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A SURFACE MAGNETIC SURVEY
of
COSHOCTON COUNTY, OHIO
A Thesis
Presented in Partial Fulfillment of the
Requirements for the Degree, Bachelor of Science
by
Rodney A. Sheets Jr •
The Department of Geology and Minerology
Ohio State University
Approved by
Hallan C. Noltimier, Advisor Department of Geology and Mineralogy
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ABSTRACT
A total field magnetometer survey of nine quadrangles in Coshocton County is presented. The survey area is bounded by 40.125 and 40.500 degrees latitude and -81.617 and -82.000 degrees longitude. The anomaly field is derived from the total field values that are corrected for the IGRF and the diurnal fields. Corrected residual values are machine gridded at one half mile spacings, corresponding to 52 rows (latitude) and 43 columns (longitude). The grid node values were then machine contoured to produce anomaly maps of the area.
en; Two qualitative interpretations of the anomalies are giv-
1.) Observed variations are due to basement faulting, or 2.) Observed variations are due to susceptibility and remanence variations across lithologic·units •
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ACKNOWLEDGEMENTS
I wish to thank Dr. Hallan Noltimier, my advisor, for suggesting this project, and for his support and assistance throughout this project.
Very special thanks go to Eric Cherry, With his kind help, this project got underway, progressed, and concluded.
Financial support for field work was provided by a grant from the Friends of Orton Hall •
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TABLE OF CONTENTS
Abstract
Acknowledgements
List of Figures
List of Tables
1.0 INTRODUCTION
2.0 THEORETICAL BACKGROUND
2.1 Elements of the Main Field
2.2 Magnetic,Field---Variations
2.3 Rock Magnetism
3.0 GEOLOGICAL AND GEOPHYSICAL STUDIES
3.1 Surface Geology
3.2 Precambrian Geology
3.3·Geophysical,Studies
~4~-0 SURVEY PROCEDURE
4.1 Field Operations
4.1.1 Survey Technique
4.1.2 The Magnetometer
4.2 Reduction-of-Data
4.2.1 Diurnal Corrections
4.2.2 Total Field Corrections
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• 4.2.3 Grid System 14
5.0 RESULTS AND INTERPRETATION 20
5.1 Effects of Remanence on Interpretation 21
• 5.2 Interpretation 1-- Faulting 21
5.3 Interpretation 2-- Lateral Susceptibility and Remanence Variations 25
• 6.0 CONCLUSIONS AND RECOMMENDATIONS 25
REFERENCES 27
APPENDICES 29
• Appendix 1- Magnetometer Specifications 30
Appendix ll- Program Geomag 32
Appendix 111- Data Tables 38
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1.
2.
LIST OF FIGURES
Elements of the Main Field
Vector Representation of the Total Magnetization
3. Postulated Basement Fault Trend and
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Lithologic Boundary on State of Ohio Map 7
4. Precambrian Structure of Southeastern Ohio 9
5.
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9.
Diurnal Variation Curves for August 24, 1983
Field Station Location Map
Contour Map of Original Field Values
Contour Map of IGRF Values
Contour Map of Residual Values
10. Proposed Grenville Apparent Polar Wander Curve
11. Fault Interpretation for Anomalies
12. Total Field Profile of Horizontally Polarized Fault Block
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13. Lateral Lithology Variation Interpretation 23
1.
2.
LIST OF TABLES
Well Logs to the Precambrian in Coshocton
Typical Susceptibilities and Polarizations for Sedimentary, Igneous, and Metamorphip
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rocks 11
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1.0 INTRODUCTION
In eastern Ohio, little is known about local structure
and lithology of the Precambrian basement complex. The only
existing data are from sparse well control and recently com
pleted aeromagnetic surveys. This surface magnetometer sur
vey of Coshocton County, Ohio was undertaken for the purpose
of learning more about the local structure and lithology of
the basement.
This survey covered approximately 350 square miles, com
pletely contained in Coshocton County, in east-central Ohio .
A rectangular region bounded by 40.125 and 40.500 degrees lat
itude and -81.617 and -82.000 degrees longitude, was chosen
to accomodate the 320 survey points and to serve as a basis
for the gridding system used.
A grid spacing of one half mile was used. Previous aero
magnetic surveys are gridded at one mile. Higher resolution
of the data is to be expected, due to the closer grid spacing
and the lower elevation.
After corrections for the diurnal variations were per
formed, the total magnetic field at grid nodes was calculated.
The International Geomagnetic Reference Field (IGRF) was then
calculated at each survey point, and gridded at similiar spac
ing, and the values were subtracted from the total field values.
The resulting residual values were interpreted qualitatively,
because of the complexity of the data. Most magnetic modelling
is variable and nonunique because it relies on many unknown
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variables .
