L, 1950, Bedrock topography of Illinois: Illinois State Geological Survey Bulletin 73,
111 p.
Kempton, J. P., R. C. Vaiden, D. R. Kolata, P. B. DuMontelle, M. M. Killey, and R. A. Bauer,
1985, Geological-geotechnical studies for siting the Superconducting Super Collider in Illinois:
Preliminary geological feasibility report: Illinois State Geological Survey Environmental Geology
Notes 1 1 1 , 63 p.
Kolata, D. R., and A. M. Graese, 1983, Lithostratigraphy and depositional environments of the
Maquoketa Group (Ordovician) in northern Illinois: Illinois State Geological Survey Circular
528, 49 p.
Lineback, J. A., 1979, Quaternary deposits of Illinois: Illinois State Geological Survey map.
McGinnis, L. D., 1966, Crustal tectonics and Precambrian basement in northwestern Illinois:
Illinois State Geological Report of Investigations 219, 29 p.
Piskin, K., and R. E. Bergstrom, 1967, Glacial drift in Illinois: Thickness and character: Illinois
State Geological Survey Circular 41 6, 33 p.
Piskin, K., and R. E. Bergstrom, 1975, Glacial drift in Illinois: Thickness and character: Illinois
State Geological Survey Circular 490, 35 p.
Vaiden, R. C, M. J. Hasek, C. R. Gendron, B. B. Curry, A. M. Graese, and R. A. Bauer, 1988,
Geological-geotechnical studies for siting the Superconducting Super Collider in Illinois: Results
of drilling large-diameter test hole in 1986: Illinois State Environmental Geology Note 124, 58 p.
Walker, C, Jr., 1988, Shallow seismic profiling for a tunnel site near Chicago, Paper presented at
58th Annual International Meeting and Exhibition: Society of Exploration Geophysics, Anaheim,
CA, Oct. 30-Nov. 3, 1988, 9 p.
Willman, H. B., J. C. Frye, J. A. Simon, K. E. Clegg, D. H. Swann, E. Atherton, C. Collinson, J. A.
Lineback, and T. C. Buschbach, 1967, Geologic Map of Illinois: Illinois State Geological Survey.
Willman, H. B., and J. C. Frye, 1970, Pleistocene stratigraphy of Illinois: Illinois State Geological
Survey Circular 94, 204 p.
Willman, H. B., 1971 , A summary of geology in the Chicago area: Illinois State Geological Survey
Circular 460, 77 p.
Willman, H. B., 1973, Rock stratigraphy of the Silurian Systems in northeastern and northwestern
Illinois: Illinois State Geological Survey Circular 479, 55 p.
Willman, H. B., E. Atherton, T. C. Buschbach, C. Collinson, J. C. Frye, M. E. Hopkins, J. A.
Lineback, and J. A. Simon, 1975, Handbook of Illinois stratigraphy, Illinois State Geological
Survey Bulletin 95, 261 p.
Willman, H. B., and Kolata, D. R. 1978, The Platteville and Galena Groups in northern Illinois:
Illinois State Geological Survey Circular 502, 75 p.
25
Appendix A Dauberman Road Field Parametersand Processing Sequence
Segment D-1
Field Parameters
Recording instruments
Record length
Sample rate
Tape format
Number of channels
Energy sourceSource interval
DFSV1 .0 sec.5 msSEGB72
Airgun
27.5 ft
Hydrophone P44Receiver type
Receivers per group
Standard configuration Split spreadFeet 1017.5-27.5 Sp 27.5-1017.5 feet
Recorded by
Date recorded
Walker Geophysical Co.
1 2/86-2/87
Processing Sequence
1. Demultiplex and QC display
2. Spherical divergence and gain recovery
3. Trace editing
4. Deconvolution type: band limited
No. of gates 1
Design type average autocorrelation
Frequency 70-300 HzOperator length 51 msWhite noise 50% outside
0% inside
5. Source and receiver datum correction
Datum 830 ft
VR 6500 ft/sec
6. Common depth point gather
7. Velocity analysis via Digicon's Velfan
8. Brute stack
9. Residual static correction
10. Velocity analysis via Digicon's Velfan
1 1
.
