ML20049J364
| ML20049J364 | |
| Person / Time | |
|---|---|
| Site: | Midland |
| Issue date: | 02/28/1982 |
| From: | WESTON GEOPHYSICAL CORP. |
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| Shared Package | |
| ML20049J362 | List: |
| References | |
| NUDOCS 8203170586 | |
| Download: ML20049J364 (500) | |
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E'! CLOSURE 1 6 e I
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I DESCRIPTION AND EVALUATION OF BEDROCK STRUCTURE IN THE VICINITY OF MIDLAND PLANT - UNITS 1 AND 2 MIDLAND, MICHIGAN Prepared for CONSUMERS POWER COMPANY February 198 2
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1 l DESCRIPTION AND EVALUATION OF l
BEDROCK STRUCTURE IN THE VICINITY OF MIDLAND PLANT - UNITS 1 AND 2 I MIDLAND, MICHIGAN I
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DESCRIPTION AND EVALUATION OF 4 BEDROCK STRUCTURE IN THE VICINITY OF i
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-EXECUTIVE SU.MMARY L Subsurface mapping in the vicinity of the Midland plant ,
site has demonstrated the presence of both northwest and northeas t s tructural . trends. W e near orthogonal intersection of these trends produces a pattern of folds and associated l
faults which persists stratigraphically from the top of the
) Marshall Sandstone (1,200 feet deep) downward to the top of the Dundee Limestone (3,500 feet deep) , and possibly to greater l depths. We structural pattern suggests that deformation resulted from compression during subsidence of the basin, which t
is interpreted to have culminated prior to the Pennsylvanian Period. Inasmuch as patterns of subsidence were basement controlled, the structural trends may also be considered l " basemen t-involved " .
The clearest expression of the northeast trend in the study I
area occurs in the vicinity of the plant site. Deformation in this area is due to localization of the maximum compressive s tress on the nose of a northwest-trending fold resulting in l complex imbricate faulting and pronounced associated drag folding. Elsewhere in the study area, the northeast trend is l
l- clearly subordinate to the northwest trend. '
%e structural geometry characteristic of the Devonian and L
Lower Mississippian units is reflected only weakly in the Upper
). Mississippian strata and is not at all evident in the Pennsylvanian sequence. A detailed study of the internal 1
geometry of the Saginaw Formation documents this relationship and assigns a minimum age (pre-Atokan, Pennsylvanian) to deformation in the area.
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( LANDSAT false color images of Michigan's lower peninsula were studied to determine the presence of lineaments attributable to bedrock faults. Most lineaments defined have been correlated to known geologic features.
A literature review was conducted to determine whether
{ stresses in the immediate area are anomalous as compared to those in the north-central United States. The investigation indicates that stresses in the Midland area are compatible with the larger regional stress field.
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LIST OF FIGURES i i
LIST OF PLATES iii PART I: ASSESSMENT OF BEDROCK STRATIGRAPHY AND STRUCTURE IN THE VICINITY OF THE MIDLAND PLANT SITE l 1.0
SUMMARY
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2.0 INTRODUCTION
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3.0 DISCUSSION I-6
4.0 CONCLUSION
S I-18 PART II: ASSESSMENT OF AGE OF FAULTING AND FOLDING IN THE VICINITY OF l THE MIDLAND PLANT SITE 1.0
SUMMARY
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2.0 INTRODUCTION
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i 3.0 PREVIOUS WORK II-3 1
4.0 STRATIGRAPHY II-6 l_ 5.0 DISCUSSION II-10
6.0 CONCLUSION
S II-19 PART III: LINEAMENT ANALYSIS / SOUTHERN MICHIGAN PENINSULA l 1.0
SUMMARY
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2.0 INTRODUCTION
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3.0 LINEAMENT IDENTIFICATION III-3 E 4.0 SURFICIAL GEOLOGY III-4 5.0 GEOLOGIC HISTORY III-5 l 6.0 LINEAMENTS III-6
7.0 CONCLUSION
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CONTENTS (Continued) ,
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Page PART IV: STATE OF STRESS MIDLAND, l MICHIGAN / CONSUMERS POWER 1.0
SUMMARY
IV-1 2.0 REGIONAL IV-1 3.0 PLANT SITE VICINITY IV-5 I
PAGE V: REFERENCES AND BIBLIOGRAPHY V-1
) FIGURES PLATES APPENDIX I MAP LOCATIONS AND ELEVATIONS OF CONTROL POINTS USED IN THIS STPDY f APPENDIX II CONTROL POINTS FOR STRUCTU".E MAPS ON TOP OF 00AL ZONE i l E
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LIST OF FIGURES I Figure No.
1 Midland Site Location l
2 Structure Contour Map - Top of Traverse l
3 Stratigraphic Column 4 Trend of Anticlinal Folding l 5 Study Areas Investigated in Plates 1, 2, 3 and 4 6 Structure Contour Map - Top of Traverse l
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Main Coal Thickness Map, Iower Shale and Upper Shale Structure Contour Map Garfield Cross Section 9 Stratigraphic Column l
10 Pre-Pennsylvanian Geologic Map, Shideler (1963) l 11 Grand Ledge and Corunna Quarries 12 Cross Section A 13 Cross Section B 14 Cross Section C 15 Cross Section D j 16 Cross Sections E and F 17 Cross Sections G and H l 18 Ideal Stratigraphy of Pennsylvanian Coal Zone 19 Cross Sections I, J and K l
20 Structure Contour Map on Top of the Coal Zone, Garfield Township B
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LIST OF FIGURES (con tinued )
Figure No.
NW 23 Cross Section N 24 Cross Sections O and P 25 Structure Contour Map on Top of the Coal Zone, l Midland-William Township 26 Michigan Oil and Gas Map 27 Lineaments Interpreted from ERTS Imagery B
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LIST OF PLATES l
Plate No.
} 1 Incation Map of Well Control 2 Struct. re Contour Map - Top of Dundee Limestone I
3 Structure Contour Map - Top of Traverse Limestone 4 Structure Contour Map 'Ibp of Marshall Sandstone l
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I f ASSESSMENT OF BEDROCK STRATIGRAPHY AND STRUCTURE IN THE VICINITY OF THE MIDLAND PLANT SITE f
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SUMMARY
Subsurface mapping in the Midland area has demonstrated I
the presence of a northeast structural trend which intersects
} the regionally dominant northwest trend perpendicularly and is the more prominent element of the structural fabric in the southeastern sector of the study area. Mapped structures referrable to both trends are vertically " stacked" at least as I
far down-section as the Sylvania Sandstone (Devonian); quite
} likely they extend to greater depths and may be related, albeit indirectly, to basement structure. The northwest trend may be f related to compressional stresses generated intrabasinally during subsidence and localized along the basin axis and in the I
higher strata. '1he northeast trend, probably with strike-slip l and rotational displacement on its component faults, also would have developed in this stress regime.
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2.0 INTRODUCTION
In March 1981, Consumers Power Company (CPC) presented to I
Weston Geophysical Corporation (WGC) a structure contour map of the " Traverse Lime" (Devonian) beneath Midland and Ingersoll townships, Midland County, in the approximate center of the l Michigan Basin (Figure 1) . 'Ihis structure map (Figure 2),
generated by Geospectra Corporation of Ann Arbor, shows several l
northeast-trending lineaments referred to by GeoSpectra as i
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" zones o f anomalous dip". Che such lineament, in sections 1 l
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l and 2 of Midland Township, is identified on the map as a fault, implying that the other features indicated are faults as well.
'Ihe proximity of the indicated features to the Midland site
{ therefore became a matter of investigation. '
WGC subsequently was retained to evaluate the GeoSpectra l
map and, specifically, to examine the evidence for faulting and other pronounced structural deformation in the vicinity of the Midland plant site. Initially, a limited number o# subsurface data acquired from the Michigan Geological Survey and from Dow Chemical Company were used to construct preliminary structure contour maps using a 25-foot contour interval, of the Dundee, l
Traverse, Sunbury, and Marshall formations (Figure 3) . Upper surfaces of these Devonian and Mississippian units are located approximately 3,608, 2,960, 2,395 and 1,180 feet, respectively below the site. In each instance, contouring revealed the presence of two structural trends - the well-established northwest alignment of structures that characterizes Michigan's Southern Peninsula (Figure 4) , and a northeast trend to which the " zones of anomalous dip" might be referred. In addition to this rectilinear structural fabric, the map set revealed that each principal structural element occurs at the same map position, at least throughout the stratigraphic interval examined, and this relationship was recorded for future reference. Finally, mapping indicated that the GeoSpectra
" zones" correspond to abrupt changes in the attitude of the l strata, not only on the Traverse surface, but on each of the other surfaces as well.
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apparent, the discrete component structures determining them remained poorly resolved. When a preliminary literature search revealed the presence in the area of at least two northeast-trending structurally controlled oil fields - the Pinconning l
and the North Adams - it became apparent that a more precise description of bedrock structure was indicated.
In July,1981, WGC conveyed its observations and l suggestions to CPC and was requested to expand its study, as necessary, to adequately define the " zones" and their l
relationship to the structural fabric and geologic history of the central Michigan Basin. Concurrently, a geologist employed by Northern Michigan Exploration Company (NMEC), a division of
( CPC, informed Weston that the northeast structural trend indeed exists, that it is expressed on several northwest-trending l
anticlinal structures as " cross folds", and that the Pinconning s tructure is a fracture.
Subsequently, additional data were obtained from the
( Michigan Survey, 00w Chemical Company and NMEC. 'Ihe study area was extended northeastward :o include the Pinconning Oil Field and southwestward to include the Porter Field. Presently, it includes most of Midland and Bay counties and a small portion 1
of Saginaw County (Figure 5); it forms a zone of inquiry about l 15 miles wide across the dominant northwest structural trend.
Stratigraphically, the study area extends from the surface downward to include the upper strata of the Devonian Dundee I
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E I l Limestone and thus incorporates the upper 3,500 feet of section I consistently penetrated in drilling operations in this area.
l These are the areal and stratigraphic limits within which most l available subsurface data have been examined and interpreted; they define the area and the interval upon which WGC has focused its efforts.
l The data base (Plate 1) shows the distribution of the l i
approximately 500 control points used in construction of the l Devonian structure contour maps; the vast majority of these are Dundee penetrations ( Appendix I) . The only control points within the designated area not independently contoured are those within the interior of the Porter and Mt. Pleasant oil I
fields; existing Dundee structure maps of these areas, and of j the Kawkawlin field , have been incorporated with the Weston Dundee map to more clearly and completely depict the dominant structural trend (Plate 2) . The " Traverse Limestone" map (Plate 3) covers a more restricted area but extends to the I
limits of dense well control and covers the area of immediate l
t concern, including the 5-mile circle centered on the plant site.
Numerous reports on structures located beyond the l designated study area vare examined for informat. ion as to the types of structures that might be anticipated within the study l'
area. Most of these are theses from Michigan universities and include reports on the Porter, Kawkawlin, Pinconning, North Adams, and Deep River structures as well as reports on i
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I-5 structures as far as 50 miles northward (Roscommon and Ogemaw counties) and as far as 100 miles southwestward ( Allegan County) and southeastward (Wayne County).
The tops of the Dundee Limestone and " Traverse Limestone" (Squaw Bay Limestone) were selected as mapping horizons because each is relatively easy to determine from well cuttings and drilling-time logs, even in the absence of downhole geophysical logs; each is routinely penetrated in drilling for minerals and hydrocarbons in the area; and each extends uninterruptedly across the central Michigan Basin. Both units are marine shelf limestones which may be assumed to have had low initial dips, and both are immediately overlain by strata deposited in low-energy environments. W e latter consideration obviates the need to account for effects of erosion on their geometry.
Accordingly, they are considered ideal marker horizons in that mappable departures from planarity may confidently be ascribed to tectonic processes, or to differential compaction or subsidence.
The top of the Marshall Sandstone was selected as a reference horizon because of its wide extent, uniform lithologic characteristics, and high str atigraphic position.
We Marshall is the youngest Paleozoic unit consistently identified in local drilling operations and the highest for which a reliable and adequate data base can be compiled. he regional distribution and internal stratigraphy of the f Marshall, and the nature of its boundaries with the underlying B 1 1
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Coldwacer Shale and overlying Michigan Formation have been descrioed in considerable detail by Monnett (1948) , who l
concluded that the Marshall top is an acceptable stratigraphic l marker ir Midland and Bay counties. In the present study, it serves as the lower limit and plane of departure for structural I analysis of the Pennsylvanian sequence (Part II) .
'Ihis submittal comprises: (1) a study of the Middle l
Devonian sequence which focuses on the geometry of the top of l
the Dandee Limestone and the top of the " Traverse Liv one" and which addresses Plate 2, Plate 3, and the availab.e oil l field maps of these units; (2) a study of the sequence between the Marshall and top of rock which describes the geometry of I
the Marshall surface, the internal stratigraphy of the Pennsylvanian Saginaw Formation, and addresses the problem of the age of such deformation as is described in (1) ; (3) an I l imagery analysis of the Southern Peninsula of Michigan to determine the presence of lineaments possibly relatable to 1
bedrock structural features; (4) an analysis of the present stress regime in Michigan's Southern Peninsula; (5) a I
bibliography of relevant literature.
l l 3.0 DISCUSSION A structural pattern of northwest-ttending low-amplitude l
folds is clearly revealed on each structure map submitted and is known from preliminary mapping of additional horizons to l
characterize the geometry of the entire stratigraphic sequence j at least as far down-section as the top of the Sylvania l
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l Sandstone and as far up-section as the top of the Bayport Limestone. The northwest trend is the dominant element of the '
structural fabric of the Michigan Basin (Figure 4) and is l particularly well-developed in the central part of the area (Figure 5) . The most significant relationship perceived in comparing Plates 2, 3, and 4 is the harmonic nature of deformation throughout the Devonian-Mississippian interval, l
wherein not only major structural elements but elements as l limited in breadth as a single map section (one mile or less) appear at each stratigraphic level at virtually the same map l position.
The same relationship has been demonstrated elsewhere in I
the Michigan Basin as, for example, in Allegan County, where l closures of a fraction of a mile in diameter coincide in map position through more than 3,000 feet of section, from the I Silurian A-1 Carbonate through the Mississippian Coldwater Shale ( Ells , 197 8) . In these instances, the structures I
described overlie either bioherms or salt pillows, but the same l
relationship has been extensively documented throughout the central Michigan Basin by oil explorationists who routinely I drill Mississippian closures and trends in exploring deeper zones such as the Traverse and the Dundee-Detroit River l
sequence. Numerous reports and theses on individual structures within the central Basin include structure maps of the Traverse and Dundee formations that similarly project the vertical I " stacking" of structural features. Accordingly, this B
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any discussion of the its tectonic hinory.
l The extensive northwest-trending anticlines (oil fields) commonly are mapped as multi-closure structurest the Porter, Mt. Pleasant, Kawkawlin, West Branch, Headquarters, and Reynolds fields are among those so defined. Structure maps of 1
these fields, and others, strongly suggest the presence of a l transcurrent northeast structural trend. The trend is reflected in northeastward-directed salients and re-entrants on the flanks of the folds and these are variously described as cross-folds, sags, swells, saddles, spurs, nodes, noses, and, l
quite infrequently, as faults or probable faults. As implied previously, these structures, and the trend they document, l
appear in corresponding map positions on successive marker l horizons.
In contouring slightly to moderately deformed areas such l
as the Michigan Basin, the general pattern is perceived earli in the study. The strike of the mapping surface and its dip, as indicated in the contour spacing , define its *undamental l
l geometric configuration. Abrupt departures from this pattern -
sharp inflections in the local trend or pronounced changes in l
the rate of dip - define local structure. Increase in the rate of dip accompanied by abrupt change in strike generally is regarded as very strong evidence for faulting; elongate closed l lows commonly are similarly interpreted. Numerous examples of l
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l these structural patterns appear on Plates 2, 3, and 4 and have been described as faults or, where the scale and configuration of fold patterns suggest the probability of rock failure as l inferred faults.
During reduction, organization, and evaluation of the l
basic data, the thickness of each of several units and sequences was monitored and compared to determine variation relatable to local s tructure. Units in the stratigraphic l vicinity of the mapped horizons, such as the " Traverse Limestone"-Bell Shale sequence , An trim Shale , and Coldwater Shale exhibit negligible thickness variation in any given sector of the study area, including those in which local 1
structure is most pronounced. Such variation is readily l attributable to the normal regional thickness trend of the interval, while structural thickening related to low-angle faults or axial surfaces is not evident. Wese observations indicated that isochore mapping was inapplicable to the l
structural problem; accordingly, no isochore maps were j generated.
Northwest Structural Trend The northwest trend includes one extensive fault and a few shorter ones. We principal structure parallels the steeper 1
(southern) limb of the northwestward extension of the Kawkawlin j anticline and may extend southeastward much farther than shown. Clearly, the dips on this fold limb are atypically
{ steep for the area, and a persistent through-going broadly 5
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sinuous fault is indicated approximately as shown. Amoun t o f l apparent offset along the fault is mapped as ranging to about 150 feet at the Traverse surface, and somewhat less as it l
affects the Dundee. %e fault clearly intersects the top of the Marshall as well and , at each horizon, appears to are southward and terminate in Hope Township. The fault appears at l approximately the same position on each map and therefore must be approximately vertical. Contour patterns a few miles l
distant, in northern Mills and Garfield townships, strongly suggest one or more similarly oriented faults.
Northwest-trending faults occur also in Lee, Larkin, and l Ingersoll townships where they tend to parallel axial trends (Ime and Larkin) or define re-entrants (Ingersoll). We fault l in Ice Township suggests a more complex structure associated I with the compressed " wrap-around" geometry of the two anticlinal noses in that area.
l All northwest-trending faults and inferred faults are interpreted as near vertical throughout the explored interval at least as far down-section as to involve the Dundee-Detroit River sequence. The literature indicates that such is the case l
with faults and fracture zones elsewhere in the central Basin outside the study area, such as the Deep River fracture zone.
l Because the same patterns of folding and inferred faulting I coincide on successive horizons, vertical repetition of structural arrangements - associations of faults and flexures -
are considered an evident and significant aspect of the central l
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Basin's s tructural style. Nothing was detected in the study l area or in the literature to suggest low-angle structures on this trend or significant refraction of structural elements l within the shaley intervals between successive mapping horizons.
I Northeast Structural Trend References of record to a northeast trend include the l Traverse map submitted by GeoSpectra Consultants, Newcombe 's (1953) Traverse map, and several theses on oil-field structures in the central Michigan Basin including the Porter (Maebius, I 1935), Pinconning (Jack son, 1958), Kawkawlin (Hyde , 19 79) , Wes t l
Branch ('Ien Have ,1979) , and North Adams (Rickey , 198 0) l fields. Jackson and Rickey described discrete northeast-trending structures; the others described or implied that the cross-trend, apparent on their maps, manifested in salients, re-entrants , and multiple "h i gh s " (closures) on northwest-1 1 trending anticlines are fault-related. Maps of the Headquarters Field in Clare and Roscommon counties support th e l
same interpretation, as do representations of several other l fields in the central Basin. Additionally, the geometry of dolomitized zones, in addition to stratigraphic and lithologic l
constraints, probably is relatable largely to fault plane l l
B intersections as concluded by Hyde for the Kawkawlin structure.
Within the study area, Jackson's contouring of the l Pinconning structure, and his interpretation of it, are considered valid. Westward of the plant site, local areas on l
the Mt. Pleasant and Porter structures were contoured at a E
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5-foot interval and in certain instances the patterns clearly indicate northward-trending near-vertical faults, as shown )n Plates 2, 3, and 4; all of these are here referred to the northeast trend.
The maximum development and clei.-aat expression of the northeast structural trend occurs within a zone, up to five miles wide, extending from the Porter anticline at the southern boundary of Midland county north-northeastward into south-eastern Larkin and southwestern Beaver townships (Plates 2, 3, E and 4) . Within this zone, the " normal" contour pattern is severely distorted. As presently resolved, the pattern describes north- to northeast-striking surfaces, and dips to the west or east, more commonly than it depicts the broader i
northwes t trend. In fact, given a map of this zone out of
= structural context, the northwest trend is virtually obscured.
'Ihe main zone of northeast-trending structures may be ;
viewed as comprising (1) the set of structures in Midland and j Ingersoll townships, as perceived by GeoSpectra Consultants, and (2) the association of structures east and northeast of the plant site in eastern Midland and Ingersoll and western J
Williams and Beaver townships.
Structurally, the area south of the plant site is a gently dipping fold limb shared by the positive Porter trend on the south and the relatively narrow syncline on the north. The exact configuration of the closure on the syncline is unknown i
owing to a data gap in northern Midland Township. Within the
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zone of deformation, the general eastward strike of the 5 first-order fold limb is interrupted and relatively tight northeastward-trending fold patterns are indicated. Where departure from the eastward strike is considered particularly acute it is accommodated in contouring by a break in the pattern and interpreted as a fault. Virtually this same pattern of deformation, comprising the same structural elements, is indicated at each mapped horizon. The zone of folding and faulting and in many instances discrete faults, occur at corresponding positions on each map.
She severely compressed and distorted contour patterns to tne east and northeast of the plant site, given the brittle and competent nature of the units involved, are still more indicative of faulting than those discussed above.
Additionally,the abrupt termination and probable dislocation of the nose of the major syncline in southwestern Williams Township, and the structural " truncation" of the associated positive structure adje ent to it on the north, present a pronounced rectilinear configuration that is compelling evidence for faulting. The sub-parallel arrangement of faults shown here is considered a conservative representation of the structure in this particular area and of the structure south of Midland as well.
As mapped and interpreted, the northeast-trending faults are predominantly linear and very steeply inclined, as are the zones of deformation which they define. The maximum apparent I
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zone of deformation, the general Eastward s trike of the first-order fold limb is interrupted and relatively tight northeastward-trending fold patterns are indicated. Where l departure from the eastward strike is considered particularly acute it is accommodated in contouring by a break in the pattern and interpreted as a fault. Virtually this same pattern of deformation, comprising the same structural i
elements, is indicated at each mapped horizon. The zone of l folding and faulting and in many instances discrete faults, occur at corresponding positions on each map.
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'Ihe severely compressed and distorted contour patterns to the east and northeast of the plant site, given the brittle and i
competent nature of the units involved , are still more l indicative of faulting than those discussed above.
Additionally,the abrupt termination and probable dislocation of l the nose of the major syncline in southwestern Willinms
'Ibwnship, and the structural " truncation" of the associated 1
positive structure adjacent to it on the north, present a l pronounced rectilinear configuration that is compelling evidence for faulting. The sub-parallel arrangement of faults l shown here is considered a conservative representation of the structure in this particular area and of the structure south of I
Midland as well.
As mapped and interpreted, the northeast-trending faults are predominantly linear and very steeply inclined, as are the
} zones of deformation which they define. The maximum apparent l
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" Traverse Limestone" surf ace in Section 36 of Midland Township .
(Plate 3); however, vertical displacement generally is no more
. than a few tens of feet. Apparent displacement along individual faults or fault segments may be systematically distributed or seemingly random, according to local relationships among actual displacement, the intensity of I associated folding, and probable northwest-trending minor folds. South of the Midland site, for example, variation in 5 the amount of apparent displacement along faults probably reflects the presence of strike-parallel minor folds on the limb of the main fold; these are not mappable on the available data base , but may reasonably be expected to occur here.
! Sense of displacement on faults referrable to either trend is difficult to describe much less resolve. While the structural azimuths demonstrated in the present study may be discussed in terms of existing deformation models and tectonic concepts, the question as to whether displacement was principally vertical or lateral remains unanswered. (Se e
- i Fisher, J. A., 1981, p. 25-37, for a comprehensive review of existing concepts) . 'Ihe map patterns suggest, however, that complex lateral and rotational faulting is more probable than systematically cumulative strike-slip displacement in the more severely deformed areas, such as the one due east of the plant site.