Two interpretations are presented:
1.) / Observed variations are due to basement fault
ing, or
2.) Observed variations are due to susceptibility
and remanence contrasts between lithologic units.
2.0 THEORETICAL BACKGROUND
To better understand the concepts and definitions of mag
netics and the magnetic field, a brief review is apprnpriate.
The nature of the Earth's magnetic field has been estab
lished on the basis of world-wide measuements. The fie~d is
considered to be comprised of three components: (Nettleton,
1976)
1.) The main field comprises the largest proportion of
the magnetic field observed at the surface of the Earth.
This field arises due to convection currents in the liq
uid iron core of the Earth and follows a slow, but pre
dictable secular change. (i.e. 'the westward drift')
2.) The smaller diurnal field behaves more erratically
with time, but approximately follows a daily cycle. This
field is due to electromagnetic currents in the upper
atmospere and can be affected by magnetic storms, related
to sunspots.
3.) The anomaly field is coused by magnetic inhomogen
eities in the crust •
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To evaluate the anomaly field with respect to lithologic
changes in the crust, it must be separated from the effects
of the main and diurnal fields.
2.1 Elements of the Main Field
The main field of the Earth can be separated into sev
eral components, each one defin~ng a specific part of the
field. F signifies the total intensity of the field, and
H, the horizontal component of the field, along the magnet
ic meridian. The inclination or,magnetic dip, I, is the
angle between F and H, and the declination, D, is defined
as the angle between H and geographic North. F, D, and I
completely define the field at any point on the Earth's
surface. (Jacob, 1963) These elements are shown vector
ally by Figure 1.
2.2 Magnetic Field Variations
As stated above, variations in the field due to sec
ular changes are slow. Isolation of anomalies, though,
depend upon knowing what this field looks and acts like at
the time of the survey. For this purpose, an International
Geomagnetic Reference Field (IGRF) was adopted in 1965, to
establish a uniformity to the field. This reference field
is calculated assuming the Earth is a perfect sphere of mag
netized material, which varies secularly and by locality.
Every five years, a new IGRF is published, which contains
coefficients for calculating the field's strength at any
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place or time in the subsequent five years. The main mag
netic field strength at the present time varies from 24,000
ganunas at some places along the equator, to 68,000 ganunas
at the poles. In my survey area, the field strength ave
raged approximately 56,200 ganunas.
If the Earth's field were measured continuously over
a fixed point, it's intensity would change over time due
to solar and lunar effects on the ionosphere. Tne solar
effect is the larger of the two, and is seen when the sur
vey is performed during the day. Determination of this
variation is essential to define the nature of the field
during a day's survey. Solar variations can reach up to
30 ganunas, whereas lunar variations are usually 2 to 3
ganunas.
Secular and diurnal variations are equally important
when determining the nature of local anomalies •
2.3 ,Rock Magnetism
The magnetic moment· of a rock body consists of two
principal components, the remanant moment (MR) and the in
duced moment (MI) • The remanant moment is the primary
magnetization and is acquired by igneous and metamorphic
rocks during cooling. The induced moment is the magnet
ization of the rocks in the present magnetic field.
The remanant moment is carried by the ferrimagnetic
minerals, magnetite and hematite, which may comprise one
to ten percent of the rock body. It's magnitude depends
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Figure 1: Elements of the ·Main Field +Z
Figure 2:
Do•n
Vector Representa.tion Total Magnetizati~
of the M
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North +)(
MR
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East
M
GeCITlCqletlc Field
Total
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on the relative amounts and grain size of the magnetic
phases. Remanence is acquired as the body cools through
the Curie temperature of the minerals (580 C-680 C) and
reflects the geomagnetic field at the time of cooling •
The induced moment reflects the magnetization of the
rock body in the present geomagnetic field. This moment
is directly related to the bulk magnetic susceptibility
(k) of the rock, and the geomagnetic field strength, H,
as given by the equation:
Mr = k*H
where k is the susceptibility in go.uss/oerstead and H is
the magnetic field strength in oerstead.
The susceptibility, k, is related to the amount of
iron in the rock, including both the ferrimagnetic oxides
and the ferromagnesium minerals.
Thus, the total magnetization, ~otal' is the vector
sum of the remanant moment (MR) and the induced moment,
(Mr), as shown by Figure 2.