Residual static correction
1 2. Normal moveout correction
13. Mute14. Trace equalization
1 5. Common depth point stack 36 fold
1 6. Signal to noise enhancement (TAU-P method)1 7. Digital filter type: bandpass
Frequency Time90-200 Hz 0.000 sec80-180 Hz 0.250 sec70-1 60 Hz 0.500 sec
1 8. Trace equalization
19. Film display
Polarity convention
Segment D-2
Field Parameters
Recording instruments
Record length
Sample rate
Tape format
Number of channels
Energy sourceSource interval
Receiver type
Receivers per group
Standard configuration
Feet 1017.5-27.5 Sp
Recorded by
Date recorded
DFSV1 .0 sec.5 msSEGB72
Airgun
27.5 ft
Hydrophone P441
Split spread27.5-1017.5 feet
Walker Geophysical Co.
1 2/86-2/87
Processing Sequence
1. Demultiplex and QC display
2. Spherical divergence and gain recovery
3. Trace editing
4. Deconvolution type: band limited
No. of gates 1
Design type average autocorrelation
Frequency 70-300 HzOperator length 51 msWhite noise 50% outside 0% inside
5. Source and receiver datum correction
Datum floating
VR 6500 ft/sec
6. Common depth point gather
7. Velocity analysis via Digicon's Velfan
8. Brute stack
9. Residual static correction
1 0. Velocity analysis via Digicon's Velfan
1 1
.
Residual static correction
1 2. Normal moveout correction
13. Mute1 4. Trace equalization
1 5. Common depth point stack 36 fold
1 6. Signal to noise enhancement (TAU-P method)1 7. Digital filter type: bandpass
Frequency Time90-200 Hz 0.000 sec80-180 Hz 0.250 sec70-1 60 Hz 0.500 sec
18. Trace equalization
19. Final datum correction
Datum 830 ft
VR 6500 ft/sec
20. Film display
Polarity convention
All data processing techniques used have maintained the recording polarity.
Normal polarity, a positive number, will be a filled peak; a negative number will be a trough (SEGY standard).
Processed by Digicon Geophysical Corp.
Houston Processing Center
Land Department
26
Segment D-3
Recording Parameters
Field acquisition
Date recorded
Field reel numbersNo. of shots on line
Recording instruments
Recording filter
NotchRecord length
Sample rate
No. of channels
Tape format
Direction of shooting
Energy source
Receiver
Source interval
Group interval
Spread
Walker Geophysical
Aug. 12-Sept. 28, 19871-11
1105DFSVLow 90 high 51 2 HzOut1 sec.5 ms72 (3x24)
SEGBN-SAirgun
P44 1 Hz22 ft
22 ft
792-22-Sp-22-770
Processing Sequence
1. Demultiplex
2. Minimum phase anti-alias filter application
3. Resample to 1 ms4. Spherical divergence
5. Display field records
6. Trace editing
7. Source and receiver static correction
Datum floating
VR 6500 ft/sec
8. Common depth point gather
9. Initial velocity analysis
10. Residual statics application
11. Spectral equalization
Frequency 70-250 Hz12. Velocity analysis
13. Residual statics application
Frequency dependent1 4. Normal moveout correction
15. Early mute1 6. Trace equalization
1 7. Common depth point stack 36 fold
1 8. Deconvolution Type: band limited
Gap length 5 msFrequency 70-250 HzWhite noise 50% outside 0% inside
Design gate 0.40-0.400 sec
19. Signal to noise enhancement20. Digital filter Type: bandpass
Time (sec) Frequency (Hz)
0.0-0.07 80-240
0.095 80-200
0.350 70-1800.600 70-140
21 Trace equalization
22 Final datum correction
Datum 830 ft
VR 6500 ft/sec
23. Film display
30 TPI 20 IPS (1 in = 330 ft)
Polarity convention
Appendix B Fermilab Parameters andProcessing Sequence
Segment NAL-1
Recording Parameters
Field acquisition
Date recorded
Field reel numbersNo. of shots on line
Recording instruments
Recording filter
NotchRecord length
Sample rate
No. of channelsTape format
Direction of shooting
Energy source
Receiver
Source interval
Group interval
Spread
Walker GeophysicalOct. 26-Nov. 28, 198713,14
153DFSVLow 90 high 51 2 HzOut1 sec.5 ms72 (3x24)
SEGBN-SAirgun
P44 1 Hz22 ft
22 ft
792-22-Sp-22-770
Processing Sequence
1. Demultiplex
2. Minimum phase anti-alias filter application
3. Resample to 1 ms4. Spherical divergence
5. Display field records
6. Trace editing
7. Source and receiver static correction
Datum 700 ft
VR 6500 ft/sec
8. Common depth point gather
9. Initial velocity analysis
1 0. Residual statics application
1 1
.