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Interpretation of Structural Fabric l The structural configurations expressed in Figur 6 and Plates 2, 3, and 4 indicate (1) that the Devonian-Mississippian l
sequence within the study area was deformed in a stress regime in which the apparent maximum compressive stress wa<, ariented l
northeast-couthwest; (2) that deformation was most pronounced l and the orientation of structural trends most clearly expressed in that region corresponding to the long axis of the basin and l
the Mid-Michigan gravity anomaly; and (3) that the northwest and northeast structural trends developed sequentially in what may be considered a single episode of compressive brittle
! deformation.
Further, areal correspondence of the zone of strongly oriented structural elements (Figure 6) and the Mid-Michigan anomaly strongly suggests that the stresses responsible were l
generated intrabasinally as the structure subsided throughout l Middle Paleozoic time which suggests, in turn, that the effects of horizontal compression (shortening o f s trata) should l increase in severity up-section as well as basinward. ;
i B Possibly, therefore, the interval explored in this study is more intensely deformed than the deeper (pre-Devonian) l section. Accordingly, the overlying Pennsylvanian sequence should be at least as severly deformed as the Devonian-I Mississippian sequence. Evidence presented in Part II of this report, however, indicates that the Saginaw Formation e
(Pennsylvanian) was not involved in the deformation that g weston seconysicci i -- -
( I-16 E affected the underlying units. %us, the episode of compressive deformation inferred to have persisted throughout Devonian and Mississippian time is interpreted here as having
[ culminated prior to deposition of the Saginaw sequence. A comprehensive literature search has revealed that this is the prevailing conclusion among geologists who have studied the Michigan Basin (see Part II) .
Assuming that compression and deformation were directly
[ related to basin subsidence, as suggested above, the absence in the Saginaw of a structural fabric relatable to compression implies cessation of subsidence or at least an abrupt decrease in the rate of downwarp prior to Atokan (Pennsylvanian) time.
%e upward progression of lithologic types in the Midland area
( (Figure 3) tends to support this implication. The study area is located near what had been the center of the basin throughout Late Paleozoic time and the pattern of lithologic response to structural subsidence should be clearest here and relatively unobscured I,/ marginal lithologic associations. In
{ this area the lithologic record from the top of the Dundee upward clearly reflects an overall pattern of progressive change from an open-marine basin undergoing active subsidence at L rate far in excess of the rate of sedimentation, E through periods of deposition in restricted-marine environments r and relatively brief episodes of clastic sedimentation, to a L
tectonic setting in which rates of sedimentation, while
[ limited, exceeded the rate of downwarp. The Saginaw Formation E
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l (no n-marine ) is the lowermost unit deposited in the tectonic j setting last described and accordingly might be expected to lack the structural effects impressed on the older units deposited prior to stabilization of the basin.
W Whether culminating in Mississippian or Early Pennsylvanian time, deformation in the study area is interpreted as having developed sequentially as follows:
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. (1) Development of large-scale, northwest-trending, I slightly asymmetrical folds represented in the study area by the Kawkawlin, Porter, and Mt. Pleasant I
anticlines and intervening synclines; probably l preceded by formation of small-scale folding of similar orientation in the competent strata; apparent maximum compressive stress was northeast.
(2) Development of second-order folds, also northwest-trending, between the first-order folds; the complex anticline in Larkin Township is an example of this development.
l (3) Concentration o f compressive s tress in the " noses" of the second-order synclines and brittle failure along lines parallel t.o the maximum compressive stress (northeas t) . Volume considerations in these areas l
indicate that the resulting deformation should be l complex and should have proceeded until stress was accommodated by a combination of lateral, rotational, i
and v ertical displacement among the rock slices, and by attendant drag-folding .
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E l I-18 (4) Development of northwest-trending faults and ultimate accommodation of the maximum compressive stress.
4.0 CONCLUSION
S Subsurface mapping in the Midland area has demonstrated l
the presence of northwest and northeast structural trends. We
! northwest trend is a pattern of slightly asymmetrical open folds and associated steeply dipping faults; the northeast trend is manifested in relatively tight folding and closely spaced subparallel faults. Map patterns suggest a continuum o f deformation in which the northwest-trending folds, northeast-trending structures, and northwest-trending faults were developed within the prevailing compressional stress regime.
We geometry of successive mapping horizons corresponds so closely as to demonstrate the near verticality and harmonic nature of deformation in this part of the Michigan Basin. he overall structural configuration is reflected at least as far down-section as the Sylvania Sandstone and may be basement-related. Similar deformation is apparent as far upsection as to involve the Bayport Limestone and thus involves the entire Mississippian sequence.
The structural system is interpreted as resulting from compression during subsidence of the basin which culminated prior to deposition of the Saginaw Formation. Inasmuch as patterns of subsidence utlimately must be considered as having been basement controlled, the stresses generated during subsidence and the Paleozoic structures generated by those stresses are basement related.
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I I-19 Displacement or amplitude on most structural elements l defined in this study are at the limit of seismic reflection profiling resolution, and the intervening salt sequence might 1
I be expected to mask the presence of such structures within the Cambro-Ordovician section. 'Ihe relationship of the I
Devonian-Mississippian structural configuration to that of the
} Precambrian basement therefore remains conjectural.
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L PART II: ASSESSMENT OF AGE OF FAULTING AND FOLDING IN THE VICINITY OF THE MIDLAND PLANT SITE E
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[ ASSESSMENT OF AGE OF FAULTING AND FOLDING IN THE VICINITY OF THE MIDLAND PLANT SITE 1.0
SUMMARY
Folding and faulting in the Midland area of the Michigan Basin has been determined to have concluded prior to Pennsylvanian (Atokan) time.
{ Folding and faulting found in the Pennsylvanian strata do not reflect the structures present in Mississippian and older b formations. Structures in the Pennsylvanian strata are related to sof t-sediment deformation and are nontectonic in origin.
[
These structures have not been identified in the study area and
{ are small scale in magnitude.
Contour maps and cross-sections of coal seams and a b mappable zone in the Saginaw Formation indicate structural trends that are not related to Marshall structural trends. The E consensus of published material supports the conclusion that the deformation occurred prior to Saginaw deposition.
{
'Ihe Mississippian age Bayport, Michigan, and Marshall
[ formations reflect the similar structural style present in Devonian s trata.
2.0 INTRODUCTION
l Mississippian and younger rocks (Figure 3) were studied in Midland, western Bay, and northern Saginaw counties of Michigan
[ to determine the age of folding and faulting (Figure 5) . This stratigraphic sequence comprises a column extending i l
[ approximately from 1,180 to 358 feet below the Midland plant l E
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l site. More than 1,300 coal, brine extraction and processed brine disposal, salt, oil, and gas wells were examined in the l
study area.
l Structure contour maps drawn on the top of the Marshall (Plate 4), Michigan, and Bayport formations indicate that the three units were folded and faulted similar to the Devonian age Dundee Formation and Traverse Group (Plates 2 and 3) .
Pleistocene and Pennsylvanian strata were examined to deterraine whe der similar folding and faulting had occurred.
The surficial Pleistocene stratum, approximately 358 feet thick beneath the site , was determined to be unusable for stratigraphic analysis because of a lack of reliable information and mappable units. 'Ihese deposits are not subdivided on oil-and-gas and brine logs, consequently for this study no detailed work could be done on this geologic l sequence. It can be reported that surface ruptures and B internal deformation of tectonic origin are not present in the l i
Pleistocene sediments occupying the Michigan Basin based on l
literature review and site area investigations. l Water wells were unusable as they rarely penetrated bedrock and lacked geologic descriptions. Brine, coal, oil, and gas well logs were generally usable in that they subdivided all of the Paleozoic units penetrated. Seismic lines that crossed the study area were not usable because of unresolvable l
noise distortion of signals from the top of the Marshall l l sandstone upwards.
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'Ihe Pennsylvanian Saginaw Formation (Figure 3) was examined in detail because it is represented by reliable data, well described in the literature, and contains units mappable l on a multi-section and/or township basis. Saginaw coals are mappable in several areas where known structures of I
post-Mississippian age are present. Past and present work on the Pennsylvanian stratigraphy has been applicable only on a l
basin-wide scale.
l Structure contour maps of the Bayport and Michigan formations were found to be generally unreliable on a regional I
scale because of erosional effects prior to and during Saginaw time. In areas where the Michigan Formation was not eroded, I
such as in Midland Township, it was found to reflect similar l structures found in the Marshall Formation and older units.
This study was undertaken to determine the age of l
deformation in the study area, and demonstrates the complex but mappable stratigraphy of the Saginaw on a local scale.
3.0 PREVIOUS WORK l Lane (1902) compiled the first work detailing the Michigan coal sequence and recognized the complexity of its internal l s tr atigraphy . He stated that the coal seams undulate independent of the general shape of the Saginaw surface and the l
basin in which it was formed. The coals were found generally l to be thicker in paleotopographic lows.
Kelly (1936) stated that the center of the basin underlies l Saginaw Bay, and that post-Devonian deformation may have I
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continued into Pennsylvanian time. @is was based on the ,
l assumption that a unit, in both Jackson and Saginaw Counties, is the Verne Limestone and was mappable. He recognized a i
series of coal beds folded around a northeast-trending axis which he felt was drape folding over positive elements on the l
pre-Pennsylvanian substrate. Kelly also recognized numerous l minor structures attributable to sof t sediment deformation, j Shideler (1963 and 1965) and in McKee and Crosby (1975) l divided the Saginaw into three units on the basis of floral and faunal differences. The boundaries cut across lithologic horizons and are difficult to apply regionally or without gcod l geologic namples (Figure 9) . Shideler indicates that the Saginaw was deposited on deformed Mississippian strata. A 1
l pre-Pennsylvanian j E paleogeologic map shows removal of the Bayport Limestone and exposure of the Michigan Shale in the core of anticlines l resulting in northwest-northeast-trending lineaments (Figure 10). %e study was done on a regional scale.
Cohee (1950) stated that the Saginaw Formation was 1
deposited on gently folded and eroded Mississippian strata. He further stated that folding was pre-Pe.nnsylvanian in age and l that subcrop mapping of the Saginaw was not possible due to its environment of deposition.
I Ma tthews (1965) evaluated the coal reserves and geology of Garfield 'Ibwnship, Bay County, for Dow Chemical Company.
Structure contour and thickness maps of the main seam, assumed l to be the thickest seam in all borings, show northwest-trending Weston Geophysical l TJ
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l folds. Pennsylvanian channel cutouts, coal splits, and l post-Pennsylvanian stream channels were determined by Matthews to be common in the area. Matthews further suggested that I there may be six separate seams rather than one major seam with splits. Folding of the main c<al was not studied.
I Kalliokoski (1976) updated Cohee's (1950) evaluation of the coal reserves and geology of the Saginaw for the Michigan Basin. Age of folding and/or faulting is post-Mississippian l, and pre-Pennsylvanian.
Prouty (1976a) states that the folding and faulting is i
pos t-Early Mississippian (pos t-Osagean) in age.
l Chittrayanont (1978) studied the hydrology of the Saginaw in Garfield 'Ibwnship, Bay County. He shows (Figure 8) tha t the l Saginaw was deposited upon deformed Mississippian strata.
Strutz (1978) studied the Bayport Limestone of I
Mississippian age, as well as Pennsylvanian and Jurassic age B. s tra ta . He found that the structure contour map for the base of the Bayport and the unconformity between the Pennsylvanian l and Mississippian shows no structural similarity. '1h e pre-Pennsylvanian paleogeologic map by Strutz shows erosion of the Bayport exposing the Michigan in the cores of northwest and northeast-trending anticlines suggesting folding occurred prior l.
to Pennsylvanian time.
l Stark and Mcdonald (1980) described the groundwater regime and geology of the coal deposits in Garfield Township, Bay County. They divided the Saginaw into basal sandstone, lower l
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shale, main coal, and upper shale (Figure 7). %e structure
) contour map on the main coal, identified as the thickest coal in each boring , shows northwes t-trending folds. % e apparent f
folding of the coal is the result of correlating the thickest seam between borings regardless of other mappable stratigraphic units present. We sandstone unit was drilled to a maximum of
( 30 meters and its base was never penetrated. Structure maps of the sandstone, the lower shale, and the upper shale units reveal no discernible trends. Folding of the main coal seam was not s tudied.
l 4.0 STRATIGRAPHY
) Marshall Formation The oldest unit examined in this study is the Marshall l Sandstone of Early Mississippian (Osagean) age (Figure 9). We sandstone consists of two informal members, the upper White I
Marshall (Napoleon Sandstone) and the lower Red Marshall. We l
Marshall varien from 100 to 250 feet thick in the study area.
Miciligan Formation l We Marshall is unconformably overlain by the Michigan Formation of Late Mississippian (Meramecian) age (Figure 9) .
The Michigan is composed predominantly of shale interbedded with sandstone, gypsum, and limestone. A brown limestone or l
dolomite commonly occurs at or near the base of the Michigan.
Identifiable marker beds used by de oil and gas industry in the Michigan Formation are the Michigan " Stray" Sandstone and the " Triple Gypsum".
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shale , main coal, and upper shale (Figure 7) . We structure l contour map on the main coal, identified as the thickest coal in each boring, shows northwest-trending folds. he apparent l
folding of the coal is the result of correlating the thickest seam between borings regardless of other mappable stratigraphic units present. W e sandstone unit was drilled to a maximum of l 30 meters and its base was never penetrated. Structure maps of the sandstone, the lower shale, and the upper shale units l
reveal no discernible trends. Folding of the main coal seam was not studied.
4.0 STRATIGRAPHY l Marshall Formation The oldest unit examined in this study is the Marshall Sandstone of Early Mississippian (Osagean) age (Figure 9) e he sandstone consists of two informal members, the upper White l
Marshall (Napoleon Sandstone) and the lower Red Marshall. We l Marshall varies from 100 to 250 feet thick in the study area.
Michigan Formation l The Marshall is unconformably overlain by the Michigan Formation of Late Mississippian (Meramecian) age (Figure 9) .
I The Michigan is composed predominantly of shale interbedded with sandstone, gypsum, and limestone. A brown limestone or dolomite commonly occurs at or near the base of the Michigan.
Identifiable marker beds used by the oil and gas industry in the Michigan Formation are the Michigan " Stray" Sandstone and the " Triple Gypsum".
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l Bayport Formation l
The Bayport Formation lies unconforrtably upon the Michigan and is of Late Mississippian (Meramecian) age (Figure 9). We l Bayport as defined by Iasemi (1975) is composed of three limestone / dolomite members with interbedded shales and l
quartzose sandstones. The Bayport was eroded or partially W
eroded by fluvial processes between Late Mississippian and Pennsylvanian time.
[ Saginaw Formation The Saginaw Formation of Pennsylvanian (Morrowan to l
Atokan) age (Figure 9) lies unconformably upon either the l
Bayport or the Michigan throughout the study area. The Saginaw is composed of fluvial and marginal-marine sandstones and j shales with minor interbedded gypsum, coal, and limestone units. We Saginaw varies from less than 100 to greater than l 700 feet in thickness.
The lowest member of the Saginaw is the Ferma Sandstone, a l
white to yellow mature sandstone, locally exceeding 200 feet in thickness (Figure 9) . The Parma represents the inir.ial erosion l
of the Mississippian strata during Pennsylvanian time . Where l the Parma is absent, either a black to gray-black shals or a gray shaley sandstone of equivalent age or younger commonly is I
present.
Overlying the Parma is a series of interbedded shales and sandstones of variable thickness. We Verne Limestone , the only other formally named member of the Pennsylvanian in I
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1 II-8 Michigan, is present only locally and poorly developed in this area (Figure 9) . The equivalent of the Verne, a brachiopod and cephalopod rich gray shale (Cross, 1981b), is present but was not consistently identified on the geologic logs. The Verne varies in thickness, lithology, extent and is probably mappable only on a local scale when present. The member was deposited by a marine invasion extending out of Illinois and Indiana that covered an embayment extending from Jackson northward to Bay City, Michigan. Kelly (1936) attempted to use this as a marker W bed and map structures. Based on Shideler (1965) and this study, it is indicated that the Verne Limestone is not acceptable as a mappable horizon on a regional scale.
Coal occurs in discontinuous, lochlly channeled, and split seams that were deposited in topographic lows or abandoned river meanders. We geometry of the coal seams indicates a complex fluvial environment interrupted by sporadically restricted marine invasions.
The coal sequences are cyclothemic. Due to differences in environment of deposition however, they are not classic cyclothems compared with those found in the Illinois or Appalachian basins (Mc Kee and Crosby , 197 5) . Marine limestones and shales are regionally thin or absent. The Saginaw coals generally are underlain by a paleosoil (underclay) or by a black shale. W e coal commonly is overlain by a black shale up to 50 feet in thickness. W e black shale, in turn, underlies a gray shale or siltstone. Split coal seams are the result of l
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overbans flooding by rivers which deposited large amounts of sand, clay, and silt in the topographic lows and interrupted coal development temporarily.
Stratigraphic members, coals, or sequences may be difficult to trace basin-wide due to rapid variations in depositional environment. The strata to the west and south of the study area show an increase in marine limestone and shale.
Also to the west there is a decrease in coal and an increase in gypsum and red beds. %e coals do not represent basin-wide B seams but can be correlated palynologically.
We strata at the Corunna (west of Corunna) and Grand Ledge (west of Lansing) quarries are good examples of complex interfingering of marginal marine and fluvial environments.
Figure 11 shows sandstone units thickening and thinning rapidly as well as overlapping. Because of scale a thin limestone present near the base of the Corunna Clay Pit facing southwest cannot be seen in the photographs. % is limestone is absent on the north side of the pit. Also, the massive shales are actually a series of interbedded siltstones, gray and black )
shales. Inw angle slump faulting is present at the Grand Ledge Quarry; this does not seem to be related to pre-Pennsylvanian I structural deformation (Cross,1981a and b) . Soft sediment deformation that has resulted in faulting has been documented l at Grand Ledge, Williamston and Sebewaing where the Pennsylvanian strata are thin and near the present subcrop boundary. % ere is no evidence from mine reports and in the s _e_
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l literature of faulting caused by soft sediment deformation in l the study area which is situated near the center of the basin.
Coals at both quarries thin, pinch out, split, and are cut by channels within short distances.
Jurassic Strata I
Upper Jurassic (Kimeridgian) strata occur in the west and l southwest parts of the study area and lie unconformably upon the Saginaw. The strata consiat of red beds, are not very well l defined, and are less than 75 feet thick.
Pleistocene and Recent Sediments l
Pleistocene and Recent sediments within the study area unconformably overlie either the Saginaw or Jurassic strata and vary from 50 to greater than 400 feet in thickness.
I 5.0 DISCUSSION Marshall Sandstone Structure Map l
%e top of the Marshall Sandstone was contoured to determine the presence of faults and folds. It was found that both the northwest and northeast structural trends are l prevalent in the Marshall (Plate 4) .
Northeast-trending faults and folds associated with the I
I Porter Oil Field (Plate 4) cross-cut and offset the major northwest axis of the anticline in several places. We Mt.
l Pleasant Field (Plate 4) shows similar secondary structures L cross-cutting and offsetting the major east-west axis.
The Kawkawlin Oil Field (Plate 4) is on a northwest-F k trending faulted fold, cross-cut and offset by a secondary e
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l northeast-trending fault system. %e most northern extension of the secondary fault system is the Pinconning Oil Field (Plate 4).
l The major northwest trend is present in the site area.
%ese northwes t structures are on trend with the Edenville, Sanford, and Carrollton oil fields (Plate 4) . The northeast trend is also present in the site area, on line with or i
parallel to the trend of the Pinconning structure. Other minor l east-west trending folds shown indicate that the area did undergo deformation.
Cros s-sections Sixteen cross-sections were drawn to determine the I
relationship of folding and faulting of pre-Pennsylvanian j strata to the Saginaw Formation in the study area (Plate 1).
Seven cross-sections, A through G, incorporated data from I surface elevation to the top of the Dundee (Devonian) Formation.
An additional cro:Is-section, H, intersecting the Kawkawlin Field includes strata from surface elevation to the top of the Marshall Sandstone. Three cross-sections, I through J, in Garfield Township utilize coal test data. Five others, L
! through P in Midland and Williams townships, incorporate coal test data that occur over mapped structures in the Marshall i
Sandstone and " Traverse Lime". %ese cross-sections have a horizontal to vertical exaggeration of approximately twenty to one.
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'Ihe purpose and intent of the cross-sections A through H l were to determine if any structural relationships exist between '
the Pennsylvanian and older s trata. Wells that did not l differentiate Pennsylvanian strata but fell near or on the cross-sections were not used. We cross-sections also were l
drawn independent of structure contour maps as their purpose l was to decipher the age of folding and faulting. Cross-sections I through P use coal test data because brine, salt, l disposal, oil, and gas wells did not contain sufficient detail that was needed to carefully map the Saginaw Formation.
I Cross-sections A to H illustrate the predominant northwest-trend and secondary northeast trend. Six of these sections intersect known oil fields. We sections illustrate previously l interpreted structures, for example, northeast-trending faulted folds (Pinconning structure), as well as known structures, such I
as northwest-trending folds (Kawkawlin, Porter, and Edenville i s tructures) .
1 Cross-section A l Cross-section A trends northeast from the Porter Oil Field, crosses the Kawkawlin anticline, and ends just north of the Pinconning Oil Field (Figure 12) . The Porter Field appears as a subtle anticline. We Kawkawlin structure is shown as a i
faulted anticline, southwest . side down. The fault has l displacements of 490 and 375 feet in the Dundee and Marshall respectively. Because the data off the plane of the cross-section were not used, the fault was given maximum B
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l possible displacement and not drawn as a faulted-fold as in l Plates 2, 3, and 4. We fault probably does not attain maximum displacement as shown in cross-section. 'Ivo shale and l siltstone units in the Saginaw Formation show no displacement or associated structure over the fault plane.
l Cross-section B l Cross-section B trends eastward, passing through the Power Block (Figure 13) . %ree faults east of the Power Block are inferred from the data. The fault closest to the Power Block is reflected in the lower part of the Traverse and top of the Dundee limestones. The other two faults suggest a graben in all of the formations except the Dundee. Wells 1D through 10M provided no data of the internal stratigraphy of the Saginaw.
Correlation between wells 11579 and 10853 fail to indicate faulting in the Pennsylvanian. A bedrock high occurs in Well 9M. mis is probably due to misinterpretation by the drill.er.
Cross-section C Cross-section C trends northeast and extends from south of the Porter Field to just north of the Kawkawlin anticline (Figure 14). The cross-section indicates a syncline flanked by the gently sloping northern limb of the Porter and the steeper 5 southwestern dipping limb of the Kawkawlin structures. The Bayport becomes progressively thinner toward the northeast due to erosion. The Saginaw Formation is predominatly shale off structure and sandstone on structure.
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II-14 l Cross-section D l Cross-section D trends southeast crossing northeast trending structures (Figure 15) . Faults clustered toward the f
northwest part of the section do not appear in the Saginaw Fo rmation. We Bayport Formation has been eroded over the l
f aults suggesting Early-Pennsylvanian stream erosion following l the trend of the faults. Upper Saginaw units do not reflect the folding and faulting interpreted in Mississippian or older l units.
Cross-section E l
Cross-section E trends southeast along the axis of the Porter Oil Field (Figure 16) . W e section intersects a sharp northeast-trending anticline which appears in all Devonian and l Mississippian strata except the Bayport. We Bayport has been eroded over the structure by a Pennsylvanian sandstone. The l \
northeast-trending anticline is not present in the Pennsylvanian section.