3.0 GEOLOGICAL AND GEOPHYSICAL STUDIES
3.1 Surface Geology
The Tuscararus and Walhoding Rivers empty into the
Muskingum River valley, draining the survey area. Being
just South of the glacial advance in Ohio, Illinoian gla
cial outwash fills the river basins and provides a ground
water reservoir, used extensively by the growing industrial
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• Figure 3:
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-r I I I I I I. I I I I I I I I I I I .,
·I I I I I I I I ----------'T· _. .. _
! I t~ a
Lithologic Boundary (Lidiak, 1966)
_, - ..__,Postulated basement fault (Zeitz, 1966) .-------,
I eRegion structurally contoured : I (Figure 4) I 1 --------·
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PRECAMBRIAN STRUCTURE: SOUTHEASTERN OHIO
e1·
+1413 I -4463 • r
• I • I ,
J82f!J -49181
- -~°'!"'- ..... • - . --I
0 5 10 15 20
KEY
PRE£ WELL- 1100 -PERMIT NUM8ER ~8411-SUB-SEA PRE-e
- lf••tl
--- - - Area of Magnetic Survey
Scale In Miles
CONTOUR INTERVAL
---500ft.
---2500ft.
Figure 4: Modified after Rowan (1984)
40-
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cities of Coshocton and West Lafayette .
Pennsylavanian rocks, of the Allegheny and Pottsville
groups, are predominately the surface rocks in the area,
with varying lithologies. Sandstones persist, with shales
and some limestones occurring, also. Just off the western
edge of the survey area, iron-rich sandstones occur (Lamborn,
1954) that could affect a magnetometer survey. No such
rocks are known to occur within the survey area. Coals
are strip-mined extensively in the South-cental and South
eastern parts of the map area. Entrance into the mined
area was possible, but measurements were restricted to
proven map locations. Active mining areas were strictly
forbidden, and as a ~esult, gaps do exist in some parts
of the maps.
3.2 Precambrian Geology
e The precambrian rocks of Ohio are known only from sub-
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surface well data. From this data, a petrologic boundary
is known to exist between older rhyolites and trachytes of
western Ohio, and younger granites, granite gneisses, and
monzonites of eastern Ohio. (Lidiak, et •. al. 1966) (See
Figure 3) East of this boundary, which is coincidental
with the Findlay Arch, a basement structural high, the pre
cambrian surface dips to the east. Due to limited drill
ing data, only a general structure map can be produced,
{See Figure 4) though several hundred feet of relief may
exist in the form of erosional remnants. (Janssens, 1966)
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In my survey area, the depth to the basement is ap
proximated at 6000 feet on the western boundary, and 7000
feet in the East, by three wells recently drilled into
the precambrian, Lithologies from these wells are shown
in Table 1.
3~3 Geophysical Studies
Few geophysical studies have been attempted in east
ern Ohio. Regional and statewide aeromagnetometer surveys
have been done and a single gravimeter survey was done that
covered parts of my survey area •
The most significant study related to my work was a
regional aeromagnetometer survey, by Zeitz (1966), cover
ing a continental strip between 38 and 41 degrees latitude,
which included my survey area. In his report, he mention
ed the possibility of a basement fault through central
Coshocton County. The approximate trend of this proposed
fault is shown in Figure 3.
A state aeromagnetic anomaly map, soon to be published,
{von Frese, personal communication 1984) shows relatively
quiet anomalies in the county, but a significantly low an
omaly field, just to the west of the county.
Rowan {personal communication 1984) recently completed
a gravimeter survey that included most of my map area. In
it, he found North-east, South-west trending lineations,
suspected to be of basement origin. Also, a gravity high
was seen in the northwest corner of the map area, that may
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County
Coshocton
Permit ~ Number
2053
3462
4118
TABLE 1
Depth to Precambrian
(in feet below~. ·sea level)
-5900
-6680
-64;\.6
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· Litholo~y
Quartz Monzonite
Pegmatite*, gneiss, hornblende gneiss
* Pegmatite believed to be derived from basal arkose
Polarization Mechanism
Sedimentary rocks:
DRM & PDRM, CRM
Igneous rocks;
TRM, CRM
Metamorphic rocks:
, TABLE 2*
Typical Polarization
Typical · Susceptibility _Anistropy
5%
(For sedimentary iron cores, these values may be increased by an order of magnitude or more)
lo-2 - lo-4 emu/cc
l0~3 - 10-4 emu/cc
* Taken from (Noltimier, 1984)
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also be controlled by the basement •
No other significant geophysical studies were com
pleted in the survey area, though several other studies
were completed in eastern Ohio, and not in the map area •
4.0 SURVEY PROCEDURE
This section takes up first, the general field procedures
performed during my survey. The measurements necessarily in
clude unwanted magnetic effects (the secular and diurnal field
disturbances) and methods for their determination and removal
are covered in the second part of this section •
4.1 Field Operations
4.1.1 Survey Technique
A major concern in the actual surface magnetic sur
vey is the effect of diurnal variations. To better un
derstand the nature of these variations, I used a 'loop
ing' technique that required returning to a base station,
or to a field station designated as a base, at regular
time intervals. On the average, each loop consisted of
between 8 and 10 field stations, which were in close
proximity to the base station. At the end of each day,
a diurnal variation curve was plotted, with field strength
of the base and time as they and x axes, respectively.