Spectral equalization
Frequency 70-250 Hz1 2. Velocity analysis
13. Residual statics application
Frequency dependent1 4. Normal moveout correction
1 5. Early mute1 6. Trace equalization
1 7. Common depth point stack 36 fold
1 8. Deconvolution Type: band limited
Gap length 5 ms.
Frequency 70-250 HzWhite noise 100% outside 0% inside
Design gate 0.080-0.400 sec19. Signal to noise enhancement20. Digital filter Type: bandpass
Time (sec) Frequency (Hz)
0.0-0.07 80-240
0.095 80-200
0.350 70-1800.600 70-140
21
.
Trace equalization
22. Film display
30 TPI 20 IPS (1 in = 330 ft)
Polarity convention
27
Segment NAL-2
Recording Parameters
Field acquisition
Date recorded
Field reel numbersNo. of shots on line
Recording instruments
Recording filter
Notch
Record length
Sample rate
No. of channelsTape format
Direction of shooting
Energy source
Receiver
Source interval
Group interval
Spread
Walker Geophysical
Nov. 22, 198717104DFSVLow 90 high 512 HzOut1 sec
.5 ms72 (3x24)
SEGBNW-SEAirgun
P44 1 Hz22 ft
22 ft
792-22-Sp-22-770
Processing Sequence
1. Demultiplex
2. Minimum phase anti-alias filter application
3. Resample to 1 ms4. Spherical divergence
5. Display field records
6. Trace editing
7. Source and receiver static correction
730 ft
6500 ft/sec
Type: Spiking
Offset Gate50 ms - 400 ms
310 ms- 500 ms
DatumVR
8. Deconvolution
Design gate
15849. Common depth point gather
1 0. Initial velocity analysis
1 1
.
Residual statics application
1 2. Secondary velocity analysis
13. Trim statics
14. Final velocity analysis
15. Residual statics application
Frequency dependent1 6. Normal moveout correction
1 7. Early mute18. Trace equalization
19. Common depth point stack 36 fold
20. Deconvolution Type: band limited
Gap length 6 msFrequency 70-250 HzWhite noise 1 00% outside 0% inside
Design gate 0.20-0.340 sec
21
.
Signal to noise enhancement22. Digital filter Type: bandpass
Time (sec) Frequency (Hz)
0.0-0.07 80-240
0.095 80-200
0.350 70-180
0.500 70-14023. Trace equalization
24. Final datum correction
Datum 700 ft
VR 6500 ft/sec
25. Film display
30 TPI 20 IPS (1 in = 330 ft)
Polarity convention
Segment NAL-3
Recording Parameters
Field acquisition Walker GeophysicalDate recorded Dec. 5, 1987-Jan.30, 19Field reel numbers 18-24
No. of shots on line 494Recording instruments DFSVRecording filter Low 90 high 512 HzNotch OutRecord length 1 sec
Sample rate .5 msNo. of channels 72 (3x24) and 96 (4x24)
Tape format SEGBDirection of shooting NNE-SSWEnergy source Airgun
Receiver P44 1 HzSource interval 22 ft
Group interval 22 ft
72 channel spread 792-22-Sp-22-770
96 channel spread 1056-22-Sp-22-1056
Processing Sequence
1. Demultiplex
2. Minimum phase anti-alias filter application
3. Resample to 1 ms4. Spherical divergence
5. Display field records
6. Trace editing
7. Source and receiver static correction
700 ft
6500 ft/sec
Type: Spiking
Offset Gate50 ms - 400 ms
31 ms -500 ms9,
10,
11.