Cross-section F l Cross-section F trends southeast, crossing the Pinconning '
Oi; Eield (Figure 16). S e cross-section indicates secondary l
anticlinal and synclinal structures in the vicinity of the oil field. Jackson (1958) interpreted a fault in this vicinity, as shown on Plate 4.
l Cross-section_G, Cross-section G trends southeast and intersects northeast-I trending structures (Figure 17) . Well 9856 identifies a B
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L II-15 syncline which has been shown as a fault on Plate 4. We Saginaw Formation over this fault indicates no similarity to structure in the lower s trata.
( Cross-section H Cross-section H trends northeast along the Kawkawlin Oil Field (Figure 17) . We top of the Marshall Sandstone (Plate 4) reflects the presence of the Kawkawlin Anticline. The top of the Michigan Formation has been beveled by processes during I
{ Saginaw time. The internal stratigraphy of the Saginaw is )
horizontal over the structure. Wis is best illustrated by a coal seam extending from well 1375 to 5831, and which is
- relatively flat lying compared to the top of the Marshall Sandstone (Plate 4).
{ Saginaw Cross-sections and Structure Maps he major coals in the Garfield and Midland-Williams coal, fields constitute a mappable zone (Figure 18) . The zone is defined as a cyclothem sequence of coal bearing strata, bounded by massive gray shales that are greater than ten feet thick.
{ We lower gray shale is underlain by a massive sandstone, also greater than ten feet. Several of the coal tests completed af ter 1950 identified the upper gray shale to be fossiliferous, containing brachiopods, suggesting this to be equivalent to the Verne Limestone. We coals were interpreted to be of Atokan age according to Wanless and Shideler's 1975 classification (McKee , 197 5) .
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he coal seam in Garfield is commonly split into two B seams, designated here as the A and B split. Further splitting is present but not common. We A split , zero to four feet I thick, is found near the base of the zone and is the most laterally persistent. Se B split present near the upper shale varies from zero to three feet thick.
Black shales are commonly associated with both coals. We l
A split generally is overlain by a black shale varying from two l to thirty feet thick and underlain by black shale less than four feet thick. The black shale overlying the B split generally is less than four feet thick.
thderclays commonly are associated with both coal and l
black shale units. Sandstones are randomly distributed both l laterally and vertically and have a thickness of less than eight feet. i l 'Ivo coal seams are present in the Midland-Williams Field and they are designated A and B (Figure 18). The Midland-l Williams zone is very similar to the interval mapped in Garfield 'Ibwnship except that the interval between the two l
seams and over the B seam is thicker. Both seams are l consistently thicker than in the Garfield Coal Field and splitting of both seams is common. Appendix II lists " top of f
zone" in elevation for coal field data.
E i Garfield Coal Field l
Ma tthews (1965), and Stark and Mcdonald (1980) showed a l main coal seam in Garfield 'Ibwnship with northwest-trending Weston Geophysical
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I folds (Figure 7). Both studies are based on the assumption j that the thickest seam in each boring is the same bed throughout the coal field. Matthews (1965) states that there l were probably several rather than one seam present. Cross-sections I through K (Figure 19) show that the strata arc l
complex and the thickest seam is not the same from well to well.
Detailed examination of the coal field data discussed by l
Ma t th ews , Stark and MacDonald indicates ten coal seams were l present. 'Itte two most extensive were consistently penetrated by drilling and found to fall within the mappable zone. The I
structure contour map of the top of this mappable zone did not show similar trends to those seen in the Marshall, Traverse, l
and Dundee formations (Figure 20) . Rather , they are l interpreted here as reflecting the local fluvial and marginal marine-fluctuations through time.
l The three cross-sections in Garfield 'Ibwnship show that the morphology of any bed in the Pennsylvanian is related to l
its environment of deposition. Bed morphology can be modified l by sof t sediment deformation, examples of which can be seen at the Grand Iedge Quarry (Cr oss , 19 81b) .
l Midland-Williams Coal Field Several large scale structures are interpreted in the l
Dundee, Traverse, and Marshall formations near the site in j southeast Midland Township, Midland County, and southwest Williams Township, Bay County. A known coal field overlies l
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I II-13 some of these deep structures and several cross-sections were '
l drawn to determine if the Pennsylvanian reflected these s tructures .
l Cross-section L and M Cross-section L (Figure 21) is a northeast trending 1
section that indicates the zone and coals have no structural similarity to Devonian-Mississippian mapped units.
Cross-section M (Figure 22) trends northeast. 'Ih e l identified zone and coal beds show no structural relationship to the lower Marshall and Traverse units.
l Cross-section N, O, and P Cross-section N (Figure 23) trends northwest and indicates the zone and coal beds do not reflect structure shown in the
( Marshall and Traverse units.
Cross-section O (Figure 24) trends southeast and l
intersects northeast trending faults and folds. The zone and l
coal indicate no relationship to the gentle folding in the Marshall Sandstone and the fault in the Traverse Limestone.
l Cross-section P (Figure 24) trends northwest and also indicates that the zone and coal seam structural configuration are independent of the structure shown in the Marshall and Traverse units.
l A structure contour map of the zone in the l Midland-Williams coal field shows no similar trends to those found in the Marshall, Traverse, and Dundee (Figure 25) .
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l A comparison of the Michigan Oil and Gas Map (1979) l (Figure 26) and work done by Shideler (1963), Strutz (1978),
and Lasemi (1975) suggest tha t many of the northwest- and l northeast-trending oil fields coincide with areas of thin or eroded Bayport Limestone. 'Ihe Saginaw in the study area lies 1
over these structures undeformed as based on cross-sections A l
through P and the two coal zone structure maps. These structures probably represent pre-Pennsylvanian topographic l highs subject to erosion before deposition of Pennsylvanian sediments.
6.0 CONCLUSION
S B Constructed cross-sections and contoor maps as well as literature indicate that deformation occurred prior to l deposition of the Sagindw Formation. Folding and faulting in Mississippian and older formations concluded prior to l
1 Pennsylvanian (Atokan) time.
Minor folding and faulting recognized within the Saginaw l
is neither tectonic in origin nor controlled by deformation in l older strata, but is due to soft-sediment slumping and basin geome try at the time of deposition. Sof t sediment deformation that has resulted in low angle faulting has been identified only at Grande Ledge and Williamston in Jackson County and l
Sebewaing in Huron County. Both localities are near the l boundary of the present day Pennsylvanian subcrop limits.
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SUMMARY
j Lineament analysis of Landsat false color imagery (scale 1:1,000,0C0) of the southern Michigan peninsula was performed l to delineate potential geologic structures within the Michigan Basin. Cultural, topographic , geomorphologic, and geologic l
linear features are observable on Landsat imagery. Mapped B lineaments (Figure 27) corresponded mainly with contacts i
between deposits associated with glaciation (moraine , outwash ,
l glacial drif t , lake sediments , and strandline deposits) .
Potential geologic explanations for the undetermined l
lineaments, designated "U", are presented. 'Ihe general orientation of the lineaments of undetermined origin appears to l
parallel and suggest coincidence with the regionally pervasive l northwest and northeast trends (the former being dominant) of bedrock structures in the Michigan Basin. For example, faint northeast-trending lineament U-11 is in the approximate planar position of deeply buried structural trends, interpreted ac l
f aults in this study shown on structure contour maps of the Devonian-Mississippian mapped units (Plates 2, 3 and 4).
l However, cross-sections (Figures 12-17, 21-24) variably l demonstrate that the Pennsylvanian rocks are: (1) unaffected by deformation mapped in the lower units; (2) mantled by thick I
glacial deposits exceeding several hundred feet; and (3) j stratigraphically characteristic of sedimentological processes I
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I III-2 l
unlike those operative in the deposition of the older rocks.
Thus, the spatial correlation of bedrock structures and "U" lineaments is considered coincidental rather than a priori.
No lineament was mapped for the linear segment of the Tittabawassee River southeast of Midland. In Midland, th e.
river appears to be controlled by man-made structures near the Dow Chemical plant. To th e sou theas t , the river flows along the somewhat linear contact between glaciofluvial over till deposits on the northeast , and glaciolacustrine and glaciofluvial deposits on the southwest. No bedrock structures mapped as faults in this study (Plates 2, 3, and 4) correlated with the linear segment of Tittabawassee River.
2.0 INTRODUCTION
Analysis of lineaments in the southern Michigan peninsula for Consumers Power Midland site was accomplished using Landsat imagery at a scale of 1:1,000,000. A mosaic of false color composite prints o f imagery bands 4, 5, and 7 was examined for lineaments and patterns indicative of geologic structures.
Lineaments were plotted on an acetate overlay and compared to available geologic and surficial geologic maps and data of the southern Michigan peninsula (Flint, 1959; Kelley , 1968; Stone &
Webster , 1978) . Lineaments were grouped by letter designation according to possible origin (G-glacial, U-undete rmined)
(Figure 27) , and are referenced in the descriptive text that follows.
l I
l _C _
l III-3 I
l 3.0 LINEAMENT IDENTIFICATION I l Lineaments interpreted for this report follow O' Leary and other s (1976) terminology: "a lineament is a mappable, simple or composite linear feature of a surface, whose parts are aligned in a rectilinear or slightly curvilinear relationship l
and which differs distinctly from the patterns of adjacent l
features and presumably reflects a subsurface phenomenon".
Linear features including cultural, topographic, geomorpho-l logic, and geologic are observable on Landsat imagery. All o f those features may indicate an underlying geological origin.
l Of the bedrock structures reported in the Michigan Basin l
(broad anticlines and synclines, monoclines, faults, and joints) faults with abrupt linear contacts should be the most l readily observed as lineaments on LANDSAT imagery. However, tectonic structures in pre-Pennsylvanian rocks are masked by l
the overlying, Pennsylvanian rocks and Pleistocene glacial I deposits. In order to have pre-Pennsylvanian faulting detected l
on LANDSAT imagery, some anomalous surficial material condi-l tions must result from subsequent draping and/or fracturing of post-Mississippian deposits. The resultant enhancement of permeability along an alignment of hydrologically-affected surficial deposits could produce lineaments visible on LANDSAT I l
imagery. 'Ihese conditions may be responsible for certain l lineaments of undetermined (U) origin described below, although it cannot be demonstrated.
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Lineaments associated with previously described, l northwest-trending structures (Deep River, Nor th Adams, Howell, Incas-Monroe , and Albion-Scipio) were not observed during this l
s tudy, although the Albion-Scipio structure (Wor thing , 1975)
W and th e Howell Anticline (Drake and Vincent , 1975) are reported to possibly correspond to observed LANDSAT lineaments. Thus, a l one to one correlation of the regionally dominant northwest-trending structures to interpreted lineaments is not possible.
l It is even more uncertain whether the less pronounced northeast-i trending pre-Pennsylvanian bedrock structures would be observed l
on LANDSAT imagery.
j 4.0 SURFICIAL GEOLOGY Michigan is covered for the most part by a thick blanket l of surficial materials associated with Wisconsinan glaciation.
Flint (1959) has mapped numerous moraines associated with the l
late Pleistocene ice margin. Material washed from the glacial l lobes produced outwash plains of sand and gravel in contact with the moraines. Sedimentation within ice-dammed, high-level l lakes lef t lake deposits of sand, silt, and clay. These deposits have been modified by shoreline processes and fluvial i
erosion to produce the presently exposed relief. Vegetation patterns corresponding to various soil profiles of the I
surficial materials have been altered and enhanced by cultural l activities (clearing , agriculture) to produce s trong lineamen ts . Such lineaments are described below under a "G" designation.
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5.0 GEOLOGIC HISTORY I The Michigan Basin is situated on the northeastern edge of the interior platform bounded by the Canadian shield to the l
north and the Appalachian Basin to the southeast. Subsidence of the Precambrian basement initiated basin development and continued at variable rates during the Paleozoic. A thick l sequence of marine clastics, carbonates, and evaporites was deposited and periodically uplifted and eroded. The varying I
sedimentary inputs and basin tectonics were related to the orogenic activity of the surrounding archs and the Appalachian geosyncline. 'Ihe Alleghanian orogeny (Late Permian) marked the l withdrawal of the epicontinental sea and the end of marine deposition in the Michigan Basin. Local lacus trine sedimentation occurred during the Jurassic, but erosion predominated from the Permian to the Recent .
I The circular subcrop pattern on the lower Michigan l peninsula reflects the basin shape. Sedimentary deposition concurrent with basin subsidence resulted in the gentle l basinward dip of the units. Iow amplitude northwest-trending folds (Figure 4) are ascribed to a number of causes: deep I
seated faulting , compaction, and evaporite dissolution ar.d flowage. The bedrock and geologic structures of the lower Michigan peninsula are known mainly from drilling data because l the overlying glacial drif t. averages 200 to 300 feet in thickness.
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I III-6 6.0 LINEAMENTS l Location of lineaments relative to cultural, vegetational, and hydrologic features, as described below, was determined l from the following 1:250,000 scale topographic sheets:
Cheboygan, Alpena, Traverse City, Tawas, Midland, Flint, Gr and I
Rapids, De tr oit , Milwaukee, and Racine.
B 6.1 "G" Lineaments j
Lineament G-1 l Lineament G-1 extends northeastward for approximately 15 miles between Kalkaska and Elmira as a sharp boundary i
between dark-toned, forested upland and light-toned, open valley. The valley is underlain by Wisconsinan age outwash sands and gravels. Ib the southeast the upland area is formed I by a section of the Port Huron moraine ( Flin t , 1959). The lineament is evident due to the contact between the two l
surficial materials, strongly enhanced by the resulting vegetational and cultural differences.
1 Lineament G-2 l Discontinuous dark-toned and contrasting dark- and light-toned lineament G-2 extends northeastward between Woodard Lake and the Sturgeon River, approximately 10 miles northeast o f Gaylo rd . To the northeast , the Sturgeon River valley cutting glacial outwash sands and gravels is the northwestern terminus of a lobe of the Port Huron moraine. The narrow dark-toned lineament of the river channel is probably l controlled by the relatively resistant till paralleling the B
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l s tream valley. Sou thwes t o f Gaylord , the lineament occurs j along the northern contact between the elevated Fayette moraine (Flint, 1959) and the essentially flat adjacent outwash sands and gravels. The southwestern segment of the lineament near Woodard Lake occurs on the contact between the Port Huron I
moraine and outwash sands and gravels. Here, parts of the elevated moraine are cleared, whereas the lower outwash l
deposits in the Manistee River valley remain forested.
I Lineament G-3 This dark-toned discontinuous lineament trends in a l
curvilinear fashion between Richville and Bad Axe, parallel to l the southeast shore of Saginaw Bay. Topographic contours indicate an increase in slope, coinciding with the northwes t I margin of the Port Huron moraine. The topographic alignment associated with the lineament is likely also enhanced by l
subparallel shoreline features occurring sporadicall.y along the lineament.
Lineament G-4 l Parallel to G-3 approximately 4 miles to the southeast is lineament G-4, coinciding with the boundary between forested I
and field vegetative patterns. The topographic relief between Vassar and southeast of Bad Axe is more subdued than that l
described for G-3.
l The lineament coincides with the southeastern limit of Saginaw ice, marked by the Port Huron moraine. This contact between till and lacustrine sands, silts, and clays is enhanced by the dark-toned vegetation along the Cass River.
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Lineament G-5 l Lineament G-5 is a wide, dark-toned, discontinuous lineament, extending northeastward between Millington and l Ubly. The linear pattern of vegetation (forest) is apparent on the Landsat imagery and the Flint, Michigan 1:250,000 scale i
topographic sheet. This lineament coincides with the l northwestern margin of the Juniata moraine (Flint, 1959), in contact with lake deposits to the northwest and outwash I deposits to the southeast.
Lineament G-6 l
North-northwest trending lineament G-6 is a narrow dark l
toned lineament extending between Croswell and Harbor Beach.
The eastern margin of the Port Huron moraine coincides with I G-6. Numerous small drainages head along the till-lake deposit contact and flow eastward towards Lake Huron. The moraine I
forms a drainage divide; just inland of the lineament streams drain westward, then south along the Black River. A strandline marking a higher lake level may also enhance the lineament as l it is superimposed upon the moraine-lake sediments contact.
Lineament G-7 I
Lineament G-7 parallel to and southwest of G-6 is a curvilinear dark-toned lineament. 'Ihis lineament corresponds to the western limit of the Port Huron moraine. The dark-toned
[ vegetation occurs in the valley of the Black River described above.
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l Lineamen t G-8 l A discontinuous contact between open fields and forested areas corresponds to lineament G-8, extending northwest from Greenville to 5 miles northwest of Big Rapids. The forested area corresponds to the Valparaiso moraine (Flint, 1959), which l
is in contact with drift and outwash sands and gravels underlying the cleared areas.
l Lineament G-9 I Lineament G-9 parallels G-8, 20 niles to the southwest.
This lineament also corresponds to discontinuous linear l
boundaries between open and forested areas. In this case the j open area generally corresponds to the Lake Border moraine i
(Fl in t , 1959), and the forested area to outwash deposits. The l Midland, Michigan 1:250,000 scale topographic sheet indicates that swampy conditions in the outwash deposits may have l
precluded clearing of the forests.
i Lineament G-10 i
Lineament G-10 is a faint, dark-toned lineament trending l northeastward between Otsego and Portland through Jordan and Tupper lakes. The northeastern section is a slight topographic trough of swamps, lakes, and the Little 'Ihornapple River.
Flint (1959) maps a narrow band of lake deposits between moraines and other glacial drif t. 'Ihis and other topographi-l cally low channels connected high levels of southern Lake Michigan and Lake Huron.
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[
Lineament G-ll Lineament G-ll coincides with the St. Joseph River, l
trending northeastward between Fort Wayne, Indiana, and Hudson,
[ Michigan. The lineament c,, curs as a thin line of darker !
{ vegetation cutting diagonally through rectilinear patterned fields. The St. Joseph River parallels the northwestern border
[ of the Wabash moraine in contact with a narrow band of stream-deposited sands and gravels.
Lineament G-12 Northwest-trending lineament G-12 parallels the Kalamazoo River through Battle Creek. It is essentially defined by the linear stretch of the river, without a strong linear vegetation pattern. 'Ihe river flows in a shallow valley, which is filled with lake deposits bounded by outwash nands and gravels and morainal deposits. Initial control of this linear valley was probably due to the surrounding moraines.
( Lineament G-13 Lineament G-13 trende, northwestward along the Madison Drain and the North Branch of the Flint River in northeastern Lapeer County. A dark vegetation band is evident on the Landsa t imagery coinciding with the linear valley. A linear
{ breech in the surrounding moraine and outwash deposits is mapped as lake deposits (sand , silt, and clay) (Flint, 1959).
Lineament G-14 Lineament G-14 is a discontinuous lineament formed by the border between dark vegetation and light-toned cleared areas.
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It trends northeastward between North Muskegon and Sylvester.
l The vegetation pattern is controlled by the types of surficial material along the lineament. Northeast of Muskegon, parallel l
to the Muskegon River, outwash deposits are in contact with I lake deposits. Parther to the northean, lobes of various moraines (Lake Border, Valparaiso) are cut by a linear trend of l outwash sands and gravels.
Lineament G-15 l
Lineament G-15 is a dark-toned lineament extending northwestward between Luzerne and Rose City along a section of l
the East Branch Big Creek. The lineament is a topographic low l
between two lobes of the West Branch moraine (Flint, 1959).
Outwash sands and gravels and lake deposits are mapped in the I
de pression. 'Ihe variation in surficial materials likely controls vegetation patterns responsible for lineament G-15.
I Lineament G-16 Light-toned lineament G-16 parallels G-15, 5 miles to the southwest. G-16 extends between the Inzerne lookout tower and l Prior Lake along the West Branch Big Creek. The lineament corresponds with a sharp boundary between dark red vegetation l
and a band of lighter red vegetation. The lineament does not j
correspond to a mapped contact between surficial materials.
Variation in vegetation types appears to correspond to I undrained swampy areas and to adjacent areas drained by established streams.
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Lineament G-17 Lineament G-17 trends northwestward between Icon Lake and Kleber Dam on the Black River. Dark vegetation streaks of l
limited length (less than 5 miles) are characteristic of the j northeastern tip of the lower Michigan peninsula (Flint, 1959). Lineament G-17, enhanced by stream orientation and the l Kleber Reservoir, stands out as one of the s trongest lineaments. Glacial streamline features such as drumlins, l
fluted surfaces, and crag and tail are responsible for many linear landforms in this region.
Lineament G-18 l Lineament G-18 trends northeastward along the Manistee River and the North Branch Manistee River, between Waterhole l
Creek and Bear Lake. This lineament is defined by the Manistee i
drainages, and a contact between Port Huron moraine and outwash I
deposits. The Manistee River skirts a lobe of the Port Huron j moraine southwest of Sharon.
Lineaments G-19, G-20 Lineaments G-19 and G-20 enclose an area of dense dark-toned vegetation with a high concentration of lakes northeastward between Jackson and Pontiac. The area of dense vegetation is underlain by ice contact s tratified drift, deposited between the Kalamazoo and Mississinewa moraines.
l Meltwater streams deposited sediments in the reentrants between the stagnant Saginaw and Huron-Erie ice lobes (Rieck , 1978) .
'Ihe boundaries of an interlobate zone of stratified drif t sands Weston Geophysical L
[ III-13 and gravels such as kames and ice-walled channel fillings, h sloping gently southwestward in contact with the morainal deposits, are likely responsible for lineaments G-19 and G-20.
A large number of kettle (?) lakes within the stratified drift enhance the interlobate zone. i Lineament G-21
( Lineament G-21 is the northeast-trending boundary of dark-toned and light-toned vegetation patterns between Rhodes and Sterling. The light-toned cleared area coincides with the Port Huron moraine, which is slightly elevated relative to the darker area to the northwest underlain by lake deposits. The
{ vegetational differences enhance the contact between surficial deposits and are responsible for lineament G-21.
Lineament G-22, G-23 Lineaments G-22 and G-23 trend northeastward between Bombay and Standish. G-23 is a narrow dark-toned spike, j
{
l slightly wider at the southwest end. It does not correspond one to one with the drainage systems in the area, however short sections of the Saganing and White creeks may be responsible for defining portions of the lineament. Lineament G-22, approximately 4 miles to the northwest, parallels G-23. This
(
{ discontinuous lineament is defined by the boundary between dark-toned and light-toned vegetation patterns. These patterns b in turn appear to be caused by contrasts between poorly drained and well-drained lake deposits.
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Lineament G-24 l
l Extending northeastward between Matherton and Bay City, lineament G-24 is a continuous lineament formed along a wide 1
dark-toned vegetation pattern and a dark-toned, light-toned contact. Vegetation is controlled by drainages (Maple River) l and variable soil drainage conditions (swamp south of Potato Creek). Surficial deposits that may control these occurrences include the elevated Fowler-St. Johns moraine (Flin t , 1959) and beach strand-lines preserved on the extensive Lake Alma deposits (sand, silt, and clay). Southwes tward-directed glacial scour by the Saginaw lobe paralleling this trend may ,
also influence patterns in this area.
Lineament G-25 Lineament G-25 is a discontinuous lineament that trends northwestward , between Wheeler and Martiny Lake. It is defined by dark-toned light-toned contacts and a faint dark-toned band across light-toned fields. Sections of various drainages including Indian Creek, Coldwater River, and Chippewa River parallel portions of the lineament. 'Ihese in turn are E controlled by the pattern of surficial deposits, including the Ionia and Fowler-St . Johns moraines and related outwash sands and gravels. The lineament generally parallels an outwash deposit that breeches the moraines along a northwest-southeast trend.
Lineament G-26 This lineament extends northwestward between Belding and Sand Lake. 'Ihe boundary between dar k-toned and light-toned Weston Geophysical
III-15 vegetation defines lineament G-26. Sections of Coopers Creek and Wabasis Creek also parallel the lineament. North of the trend outwash deposits remain forested , while to the south, morainal deposits appear to be cleared. The lineament appears to be caused to a varying degree by the above occurrences.