Most field station locations were subject to change,
due to magnetic constraints. The stations were chosen
beforehand, by road intersections and benchmarks, but
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iron objects and electric wires, which affect the nor
mal field, were often associated with these locations.
Often, an offset of up to 200 yards was needed to eli
minate their effects. Because of this, no measurements
were made in the two major towns of Coshocton and West
Lafayette.
4.1.2 The Magnetometer
For this surface magnetic survey, a Barringer Re
search Proton Precession Magnetometer was used, to meas
ure the Earth's total field. (See Appendix l) This mag
netometer operates on the principal that protons will
align themselves either parallel or perpindicular to any
external magnetic field. When the external field is re
moved, the protons will return to their original direc
tion (the Earth's field), by precessing around that field
at a discrete angular velocity. To determine the total
field, the frequency of the induced voltage, produced by
this precession, is measured by counting the number of
e cycles of the precessional voltage and timing these cyc
les. (Dobrin, 1976)
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4.2.1 Diurnal Corrections
As stated above, a primary concern in magnetic sur
veys is the effect of diurnal variations. The nature of
this diurnal field was established through the 'looping'
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method, as explained above, and for each day, a diurnal
variation curve was plotted. (See Figure 5) Every day's
'Values were added (or subtracted) to a normal value of
56,200 gammas, the average low value of the diurnal
curves. This reduced the survey readings to a common
reference point and corrected for the diurnal variation.
4.2.2 Total Field Correction
For this survey, a computer algorithm was obtained
to calculate the Internat~onal Geomagnetic Reference
Field (IGRF) for each station location. (See Appendix 2
for program listing) The algorithm uses the 1980 IGRF
coefficients and calculates the reference field at each
station location, defined by latitude and longitude. A
slight modification in the program yields the original
field value, as corrected for diurnal variation, the IGRF
value that corresponds to it, and residual value obtained
by subtraction of the IGRF from the original value. Dec
linations and inclinations of each location are also com
puted •
4.2.3 Grid System
A rectangular grid, bounded by 40.125 and 40.500
degrees latitude and ~al.617 and ~a2.ooo degrees long
itude, was placed over the original field values, the
IGRF values, and the residual values. Fifty-two rows
(latitude) and forty-three columns (longitude) resulted
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FI ELD STRENGTH
• ( ~ 0-W\w.o.S)
~ ~ .cf t3ASE(+) ~ ..,, "' !'I : !'.\ ~ !'l ~ ~ ~ :;- '1' ~ .J ~ c:6 N
- ~ "' 0 \It : .p... -,---~ __ _,__ _____ _..___ ______ ....__ __ _.,_. ' 0
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\
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• F; 9ure S: D1 tir-1\0J ~ \
Va-v-1a..+10Y\ Cu.rv~s
for- A~u.s+ 24, l'!S3 \
+-• j!J s:>
• c "" ~ "' ~ ~ ~ .t;
~ .... ... .,
.,J ,,a Uo\ "" w
""' C> 0 ..,,. ~ ~ "" 0 "' 0 "' ~ "' 0
I OF BENC '-\ MAt.\<. 74 b (~) ( I I ! ! I I
vt '/:! ~ ~ ~ ~ "" ,... ... - - ~ ~ ~ a di ~ ~ ~ ~ e 0 •
() i::- INTER SE.CT IDN eo3 (A)
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• 40 .425 ...
•
40.350 ...
•
• 40 .275 ...
•
• 40 .200 ....
•
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+ ....
+
+ t +
+ ......
+ + +
+ ·+ + + ..
+ ~ ...
+• ++ +
+
+
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... + +
+ +
+ + + +
+
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+
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+ + +
+ +
+ +
+ + + + • +
+ + + + + + ....
+ ++ + +
•+ + • ••
+ •• •• + +
++ •• : • + +
+
+
• +
+ + + + + +
+ +
•• + +
+ ... + ... + +
+ + ' +•. :· •••• +
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+ + + +
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+ • ...
•• +
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+ •+ + • +
+ • :b+ I + ...
++ +
+ + ... ... ....... ... +
+
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+ + + + •++
+ +
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+ +
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• + +
+ •++
+
+
+ ++
+ ...
•• +
+ ...
+
+
•+ +
+ + +
+ + . + + + • + ... + .... .. · . ... +
+ + +
'
+
...