12,
13,
14,
15.
16,
17,
18,
19,
20,
21
22
DatumVRDeconvolution
Design gate
1584Common depth point gather
Initial velocity analysis
Residual statics application
Secondary velocity analysis
Trim statics
Final velocity analysis
Residual statics application
Frequency dependentNormal moveout correction
Early muteTrace equalization
Common depth point stack 36 & 48 fold
Deconvolution Type: band limited
Gap length 6 msFrequency 70-250 HzWhite noise 100% outside 0% inside
Design gate 0.20-0.340 secSignal to noise enhancement
23,
24.
Digital filter
Time (sec)
0.0-0.07
0.095
0.350
0.500
Trace equalization
Film display
30 TPI 20 IPS (1 in
Polarity convention
Type: bandpassFrequency (Hz)
80-24080-20070-18070-140
330 ft)
28
Appendix C Bristol Field Parameters andProcessing Sequence
Segment BR-1
Field Parameters
Recording instruments
Recording filter
Record length
Sample rate
Number of channelsEnergy source
Source interval
Source depth
Pops/S. P.
Gun size
Receiver type
Receiver interval
Receivers per groupStandard configuration
Direction of shooting
Recorded by
Recorded for
Date recorded
DFSV90/36- 512/72 (Hz/DB/Oct)
Notch out
0.5 sec.5 ms3x24Airgun
22 ft
9ft
310 C.I.
Hydrophone -P44 (10 Hz)
22 ft
1
814-220 ft -Sp -220-814 ft
North to south
Walker Geophysical Co.
Illinois State Geological
SurveyMay 17-20, 1988
Processing Sequence
Processing length .5 secSample rate 1 ms
1. Demultiplex and QC display
2. Resample .5 to 1 ms3. Spherical divergence and gain recovery
4. Trace editing
5. Deconvolution type: band limited
No. of gates 1
Design type average autocorrelation
Frequency 60-320 HzOperator length 51 msWhite noise 50% outside 0% inside
6. Source and receiver datum correction
Datum 600 ft
VR 6500 ft/sec
7. Common depth point gather
8. Initial velocity analysis
9. Residual statics
1 0. Final velocity analysis
1 1
.
Normal moveout correction
12. Mute13. Time variant scaling
14. Common depth point stack
15. Datum correction (+71 ms.)
Datum 830 ft
VR 6500 ft/sec
1 6. Spectral enhancement 60 - 200 Hz1 7. Digital filter type: bandpass
Frequency Time60-200 Hz 0.0 - 0.5 sec
18. TAU-P domain signal enhancement19. Time variant scaling
Segment BR-3
Recording Parameters
InstrumentsTypeFormatGain control
SourceTypeInterval
DFSVSEGB
IFP
Airgun
22 ft
Sample Interval .5 msRecord length 1 secFilter 90/36-360/72 Hz
Direction shot
CableChannels 72 (3 x 24)
Geophone type P44Array Inline
Geophones/stat unknown
Interval
Geophone Freq
Spacing
22 ft
10 Hzunknown
Processing Sequence
830 ft
6500 ft/sec.
June 1988
1. Daturm elevation
2. Subweathering velocity
3. Date processed4. Demultiplex
5.Shot and trace edit
6. Gain recovery
7. Common midpoint sort
8. Datum statics
Correction to floating datum9. Initial velocity analysis
1 0. Surface consistent residual statics
1 1
.