Lineament G-27 Lineament G-27 trends parallel to the Lake Michigan shoreline through Whitehall. We northwes t-trending lineament defines the contact between dark-toned and light-toned vegetation. Wis contact coincides with the northeastern limit of the Whitehall moraine in the area. The area of slightly elevated topography is cleared of vegetation while the lower level lake sediments to the northeast remain densely vegetated, thus defining lineament G-27.
Lineament G-28, 29 Parallel lineaments G-28 and G-29 extend northwestward between West Branch and Lake Margarette, and Selkirk and Grayline. Both 1ineaments are distinguished by the contrast between very dar k-toned and dark-toned vegetation, linear segments of narrow dark-toned bands, and linear segments of light-toned bands. A section of the New York Central Railroad and route 76 enhances G-28. Portions of both lineaments correspond to map patterns defined by the Eldorado moraine in contact with outwash deposits and other glaciel drift.
Topographic relief and drainage patterns controlled by tDe i occurrences of glacial deposits are responsible for enhancement of sections of the two lineaments.
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Lineament G-30 I
Lineament G-30 extends northeastward between Lucas and Shoepack Lake. The discontinuous lineament is expressed by 1
contrasts between light-toned and dark-toned vegetation as well as alignment of light-toned areas within dar k-toned areas.
These in turn correspond to sections of the Eldorado moraine in contact with outwash deposits and other glacial drif t. Areas of high-topographic relief (moraine) enhance sections of the lineament. We northeast.ern segment of lineament G-30, which does not coincide with mapped glacial deposit contacts, may result from a dismantled railroad and the West Branch Big Crcak l between Shupac Lake and Shoepack Lake.
Lineament G-31 Discontinuous lineament G-31 extends between Boon and Waltons. We northeast-trending lineament is formed by the contact between dark-toned and light-toned areas. These tones do not correspond specifically with surficial deposits. The southwestern linear segment corresponds to the contrast between vegetated moraine of high relief in contact with cleared low relief morainal deposits. The northeastern segment corresponds to the area between cleared morainal deposits in contact with densely vegetated outwash deposits in the Manistee River valley.
Lineament G-3 2 Lineament G-32 extends northwestward from Evansport to Union City. We discontinuous lineament is composed of 8
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dark-toned linear sections of Fisher Creek and West Branch St .
( Joseph River, which cut across the northeasterly oriented moraines and outwash deposits in the area.
Lineament G-33 Discontinuous lineament G-33 extends northwestward between Schoolcraf t and Kibbie. It is distinguished on the Landsat imagery al a dark-toned band. Sections of the Black River and the East Branch Paw Paw River are responsible for th e lineament. These stream segments are apparently controlled by the pattern of surficial deposits (ou twas h , till, and lake sediments).
Lineament G-34 Lineament G-34 extends east-northeastward between l Parkville and Homer. 'Ihe lineament is discontinuous and is formed by distinct dark linear segments of vegetation and drainage. Sections of the Notawassepee and Saint Joseph rivers are controlled by the trend of surficial materials. Ou twash sands and gravels were deposited by southwesterly flowing streams between the Saginaw and Huron lobes of the Wisconsinan glaciation.
Lineament G-35 E' Lineament G-35 extends northeastward, north of Sterling.
J l
'Ihe lineament occurs at a boundary between dark-toned and l light-toned vegetation. The light-toned area coincides with the mapped extent of the elevated Port Huron moraine. The l
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dark-toned area corresponds to low lying lake deposits. A l
section of strandline deposits also corresponds to the l
northeastern section of the lineament.
Lineament G-36 l Curvilinear lineament G-36 extends north-northwest between Alcona and the Alpena Air National Guard facility. We I lineament occurs along the sharp contact between dark-toned and ,
I I light-toned vegetation. We vegetation break occurs along the contact between lake sediments near the lake and upland l morainal deposits inland.
Lineament G-37 Lineament G-37 trends northeastward between South Boardman and Kalkaska. A dar k-toned / light-toned vegetation contact l
forms the lineament. The vegetation break corresponds to the l
contact between the Port Huron moraine and outwash deposits.
Lineament G-38 -
l Two parallel northwest-trending lineaments of patchy dark-toned vegetation comprise these lineaments which extend l e between Rolland Center and Lake Mecosta, southeast of Big Rapid s . Sections of Miller Creek, Shingle Bolt Creek, Sylvester Creek, and Black Creek correspond to thie vegetation.
! The drainage does not reflect contacts of surficial' materials but may be a result of topographic relief on various glacia3, l ..
deposits. 'Ihe drainage patt.ern appears to'tiend generally 3 ,
parallel to and normal to the axis of morainal deposits; .,
'/ ,
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I III-19 l l Lineament G-39 I
Curvilinear lineament G-39 extends north-northeastward i
l between Brown City and northwest Sandus ky . The lineament occurs as a narrow dark-toned vegetated area. This band likely l corresponds to sections of drainage ditches which traverse this swampy area of low relief.
~
Lineamen t G-4 0 Discontinuous lineament G-40 extends east-northeast l __
between Portland and south Flint. Light-toned bands of varying l width define the lineament, with darker tones to the south and lighter tones to the north. The complex, discontinuous alignment corresponds, in part, with drainage divides controlled by relief on the Portland moraine (Flint, 1959) in l
contact with lake sediments and other glacial drift. The l contact between the Portland moraine and outwash deposits may be responsible for another section of the alignment, enhanced by the boundary between forested and cleared vegetation pa tlter ns. Complex discontinuous lineament G-40 may be the 1
result of a linear bedrock or structural feature which was enh$nced ormsubdued to varying degrees by overlying bedrock and/or surficial materials.
l Lineament G-41 Lineament G-41 extends northwestward between Burnside and I
Harmon Lake , southeas t of Caro. 'Ihe lineament is a very faint alignment of dark-toned and light-toned patterns. These correspond to contacts between the Juniata moraine and adjacent glacial drift and outwash sand and gravels.
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l III-20 Lineaments which could not be correlated directly with l
previously mapped glacial, lithologic, or structural features are designated U (undertermined) and are described below.
6.2 "U" Lineaments l Lineament U-l Lineament U-l extends northwestward between Sterling l lleights, north of Detroit and Mount Mortis, north of Flint. It .
is expressed as a faint, narrow, dark-toned strip and does not l
correlate with topographic relief, vegetation, or drainage.
{ Lineament U-l cuts normal to the strike of the Pennsylvanian, Mississippian, and Devonian age rocks. Surficial materials mapped by Flint (1959) do not explain the origin of the lineament. A northwest-trending anticlinal axis, bhsed on drilling information, coincides with the trend of this
{ lineament; however, corresponding lineaments are not observed for other parallel anticlinal axes (Stone & Webster , 1978) .
Therefore, the origin of this lineament remains uncertain.
Lineament U-2 j l l Lineament U-2 extends northwestward from Flint River I t
reservoir to Midland. A discontinuous lineament, it varies L
between contrasting vegetation patterns, narrow dark-toned
[ bands , and lighter-toned bands. mis lineament parallels U-1, resulting in the same cross-cutting relationships to lithology j and surficial deposits. %e origin of lineament U-2 is uncertain.
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Lineament U-3 Lineament U-3 extends northeastward between Ionia and Alma. It is a very faint linear tone variation which does not l
correspond to topographic relief or distinct vegetation l
differences. Surficial deposit contacts cut across at an angle, and therefore cannot readily explain the origin of the l feature. Lithologic contacts are buried beneath at least 200 feet of glacial deposits. The northwest-trending l
anticlinal s tructures s trike normal to lineament U-3. We origin of this lineament remains to be determined.
Lineament U-4 l This lineament extends northeastward between Grand Haven and Moun t Pleasant. We lineament is defined by light-toned lines, dark-toned lines, and contacts between dark and I light-toned areas. A relationship between contacts of glacial f
deposits and the lineament cannot be made. However, a broad l change in gross pattern of the surficial materials is apparent crossing the litieament. This also coincides with indentations of the lake sediment borders at either end of the lineament. A number of northwest-trending anticlinal axes are terminated I
along a trend parallel to lineament U-4. Linear anomalies are l also weakly defined on the aeromagnetic and Bouguer gravity anomaly maps of Michigan (Hinze, et al, 1971). No s tructures I are currently mapped to explain the above data.
Lineament U-5 l
Lineament U-5 extends between Rothbury and Paris. It is a l northeast-trending discontinuous lineament formed mainly on l
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boundaries between dark-toned and light-toned vegetated areas.
l Vegetation patterns do not correspond directly with the mapped l occurrences of moraines, outwash, and lake sediments.
Lithologic contacts s trike generally perpendicular to the trend l of lineament U-5. Ibrthwest-trending anticlinal axes are also perpendicular to the trend of this lineament. The origin may be due to a coincidence of alignment of cultural patterns, or to some yet unexplained structural feature. ,
l )
Lineament U-6 l
Lineament U-6 extends northwestward in a curvilinear trend from Tawas Bay to West Lake. We discontinuous lineament is drawn on the contacts between dark-toned and light-toned areas, l
and between very dark-toned and dark-toned areas. The l
vegetation pattern does not correspond well to the pattern of surficial materials mapped along the trend of the lineament l
(Fl in t , 1959). Lithologic contacts do not correspond to the l trend o f lineament U-6. W e axes of mapped anticlinal structures do not correspond to the trend of this linecment. A l
geologic or structural origin of lineament U-6 is not certain.
Lineament U-7 Lineament U-7 extends northeastward between Walkerville j and Bristol. It is defined by a very faint linear pattern of various tones including light , dark , and very dark-toned patterns. Surficial deposits do not correspond to the lineament orientation. The lineament parallels the strike of l
sections of the contact between Pennsylvanian and Mississippian l
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rocks in the area. The extremely vague nature of the lineament may indicate that buried lithclogic variations are a cause of this lineament.
Lineament U-8 l Lineament U-8 extends northeastward from Rose Lake toward Houghton Lake State Forest. A discontinuous pattern of contrasting light-toned and dark-toned areas is responsible for j the lineament. This particular alignment may be coincidental l
because no correlation can be made with the mapped occurrence of glacial deposits. Lithologic contacts and northwes t-trending l
anticlinal axes also do not correlate with lineament U-8.
l Lineament U-9 Lineament U-9 parallels a segment of the southeastern l
shoreline of Saginaw Bay and the Quanicassee River. This alignment does not parallel mapped surficial or lithologic contacts. Based on Landsat lineaments, topography, gravity and l magnetic anomalies, and well data, Drake (1976) suggests the existence o f a northeast-trending graben extending southwest-l ward from beneath Saginaw Bay into the central Michigan peninsula. Stone and Webster (1978) report inferred faults I
defining the borders of this graben. The southwestern border of the inferred structure corresponds in part to lineament l
U-9. However, this lineament could not be traced southwestward into the central Michigan peninsula. Southwestward directed glacial scour by the Saginaw lobe also may have been responsible for lineament U-9.
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Lineament U-10 Lineament U-10 extends between Three Oaks and Lawton. The discontinuous lineament follows the contact between light- and l
dark-toned vegetative patterns. The southwestern segment of l lineament U-10 cuts across the boundaries between till and other glacial drift ( Fl in t , 1959). The northeastern segment coincides with a contact between glacial outwash and lake B sediments. The northeastern e i corresponds to a section of the New York Central Railroad between Decatur and Law'7n.
l Possible faults and anticlinal and synclinal axes are shown parallel to the trend of the lineament (Stone and Webster, l 1978). These structural features are on strike with the southwestern inferred fault of the Saginaw Bay graben described l
above (U-9).
Lineament U-ll Lineament U-ll extends northeastward between Porter and l Beaver, through Midland. % is lineament occurs as an indistinct light-toned zone of vegetation cutting through forest vegetation northwest of Midland. his pattern is enhanced by the Pine River and a road. North of Midland, the lineament is characterized by the contrast between dark-toned l vegetation to the northwest and light-toned vegetation to the southeast. Iake deposits comprise the surficial materials l around Midland. No contacts between surficial deposits or elevated shorelines are mapped along Lineament U-ll. Deeply buried lithologic contacts do not coincide with this l
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lineament. The trend of faults interpreted from drilling I
records from the Marshall sandstone, Traverse limestone, and l l
Dundee limestone does coincide with the northeast-trending lineament. However, since the overlying Pennsylvanian section l does not reflect thece features, it seems unlikely that they are responsible for the lineament.
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7.0 CONCLUSION
S B Lineaments observed on 1:1,000,000 scale Landsat false color imagery correspond mainly to contacts arrong deposits l associated with glaciation, enhanced by differences in vegetation. Glacial deposits include moraines, outwash, ice-contact deposits, undifferentiated glacial drift, lake sediments, and strandline deposits. We underlying lithology ,
l structure, and bedrock topography likely influence the distribution of these deposits, but due to the thickness of the glacici cover, the exact association is uncertain.
Certain lineaments of undetermined origin do not correspond directly to mapped glacial, bedrock, or structural l
features. %ese tend to be very indistinct and may be the result of coincidental alignments of unrelated linear features. Wey may, however, reflect the orientation of l Pennsylvanian channel deposits which radiate southwestward and westward from the Saginaw Bay area (Shideler , 196 3) . Another i
possibility is that the lineaments reflect pre-Pennsylvanian s tructural or lithologic alignments. Wis seems the least B
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I l III-26 likely due to the considerable thickness of overlying and l
tectonically undeformed Pennsylvanian rocks and Plei:it Ocene B glacial deposits.
l.
Northeast-trending lineament U-11 mapped in the vicinity l of Midland corresponds to a structural trend interpreted from drilling records. The trend appears on maps of the Marshall Sandstone, Traverse Limestone, and Dundee Limestone (Plates 2, 3, and 4). However, no lineaments were found to correspond l
with other mapped faults in the Michigan Basin, such as the l
Deep River , Nor th Adams, Howell, Lu cas-Monroe, and Albion-Scipio s tructures. If indeed lineament U-ll does represent bedrock control it would be most likely attributable to post-Mississippian depositional and/or erosional patterns.
I A possible structural origin has been proposed for a l
linear segment of the Tittabawassee River extending 5 miles to the southeast of Midland. This speculation was raised during I cross-examination of testimony presented by Kimble (1981).
However, the river appears to be controlled in Midland by
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man-made structures in the vicinity of the Dow Chemical plant.
To the southeast the river flows along a weakly defined contact between glaciofluvial over till deposits on the northeast, and l glaciolacustrine and glaciofluvial deposits on the southwest (Hutchinson , 197 9) . Northwes t-trending s tructural alignments in the pre-Pennsylvanian rocks may have influenced the distribution of Pennaylvanian strata in the area. However, f
northwest- and northeast-trending structures found in Weston Geophysical
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Mississippian rocks are not observed in Pennsylvanian rocks (Section II) . Structural control of the river, therefore, is I unlikely.
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l l STATE OF STRESS I MIDLAND, MICHICAN/ CONSUMERS POWER 1.0
SUMMARY
In response to intervenor concern and NRC interest in the I
potential for fault movement stimulated by Dow Chemical's fluid l injection program in the Midland Plant site vicinity, published literature has been reviewed concerning stress data for the Michigan basin and adjacent areas. In addition, Weston i
I Geophysical Corporation has interviewed Dow Chemical operations personnel (principally, Bob Nagel, Well Department Manager) to l determine past and current hydrofracture and fluid injection practices. Present available evidence does not suggest l anomalous stress buildup in the Michigan Basin. 'Ihe s tress field is compatible in magnitude and orientation to that ok the I
north-central United States. Present differential post-glacial j rebound rates are uniform over a wide area with no potential for producing anomalous stress buildup at the site. Injection l wells near the site are operated by Dow Chemical Company at pressures significantly below lithostntic loading and therefore I
do not represent a potential for inducing fault motion.
l 2.0 REGIONAL In recent years, active and residual tectonic stress data l for North America hava been reported in a number of studies utilizing earthquake fault plane solutions, in-situ stress l
determination by overcoring and hydrofracturing, x-ray techniques and geologic observations (Sbar and Sykes,1973) .
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l Active tectonic stresses are due to present stresses in the i
I crust while residual tectonic stresses were locked into the rocks during previous tectonic regimes (Eisbacher and l . Bielenstein, 1971). From these data, a broad regional pattern of east- to northeast-trending horizontal compression is evident, extending west of the Appalachian mounta.ns to B mid-continent and from Illinois to southern Ontario, Canada.
The orientation and regional extent of the compressive stress
( in this area supports the hypothesis that the mechanism driving the North American lithospheric plate may be responsible for l
the observed stress (voight , 1969, Sbar and Sykes,1973; Zoback B and Zoback, 1981).
Four hydrofracture tests in a 17,466 foot deep well in
} Gratiot County Michigan, approximately 40 miles southwest of Midland, provide data on the in-situ stress field of the central Michigan Basin rocks ( Ha imson , 197 8 ) . Hydro fracture tests were successful at 4034, 9200, 12,005, and 16,744 foot I
depths in the Devonian Amherstburg Formation, Ordovician j Prairie du Chien dolomite, Cambrian Mt. Simon sandstone, and Precambrian red shale, respectively. Calculated horizontal l stresses increase with depth at the same rate as lithostatic loading. Stress in the Precambrian basement as well as in the l
other tested intervals is not anomalously high relative to the lithostatic load. Horizontal stresses determined at a depth of 4034 feet ( bin, 4278 psi' bax, 7324 psi), agree with I the regional data of horizontal stress exceeding lithostatic B
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L stress in the upper kilometer of the crust. Halmson (1978)
B explains the relatively high levels of horizontal stress at t
4034 feet relative to the deeper tests as the result of j compression due to downwarping of sedimentary layers in the central basin, attaining maximum values in the upper bent l layers.
Stress orientations were not obtained in the hydro-1 fraJtured borehole studied by Ibimson (1978). He presumes the l regional direction of maximum horizontal stress to be N60 *E-N70'E in the Michigan Bas in. Win is substantiated by a l borehole television log report on Dow Chemical brine well number 64 which was hydrofractured. Vertical breakdown 1
fractures observed in the Devonian Sylvania sandstone, between l
4 650 and 4 810 feet , s trik e N72 'E (Seismograph Service Corpora tion, 1970) .
l At a depth, generally greater than 1,000 feet, where l
vertical stress (o y) is either the intermediate or minimum principal stress, hydrofracturing produces vertical fractures.
The maximum horizontal stress (o Hmax) corresponds to the fracture orientation while the minimum horizont.41 stress ;
l (o Hmin) is perpendicular to the fracture plane (Roegiers and
- icLennan , 197 9) . Were is no evidence available from Dow l
Chemical's report on brine well number 64 to determine if pre-existing fractures influenced induced fracture orientations. However, recent work by Abou-Sayed et al, l reported by Roegiers and McLennan (1979) indicates that for B
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( H- v) / 0 fractures tend to propagate perpendicular to the minimum horizontal stress rather than along existing l
fractures. Based on the above discussion and the correlation j of the observed maximum horizontal stress in brine well 64, with previously reported orientations in the north-central United States, the data appears to be valid.
Haimson (1978) explains the lack of seismicity in the l
Michigan Basin as due to low shear stress relative to the mean l stress, 1/2 (oQ+0Hmin). In an alternative explanation cf seismicity, Zoback and Zoback (1981) report that the stress I field is uniform over the north-central region. They speculate that if the broad-scale stress regime dominates local stresses, l
then the location of intraplate earthquakes may be controlled l
by localized areas of inherent crustal rock weakness such as at Anna, Ohio and Attica, New York rather than by areas of concen-l trated s tress. 'Ihus, low seismic activity in the Michigan Basin suggests the lack of properly oriented, potential weak l
zones. Diment (1980) in discussing the significance of aseismic regions of eastern United States points out that areas such as the Michigan Basin may be decoupled from underlying l stress regimes by salt beds and/or thick horizontally-bedded sediments with deformable members. In this latter case, l
release of deep-seated strain, such as that associated with lithospieric plate motion, could be through aseismic slip in the weaker sedimentary layers. The lack of significant seismic l activity in the Michigan Basin may be the result of one or more of the above reported phenomena.
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l Present rates of post-glacial crustal uplif t calculated j from extensive studies of changes in water levels in the Great I
Lakes are on the order of 1.0 to 1.5 millimeters per year for the Midland area. The rate varies from 2.5 taillimeters per year at the northern tip of the lower peninsula to no rebound at the southern Michigan border (Walco tt , 1972). The uniform pattern of differential rebound which occurs over a broad area has no potential for development of. anomalous stress conditions at the Midland site.
3.0 PLANT SITE VICINITY Dow Chemical Corporation in Midland Michigan injects processed brine solutions into the Devonian Sylvania Sandstone, and Dundee Limestone. Presently, three injection wells and a brine well are operating. Data from Dow Chemical (Stone &
Webs ter , 1978) (Washington,1981, personal communication) and interviews with Dow Chemical operations personnel ( Nagel, 19 01, personal communication) indicate that fluids are injected under pressures significantly below lithostatic loads at injection depths.
For example, well number 28 with the highest listed injection pressure of 1,775 psi is 3,580 feet deep. With a lithostatic gradient of 1.15 psi / foot the lithostatic load is calculated to be 4117 psi at this depth. Futhermore, Dow Chemical Company has attempted hydrofracturing in the past.
Breakdown pressures were within predicted estimates based on lithostatic loading, consistent with Haimson (1978). The 5
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hydrofracturing technique is neither cost effective nor l necessary to recover brine and Dow Chemical has no future plans to employ this technique (Nagel,1981, personal communication) .
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l E PART V: REFERENCES AND BIBLIOGRAPHY B ,
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B l REFERENCES AND BIBLIOGRAPHY I Amoruso, J. J., 1957, A structural study of the Northville Oil Field , Wayne , Washtenaw, and Oakland Counties, Michigan:
Master's Thesis, Univer sity of Michigan, Ann Arbor ,11 p. ,
dia grams .
1 Andrews, J. T., 1970, Present and postglacial rates of uplif t B for glaciated northern and eastern North Acerica derived j from postglacial uplift curves: Canadian Journal of Earth Sciences, v. 7, no. 2, par t 2, p . 70 3 -715.
Ardrey, R. H., 1978, Diagenesis of the Trenton Limestone in the Northville Oil Field , Michigan: Geological Society of America Abstracts with Programs, v . 10, no. 6, p. 245-6.
l Arnold, C. A. , 194 9, Fossil flora of the Michigan Coal Basin:
University of Michigan Press, Contributions from the Museum B of Paleontology, Ann Arbor, Michigan, v. VII, no . 9,
- p. 131-269.
l Asseez, L. O., 1969, Paleogeography of Inwer Mississippian rocks of Micnigan Basin: American Association of Petroleum Geologicts Dulletin, v. 53, no. 1, p. 127-135.
Au tra , M. D., 1977, Regional study of the Niagaran and Iower l Salina of the Michigan Basin: Master's Thesis, Michigan State University, Eas t Lansing.
Badiozamani, K., 1973, The Dorag dolomitization model -
application to the Middle Ordovician of Wisconsin: Journal of Sedimentary Petrology, v. 43, no. 4, p. 965-984.
{ Behrens, E. W., 1958, An extension and reinterpretation of a regional magnetometer survey of part of southeastern I Michigan: Maste r 's 'Ihesis , University of Michigan, Ann
} Arbor, 10 p.
Bennett, G. H., 1978, Sedimentology of the Antrim Shale from five drill sites in the Michigan Basin: Master 's Thesis ,
Michigan Technological University, Houghton, Michigan, 75 p.