+ + •
+
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......
+ ...
+ + + . -81 .800
.... +
++ + ..
+ + +
+
+ + ... .
+ ++
-81 .700 '
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40.425
40 .350
40.275
40 .200
40 .125 -82.000 -81 .900 -81 .800 -s-1. 700
Figure 7: Contour Map of Original Field Values (CI= 20 gammas)
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40. 425
40. 350
40.275
4C: .2'.~::: -
-81 .900 -81 .800
Figure 8: Contour Map of IGRF values (CI= 20 garrnnas)
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-81 • 700
0 200
0 000 00
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40.425
40 . .350
40.275
40 .200
40 ·~~~.ooo -B1 .900 -81 .800 -81 . 700
Figure 9: Contour Map of Residual Values (CI= 20 gammas)
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in a grid spacing of one half mile. The grid nodes
were calculated using a nearest eight neighbor approx
imation, with one over the distance to the points, as
the weighting parameter. (Surface II Graphics, 1976)
The grid points were machine contoured with Bessel
function smoothing.
The original survey point locations are shown in
Figure 6, with the contour maps of the original total
field values, the IGRF field values, and the residual
values shown in Figures 7,8, and 9, respectively.
Block diagrams of each set of values are shown in plates
1,2, 'and 3, respectively.
5.0 RESULTS AND INTERPRETATION
Residual values were obtained by subtracting the IGRF
values from the corrected field values. These residuals are
shown in Appendix 3. The values were gridded and contoured
(as above) to obtain the anomaly map in Figure 9.
Potential field data (gravity and magnetics) is affected
by many variables whose parameters are not always known. In
magnetic interpretation, one interprets a situation as if it
were geologically simple, to control variables that are un
known. Many times, a situation can be resolved using differ
ent interpretations. Because of this nonnniqueness of inter
preting anomalies, a complex area, such as this one, can be
interpreted in many ways, which may be equally correct.
Before interpretation of the anomalies, a background of
21
remanence effects is given, to serve as a basis for the in
terpretation. Because of the magnetic complexity of the reg
ion, two qualitative interpretations are presented:
1.) Observed variations are due to basement faulting, or
2.) Observed variations are due to susceptibility and
remanence contrasts between lithologic units.
5.1 Effects of Remanence on Interpretation
The thick sedimentary cover in eastern Ohio is trans
parent in magnetics, due to susceptibility and remanence
differences between the sediments and the igneous or meta
morphic basement rocks. The total magnetic field is whole
ly controlled by structural events in the basement, or by
the basement rocks themselves. Typical polarizations and
susceptibilities, shown in Table 2, indicate that sediments
are virtually nonexistent, magnetically speaking.
The precarnbrian rocks of eastern Ohio are known to be
of the Grenville Province, whose apparent polar wander curve
(APW) indicates that it was at, or close to, the equator. at
the time of its formation, one billion years ago. (See Fig
ure 10) This information suggests that the remanant polar
ization of the basement in my survey area is approximately
East-West. This polarization will accentuate anomalies
associated with thin slabs (faults) in the basement, and
with changes. of .. lithology, across the basement.
5.2 Interpretation 1-- Faulting
Upon inspection of the anomaly map (Figure 9), a pair
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Figure 10: Proposed Grenville Apparent Polar Wander Curve (Berger, et. al. 1976)
W E
,. :~ )"
~
> "
)I. .. "' .It
Figure 12: Total Field Profile of Horizontally --polarized Fault Block
'! - -0
Low
1
--..... "
' ' j)
IJ \
.. \p .·· ;/ CJ
0 -~g Low
tD
+ (Gneiss)
I
I
+ (? Gra..t\·,te)
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Figure 11: Fault,Inter-. pr eta ti on for Anomalies
(Solid lines represent lineations interp. by faults--dashed refer to anomaly· changes that may be due to faults)
Figure 13~ Lateral Lith. ology--..Vari~tion -...Interpretation
(Solid lines represent lineations interp. by lithological boundariesArrows point to lithology of lower susceptibility)
24
of lineations is seen; one that trends northeast-south
west (NE-SW) and a second that trends northwest-south-
east (NW-SE) • (See Figure 11) Associated with the first,
and most prominent, lineation are small negative and pos
itive anomalies of up to 2 mile in diameter. As they are
controlled by 3 or more data points, it is unlikely they
are spurious anomalies. Their position along the lineation
leads me to believe that they could be a result of fault
ing and subsequent remineralization or alteration of mag
netic minerals. In a paper by Henkel and Guzman (1977),
the oxidation of magnetite to hematite along fracture
zones was associated with local magnetic minima. This is
possibly applicable to this situation.