Final velocity analysis
12. Normal moveout removal
13. Mute1
4
Amplitude equalization
15 Datum statics
Correction to datum1 6. 3600% stack
1 7. Predictive deconvolution
Operator length 50 msPrediction lag 10 msDesign window 1 00-500 ms
18. Signal enhancement19. Wave equation migration
20. Bandpass filter 80 - 1 92 Hz22. Automatic gain control 200 ms23. Display
20 tr/in
Polarity
20 in/s
Black peaks are positive
29
Appendix D Lily Lake Field Parameters andProcessing Sequence
Field Parameters
Recording instruments
Recording filter
Record length
Sample rate
Number of channelsEnergy sourceSource interval
Source depth
Charge size
Receiver type
Receiver interval
Receivers per groupStandard configuration
Direction of shooting
Recorded byRecorded for
Date recorded
DFSV90/36 - 360/72 (Hz/DB/Oct)
Notch out
2.0 sec
1 ms56Dynamite55 ft
24 ft
.33 to 1 lb.
Hydrophone -P44(10Hz)55 ft
1
SP - Ch. #1 - Ch. #50-55 - 3080 ft
North to south
Walker Geophysical Co.
Illinois State Geological
SurveyMarch 16-19, 1986
Processing Sequence
Processing length
Sample rate
1 sec
2 ms
1. Demultiplex and QC display
2. Resample 1 to 2 ms3. Spherical divergence and gain recovery
4. Trace editing
5. Deconvolution type: band limited
No. of gates 1
Design type average autocorrelation
Frequency 70-250 HzOperator length 81 msWhite noise 50% outside 0% inside
6. Source and receiver datum correction
Datum 830 ft
VR 6500 ft/sec
7. Common depth point gather
8. Initial velocity analysis
9. Residual statics
10. Final velocity analysis
1 1
.
Normal moveout correction
12. Mute13. Residual statics
1 4. Time variant scaling
15. Common depth point stack
1 6. Spectral enhancement50-150 Hz
1 7. Digital filter type: bandpassFrequency Time50-150 Hz 0.0-1.0 sec
18. TAU-P domain signal enhancement1 9. Time variant scaling
30
II Seismic Refraction Profiling
R 7 E R 8 E R 9 E
R 6 E
seismic refraction lines
seismic rellection line
R 7 E R 8 E R 9 E
6 mi.
9 km.
Figure 1 Index map-location of seismic refraction profiles.
Introduction
More than 80 line-miles of seismic refraction data were gathered in Kane, Kendall, Du Page, andWill Counties, Illinois (fig. 1 ) to define the geologic framework of the near-surface deposits in the
proposed site for the Superconducting Super Collider (SSC). The results of this seismic refraction
survey provided information relevant not only to the construction of the SSC tunnel and the loca-
tion of its attendant vertical service shafts, but also to other future construction and to evaluation
of groundwater, aggregate (crushed stone), and sand and gravel resources in the region.
The results of the seismic refraction survey include information on compressional wave velocities
of the glacial drift and rocks in the bedrock surface (appendix A), which permit inferences to bemade concerning the lithologic character of the glacial drift and the bedrock surface. Lowvelocities of the glacial drift may be indicative of sand and gravel deposits; higher velocities maybe indicative of till. In an area where rocks that constitute the bedrock surface have a uniform
lithology, lower velocities likely correspond to pronounced weathering and/or fracturing. Fractures
in the upper bedrock often serve as conduits for transmitting sizeable quantities of groundwater in
this region.
33
Table 1 Length of cable and geophone intervals for estimated depth to bedrock in the study area.
Cable length (ft) Geophone interval (ft) Estimated depth to bedrock (ft)
300 25 <30600 50 30-150
1200 100 150-300
The results of the seismic refraction survey also include drift thickness or depth-to-bedrock values
(appendix A). Together with information from existing discrete drill holes, the depth-to-bedrock
values have been used to construct an improved bedrock topography map and delineate buried
bedrock valleys. When filled with coarse-grained glacial deposits, the bedrock valleys are often
sites of shallow groundwater supplies.