Be rgs trdm , S . M. , Faber, J. A., and Ibltmier, H. C., 1980, I Geomagnetic reversal stratigraphy and conodont bios tratigra phy o f the Middle Ordovician Trent Limestone ,
B Michigan Basin: American Geophysical Union Transactions, l
- v. 61, no. 5, p . 50.
Black, D. F. B . , Ma cQu own , W . C. , a nd DeHa as , R.J., 19 81, Th e l relation of dolomite associated with faults to the I
stragigraphy and structure of central Kentucky: U.S.
Geological Survey Professional Paper ll51-A, p. A7-A9, A-19.
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l Bleuer, N. K., 1980, Correlation of Pre-Wisconsinan fills of the Lake Michigan lobe and Huron-Erie lobe through the
- 1 bays Valley fill
- Geological Society of America Abstracts with Programs, v . 12, no. 5, p. 219.
B Boudouris, J., 1955, A lithofacies analysis of the Bass Island I and Salina Formations in the Michigan Basin: Master's The s i s , University of Michigan, An n Arbo r , 52 p .
Bradley, J. W. and Hinze, W. J., 1976, Deep borehole gravity l
survey in Michigan: American Geophysical Union Transactions, v. 57, no. 4, p. 326.
l Bricker, D. M., 1977, Seismic disturbances in Michigan:
I
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Michigan Department of Natural Resources, Geological Survey Division, Circular 14, 13 p.
I l
I Brigham, R.J., (1972), Structural geology of southwestern Ontario and Southeastern Michigan: Canadian Mines and Northern Af fairs, Petroleum Resources Section, Ibronto, Pape r 71- 2, 110 p .
Burgis, W. A., 1977, Late Wisconsin history of northeastern I lower Michigan: Ph.D. Dissertation, University of Michigan, Ann Ar bo r , 444 p., microfiche, University Microfilms, Ann Arbor, Michigan #78-4659.
1 Burgis, W. A., 1978, Correlation of ice-front positions with proglacial lakes in northeastern lower Michigan:
Geological Society of America Abstracts with Programs,
- v. 10, no . 6, p. 24 8.
Cambray, F. W., 1977, The geology of the Marquette district - a
) field guide: Michigan Basin Geological Society Field Conference , Gu idebook ,
Ca tacosinos, P. A., 1976, Tectonic development of the Michigan Basin during Late Cambrian time: Geological Society of America Abstracts with Programs, v. 8, no. 4, p. 471.
l Chandler, v. M., 1977, Correlation of Gravity and Magnetic I
I Data over the Great Lakes Region, North America:
dissertation, Purdue University , 18 8 p .
PH.D Chillingar, G. V., 1956, Use of Ca/M g ratio in porosity I studies: American Association of Petroleum Geologists Bulletin, v. 40, no. 10, p. 2489-2493.
I
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Chit trayanon t , S., 1978, A geohydrologic study of the Garfield Township Coal Basin area, Bay County, Michigan:
Master 's Thesis, Michigan Technological University,
(
Houghton, 183 p.
g weston seopnyscoi i _ ---
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Chung, P. K., 197 3, Mississippian Coldwater Formation of the B Michigan Basin: Master's Thesis, Michigan State l University, East Lansing, 129 p.
Cohee, G. V. , 1948, Cambrian and Ordovician rocks in Michigan B Basin and adjoining areas: American Association of l Petroleum Geologists Bulletin, v. 32, no. 8, p. 1417-1448.
Cohee, G. V. , Burns, R. N., Br own , Andrew , Brant, R. A., and l Wright, Dorothy,1950, Coal resources of Michigan: U.S.
Geological Survey Circular 77, 56 p.
j Cohee, G. V. and Landes, K. K., 1958, Oil in the Michigan Basin in Weeks, L. G. , ed . , Habitat of Oil: The American Association of Petroleum Geologists, Tulsa, Oklahoma,
- p. 473-493.
Consumers Power Company, 1979, Final safety analysis report, I Midland Plant - Units 1 and 2, vol. 2: Sections 2.2-2.4, ;
l prepared by Dames and Moore and Bechtel Corporation. (
Consumers Power Company, 1978, Seismic lines for Arenac and Bay Counties, Michigan: BOC P 3 4, 35, 42, 43; prepared for i
Consumers Power Company by Teledyne Exploration, March, 1978, proprietary information.
l Co rd e r , P. G., 197 9, Soil survey of Clare County, Michigan:
Joint publication of U.S. Department of Agriculture, Soil Conservation Service in cooperation with Michigan j Agricultural Experiment Station, 122 p. and figures.
Cross, A. T. , 19 81a , Personal communication to S. A. Tedesco,
- Weston Geophysical Corporation, September 29, 1981.
1 Cross , A. T. , 19 81b, Personal communication to S. A. Tedesco, I
t Weston Geophysical Corporation, October 2, 1981.
Currie, W. W., Annotated list of the publications of the Michigan Geological Survey: Michigan Department of Natural l
t Resources, Geological Survey Division, Circular 16, 38 p.
Cushman, J. A., and Waters, J. A., 1927, Pennsylvanian B Foraminifera from Michigan: Contributions from the Cushman
} Laboratory for Foraminiferal Research, Sharon, Massachusetts, v. 3, pa r t 2, p . 107-110. l l
Dastanpour, M., 1977, An investigation of the carbonate rocks in the Reynolds Oil Field, Montcalm County, Michigan:
Master's Thesis, Michigan State University, East Lansing, 59 p.
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l DeWitt , W. , 1970, Age of the Bedford Shale, berea Sandstone and Sunbury Shale in the Appalachian and Michigan Basins, Pennsylvania, Ohio, and Michigan: U.S. Geological Survey I Bulletin 1294-G, p. Gl-11.
Diment , 'W . H., 1980, Significance of the aseismic regions l of the eastern United States: Geological Society of America Abstracts with Programs, v. 12, no. 2, p. 30-31.
Dixon Management Corporation, 1971a, sidewall neutron porosity log for Well " Harrison T. Plum #1" (permit #2856 5) , Sec.
24, Bay County, Michigan: Re ference M8786B, prepared by Schlumberger for Dixon Management Corporation, September l 1971.
Dixon Management Corporation, 1971b, Sidewall neutron porosity l log and dual laterolog for Well " Gary L. de Shano #1" (permit # 28566) , Sec. 14, Bay County, Michigan: Re ferences I M8785D and M878 5E, prepared by Schlumberger for Dixon Management Corporation, September 1971.
Do b r i n , M . B . , 1977, Seismic exploration for stratigraphic I traps in Payton, C. C., ed., Seismic stratigraphy -
l applications to hydrocarbon exploration: American I Association of Petroleum Geologists Memoir no. 26,
- p. 329-351.
Dow Chemical Company,1951, Electrical log for Well "#18 Brine", Section 20, Bay County, Michigan: Reference M8247D, prepared by Schlumberger Well Surveying Corporation
) for Dow Chemical Company.
Dow Chemical Company, [1979], Hydrogeologic Study: In-house j
hydroc,eologic evaluation for landfill proposed for Dow facilities in Midland, Michigan, 23 p., 4 appendices.
Dr a k e , B . , 1976, Saginaw Bay Graben and its implications for the origin of the Michigan Basin and Pleistocene glaciation:
American Geophysical Union Transactions, v. 57, no.10,
- p. 760-761.
I l
Drake, B., 1978, Geologic features of the southern peninsula of Michigan mapped from LANDSAT data: Geological Society of America Abstracts with Programs, v. 10, no. 7, p. 392.
Drcke , B. and Vincent, R. K., 1975, Geologic Interpretation of
, Landsat-1 Imagery of the Greater Part of the Michigan Basin: International Symposium on Remote Sensing of Environment, 10th, Ann Arbor, Michigan, Proceedings, p.
933-948.
l l
Weston Geophysical l .
V-5 Drexle r , C. , 1977, Evidence for revising the correlation of I proglacial lake stages in the western end of the Lake Superior Basin with those in the eastern end and in the I Lake Huron and Lake Michigan Basins: Geological Society of America Abstracte with Programs, v. 9, no . 5, p . 59 0-5 91.
Eg les ton , D. L., 1958, Relationship of the magnesium / calcium ratio to the structure of the Reynolds and Winfield Oil I Fields, Montcalm County, Michigan: Master's Thesis, Michigan State University, Eas t Lansing , 5 2 p .
Eisbacher, G. H. and Bielenstein, H. U., 1971, Elastic strain recovery in Proterozoic rocks near Elliot Lake, Ontario, Journal of Geophysical Research, v. 76, no. 8, p. 2012-2021.
I Ells , G . D. , 1962, Silurian rocks in the subsurface of southern Michigan in Silurian rocks of the southern Lake Michigan area: Micfiigan Basin Geological Society, Guidebook, 49 p.
Ells, G. D., 1969, Architecture of the Michigan Basin:
3 Michigan Basin Geological Society Fieldtrip, Guidebook, E p. 60-88.
Ells, G. D., 1978, Michigan's Silurian oil and gas pools:
Michigan Department of Natural Resources, Geological Survey I Division, Report of Investigations 2, 49 p.
Ells , G. D., 1979, Stratigraphic cross-sections extending from I Devonian Antrim Shale to Mississippian Sunbury Shale in the Michigan Basin: Michigan Department of Natural Resources, Geological Survey Division, Report of Investigations 22, I Lansing, 186 p.
Eschman, D. F., 1980, Some evidence of Mid-Wisconsinan events in Michigan: Michigan Academician, v. XII, no. 4, B p. 4 23-4 36.
I Everett, E. E., 1977, Suitability of lacustrine clays in Bay County, Michigan for land disposal of hazardous wastes:
Master 's Thesis, The University of Toledo, 'Ibledo, Ohio, 116 p.
Feenstra, J. E., 1979, Soil survey of Gratiot County, Michigan: Joint publication of U.S. Department of g Agriculture, Soil Conservation Service in cooperation with 5 Michigan Agricultrual Experiment Stakion,141 p. and figures.
Feldmann, R. M., Coogan, A. H., and Heimlich, R. A., 1977, Southern Great Lakes: Dubuque, Iowa, Kendall/ Hunt Publishing Company, 241 p.
g __
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l Fisher, J. A., 1981, Fault patterns in southeastern Michigan:
B Master 's hesis, Michigan State University, East Lansing ,
80 p., 9 plates.
l Fisher, J. C., 1969, The distribution and characteristics of i the " Traverse Formation" of Michigan: Master's %esis, 1
Michigan State University, East Lansing, 60 p. and maps.
Fisher, J. H., 1976, Structural history of the Michigan Basin:
} Middle Ordivician through Silurian time: Geological Society of America Abstracts with Programs, v. 8, no. 4, B p. 477.
Fisher, J. H., ed., 1977, Reefs and evaporites - concepts and depositional models: Studies in geology no. 5, American Association of Petroleum Geologists, Tulsa, Oklahoma, 91 p.
Fisher, J. H., 1979, Structural evolution of Michigan Basin and its petroleum potential: American Association of Petroleum I l Geologists Bulletin, v. 6 3, no. 3, p . 45 0-4 51.
Fletcher, J. B., Sbar, M. L. , and Sykes, L. R., 1978, Seismic l
trends and travel-time residuals in eastern North America 1 and their tectonic implications: Geological Society of America Bulletin, v. 8 7, p. 165 6-167 6, 10 figs.
l Fletcher, J. B., and Sykes, L. R., 1977, Earthquakes related to hydraulic mining and natural seismic activity in western I New York state: Journal of Geophysical Research, v. 82, no. 26, p. 3767-3780.
l Flint, R. F., 1959, Glacial Map of the United States east of the Rocky Mountains: Geological Society of America, Map MC-1, l 2 sheets, scale 1:1,7 50,0 00.
Fo rtin , J. L, 19 81, Stony Lake Field: Consumers Power Company l internal report concerning Midland nuclear generating facility.
Fowler, J. H., 1978, A Keweenawan turbidite basin in Michigan:
analysis, interpretations, and tectonic implications of the Gratiot County deep borehole red beds: Geological Society I of America Abs tracts with Programs , v. 10, no. 6, p. 234.
Fowler, J. H. and Kuenzi, W. D., 1978a, Keweenawan turbidites in Michigan (deep borehole red beds): a foundered basin ,
l sequence developed during evolution of a protoceanic rift system: Journal of Geophysical Research, v. 83, no. B12,
- p. 5833-5843.
Weston Geophysical
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I Fowler, J. H. and Kuenzi, W. D., 197 8b , Keweenawa n thermotectonic and foundered sedimentary basin sequences developed during evolution of a protoceanic rif t system in the Great Lakes region: Geological Society of America Abstracts with Programs, v.10, no. 6, p . 254.
Gardner, W. C., 1974, Middle Devonian stratigraphy and I depositional environments in the Michigan Basin: Michigan Basin Geological Society, Special Paper no. 1, 138 p. and 11 plates.
Gardner, W. C. ,1976, Middle Devonian depositional environments of the Michigan Basin: Geological Society of America Abstracts with Programs, v. 8, no. 4, p. 478.
Gill, D., 1977, The Belle River Mills gas field: productive Niagaran reefs encased by sabkha deposits, Michigan Basin:
Michigan Basin Geological Society, Special Paper no. 2,
_I 18 7 p .
Goodrich, R. E., 1957, Geology of the Reynolds Oil Field in Montcalm and Mecosta Counties, Michigan: Master's Thesis, Michigan State University, East Lansing, 59 p.
I Haimson, B. C., 1976, Crustal stress measurements 'through ultra deep well in the Michigan Basin: American Geophysical Union Transactions, v. 57, no. 4, p. 326.
an Haimson, B. C., 1978, Crustal stress in the Michigan Basin:
Journal of Geophysical Research, v. 83, no. B12,
- p. 5857-5863.
Hamrick , R. J. , 1978, Dolomitization patterns in the Walker Oil Field, Kent and Ottawa Counties, Michigan: Master's Thesis, Michigan State University, East Lansing, 86 p.
Harding , T. P., 1974, Petroleum traps associated with wrench American Association of Petroleum Geologists I
faults:
Bulletin , v. 5 8, no . 7, p . 129 0-130 4.
Haxby, W. F., Turcotte, D. L., and Bird, J. M., 1976, Thermal I and mechanical evolution of the Michigan Basin:
Tectonophysics, v. 36, no. 1-3, p. 57-75.
Helmboldt, D., 19 81, Porter Field:
I Consumers Power Company internal report concerning Midland nuclear generating facility.
Hinze, W. J., 1963, Regional gravity and magnetic anomaly maps of the southern peninsula of Michigan: Michigan Geological Survey, Report of Investigation no.1.
g mm e-m
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1 Hinze, W. J., Bradley, J. W., and Brown, A. R., 1970, i
I Gravimeter survey in the Michigan Basin deep borehole:
Journal of Geophysical Research, v. 8 3, no. 812,
- p. 5864-5868.
Hinze, W. J. and Kellogg, R. L., 1971, Gravity and aeromagnetic anomaly maps of the southern peninsula of Michigan:
Michigan Department of Natural Resources, Geological Survey I Division , Report of Investigation 14, 15 p., 2 plates.
Hinze, W. J., Kellogg, R. L. and Merritt, D. W., 1971, Gravity I and aeromagnetic anomaly maps of the southern peninsula of Michigan: Michigan Geological Survey Report of Investigation 14, 14 p.
Hinze, W. J., Kellogg, R. L., and O'Hara, N. W., 1975, Geophysical studies of basement geology of southern peninsula of Michigan: American Association of Petroleum I Geologis ts Bulletin , v. 5 9, no . 9, p . 1562-1584.
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southern peninsula of Michigan: Michigan Basin Geological l Society Field Conference, Guidebook, p. 28-59.
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l]
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Weston Geophysical l .
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u
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e
V-13 Michigan Geological Survey, Michigan River Basins Map:
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{
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DESCRIPTION AND EVALUATION OF BEDROCK STRUCTURE B MIDLAND PLANT - UNITS 1 & 2 STRUCTURE CONTOUR MAP - TOP OF TRAVERSE I
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- plates I thru 4.
2 Clayton
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q ,,, ,
REFERENCE-G.0 EHs, et al, Mictiigan Oil and Gas Fields,1975, Annual Statistical Summary 24(1976), Michigan Department of Natural Resources, Geological T US C oL ' surver wsion.
Consomers Power Company, Midland Plant Units
' 18 2 Final Saf ety Arslysis Report, Figur e 2.5 + 14 , ( Re v ision I,11/ 77 ).
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DESCRIPTION AND EVALUATION OF BEDROCK STRUCTURE E
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APPENDIX I MAP LOCATIONS AND ELEVATIONS OF CONTROL POINTS USED IN THIS STUDY B
l B
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l APPENDIX I MAP LOCATIONS AND ELEVATIONS OF CONTROL POINTS USED IN THIS STUDY Datum = Mean Sea level; M = Dow Brine Well, D = Dow Disposal Well, S = Dow Salt Well; CC = Calcium Chloride Well; All Others are Oil- and -Gas Wells l
Marshall "Tr ave r s e Rogers City-Township / Sandstone Lim e" Dundee County Section Well NJmber To p To p To p Bay Beaver /6 17074 -172 -1917 -2656
\
Bay Be aver /10 31206 - 7 -1732 -2441 Ba y Beaver /10 30708 52 -- --
[
Bay Be aver /10 5288 30 -1736 -2426 Bay Beaver /10 18140 - 24 -1735 -2440 Bay Be aver /10 31191 - 13 -1748 -2456 Bay Beaver /13 10728 92 -1637 -2347 Bay Be aver /14 28566 43 -1664 -2378 l
Bay Be ave r /24 12364 30 -- --
l Bay Beaver /24 28565 - 16 -1708 -2414 Bay Beaver /31 18649 -498 -2248 -2953 1
Bay Be aver /31 19445 -478 -- --
Bay Franken1u s t /4 20114 -293 -- --
l Bay Fr anken1us t /7 10275 -260 -- --
l Bay Fras er /l 13823 355 -1416 --
Bay Fr aser/1 12399 319 -1438 -2202 Bay Fras er/2 12177 --
-1452 -2216 l Bay Fraser /2 11315 --
-1455 -2225 l
Weston Geophysical
B l
A-2 l l APPENDIX I (Continued)
B Marshall "Tr a ve r s e Rogers City-Township / Sandstone Lime" Dundee County Section Well Number To p To p To p l f
Ba y Fras er/2 12740 241 -1456 -2222 Bay re ner/2 12923 253 -1429 -2221 Bay Fras er/2 11192 2 61 -1463 -2223 l Bay Fr a s er /2 10944 193 -1471 -2215 Bay Fras e r/2 14501 --
-1472 -2223 l
Bay Fraser/2 11603 299 -- --
I Bay Fras er/2 13745 263 -- --
I Bay Fr a ser /2 11966 257 -- --
l Bay Fr as er /2 12214 266 -- --
Bay Fr aser /2 13770 248 -- --
Bay Fraser/3 12638 18 5 -- --
B.f Fraser/9 32150 177 -1542 -2317 Bay Fraser/9 1016 14 8 -162 3 -2384 Bay Fraser /10 15949 --
-l %8 -2298 l
Bay Fraser /10 21853 --
-159 0 -2353 l Bay Fraser/15 22290 63 -1709 -2447 Bay Fras er/2 2 21668 22 -1764 -2504 l
Bay Fr aser/30 11434 - 17 -1827 -2585 l
Bay Ga rfieid/2 29122 - 22 -174 6 -2484 l Bay Garfield /6 4876 -12 9 -1899 -2666 Bay Ga rfield/9 10417 -108 -1903 -2628 Bay Ga rf ield/12 31808 91 -1723 -2453 1
l weston eeopnysicai
l B l l l A-3 l l
l l
APPENDIX I (Continued)
I Marshall "Tr aver s e Rogers City-
'Ibwnsh ip/ Sand s t o.ie Lime" Dundee County Section Well N2mber To p To p To p 1
Bay Ga rfield /12 12407 118 -1654 -2392 Bay Ga rf ield/14 16991 - 62 -1822 -2557 I
Bay Ga rfield /17 18814 --
-1943 --
f Bay Ga rf ield/19 12476 -129 -1923 -2650 Bay Ga rfield/20 44 61 -13 3 -1901 -2625 1
Bay Garfield /20 13174 -107 -- --
I Bay Garfield /21 10320 - 75 -1874 -2590 Bay Ga rf ield/22 11932 - 46 -1816 -2564
( Bay Ga rfield/2 3 16140 - 51 -1820 -2555 Bay Garfield /23 10795 - 39 -1843 -2565 Bay Ga rfield/2 3 25771 - 62 -1833 -2561 I Bay Garfield /26 13337 - 95 -1857 -2586 l
Bay Ga rfield/30 16549 -158 -1863 -2573 l
Bay Ca rf ield/31 12633 - 61 -1809 -2541 Bay Garfield /33 11772 -19 9 -1968 -2714 l Bay Garfield /35 3247 82 -1783 -2532 l
1 Bay Kawkawlin/5 13960 - 23 -- --
l Bay Kawkawlin/8 19093 21 -- --
l Bay Kawkawlin /10 2054 33 -- --
( Bay Kawk awlin/14 2210 1 12 -1646 -2372 Bay Kawkawlin/20 8403 181 -1551 -2297 I
Bay Kawkawlin/21 19949 147 -1582 -2293 l
Weston Geophysical i
l A-4 l