Upon observation of the NE-SW lineation, one sees a
general decrease in anomaly values from East to West, of
about 100 gammas. The NW-SE lineation exhibits a decrease
of a similiar amount, from West to East. A horizontally
polarized fault block exhibits anomalies that could be
assimilated to this situation. (See Figure 12) A high
anomaly field is associated with,the negative pole, or
the eastern edge of the block. A low anomaly field is
coincident with the positive pole, or the western edge of
the block. Figure 11 shows the general structure that
could produce the anomalies seen in my survey area. The
faults are drawn essentially vertical to produce sufficient
relief.
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5. 3 Interpretation 2-- Lateral Susceptib:ili:ty,and, Remanence
Variations
Changes in lithology which give rise to lateral con
trasts in susceptibility show up in the magnetic contours
more readily than topographic features on the basement.
(Dobrin, 1976)
In this survey area, the magnetic contours produced
can be interpreted as lateral variation of lithology; herice,
susceptibility. The three well logs in the area indicate
that a noticeable change of lithology occurs. (See Table 1)
In the western part 1 of the survey area, a quartz monzonite
basement exists, and in the northeast a gneissic one. These
two different lithologies may indicate a significant change
in susceptibility, which will cause a change in the charact
er of anomalies produced.
The lineations described above, may just as well be in
terpreted as a contact between basement rocks of differing
lithologies and susceptibilities. In Figure 13, possible
lithologic regions are shown that may account for the anom
aly lineations and the change in appearance of the anomaly
fields.
6. 0 CONCLUSIONS AND· RECOMMENDAT·IONS
The magnetic anomaly map of Coshocton County, Ohio is com
plicated. Two qualitative interpretations of the area are:
1.) Observed variations are due to basement faulting, or
26
2.) Observed variations are due to susceptibility and
remanence contrasts between lithologic units.
Further studies could better determine the nature of the
body producing the anomalies. Three further analyses of the
data that could increase the amount of processable information
are:
1.) Reduction to the Pole
2.) Frequency Filtering
3.) Upward Continuation
Reduction to the pole procedures makes it possible to
determine, from the observed total field, the position and
depth of the pole that has a magnetic effect equivalent to
that of an extended source with inclined magnetization.
(Dobrin, 1976) This technique involves separating the field
into its symmetric and antisymmetric parts and can be imple
mented through the use of algorithms written just for this
purpose.
Frequency filtering and upward continuation both re9ult in
smoothing of the resulti.ng magnetic contours. Upward contin
uation is sometimes used to simplify the appearance of magnetic
maps, by suppressing local features. Frequency filtering re
moves undesired signals (noise) from the area, leaving primary
frequencies, which are important in interpreting. These are
also easily implemented by computer programs.
27
REFERENCES
Barringer Research Limited, Operation Manual, Ground Magnetometer Model GM-122, Toronto, Canada, 10 pp.
Berger, G. w., York, D. and Dunlop, D. J., 1979, Calibration of Grenvillian paleopoles by 4UA/39Ar dating. Nature 277, pp. 46-48.
Dobrin, M., 1976, Geophysical Prospecting, New York, McGrawHill, pp. 509-512.
Henkel, H., Guzman, M., Magnetic features of fracture zones. Geoexploration 15, 1977, pp. 173-181.
Jacob, J. A., "The Earth's Core and Geomagnetism", The Macmillan Company, pp. 45-48, 1963.
Janssens, A., 1973, Stratigraphy of the Cambrian and lower Ordovician rocks of Ohio. Ohio Geel. Surv. Bull. 64, pp. 197.
Landorn, R. A., Geology of Coshocton County. Geel. Soc. of Amer. Bull., 1954, pp. 10-12.
Lidiak, E.G., Marvin, R. F., Thomas, H. H., and Bass, M. N., 1966, Geochronology of the Midcontinent Region, United States: No. 4 eastern area. Jour. of Geophy. Res., v. 71, no. 12, pp. 1427-1448.
Nettleton, L. L., "Geophysical Prospecting for Oil", McGrawHill. New York, 1976.
Noltimier, H. C., Paleomagnetism Seminar notes: G&M 820, The Ohio State University, 1984.
Rowan, D. J., Personal Communication- Gravity Survey of Coshocton County, The Ohio State University, 1984.
Surface II Graphics, Manual, Kansas State Geological Survey, 1976, 250 pp.
von Frese, R. R. B., Personal Communication-Future publication of Ohio aeromagnetic maps by O.G.s and u.s.G.s., The Ohio State University, 1984
28
Zeitz, I., King, E. R., Geddes, w., and Lidiak, E.G., 1966, Crustal Study of a continental strip from the Atlantic Ocean to the Rocky Mountains. Geol. Soc. Amer. Bull., v. 77, no. 12, pp. 1045-1048.