Seismic Refraction Method
In the seismic refraction method, the time between the initiation of seismic waves by an explosion
or some other energy source and the first disturbances indicated by a geophone at somemeasured distances from the energy source (shot point) are observed. The first disturbances or
arrivals correspond to the onset of compressional waves, the fastest traveling waves. According
to Fermat's principle, the waves that cause the first disturbances are the ones that have traveled
the minimum time path between the shot point and the geophones. By observing first arrivals for
several shot-to-geophone distances, a time-distance plot can be constructed.
The time-distance plot can be analyzed by comparing the variation of minimum time paths with
distance. Deductions can be made about the nature and depth of the elastic discontinuities
(velocity discontinuities) required to account for the observed time-distance relationships. Elastic
discontinuities then may be interpreted to define the nature, depth, and orientation of geologic
units below the earth's surface (Nettleton, 1940).
Successful application of the seismic refraction method requires that the compressional wavevelocities of the geologic units of interest increase monotonically with depth. This requirement
was met in the SSC study area, where there were essentially three shallow geologic units of inter-
est:
• the so-called weathered layer at the earth's surface, which is generally quite
thin and has a relatively low velocity;
• the layer of unconsolidated deposits, consisting of glacial till or sand and
gravel, which has a higher velocity; and
• the bedrock, which has a still higher velocity, even where it is weathered
and/or fractured.
Difficulties arise using the seismic refraction method when a velocity inversion exists at depth,
that is, when a geologic unit has a velocity less than that of the overlying unit. This situation com-monly occurs in bedrock valleys where compact glacial tills may overlie the loose, valley-fill sands
and gravels.
The low velocity unit is called the hidden layer because it is not apparent on time-distance plots of
first arrivals. Straightforward application of analytical interpretive techniques, which assumemonotonically increasing velocities with depth, will yield erroneously excessive depths to all elas-
tic discontinuities below the hidden layer. In the case of a bedrock valley containing a unit of thick
basal sand and gravel overlain by a compact till unit, the calculated depth to the valley floor will
be greater than it is in reality. This means that the thalwegs of such bedrock valleys will be exag-
gerated and, therefore, more readily discerned; but accurate determination of depth to the valley
floor and thickness of the hidden sand and gravel unit requires reference to the nearest drill holes
that penetrate bedrock.
34
* Shotpoint
A Geophone
Layer 3
Figure 2 Shot and geophone arrays used with FRAC and SIPT programs
Equipment
Seismic refraction data were acquired using two multichannel signal-enhancement seismographs
(EG&G Geometries models ES-2415F and ES-1225) from the Illinois State Geological Survey.
The 24-channel ES-2415F was used for most of the data acquisition. The 12-channel ES-1225,
which is lighter and more portable, was used when it was necessary to hand-carry a seismograph
to a field site. Mark Products 14 Hz vertical component geophones were used for detecting first ar-
rivals.
Field Procedures
To obtain optimum results from shallow refraction surveying, it is necessary to choose ap-
propriate shot and geophone arrays. These choices depend primarily on the layering parameters
(velocities and thicknesses) of the near-surface materials and depth to the lowest refracting inter-
face of interest. It is also important that the shot and geophone arrays are compatible with com-puter programs for processing and interpreting the data.
In this study, the lowest refracting interface of interest was the glacial drift-bedrock contact. Es-
timates of the depth to this interface and the layering parameters of the near surface materials
were made from drill hole information and results of previous seismic refraction work.
Table 1 summarizes cable length and geophone intervals used for the estimated depth to
bedrock throughout the study area.
The computer programs, FRAC and SIPT-1 , used for processing and interpreting the data
gathered in this survey, were compatible with the shot and geophone arrays shown in figure 2.
Dynamite charges, detonated in holes 4 to 5 feet deep, were the energy sources employed in
most of the seismic refraction surveying. The size of the charges ranged from as small as 1/6
pound to as large as 1 pound, depending on the character of the unconsolidated, near-surface
deposits and the estimated depth to bedrock. Where utilities and other cultural obstructions
prevented the use of dynamite, a self-propelled, drop-hammer, pavement-breaking machine wasused as a "thumper" source. Because the thumper does not provide nearly as much energy in a
single blow as a dynamite blast, signals from several blows of the thumper had to be stacked
before printing a seismic record.