APPENDIX I (Continued) l Marshall "Tr a ve r s e Rogers City-Township / Sandstone Lim e" Dundee County Section Well Number To p Top To p Ba y Kawkawlin/2 2 19625 87 -1573 -2294 Bay Kawk awlin /26 11280 182 -- --
Bay Kawk awlin/2 6 12599 208 -- --
l Bay Kawkawlin/26 10342 176 -- --
Ba y Kawkawlin/2 6 11177 1 14 -- --
Bay Kawk awlin /27 18887 149 -- --
Bay Kawkawlin /2 7 19025 214 -- --
Bay Kawkawlin/27 9927 213 -- --
Bay Kawkawlin/2 7 18670 134 -- --
l Bay Kawkawlin/27 9613 12 8 -- --
l Bay Kawkawlin/2 7 13979 16 0 -- --
Bay Kawkawlin/27 12063 18 5 -- --
l Bay Kawkawlin/28 9850 172 -- --
Bay Kawkawlin/28 9709 169 -- --
Bay Kawkawlin/28 9928 18 0 -- --
l Bay Kawkawlin/28 13607 136 -- --
Bay Kawkawlin/28 10026 14 0 -- --
Bay Kawkawlin/28 9919 150 -- --
Ba y Kawkawlin /28 16156 13 8 -- --
l Bay Kawkawlin/28 15645 132 -- --
} Bay Kawkawlin/28 15290 174 -- --
Bay Kawkawlin/28 9734 156 -- --
Bay Kawkawlin/28 10249 16 0 -- --
l Weston Geophysical i
E A-5 I
I APPENDIX I (Continued)
( Marshall "Tr avers e Rogers City-Township / Lime" I County Section Well Number Sandstone To p To p Dundee To p Bay Kawkawlin /28 15761 18 3 -- --
Bay Kawkawlin/28 11389 172 -- --
I I Bay Kawkawlin/28 9670 17 6 -- --
Bay Kawkawlin/28 16282 167 -- --
l ,
Bay Kawkawlin/29 16574 17 0 -- --
Bay Kawkawlin/29 16423 14 8 -- --
Bay Kawkawlin /29 16675 19 3 -- --
l s
Bay Kawkawlin/32 10300 - 88 -- -- '
Bay Kawkawlin/33 9970 19 3 -- --
l Bay Kawkawlin/33 9996 14 9 -- --
l Ba y Kawkawlin/33 13555 112 -- --
Bay Kawkawlin/33 9856 1 13 -- --
l Bay Kawkawlin/33 13475 13 8 -- --
Bay Kawkawlin/33 9969 174 -- --
l Bay Kawkawlin/33 BD103 18 3 -- --
l Bay Kawkawlin/33 BD5 6 153 -- --
Bay Kawkawlin/33 13606 108 -- --
I Bay Kawkawlin/33 9991 89 -- --
Bay Kawkawlin/33 9696 18 8 -- --
l Bay Kawkawlin/33 13396 198 -- --
} Bay Kawkawlin/33 8842 15 3 -- --
Bay Kawkawlin/33 8452 li b -- --
Bay Kawkawlin/33 BD101 18 8 -- --
B l
Weston Geophysical 1 - - - - - -
E 1 A-6 APPENDIX I (Continued) 1 Marshall "Tr a ve rs e Rogers City- '
Township / Sands ton e Lime" Dundee County Section Well Number To p Top Top Bay Kawkawlin/33 9836 18 0 -- --
Bay Kawkawlin/33 10119 179 -- --
Bay Kawkawlin/34 9990 165 -- --
Bay Kawk awlin /34 13477 181 -- --
Bay Kawk awli n /34 13266 16 3 -- --
Bay Kawkawlin/34 8917 151 -- --
Bay Kawkawlin/34 8713 202 -- --
Bay Kawk awlin /34 13395 169 -- --
Bay Kawkawlin/34 12417 226 -- --
Bay Kawkawlin/34 9739 150 -- --
Bay Kawkawlin/34 9824 15 6 -- --
Bay Kawkawlin/34 13954 213 -- --
Bay Kawkawlin/34 15170 14 0 -- --
Bay Kawkavlin/34 8861 191 -- --
Bay Kawkawlin/34 9137 13 2 -- --
Bay Kawkawlin/34 13476 142 -- --
Bay Kawkawlin/34 9878 16 2 -- --
1 Bay Kawkawlin/34 9641 158 -- --
Bay Kawkawlin/34 8 613 18 7 -- --
Bay Kawk awlin/34 15070 196 -- --
Bay Kawkawlin/34 13412 16 3 -- --
Bay Kawkawlin/34 8648 188 -- --
Bay Kawkawlin/34 9360 10 9 -- --
l 1
Weston Geophysical l
l A-7 l APPENDIX I (Continued) f Marshall "Tr avers e Rogers City-Township / Sandst on e Lime" Dundee County Section Well N2mber To p Top To p l Bay Kawkawlin/34 10551 17 8 -- --
Bay Kawkawlin/35 9753 12 3 -- --
l Bay Kawkawlin/35 13740 169 -- --
j Bay Kawk awlin/35 10161 2 01 -- --
Bay Kawkawlin/35 10116 216 -- --
l Bay Kawkawlin/35 13222 169 -- --
Bay Kawkawlin/35 10543 218 -- --
l Bay Kawkawlin/35 10348 225 -- --
Bay Kawk awlin/35 13741 233 -- --
l Bay Kawkawlin/35 10544 132 -- --
( Bay Kawk awlin/35 11102 14 2 -- --
Bay Kawkawl'n/35 15069 12 5 -- --
l Bay Kawkawlin/3 5 10820 19 6 -- --
Bay Kawkawlin/35 13805 226 -- --
l Bay Kawkawlin/3 5 15360 19 6 -- --
l Bay Kawkawlin/35 13944 211 -- --
Bay Kaukawlin/35 13942 13 7 -- --
Bay Kawkawlin/35 10966 181 -- --
Bay Kawkawlin/35 14763 162 -- --
l Bay Kawkawlin/35 11968 18 6 -- --
l Bay Kawkawlin/35 14791 13 7 -- -- '
Bay Kawkawlin/36 12096 208 -- --
k Bay Kawkawlin/36 12367 213 -- --
l l weston seopnysicci
L A-6 APPENDIX I (Continued)
Marshall " Traverse Rogers City-Township / Sandst on e Lim e" Dundee County Section Well N2mber To p To p To p Bay Kawkawlin/36 11945 15 6 -- --
Bay Kawkawlin/36 13943 170 -- --
I Bay Kawkawlin/36 12034 16 3 -- --
j Bay Kawkawlin/36 15410 224 -- --
Bay Kawkawlin/36 13774 19 3 -- --
f Bay Kawkavlin/36 15319 190 -- --
Bay Kawkawlin/36 14549 18 5 -- --
I Bay Kawkawlin/36 13923 122 -- --
Bay Kawkawlin/36 15853 245 -- --
l Bay Kawkawlin/36 4821 86 -- --
Bay Kawkawlin/36 15854 17 0 -- --
I l
Bay Monitor /1 9932 189 -- --
Bay Monitor /1 13806 2 01 -- --
Bay Monitor /1 9783 16 6 -- --
l Bay Monitor /1 14691 18 3 -- --
Bay Monitor /1 9272 137 -- --
l Bay Monitor /1 20367 19 6 -- --
Bay Monitor /1 14447 223 -- --
l Bay Monitor /1 20767 141 -- --
l Bay Monitor /1 9400 161 -- - - -
Bay Monitor /1 13835 191 -- --
Bay Monitor /1 9823 178 -- --
1 Weston Geophysica
A-9 APPENDIX I (Continued)
{ 'Ibwnsh ip/
Marshall Sands t one "Tr aver s e Lime" Rogers City-Ibndee County Section Well Number To p To p Top Bay Monit or /1 14556 19 6 -- --
Bay Monitor /1 11992 157 -- --
Bay Monitor /1 13084 191 -- --
Bay Monitor /1 20876 188 -- --
Bay Monitor /1 4080 18 0 -- --
l Bay Monitor /1 10313 178 -- --
Bay Monitor /1 9658 174 -- --
l Bay Monitor /1 14777 19 6 -- --
Bay Monitor /1 10560 17 6 -- --
l Bay Monitor /1 10748 152 -- --
l Bay Monitor /1 15516 214 -- --
Bay Monitor /1 11222 122 -- --
I Monitor /1 I
Bay 15318 169 -- --
Bay Monitor /2 8637 17 5 -- --
Bay Monitor /2 8597 17 0 -- --
Bay Monitor /2 8655 164 -- --
Bay Monitor /2 9095 164 -- --
Bay Monitor /2 9269 172 -- --
Bay Monitor /2 15818 14 8 -- --
l Bay Monitor /2 8656 218 -- --
l Bay Monitor /2 9 615 19 2 -- --
Bay Monitor /2 10673 169 -- --
l l
weston seopnysicci l
L
1 l
1 A-10 l
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l Bay Monitor /2 9268 19 5 -- --
Bay Monitor /2 8840 198 -- --
l Bay Monit or/2 9430 19 6 -- --
Bay Monitor /2 7900 226 -- --
Bay Monit or/2 9905 239 -- --
l Bay Monitor /2 9097 184 -- --
Bay Monitor /2 9712 228 -- --
l Bay Monitor /2 8941 181 -- --
Bay Monitor /2 31386 217 -- --
Bay Monitor /2 8642 213 -- --
Bay Monitor /2 2 0141 18 4 -- --
Bay Monitor /2 12606 217 -- --
Ba y Monitor /2 5441 214 -- --
Bay Monitor /3 9597 183 -- --
Bay Monitor /3 20701 181 -- --
Bay Monitor /3 9456 1 13 -- --
Bay Monitor /3 13022 206 -- --
Bay Monitor /3 9600 212 -- --
Bay Monitor /3 8599 15 4 -- --
Bay Monitor /3 12017 176 -- --
Bay Monitor /3 9 016 16 7 -- --
Bay Monitor /3 10190 12 3 -- --
l Bay Monitor /3 8247 17 2 -- --
Weston Geophysical l
1
A-11 B
l APPENDIX I (Continued) i Marshall "Tr ave r s e Rogers City-Township / Sandston e Lim e" Dundee County Section Well Number To p To p To p l Ba y Monitor /3 8 618 18 8 -- --
Bay Monitor /3 8397 196 -- --
j l
Bay Monitor /3 8598 18 0 -- --
j Bay Monitor /3 8545 190 -- --
l Bay Monit or/3 8306 14 3 -- --
f Bay Monitor /3 9600 156 -- --
Bay Monitor /3 9 015 172 -- --
f Bay Monitor /3 9986 159 -- --
Bay Monitor /3 9046 171 -- --
Bay Monitor /3 13349 195 -- --
l Bay Moniter /10 5831 - 65 r --
Bay Monitor /.1 15572 161 -- --
Bay Monitor /11 13787 14 2 -- --
Bay Monitor /11 10085 213 -- --
1 Bay Monit or /11 10248 14 9 -- --
Bay Monitor /12 9598 183 -- --
l Bay Monitor /12 15468 229 -- --
l Bay Monitor /12 10384 192 -- --
Bay Monitor /12 14520 222 -- --
l Bay Monitor /12 9731 274 -- --
Bay Monit or /12 14695 13 6 -- --
Bay Monitor /12 10035 195 -- --
{ Bay Monitor /12 10202 250 -- --
k WeNon Geophysicai
i A-12 APPENDIX I (Continued) l Ma rshall "Tr ave r s e Rogers City-Township / Sands t on e Lime" Dundee County Section Well M2mber To p To p To p
{ Bay Monit or /12 15171 18 6 -- --
Bay Monitor /12 8661 14 0 -- --
l Bay Monitor /12 10121 161 -- --
Bay Monitor /12 14573 178 -- --
l Bay Monitor /12 11771 204 -- --
Bay Monitor /12 10461 12 9 -- --
Pinconning/19 l Bay 16332 249 -- -- .
Bay Pinconning/19 14117 240 -- --
Bay Pinconning/19 14761 250 -- --
Bay Pi nconning/20 13587 253 -- --
Bay Pinconning/20 13301 258 -- --
Bay Pinconning/20 16656 292 -- --
Bay Pinconning/21 16658 277 -- --
Bay Pinconning/21 13737 322 -- --
Bay Pinconning/23 20134 319 -- --
Bay Pinconning/24 17476 319 -- --
Bay Pinconning/25 17866 315 -- --
E Bay Pinconning/25 17093 295 -- --
Ba y Pinconning/25 18040 226 -- --
Bay Pinconning/25 18377 276 -- --
Bay Pinconning/25 17406 171 -- --
Bay Pinconning/25 11193 239 -- --
Westen Geophysical
i 1
A-13 l
APPENDIX I (Continued) l Marshall "Tr a ve rs e Rogers City-Township / Sandstone Lim e" Dundee I County Section Well Number To p To p To p I
Bay Pinconning/25 22960 267 -- --
Bay Pinconning/26 17955 280 -1443 -2224 Bay Pinconning/2 7 2749 212 -- --
l Bay Pinconning/28 16657 264 -- --
Bay Pinconning/29 15297 19 5 -- --
Bay Pinconning/29 15220 179 -- --
Bay Pinconning/29 15970 19 6 -- --
Bay Pinconning/29 16510 246 -- --
l Bay Pinconning/29 16178 244 -- --
Bay Pinconning/29 16397 227 -- --
l Bay Pinconning/29 15476 262 -- --
Bay Pinconning/29 15604 265 -- --
l Bay Pinconning/31 29137 14 2 -- --
Bay Pinconning/32 13838 236 -- --
Bay Pinconning/32 15453 19 2 -- --
l Bay Pinconning/33 27129 275 -- --
Bay Pinconning/33 15708 269 -- --
1 Bay Pinconning/33 22404 258 -- --
Bay Pinconning/34 13688 258 -- --
Bay Pinconning/35 12224 259 -1462 -2227 l Bay Pinconning/35 12 615 234 -1447 -2228 Bay Pinconning/35 12213 230 -- --
Bay Pinconning/35 13811 286 -- --
Weston Geophysical
I l
A-14 l
APPENDIX I (Continued) l Marshall " Traverse Rogers City-I l
County Ibwnship/
Section Well Number Sands tone To p Lime" Top Dundee To p Ba y Pinconning/35 13951 2 71 -- --
Bay Pinconning/35 11158 284 -- --
Bay Pinconning/35 12860 247 -- --
l Bay Pinconning/35 13809 220 -- --
Bay Pinconning/35 13765 276 -- --
I Bay Pinconning/35 13919 297 -1448 -2222 Bay Pinconning/35 13969 292 -1466 -2226 Bay Pinconning/36 17174 225 -- --
l Bay Pinconning/36 14228 265 - --
Bay Williams /8 33341 -440 -2210 -2874 Bay Williams /8 34080 -434 -- --
i l l Bay Williams /9 10868 -446 -2191 -2877 l Bay Williams /17 19861 -443 -2217 -2890 Bay Williams /18 3237 -475 -2234 -2922 l Bay Williams /19 16399 -524 -2314 -2979 Bay Williams /19 35M -526 -2322 -2984 l
Bay Williams /20 17943 -447 -2229 -2911 Bay Williams /21 6D -4 51 -2213 -2881 Bay Williams /27 4423 -408 -2151 -2809 h Bay Williams /29 36M -506 -2292 -2953 Bay Williams /30 11D -514 -2324 -2977
\
Bay Williams /31 10853 -494 -2301 -2939 Bay Williams /31 22M -522 -2266 -2912 Weston Geophysical l
A-15 F
l APPENDIX I (Cont inue d )
l Marshall "Tr a vers e Rogers City-Tbwnship/
I l
County Section Well Number Sandstone Top Lime" To p Dundee To p Midland Edenville/4 8491 -583 -- --
E Midland Ed enville/5 4514 -583 -- --
l Midland Edenville/5 20154 -578 -- --
} Midland Edenville/5 12782 -579 -- --
Midland Edenville/6 17743 -610 -- --
Midland Ed enville/7 2977 -652 -- --
Midland Edenville/8 4299 -595 -- --
I Midland Edenville/9 4725 -585 -- --
Midland Edenville /10 15103 -597 -- --
l Midland Edenville/10 6392 -588 -- --
l Midland Edenville /11 12164 -585 -- --
Midland Ed enville/13 7066 -606 -- --
l Midland Edenville /15 10719 -580 -- --
Midland Ed enville/19 4922 -663 -- --
Midland Edenville/20 5137 -648 -- --
Midland Edenville/22 4848 -603 -- --
Midland Edenville/22 4808 -588 -- --
Midland Edenville/23 18085 -578 -- --
B Midland Edenville/2 3 21977 -576 -- --
t Midland Edenville/23 13375 -588 -- --
} Midland Edenville/2 3 8969 -583 -- --
Midland Edenville/25 4813 -596 -- --
l Midland Edenville/26 5165 -588 -- --
L l weston seonnysicci i
A-16 APPENDIX I (Continued)
Marshall "Tr ave rs e Rogers City-Township / Sandstone Lime" Dundee County Section Well thmber To p To p To p Midland Edenville/26 3567 -579 -- --
Midland Edenville/26 4955 -577 -- --
Midland Edenville/26 4966 -596 -- --
!. Midland Edenville/26 4962 -591 -- --
Midland Edenville/26 4946 -586 -- --
l Midland Edenville/26 4947 -566 -- --
Midland Edenville/26 4866 -594 -- --
l Midland Edenville/26 4964 -580 -- --
f Midland Edenville/2 7 5135 -584 -- --
l l
Midland Edenville/27 5157 -579 -- --
Midland Edenville/2 7 5687 -586 -- --
Midland Edenville/27 4816 -587 -- --
Midland Edenville/27 4832 -581 -- --
I Midland Edenville/27 4815 -588 -- --
Midland Edenville/27 4823 -588 -- --
Midland Edenville/27 4948 -582 -- --
Midland Edenville/27 5058 -589 -- --
I Midland Edenville/27 4960 -570 -- --
Midland Edenville/27 4799 -598 -- --
Midland Edenville/27 4724 -583 -- --
Midland Edenville/27 4984 -619 -- --
Midland Edenville/27 4849 -586 -- --
Midland Edenville/27 4906 -582 -- --
E l
Weston Geophysical i - - - --- -
A-17 E
l APPENDIX I (Continued)
I l Marshall "Tr ave rs e Rogers City-Township / Sands t one Lime" Dundee County Section Well Number To p To p To p Midland Edenville/27 4926 -590 -- --
Midland Edenville/27 4798 -576 -- --
I Midland Edenville/27 4797 -567 -- --
Midland Edenville/27 4907 -580 -- --
l Midland Edenville/2 7 4874 -577 -- --
Midland Edenville/27 4306 -580 -- --
Midland Edenville/27 4908 -571 -- --
l Midland Edenville/27 5136 -568 -- --
Midland Edenville/2 7 5370 -583 -- --
Midland Edenville/27 5308 -569 -- --
l Midland Edenville/27 5120 -579 -- --
Midlend Edenville/27 5357 -580 -- --
Midland Edenville/2 7 5356 -599 -- --
Midland Edenville/27 5158 -574 -- --
Midland Edenville/27 5054 -579 -- --
Midland Edenville/27 4961 -582 -- --
Midland Edenville/28 52 51 -557 -- --
Midland Edenville/28 5100 -589 -- --
Midland Edenville/30 4933 -599 -- --
Midland Edenville/33 5153 -585 -- --
l Midland Edenville/35 4883 -612 -- --
B B
1 Weston Geophysical
A-18 APPENDIX I (continued)
Marshall "Tr averse Rogers City-Township / Sandstone Lim e" Dundee County Section Well Number To p Top Top Midland Geneva /3 9771 -574 -- --
Midland Geneva /4 31192 -577 -- --
Midland Geneva /4 30126 -563 -- --
Midland Geneva /4 16830 -554 -- --
Midland Geneva /4 13889 -568 -- --
Midland Geneva /6 12080 -592 -- --
Midland Geneva /10 585 -603 -- --
Midland Geneva /12 14884 -577 -- --
Midland -638
{ Geneva /15 30457 -- --
Midland Geneva /15 31134 -582 -- --
Midland Geneva /16 8 614 -581 -- --
Midland Geneva /19 2521 -587 -- --
[ Midland Geneva /19 3934 -581 -- --
Midland Geneva /19 3128 -592 -- --
Midland Geneva /19 3329 -595 -- --
Midland Ge neva/19 3080 -589 -- --
Midland Geneva /19 736 -6 01 -- --
Midland Geneva /20 2894 -590 -- --
Midland Geneva /20 3127 -570 -- --
Midland Geneva /20 3125 -588 -- --
Midland Geneva /20 20863 -630 -- --
Midland Geneva /20 20173 -530 -- --
Midland Geneva /21 3190 -592 -- --
j Weston Geophysical
B A-19 l
APPENDIX I (Continued)
I l Marshall "Tr ave rs e Rogers City-Township / Sands ton e Lime" Dundee B
County Section Well tbmber Top To p To p Midland Geneva /2 2 25969 -532 -- --
Midland Geneva /27 10726 -571 -- --
l Midland Geneva /28 33499 -555 -- --
l Midland Geneva /28 21257 -609 -- --
Midland Geneva /2 9 3318 -595 -- --
Midland Ge neva/29 49542 -587 -- --
Midlard Geneva /2 9 662 -551 -- --
f Midland Ge neva /31 14653 -585 -- --
l Midland Geneva /33 767 -555 -- --
Midland Geneva /33 19098 -569 -- --
1 Midland Greendale /1 1370 -503 -2263 -2866 L
Midland Greendale/2 12 39 -545 -2236 -2852 Midland Greendale/2 19703 -547 -2252 -2853 l
Midland Greendale/4 1062 -478 -2252 -2858 b Midland Greendale/9 1286 -439 -- --
Midland Greendale/9 14 32 -453 -- --
l Midland Greendale/9 14962 -493 -- --
Midland Greendale/9 2382 -442 -- --
Midland Greendale/9 2895 -457 -- --
- l. Midland Greendale/10 12 51 -442 -- --
Midland Greendale /10 1526 -468 -- --
i Midland Greendale/11 1446 -4 61 -2230 -2823 5
l Weston Geophysical i
B l
A-20 APPENDIX I (Continued)
I f Marshall "Tr a ver se Rogers City-Township / Sands tone Lime" Dundee B County Section Well Number To p To p To p Midland Greendale /11 1406 -459 -2196 -2816 I Midland Greendale/11 1467 -477 -2207 -2817 Midland Greendale /11 1567 -442 -2202 -2820 ,
{ Midland Greendale/11 1416 -460 -2210 -2817 Midland Greendale /11 1407 -470 -2223 -2823 l
Midland Greendale/11 12031 -4 81 -2221 -2814 Midland Greendale /11 1458 -478 -2223 -2828 1.
Midland Greendale/11 1455 -478 -2218 -2829 l Midland Greendale /11 1466 -470 -2200 -2811 Midland Greendale/11 1357 -470 -2202 -2822 Midland Greendale /11 1243 -448 -2219 -2826 Midland Greendale /12 12 74 -523 -2205 -2834 Midland Greendale /12 1429 -446 -2216 -2825 Midland Greendale/12 1270 -527 -2173 -2832 l
Midland Greendale /12 14 61 -473 -2205 -2833 Midland Greendale/12 1373 -476 -2251 -2835 Midland Greendale /12 3720 -506 -2224 -2838 Midland Greendale/12 1318 -4 48 -2223 -2832 Midland Greendale /12 14 71 -473 -2195 -2829 Midland Greendale/12 1278 -473 -2198 -7822 l Midland Greendale /12 134 3 -482 -2231 -2842 Midland Greendale/12 1348 -528 -2175 -2838 1
Midland Greendale /12 1592 -477 -2200 -2816 1
Weston Geophysical l
A-21 i APPENDIX I (Cont inue d )
L
[ ! Marshall "Tr a vers e Rogers City-L Tbwnship/ Sands tone Lim e" Dundee County Section Well Number To p Top To p g Midland Greendale /12 1294 -482 --
-2823 j Midland Greendale/12 1. -
-4 78 -2208 -2829 Midland Greendale /12 1537 -476 -2206 -2832 Midland Greendale/12 1346 -486 -2116 -2826
/
Midland Greendale /12 1339 -52 3 -2226 -2826 Midland Greendale/12 19830 -526 -2148 -2824 Midland Greendale /12 1358 -462 -2200 -2823 Midland Greendale/13 1273 -517 -2200 -2829 Midland Greendale /13 132 7 -512 -2196 -2842 Midland Greendale/13 1368 -516 -2199 -2836
[ Midland Greendale /13 1382 -484 -2223 -2856 Midland Gre endale/13 1197 -503 --
-2846 Midland Greendale /13 1423 -508 -2193 -2824 Midland Greendale/13 1363 -509 -2194 -2835 I
Midland Greendale /13 1329 -479 -2181 -2841 j Midland Gre endale/13 1548 -499 -2222 -2824 Midland Greendale /13 1227 -472 -2202 -2845
. Midland Greendale/13 1390 -510 -2217 -2846 Midland Greendale /13 1316 -51 1 -2218 -2842 i -2211 -2824 Midland Greendale/13 1371 -5 01 Midland Greendale /13 1334 -507 -2199 -2813 Midland Gre endale/13 1282 -512 -2199 -2825 l Midiand Greendale /13 S818 -516 -2214 -2831 5
1 5 *est " ee o"v,>ce L .
B A-22 I
APPENDIX I (Continued)
B l Marshall "Tr aver s e Rogers City-Township / Sands ton e Lim e" Dundee B County Section Well Ibaber To p Top Top Midland Greendale /13 3683 -519 -2221 -2849 B
, Midland Greendale/13 3472 -509 -2209 -2838 l
Midland Greendale /13 2818 -518 -2220 -2840 l Midland Greendale/14 1145 -452 -2209 -2818 Midland Greendale /14 1538 -508 -2181 -2837 l Midland -473 -2213 -2830 Greendale/14 1405 Midland Greendale /14 1389 -451 -2208 -2817 f
Midland Greendale/14 1230 -445 -2198 -2830 l
Midland Greendale /14 1320 -496 -2228 -2850 Midland Gre enda'.e /14 1394 4 56 --
-2829 Midland Greendale /14 1376 -444 -2223 -2832 Midland Greendale/14 1350 -469 -2206 -2816 l
Midland Greendale /14 1452 -4 C1 -2211 -2818 Midland Greendale/14 1321 +61 -2218 -2825 l
Midland Greendale /14 18226 574 -2199 -2817 l Midland Greendale/14 2350 -445 -2210 -2823 Midland Greendale /14 18916 -458 -2218 -2815 1
Midland Greendale/14 1836 --
-2215 -2809 Midland Greendale /14 1252 -458 -2208 -2828 Midland Greendale/14 1433 -452 -2219 -2841 f Midland Greendale /14 1531 -467 -2210 -2821 Midland Greendale/14 1595 -446 -2096 -2814 l
Midland Greendale /14 1304 -480 -2203 -2838 B .