29
APPENDICES
30
APPENDIX 1: MAGNETOMETER SPECIFICATIONS
SPEC I Ff CATIONS
Range:
Accuracy:
Sensitivity:
Gradient Tolerance:
P<Mer:
P<.Mer Consumption:
Polarizing Power:
Number of Readings with 1 Battery Set:
Frequency of Readings-:
Controls:
• Output:
Indicators:
31
20,000 to 99,999 in 12 ranges
± 1 y through operating temperature range
1 y
600 y/ft.
12 "O" ce 1 Js
< 50 Joules (Wsec) per reading
0.8 ~@ 13.5 V for 1.5 sec. (3 second cycle}
0.8 A @ 13.5 V for 3 sec. (6 second cycle}
2,000 - 10,000 depending on type of batteries
1 every 3 seconds 1 every 6 seconds
Pushbutton switch Range Selection switch - Slide switch for 3 and 6 sec. located on P/C Board
5 digit incandescent filament readout
LED point Lock Indicator - last three digits of the display blanked off when phaselock not achieved Segment Function Indicator - all segments light up to permit visual inspection of the display function
..
APPENDIX ~: PROGRAM GEOMAG
with
1980 IGRF coefficients
32
1. 2. 3. 4. 5. 6. 7. 8. 9.
10. 11. 12. 13. 14. 15. 16. 17. 18. 19. 20. 21. 22. 23. 24. 25. 26. 27. 28. 29. 30. 31. 32. 33. 34. 35. 36. 37. 38. 39. 40. 41. 42. 43. 44. 45. 46. 47. 48. 49. 50. 51. 52. 53. 54. 55. 56. 57. 58. 59.
// JOB /*JOBPARM LINES=2000 // EXEC PLOTV //GO.SOURCE DD * c
33
c c c c c c c
THIS PROGRAM CALCULATES THE IGRF FIELD AT ANY POINT, USING THE MOST RECENT IGRF COEFFICIENTS (1980>. IT ALSO CALCULATES THE DIFFERENCE BETWEEN THE MEASURED FIELD AND THE IGRF <DIFF> AND THE DECLINATION CDEC> AND INCLINATION CINC> OF THE FIELD AT THE POINT.
c c
IMPLICIT REAL*BCA-H,O-Z> REAL*8 INCC50>,DECC50) ELV=0 LL= 1 CALL FIELDG C0.,0.,0.,0.,18,LL,Ql,Q2,Q.3,Q4) DO 10 I= 1 , 322 READ (5,90> YEAR,APHl,ATHETA,Ft CALL FIELDG <ATHETA,APHI,ELV,YEAR,50,LL,X,Y,Z,FF> H=DSQRTCX**2+Y**2> INCCJ>=DATAN<Z,H> DECCJ>=DATANCY,X> PI=4.00*ATAN<t.00)/180.00 INC< J) =INC< J) /PI DECCJ>=DECCJ)/PI DIFF=Ft-FF WRITE <6,91) YEAR,APHI,ATHETA,Fl,FF,DIFF,INC<J>,DEC<J>
10 CONTINUE 90 FORMAT <2X,F7.2,1X,F8.4,2X,F7.4,2X,F7.1) 91 FORMAT <2X,F7.2,1X,F8.4,2X,F7.4,3C2X,F7.1),2(5X,F7.4>>
STOP END
SUBROUTINE FIELDG <DLAT,DLONG,ALT,TM,NMX,L,X,Y,Z,F>
c *************************************************************** C FOR DOCUMENTATION OF THIS SUBROUTINE AND SUBROUTINE FIELD SEE C NATIONAL SPACE SCIENCE DATA CENTER*S PUBLICATION C **COMPUTATION OF THE MAIN GEOMAGNETIC FIELD C FROM SPHERICAL HARMONIC EXPANSIONS** C DATA USERS' NOTE, NSSDC 68-11, MAY 1968 C GODDARD SPACE FLIGHT CENTER, GREENBELT, MD. c *************************************************************** c C DLAT ** LATITUDE IN DEGREES POSITIVE NORTH C DLONG ** LONGITUDE IN DEGREES POSITIVE EAST C ALT ** ELEVATION IN KM <POSITIVE ABOVE, NEGATIVE BELOW C EARTH'S SURFACE> C TM ** EPOCH IN YEARS C NMX ** SET TO INTEGER GREATER THAN DEGREE OF EXPANSION C L ** SET TO 1 ON INITIAL DUMMY CALL, SET TO 0 ON SUBSEQUENT C CALLS c C SUBROUTINE RETURNS GEOMAGNETIC FIELD DIRECTIONS <X,Y,Z>, POSI-C TIVE NORTH, EAST AND DOWN, RESPECTIVELY, AND MAGNITUDE OF TOTAL C FIELD, F---ALL VALUES ARE IN GAMMAS c c
60. 61. 62. 63. 64. 65. 66. 67. 68. 69. 70. 71. 72. 73. 74. 75. 76. 77. 78. 79. 80. 81. 82. 83. 84. 85. 86. 87. 88. 89. 90. 91. 92. 93. 94. 95. 96. 97. 98. 99.