35
Processing of Seismic Refraction Data
The data processing for the study consisted of assembling seismic refraction information, con-
structing an accurate index map to show locations of all seismic refraction profiles in the SSCstudy area (fig. 1), and preparing observed seismic refraction data for input into computer
programs. The programs produce the layering parameter (velocity and thickness) solutions, whichcan be interpreted to define the nature, depth, and orientation of geologic units near the earth's
surface.
First-arrival times were picked manually from printed records and plotted against distances from
shot points to geophones. The least-squares line segments associated with discrete near-surface
geologic units were fitted to the time-distance plots. Intercept times and slopes of the line seg-
ments were determined. The inverse of the slope of the line segment passing through the origin is
the true velocity of the weathered surficial material. Where the weathered layer is relatively thin
compared to geophone spacing, there may be no evidence of the weathered layer on the time-dis-
tance plot. In such cases a "true" velocity of 1 ,500 ft/sec was assigned to the weathered layer.
The inverse of the slopes of the other two line segments are apparent velocities of the layer of un-
consolidated deposits and the bedrock surface. The relationship of an apparent velocity to the
true velocity of a geologic unit depends on the direction and amount of dip on the upper surface
of a geologic unit under a seismic refraction profile.
The final step in preparing input to the seismic refraction computer programs, FRAC and SIPT-1
,
was determining shot point and geophone elevations from 7.5 minute topographic maps.
The FRAC program for inverting seismic refraction data follows a method set forth by Heiland
(1940), which assumes that velocity inceases monotonically with depth and planar surfaces
bound the near-surface geologic units of interest during the seismic refraction profile. Heiland's
method requires reverse profiling, that is, first-arrival times from shots placed at both ends of the
seismic refraction profile are employed. The input to the program includes shot elevation, inter-
cept times, and velocities associated with both the forward and the reverse shots. As mentioned
above, except for the weathered layer, the input velocities are apparent velocities. The output
from this program includes depths to the tops of layers corresponding to geologic units under the
shot points and the true velocity of each layer.
SIPT-1 (Seismic Interpretation Program Two) was used to process much of the seismic refraction
data in this study. The program, originally developed by Scott et al. (1972) to run on mainframe
computers, was modified later by Haeni (1986) for microcomputer use.
Like the FRAC program, the algorithm of the SIPT-1 program also assumes velocity increases
monotonically with depth; but unlike the FRAC program, the algorithm of the SIPT-1 program as-
sumes all layer boundaries are represented by a series of straight-line segments connected end-
to-end beneath geophone locations and extended from one end of the seismic refraction profile to
the other.
The SIPT-1 program is based on the delay-time method described by Pakiser and Black (1957),
but it also uses an interactive ray-tracing technique developed by Scott et al. (1972) to minimize
discrepancies between the measured and computed first-arrival times. The program requires data
obtained by overlapping arrays of 12 geophones and locating shots at the ends and offset from
the ends of the geophone arrays (fig. 2). The input to the program includes shot locations and
elevations, geophone locations and elevations, and first-arrival times. The output from the SIPT-1
program includes true velocity of each layer, depths to the tops of each layer below each
geophone along with the corresponding elevation, and ray-tracing data. The SIPT-1 program is
especially useful in processing seismic refraction data obtained in regions where the earth's sur-
face and/or the boundaries of the subsurface geologic units are topographically rough.
Results
Results of the seismic refraction survey in the study for the Superconducting Super Collider are
given in appendix A. Along with information concerning the locations of the seismic refraction
36
profile, this appendix includes compressional wave velocities of the weathered layer, the sub-
jacent layer of unconsolidated deposits, and the bedrock surface beneath the profiles. Theprimary value of the velocity data is that they allow inferences to be made concerning the
lithologic character of the near-surface deposits. The velocity data also are valuable in defining
those areas where a bedrock surface of a constant lithology has experienced considerable
weathering and/or fracturing. Appendix A also includes the elevation of the earth's surface anddepths to the top of the layer of unconsolidated deposits and to the bedrock surface beneath the
end points of each seismic refraction profile.