Weston Geophysical
l l
A-2 3 B
APPENDIX I (Continued) l Marshall "Tr ave r s e Rogers City-Township / Sands t one Lim e" Dundee County Section Well Number To p To p __ Top Midland Greendale /14 1209 -484 -2202 -2832 Midland Greendale/15 1421 -425 -2199 -2814 Midland Greendale /15 1668 -472 -2202 -2809 l Midland Greendale/15 1424 -459 -2199 -2830 1 Midland Greendale /15 1220 -446 -2141 -2824 Midland Greendale/15 1397 -435 -2205 -2818 Midland Greendale /15 1507 -418 -2213 -2815 l
Midland Greendale/15 1248 -443 -2203 -2811 Midland Greendale /15 1441 -458 -2208 -2821 l
Midland Greendale/16 1366 -489 -2209 -2816 l Midland Greendale /16 8955 -458 -2193 -2826 Midland Greendale/16 1445 -4 44 -2209 -2825 Midland Greendale /16 229 -418 -2178 -2833 Midland Greendale/20 388 -470 -2205 -2823 Midland Greendale/20 1557 -486 -2210 -2834 l Midland Greendale/21 1391 -438 -2204 -2822 Midland Greendale/24 43M -535 -2250 -2855 Midland Greendale/26 1210 -472 -2196 -2812 Midland Greendale/2 7 3369 -392 -2163 -2764 Midland Greendale/28 26694 -4 41 -2185 -2793 l Midland Greendale/29 2318 -457 -2167 -2780 Midland Greendale/32 1430 -489 -2154 -2725 Midland Greendale/33 13553 -406 -2161 -2758 B
1 Weston Geophysical
H I
A-24 L APPENDIX I (Continued)
Marshall " Traverse Rogers City-Township / Sandston e Lim e" Dundee County Section Well Number To p Top Top Midland Greendale/33 3761 -465 -2159 -2743 Midland Greendale/34 2598 -363 -2161 -2743 l
Midland Greendale/35 1349 -4 31 -2152 -2740 j Midland Greendale/36 1293 -4 34 -2170 -2762 k Midland Ibmer/1 9951 -641 -- --
Midland llamer /2 IIA --
-2435 -3128 i
Midland Ibmer /15 10969 -591 -2389 -3038 Midland 110mer /22 16M -580 -2360 -3011 Midland Ibmer/23 15M -579 -2359 -3027 l Midland Homer /24 14M -575 -2350 -2997 Midland Ibme r/33 23D -330 -2283 -2905 l
Midland llomer /34 35D -544 -2313 -2946 Midland Ibmt.r/35 22D -554 -2312 -2940 l
Midland flomer/36 34D -552 -2317 -2943 l Midland Ibmer/36 17788 -546 -2295 -2924 I Midland flope/9 24032 -525 -- --
Midiand Ibpe /10 23841 -519 -2342 -3077 l
Midland flope/14 5398 -545 -2355 -3090 l Midiand Ibpe /15 32029 -527 -2356 -3078 Midland Ilope/16 5947 -560 -2358 -3096 Midland Ibpe/22 16484 -633 -2438 -3155 Midland Ho pe /36 11046 -549 -2333 -3070 Weston Geophysical 1
I l
A-2 5 B
l APPENDIX I (Continued) <
l Marshall "Tr avers e Rogers City-Ibwnship/ Sandstone Lime" Dundee County Section Well Number To p To p To p Midland Ingerso11/2 12020 --
-2254 -2884 Midland Ingerso11/2 20D -496 -2261 -2889 Midland Ingerso11/3 ISD -568 -2196 -2902 Midland Ingerso11/3 30M -518 -2281 -2903 l
Midland Ingerso11/3 31M -477 -2252 -2883 Midland Ingerso11/3 29M -509 -2289 -2947 Midland Ingersoll/5 33D -541 -2289 -2920 l
Midland Ingerso11/7 62M -515 -2270 -2881 Midland Ingerso11/7 55M -54 3 -2281 -2897 l
Midland Ingerso11/8 54M -543 -2288 -2905 l Midland Ingerso11/8 53M -52 7 -2269 -2894 Midland Ingerso11/9 5422 --
-2267 -2891 l -2861 Midland Ingersoll /10 32M -463 -2231 Midland Ingersoll/11 6406 -487 -- --
Midland Ingerso11/13 31D -456 -2191 -2830 l Midland Ingersoll/I5 33M -490 -2215 -2846 Midland Ingersoll /17 29D -51 1 -2243 -2843 Midland Ingerso11/19 64M -4 69 -2184 -2783 Midland Ingerso11/21 34M -482 -2221 -2820 l
Midland Ingerso11/21 1258 -458 -2192 -2803 Midland Ingerso11/24 11711 -424 -2175 -2793 l
Midland Ingerso11/26 1880 -376 -2161 -2771 l Midland Ingerso11/28 16D -460 -2195 -2793 B
E weston econnysica L
A-26 APPENDIX I (Continued)
Marshall " Traverse Rogers City-Tbwnship/ Sands tone Lim e" Dundee B County Section Well Number To p To p To p l
Midland Ingerso11/28 44M -459 -2259 -2804 Midland Ingerso11/28 45M -402 -2243 -2765 Midland Ingerso11/29 63M -473 -2208 -2800 l Midland Ingersoll/32 32D -421 -2146 -2740 Midland Ingerso11/34 30D -396 -2137 -2742 I
B Midland Jerome/2 4932 -6 01 -2385 --
f Midland Jerome/3 4790 -603 -2384 -3097
( Midland Jerome/3 5018 -576 -2372 -3056 Midland Jerome/6 14294 -551 -2331 -3017 Midland Jerome/6 14255 -553 -- --
Midland Jerome/6 14221 -548 -2315 -2998 I I Midland Jerome/6 5738 -555 -- --
l Midland Jerome/7 15713 -549 -2314 -3033 Midland Jerome/7 14764 -581 -- --
Midland Jerome/7 14007 -541 -- --
Midland Jerome/7 14238 -542 -- --
l Midland Jerome/7 14448 -544 -- --
Midland Jerome/7 13837 -540 -- --
Midland Jerome/7 15034 -553 -- --
l Midland Jerome/7 14617 -553 -- --
Midland Jerome/7 13643 -562 -- --
l Midland Jerome/7 12781 -548 -- --
L E weston seopnysicci
l A-2 7 L APPENDIX I (Continued)
Marshall "Tr ave r s e Rogers City-Ibwnship/ Sandstone Lime" Dundee County Section Well N2nber To p Top Top Midland Jerome/7 14290 -548 -- --
p Midland Jerome/7 14142 -571 -- --
l Midland Jerome/8 17062 -571 -2326 -3024 Midland Jerome/8 17654 -586 -2353 -3028 l
Midland Jerome/9 4971 -546 -2329 -3022 l Midland Jerome/11 22993 -587 -2362 --
Midland Jerome /12 22472 -564 -2348 -3024 l
Midland Jerome/12 22678 -562 -2356 -3033 Midland Jerome /12 21810 --
-2347 -3035 Midland Je rome /13 16533 -556 -2359 -3035 l Midiand Jerome /13 19517 -556 -2324 -3018 Midland Jerome/13 17437 --
-2336 -3009 Midland Jerome /13 22042 -576 -2351 -3026 Midland Jerome/13 22679 -585 -2360 -3034 Midland Jerome /13 19957 -574 -2338 -3019 l Midland Jerome/13 21253 -560 -2348 --
Midland Jerome /13 19182 -577 -2340 -3008 Midland Jerome/13 19809 -577 -2336 -3011 Midiand Jerome /13 22896 -5 61 -2334 -3016 l
Midland Jerome/15 9358 -594 -- --
l Midland Jerome /17 1255 -553 -2346 -3034 Midland Jerome/17 8 91 -608 -- --
l Midland Jerome/24 23630 -587 -2354 -3044 Midland Jerome/36 4086 -638 -2430 -3095 1
l weston seopnysica
l i
A-28 l
APPENDIX I (Continued)
B l Marshall " Traverse Rogers City-Township / Sandston e Lime" Dundee County Section Well Number To p Top Top i
I Midland larkin/7 27D -578 -2361 -3066 B Midland Larkin/9 1899 -546 -2335 -3052 l
Midland larkin/9 49M -582 -2366 -3076
}
Midland Larkin/10 68M -552 -2349 -3075 Midland Larkin /12 30378 -447 -2266 -2972 Midland Larkin/14 39D -570 -2377 -3080 Midland Larkin /15 48M -601 -2355 -3069 l
Midland Larkin/17 40D -570 -2355 -3054 l
Midland Larkin /19 7325 -549 -2344 -3028 Midland Larkin/20 26D -526 -2315 -3014 l Midland Larkin/20 11556 -506 -2346 -3008 Midland Isrkin/21 10307 -512 -2310 -2992 l
Midland Larkin/21 15872 -524 -2328 -3028 Midland Larkin/22 17D -526 -2312 -3009 Midland Ierkin/22 37M -533 -2291 -2994 l Midland Larkin/22 4 7M -528 -2309 -3019 Midland Larkin/23 5201 -563 -2355 -3035 1 Midland Larkin/27 15422 -504 -2290 -2992 B
i Midland Larkin/2 7 66M -503 -2297 -2976 l
Midland Larkin/29 4606 -523 -2295 -2999 l Midland Larkin/32 4982 -552 -2362 -3062 Midland Larkin/33 3391 -530 -2322 -3018 Midland larkin/33 28D -545 -2328 -3027 B
1 B --
l _
A-2 9 APPENDIX I (Continued)
B l Marshall " Traverse Rogers City-Tbwnsh i p/ Sands tone Lime" Dundee County Section Well Number To p Top Top Midland larkin/35 22249 -508 -2262 -2946 Midland Larkin/35 11302 -525 -2274 -2955 i
Midland Larkin/35 20554 -513 -2278 -2947 l
Midland Larkin/35 21M -521 -2273 -2970 '
Midland Larkin/35 27M -533 -2300 -2991 Midland Larkin/36 19255 -477 -- --
Midland larkin/36 38D -504 -2270 -2956 B Midland l lee /6 1360 -484 -2249 -2864 Midland Ice /7 2358 -502 -2227 -2830 Midland Lee /7 1332 -513 -2218 -2833 Midland Ice /7 1999 -537 -2230 -2845 l
Midland Ime/7 1292 -518 -2217 -2836 Midland Iee/7 2797 -527 -2230 -2853 Midland Lee /7 1543 -535 -2236 -2848 l Midland Ice /7 3557 -525 -224 0 -2863 Midland Lee /8 1686 -519 -2309 -2922 l
Midland Ice /8 169 9 -534 -2233 -2857 Midland Lee /9 1224 -532 -2249 -2938 l
Midland Ice /10 15463 -596 -2301 -2979 l Midland Lee /13 1516 -539 -2368 -2983 Midland lee /13 17M -573 -2345 -2982 Midland Ime/15 2 0M -566 -2278 -2920 B
i E weston econnys,ca i
B l
A-30 B l APPENDIX I (Cont inue d )
l Marshall "Tr avers e Rogers City-Tbwnship/ Sands ton e Lime" Dundee B County Section Well Number To p Top Top Midland le e /18 1750 -512 -2232 -2910 B Midland Le e/18 1187 -5 32 -2237 -2852 I
Midland le e /18 1375 -518 -2233 -2833
( Midland Lee /18 1369 -523 -2222 -2858 Midland Le e /19 1238 -496 -2218 -2878 Midland Lee /19 42M -545 -2255 -2878 Midland Ice /20 16696 -524 -2273 -2886 l
Midland Lee /20 41M -587 -2289 -2922 j Midland Ice /23 19M -549 -2289 -2918 Midland Lee /24 18M -597 -2322 -2955 Midland Ice /26 1223 -475 -2185 -2879 Midland Ime/26 36D -538 -2282 -2908 l
Midland Ic e/2 7 24D -554 -2270 -2897 Midland Lee /27 2 5D -549 -2252 -2885 Midland Ice /28 37D -536 -2275 -2888 l Midland Lee /36 59M -526 -2251 -2844 Midland Ice /36 60M -520 -2240 -2858 1
B j Midland Lincoln /1 32080 -595 -2390 -3111 1
Midland Lincoln /9 6007 -589 -2378 -3089 l Midland Lincoln /11 2060 -622 -- --
Midland Lincoln /15 5001 -609 -2384 -3069 Midland Lincoln /21 19502 -585 -2353 -3038 B
t B .- e_,e
I A-31 APPENDIX I (Continue d )
l Marshall "Tr ave rs e Rogers City-Ibwnship/ Sands tone Lime" Dundee B County Section Well NJmber Top To p Top Midland Lincoln /21 19428 -593 -2351 -3036 Midland Lincoln /26 1778 -541 -2346 -3056 Midland Lincoln /28 11732 -566 -2344 -3034 Midland Lincoln /28 18010 -574 -2357 -3030 Midland Midland /2 26M -557 -2331 -3004 Midland M! dland/12 2 5M -577 -2346 -3008 Midland Midland /13 24M -570 -2374 -3040 Midland Midland /19 12M -590 -2340 -3010 Midland Midland /19 13M -577 -2347 -2986 Midland Midland /19 5430 -561 -2374 -3017 Midland Midland /20 31Z -584 -2358 -3016 Midland Midland /20 32Z -586 -2355 -3014 Midland Midland /20 33Z -58 0 -2354 -3016 Midland Midland /20 34Z -596 -2360 -3013 Midland Midland /20 11M -578 -2353 -3014 Midland Midland /20 ?. 3Z -567 -2357 -3002 Midland Midland /20 24Z -568 -2358 -2996 Midland Midland /21 4Z -572 -2379 -3019 Midland Midland /21 CC1 -558 -2364 -3030 Midland Midland /21 CC2 -590 -2375 -3020 Midland Midland /21 1Z -567 -2364 -3029 Midland Midland /21 2Z/3D -580 -2384 -3039 B Weston Geophysicai
A-32 APPENDIX I (Continued)
Rogers City-Marshall "Tra vers e Ibwnship/ Sandst one Lime" Dundee County Section Well Number To p To p Top Midland Midland /21 8Z -598 -2343 -3000 Midland Midland /21 3Z -5 72 -2372 -3017 l
Midland Midland /21 2M -583 -2354 -3015 l Midland Midland /22 2D -584 -2366 -3002 Midland Midland /24 23M -547 -2252 -3006 Midland Midland /24 1028 -507 -- --
B Midland Midland /24 12D -- --
-3018 Midland Midland /25 10D -545 -2313 -2970 f Midland Midland /2 6 8M -560 -2390 -3010 Midland Midland /26 4M -569 -2355 -3018 Midland Midland /2 6 9D -556 -2440 -3009 Midland Midland /26 7D -569 -2347 -3016 l
Midland Midland /2 6 6M -554 -2361 -3024 l Midland Midland /26 7M -358 -2353 -3063 Midland Midland /2 7 SM -574 -2371 -3014 Midland Midland /27 IM -574 -2354 -2999 Midland Midland /2 7 ID -565 -2342 -2990 l
Midland Midland /27 3M -561 -2341 -2990 l Midland Midland /2 7 8D -595 -2339 -2998 Midland Midland /27 10Z -586 -2343 -2985 l Midland Midland /2 7 17Z -563 -2343 -2991 Midland Midland /27 3664 -567 -2344 -2987 i
Midland Midland /28 5Z -- --
-2990 E wesion oeopnysicci t
E I
A+33 APPENDIX I (Continued) l Marshall "Tr ave r s e Rogers City-
, Ibwnship/ Sandstone Lime" D.indee County ,Section Well Number To p To p Top W Midland Fidland/28 11Z -566 -2336 -2981 l
Midland Midland /28 Ch em 3 -590 -2344 --
Midland Midland /28 12Z -577 -2327 -2980 Midland Midland /28 13Z -585 -2342 -2972 l Midland Midland /28 14Z -58 6 -2328 -2974 j Midland Midland /28 7Z -580 -2368 -3017 l
Midland Midland /28 6Z -- --
-3013 Midland Midland /28 9Z -595 -2339 -2990 Midland Midland /28 18Z -535 -2329 -2973 l Midland Midland /28 19Z -536 -2333 -2972 Midland Midland /28 20Z -569 -2336 -2978 l
Midland Midland /28 15Z -- --
-2980 B Midland Midland /28 16Z -- --
-2968 Midland Midland /29 2 7Z -580 -2353 -2995 l Midland Midland /29 MJ -545 -2330 -2957 Midland Midland /29 21Z -598 -2346 -3002 Midland Midland /29 22Z -593 -2353 -2999 Midland Midland /29 2 6Z -583 -2352 -2983 l
Midland Midland /29 2 8?. -577 -2357 -2993 l Midland Midland /29 29' -580 -2347 -2994 i
Midland Midland /29 30Z -57 7 -2338 -2990 l Midland Midland /29 25Z -583 -2343 -2986 Midland Midland /31 21D -518 -2300 -2920 l
Weston Geophysical l
[ ___ _ _ _ _ _ _ _ _ _ _
B A-34 APPENDIX I (Continued)
Marshall "Tra verse Rogers City-B Township / Sands ton e Lime" Dundee l
County Section Well Number To p Top Top Midland Midland /33 28M -592 -2345 -2978 Midland Midland /33 11579 --
-2342 -2978 I Midland Midland /36 9M -562 -2507 -2940 Midland Midland /36 10M -551 -2493 -2981 l Midland Midland /36 11718 --
-2338 -2904 Midland Mills /1 21846 -143 -1979 -2728 B Midland Mills /1 20320 -18 2 -1958 -2693 l
Midland Mills /1 11436 -170 -1975 -2716 j Midland Mills /11 20855 -168 -1966 -2707 Midland Mills /11 4890 -154 -1980 -2705 f Midland Mills /12 10209 -16 6 -194 7 -2687 Midland Mi118 /18 92M -4 61 -2281 -3001 1
Midland Mills /21 2132 -283 -2088 -2817 Midland Mills /24 2200 -127 -1909 -2637 Midland Mills /29 51M -52 9 -2329 -3050 l Midland Mills /29 65M -474 -2302 -3024 Midland Mills /31 32323 -540 -2369 -3078 h
Midland Mills /31 31146 -572 -2364 -3072 B Midland Mills /31 52D -542 -2349 -3054 Midland Mills /32 50M -555 -2345 -3077 l
l l Weston Geophysical i
B l
A-3 5 l
APPENDIX I (Continued) l Marshall " Traverse Rogers City-B Township / Sands tone Lime" Dundee l County Section Well Number To p Top Top Mioland Mt. Haley/3 1451 -485 -2247 -2852 Midland Mt. Haley/4 1226 -508 -2268 -2891 Midland Mt. Haley/9 58M -529 -2246 -2854 Midland Mt. Maley/10 57M -503 -2256 -2868 Midland Mt. Haley /11 1738 -493 -2247 -2846 Midland Mt. Haley/12 20252 -517 -- --
Midland Mt. Haley /12 56M -506 -2273 -2886 Midland Mt. Haley/13 18740 -493 -2217 -2813 Midiand Mt. Haley /13 51D -51 1 -2235 -2843 Midland Mt. Haley/15 6156 -481 -2213 -2821 Midland Mt. Haley /16 1525 -455 -2193 -2800 Midland Mt. Haley/21 MHA -- --
-2818 Midland Mt. Haley/23 26264 -460 -2193 -2780 Midland Mt. Haley/23 20250 -474 -2191 -2791 Midland Mt. Haley/25 2293 -429 -2216 -2772 Midland Mt. Haley/26 MHB -- --
-2774 Midland Mt . Haley/27 27202 -419 -2197 -2786 Midland Mt. Haley/28 2267 -396 -2167 -2781 Midland Mt. Haley/28 2142 -390 -2153 -2745 Midland Mt. Haley/33 2646 -398 -2124 -2726 Midland Mt. Haley/34 952 -403 -2088 -2755 I
B __
L L
A-36 F
L APPENDIX I (Continued)
Marshall " Traverse Rogers City-Ibwnship/ Sands tone Lim e" Dundee j County Section Well hamber To p To p Top Midland Port er/2 61M -504 -2234 -2848 Midland Port er/4 67M -459 -2207 -2790 Midland Porter /4 1527 -381 -2172 -2778 ,
I Midland Port er/6 1540 -425 -2173 -2752 Midland Porter /6 3345 -447 -2145 -2740 Midland Port er/7 3806 -4 08 -2142 -2730 Midland Porter /7 3232 -392 -- --
Midland Port er/7 3530 -368 -- --
Midland Porter /7 3982 407 -- --
Midland Port er/7 3862 -364 -- --
Midland Porter /7 2270 -340 -- --
Midland Port er/7 2488 -406 -- --
Midland Porter /7 1898 -344 -- --
Midland Port er/7 3529 -356 -- --
Midland Porter /8 1786 -4 21 -2137 -2730 Midland Port er/8 1504 -383 -2152 -2730 l
Midland Port er/8 1790 -381 -2126 -2740 Midland Port er/8 1903 -399 -2130 -2722 Midland Porter /8 2223 -375 -2175 -2740 Midland Port er/8 2178 -401 -2127 -2717 Midland Porter /8 3550 -370 -2145 -2724 Midland Port er/9 24426 -411 -2123 -2699 Midland Porter /9 3876 -374 -2140 -2740
[
J Weston Geophysical L_ _ _ _
I l
A-3 7 APPENDIX 1 (Continued)
B l Marshall "Tr aver s e Rogers City-I I
County
'Ibwnsh ip/
Section Well Number Sands tone To p Lime" To p Dundee Top Midland Porter /9 1822 -368 -2137 -2756 Midland Port er/9 3249 -379 -- --
Midland Port er /10 8030 -391 -2107 -2692 Midland Port er /10 22782 -413 -2126 -2708 Midland Port er /10 7867 -393 -2116 -2691 Midland Port er/10 21578 -406 -2139 -2711 Midland Porter /10 24682 --
-2151 -2725 Mid1and Port er/10 22028 -398 -2129 -2702 Midland Porter /10 8191 -406 -2112 -2696 Midland Port er/11 3231 -4 44 -2178 -2769 Midland Port er /14 2844 -3 61 -2135 -2692 Midland Port er/14 1937 -379 -2122 -2683 Mid1and Port er /14 2533 -383 -2119 -2695 Midland Port er/14 3013 -364 -2119 -2683 Midland Port er /14 14019 -402 -2126 -2690 Midland Port er/15 1503 -406 -2086 -2695 Midland Porter /15 8127 -387 -2091 -2692 Midland Port er/15 8341 -413 -2102 -2685 Midland Porter /15 23431 -413 -2118 -2687 Mid1and Port er/15 24067 --
-2118 -2696 Midland Porter /15 1636 -373 -2106 -2676 Midland Port er/15 1532 -373 -2093 -2672 Midland Porter /15 3499 -376 -2109 -2682 I
Weston Geophysical
l l
A-38 l
APPENDIX I (Continued)
I l "Tr averse Marshall Rogers City-Township / Sands tone Lime" Dundee B County Section Well Number To p Top Top Midland Port er /15 7130 -378 -2113 -2680 Midland Port er/15 7341 -395 -2115 -2685 Midland Port er /15 2169 -372 -2104 -2687
{ Midland Port er /16 8679 -402 -2124 -2685 Midland Port er /16 2454 -390 -2130 -2707 Midland Port er /16 2024 -340 -2101 -2680 Midland Port er /16 1474 -377 -2124 -2675 Midland Po rt er /16 1659 -398 -2134 -2712 Midland Port er /16 2199 -391 -2112 -2686 Midland Port er/16 1657 -372 -2117 -2689 Midland Port er /16 2038 -357 -2112 -2673 Midland Port er/16 2096 -378 -2115 --
Midland Port er /16 1556 -360 -2106 -2681 MidIand Port er/16 1535 -385 -2101 -2666 Midland Port er /17 1677 -375 -2140 -2703 MidIand Port er/17 1772 -317 -2115 -2702 Midland Port er /17 1644 -382 -2117 -2698 MidIand Port er/17 2520 -353 -2118 -2692 Midland Porter /17 1675 -344 -2122 -2702 Midland Port er/17 2125 -387 -2142 -2702 Midland Porter /21 1919 -337 -2109 -2687 Midland Port er/22 1477 -355 -2114 -2694 I Midland Port er/2 3 3058 -395 -2105 -2712 Weston Geophysical
B l
A-39 l
APPENDIX 1 (Continued)
I Marshall " Traverse Rogers City-Township / Sandstone Lime" Dundee B County Section Well Number To p Top Top Midland Porter /23 3602 -379 -2104 -2697 Midland Port er/23 12 31 -385 -2110 -2700 Midland Port er/2 3 3653 -395 -2115 -2704 Midland Port er/23 2003 -386 -2104 -2710 Midland Porter /24 1529 -346 -2131 -2754 Midland Port er/24 26889 -3 72 -2124 -2740 Midland Port er/2 5 1554 -356 -2126 -2694 Midland Port er/26 1523 -370 -2096 -2702 Midland Porter /2 6 20257 -355 -2107 -2709 Midland Port er/26 1170 -366 -2064 -2665 Midland Port er/2 7 33030 -387 -2129 -2708 B Midland Port er/27 1924 -383 -2105 -2699 Midland Port er/2 7 1289 -391 -2101 -2698 Mid1and Port er/27 1785 -361 -2106 -2715 Midland Port er/35 5902 -354 -2083 -2680 Midland Port er/36 1732 -332 -2062 -2675 Midland Le er/36 1612 -357 -2079 -2672 B
Sa gi . taw Kochville/20 11597 -239 -- --
Saginaw Kochville/33 12262 -12 6 -- --
I Saginaw Richland/2 70157 -366 -- --
Saginaw Richland/3 69M -370 -- --
I Weston Geophysical
E A-40 APPENDIX I (Contiaued) 5 Marshall "Traver s e Rogers City-
'Ibwnshi p/ Sands tone Lime" Dundee W County Section Well Number Top To p Top Saginaw Richland/4 46M -365 -- --
Saginaw Richland/4 11079 -373 -- --
Saginaw Richland/4 52M -363 -- --
Saginaw Richland/7 1544 -354 -- --
S W Saginaw Richland/9 47D -356 -- --
Saginaw Richland/11 72M -347 -- --
Saginaw Richland /11 15395 -324 -- --
Saginaw Richland/12 49M -360 -- --
Saginaw Richland /12 74M -340 -- --
Saginaw Richland /14 41D -337 -- --
Saginaw Richland /15 73M -333 -- --
Saginaw Richland/16 1789 -298 -- --
Saginaw Richland/22 1309 -298 -- --
Saginaw Rich land /23 75M -310 -- --
Saginaw Richland/25 42D -332 -- --
Saginaw Richland/26 7 7M -259 -- --
5 Saginaw Richland/31 3015 -315 -- --
Saginaw Richland /31 3548 -2 64 -- --
Saginaw Richland/33 2071 -241 -- --
Saginaw Rich land /33 12783 -242 -- --
Saginaw Richland/36 79M -223 -- -- i Saginaw Richland/36 78M -255 -- --
it
- g ._ e_
A-41 I
APPENDIX I (Continue d )
Marshall " Traverse Rogers City-I County Township /
Section Well Number Sands tone To p Lime" Top Dundee Top Saginaw Thomas /2 1760 -383 -- --
Saginaw Th omas /7 11503 -275 -- --
Saginaw Thomas /19 76D -307 -- --
Saginaw Thomas /31 5472 -230 -- --
Saginaw Tit t abawas s e e /1 11048 -253 -2010 -2661 Saginaw Tittabawassee/6 18772 -487 -2274 -2920 Saginaw Titt abawasse e/6 38M -476 -2254 -2887 Saginaw Titt abawas s ee/8 39M -485 -2256 -2882 Saginaw Titt abawasse e/8 40M -474 -2229 -2860 Saginaw Titt abawassee/15 1303 -364 -2142 -2776 B
B B
B B
B B
g __
I I
I I
I I
APPENDIX II CONTROL POINTS FOR STRUCTURE B MAPS ON TOP OF COAL ZONE (DATA FROM DISPOSAL, BRINE, SALT, OR OIL AND GAS WELLS WERE NOT USED)
B B
B B
B B
B B
B
A-1 Top of Zone Township / (Ft. Above County Section Well Number Sea Level)
Bay Garfield / 2 805 Glacial l Ba y Garfield /3 810 508 Bay Ga rfield/4 14 9 546 l
Ba y Garfield /4 308 518 Bay Ga rfield/4 151 552 Ba y Garfield /4 1387 517 Bay Ga rfield/4 315 497 Ba y Garfield /4 313 528 Bay Ga rfield/4 14 0 524 Bay Garfield /4 147 510 Bay Garfield /4 144 544 Ba y Garfield /4 138 Glacial Bay Ga rfield/5 154 526 Ba y Garfield /5 158 526 Bay Ga rfield/5 159 533 Ba y Garfield /5 187 526 Bay Ga rfield/5 18 5 520 Ba y Garfield /5 180 538 Bay Garfield /5 184 515 Ba y Garfield /6 947 533 Bay Ga rfield/6 934 531 Ba y Gar field /6 876 529 Bay Ga rfield/6 955 520 Ba y Garfield / 6 919 546 g -e_
l B
l A-2 Top of Zone B County Township /
Section Well Number (Ft. Above Sea Level)
Bay Ga rfield/6 911 517
{ Ba y Ga r field / 6 895 515 Bay Ga rfield/6 830 517 l
l Ba y Garfield /6 854 539 Bay Ga rfield/6 839 535 Ba y Garfield /7 212 513 l Bay Garfield /7 204 484 Ba y Gar field / 7 823 516 Bay Ga rfield/8 208 535 Ba y Gar field / 8 295 507 Bay Garfield /8 803 510 Bay Garfield'8 171 Not Deep Enough Bay Garfield,8 319 498 Bay Garfiel ./ 3 161 485 Bay Ga rfield/8 164 532 Bay Garfield /8 155 520 Bay Ga rfield/9 183 505 Bay Garfield /9 931 507 Bay Ga rfield/9 17 0 520 Ba y Garfield /9 168 Glacial Bay Ga rfield/9 16 5 530 Bay Garfield /9 167 550 Bay Ga rfield/10 350 513 Bay Garfield /10 351 519 5
\
Weston Geophysical
l A-3 l
Top o f Zone Township / (Ft. Above l
County Section Well Number Sea Level)
Bay Ga rfield/10 945 483 k Ba y Garfield /10 342 525 Bay Garfield /10 346 Not Deep Enough j Bay Garfield /10 348 525 l
Bay Ga rfield/10 345 530 Ba y Garfield /10 339 505
( Bay Garfield /10 16 3 534 Ba y Garfield /10 322 503 Bay Ga rfield/10 329 501 i I Ba y Garfield /10 335 498 l
Bay Ga rfield/10 367 497 Ba y Garfield /10 334 Glacial Bay Garfield /ll 137 513 Bay Garfield /ll 956 No t Deep Enough B Bay Ga rfield/11 826 540 Bay Garfield /12 837 543 Bay Ga rfield/13 808 Not Deep Enough Bay Garfield /14 824 Glacial Bay Ga rfield/15 340 516 Bay Garfield /15 366 511 Bay Ga rfield/15 649 524 Bay Garfield /15 386 524 Bay Ga rfield/15 357 527 Bay Garfield /15 841 489
-~,-
I
B l A-4 l
l Top o f Zone Township / (Ft. Above B County Section Well Number Sea Level)
Bay Ga rfield/15 378 Not Deep Enough
( Ba y Garfield /15 435 No t Deep Enough Bay Ga rfield/15 447 500 Bay Garfield /15 468 518 Bay Ga rfield/16 17 2 Glacial Ba y Garfield /16 150 500 Bay Ga rfield/16 14 6 Glacial Ba y Garfield /16 938 515 Bay Ga rfield/16 14 5 523 Ba y Garfield /16 389 485 Bay Garfield /16 128 485 Ba y Garfield /16 127 484 Bay Ga rfield/16 383 484 Ba y Garfield /16 126 482 Bay Ga rfield/16 125 482 Bay Garfield /16 132 496 Bay Garfield /16 129 490 Bay Garfield /16 131 478 Bay Ga rfield/16 13 5 503 Bay Garfield /16 936 482 Bay Ga rfield/16 124 494 Bay Garfield /16 139 485 Bay Ga rfield/17 15 3 524 Ba y Garfield /17 173 Glacial I !
g _m- ,
B A-5 B
Top of Zone Township / (Ft. Above Coung Section Well Number Sea Level)
{
Bay Ga r field /17 304 516 l
Ba y Garfield /18 314 507 t
Bay Ga rfield/18 305 517 l Bay Garfield /18 743 514 Bay Ga rfield/18 784 502 l
Bay Garfield /18 310 Not Deep Enough Bay Ga r field /18 17 8 Glacial l
Ba y Garfield /l8 299 486 l Bay Ga rfield/19 302 474 Ba y Garfield /19 192 Glacial Bay Ga rfield/19 194 512 Ba y Garfield /19 159 Not Deep Enough Bay Ga rfield/19 321 460 Bay Garfield /19 294 500 Bay Garfield /19 326 517 Ba y Garfield /19 318 Glacial Bay Ga rfield/19 328 Glacial Ba y Garfield /19 330 Glacial Bay Ga rfield/19 210 Glacial Ba y Garfield /19 248 545 Bay Ga rfield/20 197 506 Bay Garfield / 20 202 Glacial Bay Ga rfield/20 177 Glacial Ba y Garfield / 20 174 504 5
g _e_
o
I l A-6 I
l Top of Zone Township / ( Ft . Above County Section Well Number Sea Level)
Bay Ga rfield/20 333 Glacial Ba y Ga rfield/ 20 179 507 Bay Garfield /21 737 500 Bay Gar field / 21 283 495 Bay Ga rfield/21 282 Glacial Ba y Garfield /21 281 492 Bay Ga rfield/21 280 492 Bay Garfield /21 930 499 Bay Garfield / 21 927 480 Ba y Garfield / 21 939 Glacial Bay Ga rfield/21 714 Glacial Ba y Garfield /21 9 21 490 Bay Garfield /21 918 Glacial Bay Gar field / 21 906 Not Deep Enough Bay Ga rfield/21 904 503 Ba y Garfield /21 905 488 Bay Ga rfield/21 886 481 Ba y Garfield /21 907 480 Bay Ga rfield/ 21 885 Glacial Bay Garfield /21 893 487 Bay Ga rfield/22 993 518 Bay Garfield /22 166 512 Bay Ga rfield/22 885 519 3 Bay Garfield / 22 912 511 g -e_
I A -7 Top of Zone
,B County Township / (Ft. Above Section Well Number i Sea Level)
Bay Ga rfield/2 2 250 517 I Ba y Gar field /22 892 524 Bay Ga rfield/22 884 512 Ba y Ga rfield/ 22 247 518 Bay Ga rfield/22 241 504 i
Bay ! Garfield /22 869 501 Bay Ga rfield/22 242 506 Ba y Ga rfield/22 243 4
516 Bay Ga rfield/22 251 523 Ba y Garfield /22 249 511 Bay Ga rfield/22 252 513
- Ba y Gar field / 22 293 505 Bay Garfield /22 404 504 Ba y Garfield / 22 628 507 Bay Garfield /22 287 505 Bay Garfield / 22 285 508
- Bay Garfield /22 398 509 Ba y ,
Garfield / 22 286 512
! Bay Ga rfield/22 284 519 Ba y Garfield /22 288 524
! Bay Garfield /22 289 512 Bay Garfield /22 492 511 Bay Ga rfield/22 481 516
! Ba y Garfield /22 473 498 1
, i
,i Weston Geophysical
A-8 Tbp of Zone Township / (Pt. Above County Section Well Number Sea Level)
Bay Ga r field /2 2 253 505 Ba y Garfield /22 254 529 Bay Ga rfield/2 2 228 515 Ba y Gar field / 22 227 513 Bay Ga rfield/2 2 260 511 Ba y Gar field / 22 259 513
- Bay Ga rfield/2 2 224 506 Ba y Gar field / 22 245 496 Bay Ga rfield/2 2 907 480 Ba y Ga r field / 22 629 501 Bay Ga rfield/2 2 244 499 Ba y Gar field / 22 290 508 Bay Ga rfield/2 2 246 511 i
Ba y Garfield /22 248 519 Bay Ga rfield/22 630 509 i
Ba y Gar field / 22 501 518 Bay Ga r field /23 420 Glacial Ba y Ga r field / 23 268 510 Bay Ga rfield/23 269 503 Ba y Ga r field / 23 390 498 l Bay Ga rfield/23 1177 474 Ba y Gar field / 24 332 481 Bay Ga rfield/24 317 505 Bay Ga r field / 24 353 457 1
l Weston Geophysical
l l A -9 l
E
'Ibp o f Zone Township / (Pt. Above County Section Well Number Sea IEvel)
Bay Garfield /24 312 448 l Bay Ga r field / 25 783 496 Bay Garfield /25 787 452 Ba y Garfield /26 1321 489 Bay Ga rfield/26 382 485 Day Ga r field / 26 1172 490 Bay Ga rfield/26 1205 495 Ba y Garfield /26 804 485 Bay Ga rfield/26 1192 460 Ba y Ga r field / 26 1213 473 Bay Ga rfield/26 788 475 Bay Ga r field / 26 1188 468 Bay Garfield /26 831 511 Ba y Garfield /26 1198 494 Bay Ga rfield/26 853 495 Ba y Gar field / 26 825 467 Bay Ga rfield/26 1322 475 Ba y Garfield / 27 510 434 Bay Garfield /27 271 444 Ba y Ga r field / 27 272 450 Bay Ga rfield/27 234 471 Ba y Ga r field / 27 233 471 Bay Garfield /27 773 446 Ba y Ga r field / 27 279 490 Weston Geophysical
A-10 E
l Top of Zone Township / (Ft. Above County Section Well Number Sea Invel)
Bay Ga rfield/27 213 489 j Bay Ga r f ield/ 27 230 500 Bay Ga rfield/27 235 504 Ba y Ga r field / 27 236 505 Bay Garfield /27 229 484 Ba y Ga r field / 27 223 505 l Bay Ga r field /27 222 503 Ba y Garfield /27 255 503 l
Bay Garfield /27 278 486 Ba y Ga r f ield/ 27 277 480 l
Bay Garfield /27 276 486 l
Ba y Garfield /27 256 481 Da y Ga rfield/27 275 460 Ba y Ga r field /27 257 459 Bay Garfield /28 866 497 f
Ba y Ga r field / 28 928 473 i
l Bay Ga rfield/28 705 439 Ba y Ga rfield/ 28 699 441 f Day Ga rfield/28 762 474 Ba y Ga r f ield/ 28 759 467 Bay Ga r field /28 262 421 E Ba y Garfield /28 218 430 Day Ga r field /28 541 436 l Ba y Ga r field / 28 770 Glacial l
Weston Geophysical
l A -11 l
l Top of Zone Township / (Ft. Above l
County Section Well Number Sea Level)
Bay Garfield /28 774 Glacial l Ba y Ga r field / 28 754 447 Bay Garfield /28 563 455 Ba y Garfield /28 219 467 lv Bay Garfield /28 217 447 !
Ba y Gar field / 28 216 467 Bay Garfield /28 220 480 Ba y Ga r field / 28 874 469 Bay Garfield /28 888 Glacial Ba y Gar field / 28 261 465 Bay Ga rfield/29 18 3 Not Deep Enough Ba y Ga r field / 29 672 Not Deep Enough Bay Garfield /29 515 501 Ba y Ga r field / 30 516 510 Bay Ga rfield/30 419 Not Deep Enough Ba y Garfield /30 198 Not Deep Enough Bay Ga rfield/30 19 3 472 Ba y Gar field / 30 195 490 Bay Garfield /30 203 499 Ba y Garfield /30 186 487 Bay Garfield /30 18 9 485 Day Gar field / 31 206 521 l Bay Ga r field / 31 661 481 Ba y Ga r field / 32 336 Glacial Weston Geophysical
A-12 l
Top of Zone
' Township / (Ft. Above County Section Well Number Sea Level)
Bay Ga rfield/3 2 306 Glacial Ba y Ga r field / 32 299 Glacial l Bay Ga rfield/3 3 289 Glacial Ba y Gar field / 33 294 Glacial l
Bay Ga rfield/3 3 701 467 Ba y Ga r field / 34 689 Glacial Bay Ga rfield/3 4 690 Glacial /
l Ba y Ga rfield/ 34 658 496 Bay Ga rfield/36 799 tbt Present I
Bay Williams /19 380 Glacial l
Ba y Williams /19 375 Glacia1 l Bay Williams /19 814 412 Day Williams /19 1053 406 Ba y Williams /20 394 Glacial Bay Williams /21 520 Glacial l
Ba y Williams /28 374 Glacial l
Bay Williams /29 1262 475 Ba y Williams /30 1206 455 l Ba y Williams /30 1233 454 Bay Williams /30 1142 428 l
Bay Williams /30 1092 408 Bay Williams /30 1095 419 Bay Williams /30 1109 424 l '
weston econnysicci l
i - - - - - - - - -
l l
A-13 l
I l
County Township /
Section Well Number
'Ib p o f Zon e (Ft. Above Sea IEvel)
Ba y Williams /30 1250 441 l Ba y Williams /30 1259 438 Ba y Williams /30 1114 425 Bay Williams /30 1163 453 Bay Williams /30 1243 433 Ba y Williams /30 1255 433
( Bay Williams /30 1171 421 Ba y Williams /30 1268 Glacial l
Bay Williams /30 1263 Glacial I Ba y Williams /30 1154 434 1
Ba y Williams /30 1178 460 l Ba y Wi11iams/30 1209 443 Bay Williams /30 1273 453 Ba y Williams /31 1202 445 Bay Williams / 31 1226 455 1
Bay Williams /31 1218 465 l Bay Williams /31 1237 Not Deep Enough Bay Williams /31 1217 446 l Bay Williams /31 1227 449 Ba y Williams /31 362 429 l
Bay Williams /31 438 390 Ba y Williams /31 1241 432
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Bay Williams /31 424 Glacial I Bay Williams /32 483 434 I
L Weston Geophysical
l l A-14 I
'Ibp o f Zone l Township / (Ft. Above County Section Well Number Sea Level)
Midland Ingersoll/ 2 846 446 l Midland Ingersoll/2 311 455 Midland Ingersoll/ 2 782 Glacial Midland Inger soll/ 2 753 Glacial I Midland Inger soll/ 2 883 Glacial I
l Midland Midland / 24 1020 404 Midland Midlan d/2 4 752 Glacial Midland Midland /24 769 Glacial Midland Midland /24 1387 Glacial l
Midland Midland / 24 991 Glacial l Midland Midland /24 1076 Glacial Midland Midland /24 1003 Glacial Midland Midland /24 917 417 Midland Midland / 24 747 422 Midland Midland /24 953 407 Midland Midland / 24 1271 408 l
Midland Midland /24 1273 414 l Midland Midland /24 865 393 Midland Midland /24 1274 408 1
Midland Midland /24 877 413 Midland Midland /24 1270 408 Midland Midland /24 1262 401 l Midland Midland /24 1250 398 1
weston seconysicai l
A-15 I l
Top of Zone Township / (Pt. Above B County Section Well Number Sea Level)
Midland Midland /24 1382 408 l Midland Midland /24 503 381 Midland Midland /24 828 412 Midland Midland /24 1040 406 i E
l
. Midland Midland /24 1384 394 l
Midland Midland /24 847 381 l Midland Midland /24 795 401 Midland Midland /24 1346 Not Deep Enough Midland Midland /24 1347 Not Deep Enough Midland Midland /24 1348 402 l
Midland Midland /24 1272 401 l
Midlatid Midland /24 972 396 Midland Midland /25 1180 383 I Midland Midland / 25 1385 395 Midland Midland /25 891 Glacial l
Midland Midland / 25 1269 402 Midland Midland /25 1386 394 Midland Midland / 25 1072 394 l Midland Midland /25 1269 402 Midland Midland /25 1195 405 Midland Midland /25 1093 408 Midland Midland /25 1264 428 I
Midland Midland /25 1165 Not Deep Enough j Midland Midland /25 963 433 Weston Geophysicot i
l A-16 I
l Top of Zone I County Township /
Se ct ic.n Well Number (Ft. Above Sea Level)
Midland Midland /25 621 Glac'ial Midland Midland /25 901 433 Midland Midland /25 1099 420 I Midland Midland / 25 1268 434 Midland Midland /25 1265 423 l
Midland Midland /25 1094 419 Midland Midland /27 606 Glacial Midland Midland / 27 758 Glacial l Midland Midland /3 3 771 Glacial Midland Midland / 34 342 Glacial l
Midland Midland /35 287 437 Midland Midland /35 657 417 Midland Midland /35 593 410 l Midland Midland / 35 656 407 Midland Midland /3 5 659 417 Midland Midland / 35 896 Glacial B Midland Midland /3 5 654 439 Midland Midland /35 269 432 l Midland Midland /35 285 440 Midland Midland / 35 660 421 l Midland Midland /3 5 302 429 Midland Midland /35 336 429 l
Midland Midland /35 658 437 Midland Midland / 35 655 432 I
Weston Geophysical
l A-17 l
E Township /
'Ib p o f Zon e (Ft. Above County Section Well Number Sea Level)
Midland Midlan d/35 967 435 Midland Midland /35 265 424 Midland Midland /35 767 431 Midland Midland /35 298 434 Midland Midlan d/3 5 292 455 Midland Midlar.J/ 35 661 442 l Midland Midland /35 263 448 Midland Midland /35 290 436 Midland Midland /3 5 304 439 Midland Midland /35 653 447 Midland Midland /35 331 445 Midland Midland /35 320 450 Midland Midlan d/35 303 450 Midland Midland /35 291 432 Midland Midlan d/35 296 455 Midland Midland /35 310 467 Midland Midlan d/35 313 469 Midland Midland /35 319 452 Midland Midlan d/36 923 433 E Midland Midland /36 543 454 Midland Midlan d/36 532 417 Midland Midland /36 572 No t Deep Enough E
E Weston Geophysical
A-18 Top of Zone Township / (Ft. Above County Section Well Number Sea Level)
Sagintsw Tittabawassee/5 495 441 l Saginaw Ti ttabawassee/ 5 496 455 Saginaw Tittabawassee/5 604 Not Deep Enough Saginaw Tittabawassee/5 617 Glacial Saginaw Tittabawassee/5 864 431 Saginaw Tittabawassee/6 451 401 Saginaw Tittabawassee/6 282 423 l
Saginaw Ti ttabawassee/ 6 558 Glacial Saginaw Tittabawassee/6 505 Glacial Saginaw Tittabawassee/6 576 414 l
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