As mentioned above, a constant compressional wave velocity of 1 ,500 ft/sec was assigned to the
thin weathered layer at the earth's surface. Velocities associated with the layer of unconsolidated
deposits below the weathered layer and above the bedrock surface range from slightly less than
3,000 ft/sec to slightly more than 8,000 ft/sec. Velocities less than 4,500 ft/sec in the uncon-
solidated deposits commonly correspond to loose sands and gravels, whereas velocities greater
than 4,500 ft/sec correspond to glacial tills. Velocities associated with the bedrock surface range
from as low as 9,000 ft/sec to more than 20,000 ft/sec. Lower velocities for the bedrock surface
correspond to clastic rocks and higher velocities correspond to carbonate rocks. However,
weathering and/or fracturing of the bedrock may result in anomalously lower velocities. Some of
the lower velocities associated with the intermediate layer of unconsolidated deposits may cor-
respond to materials that make up the weathered layer and some of the higher velocities as-
sociated with the intermediate layer may correspond to rocks composing the bedrock surface. In
such cases, information gathered from nearby boreholes can often help in assigning velocities to
the proper geologic units.
Bedrock surface elevations vary considerably within the study area (fig. 3). Elevations as low as
381 feet and as high as 869 feet above mean sea level have been determined using the seismic
refraction data. Glacial drift thickness in excess of 300 feet has been noted.
Summary
More than 80 miles of seismic refraction profiling provided additional information to the databaseon the near-surface geologic framework of northeastern Illinois. This database is important in solv-
ing a number of local and regional geological, hydrological, and engineering problems.
An updated bedrock topography map (fig. 3), which incorporates information gathered in this
study, has relevance not only to future construction, but also to the location of shallow
groundwater and aggregate resources. Buried bedrock valleys often contain large quantities of
sand and gravel; thus, these valleys often serve as conduits for shallow groundwater supplies.
The location of these shallow aquifers also is an important consideration in the location of wastedisposal sites. The additional information provided by the seismic refraction surveying on depth to
bedrock and the nature of both unconsolidated deposits and the bedrock surface (inferred from
velocity data) will be useful in siting future sand and gravel pits and quarrying operations.
37
R6E R7E R8E R9E
Figure 3 Bedrock topography map of study area.Contour interval 50 ft
38
References
Dobrin, M. B., 1976, Introduction to geophysical prospecting: McGraw-Hill Book Co., New York,
630 p.
Haeni, F. P., 1986, Application of seismic refraction methods in groundwater modelling studies in
New England: Geophysics, v. 51 , pp. 236-249.
Heiland, C. A., 1968, Geophysical exploration: Hafner Publishing Co., New York, 1013 p.
Nettleton, L. L, 1940, Geophysical prospecting for oil: McGraw-Hill Book Co., Inc.
New York, 444 p.
Pakiser, L. C, and R. A. Black, 1957, Exploring for ancient channels with the refraction
seismograph: Geophysics, v. 22, no. 1, January, pp. 32-47.
Scott, J. H., B. L. Tibbetts, and R. G. Burdick, 1972, Computer analysis of seismic refraction data:
U.S. Bureau of Mines, Rl 759S, 99 p.
Sharma, D. V., 1976, Geophysical methods in geology: Elseivier Publishing Co., 428 p.
Telford, W. M., L. P. Geldart, R. E. Sheriff, and D. A. Keys, 1976, Applied geophysics:
Cambridge University Press, 860 p.
39
Appendix A Results of Seismic Refraction Profiling
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43
Appendix A continued
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Appendix A continued
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Appendix A continued
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Appendix A continued |
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47
Appendix A continued
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Appendix A continued
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Appendix A continued
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Appendix A continued
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Appendix A continued
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