100. UH. 102. 103. 104. 105. 106. 107. 108. 109. 110. 111. 112. 113. 114. 115. 116. 117. 118. 119.
c c
c
EQUIVALENCE <SHMITC1,1>,TGC1,1>> COMMON /NASA/ TG< 18, 18) COMMON /FLDCOM/ ST,CT,SPH,CPH,R,NMAX,BT,BP,BR,B
34
DIMENSION GC18,18), GTC18,18), SHMITC18,18), AIDC11), GTTC18,18) DATA A/0./
TLAST=0.0
IFCA.EQ.6378.16) IF<L> 210,100,110
A=6378. 16 FLAT=l.-1./298.25 A2=A**2 A4=A**4 B2=<A*FLAT>**2 A2B2=A2*<1.-FLA1'**2> A4B4=A4*Cl.-FLAT**4> IF CL> 160,160,110
100 IF <TM-TLAST> 190,210,190 110 READ <3,260) J,K,TZERO,CAIDCI>,I=l,11)
L=0 WRITE (6,270) J,K,TZERO,<AID<I>,I=l,11) MAXN=0 TE.MP=0.
120 READ <3,280> N,M,GNM,HNM,GTNM,HTNM,GTTNM,HTTNM IF <N.LE.0> GO TO 130 MAXN=<MAX0<N,MAXN>> GCN,M>=GNM GTCN,M>=GTNM GTTCN,M>=GTTNM TE.MP=AMAXl<TE.MP,ABSCGTNM>> IF CM.EQ.l) GO TO 120 GC M- 1 , N> = HNM GT< M-1, N> =HTNM GTT<M-1,N>=HTTNM GO TO 120
130 WRITE <6,290> DO 150 N=2,MAXN DO 150 M=l,N
MI=M-1 IF <M.EQ.l) GO TO 140 WRITE < 6, 300) N,M, G< N, M> ,GCMI, N>, GTC N ,M> ,GTC111 ,1'0, GTTCN ,M> ,GTTC
1 Ml ,N> GO TO 150
140 WRITE C6,310) N,M,GCN,M>,GTCN,M>,GTT<N,M> 150 CONTINUE
WRITE C6,320> IF <TE.MP.EQ.0.) L=-1
160 IF CK.NE.0> GO TO 190 SHMIT< 1, 1) =-1. DO 170 N=2,MAXN
SHMIT<N,1>=SHMITCN-1,l)*FLOATC2*N-3)/FLOATCN-1> SHMIT< 1,N> =0. JJ=2
DO 170 M=2,N SHMIT<N,M>=SHMITCN,M-l>*SQRT<FLOATCCN-M+l)*JJ)/FLOATCN+M-2>> SHMIT<M-1,N>=SHMITCN,M>
170 JJ=l DO 180 N=2,MAXN DO 180 M=l,N
35
120. G< N, l'I> =G< N, n> *SHPIIT< N, n> 121. GT<N,M>=GT<N,l'l>*SllMITCN,n> 122. GTTCN,M>=GTT<N,M>*SllMITCN,n> 123. IF CM.EQ.1) GO TO 180 124. G(M-1,N>=G<M-1,N>*SllMIT<M-1,N> 125. GT<M-1,N>=GT<M-1,N>*SllMIT<M-1,N) 126. GTT<M-1,N>=GTT<M-1,N>*SllMIT<M-1,N> 127. 180 CONTINUE 128. 190 T=TM-TZERO 129. DO 200 N=l,MAXN 130. DO 200 M= 1,N 131. TG<N,M>=G<N,M>+T*CGT<N,n>+GTTCN,M>*T> 132. IF <M.EQ.1) GO TO 200 133. TG<M-1,N>=G<M-1,N>+T*<GT<M-1,N>+GTT<M-1,N)*T> 134. 200 CONTINUE 135. TLAST=TM 136. 210 DLATR=DLAT/57.2957795 137. SINLA=SIN<DLATR> 138. RLONG=DLONG/57.2957795 139. CPH=COS<RLONG> 140. SPH=SIN<RLONG> 141. IF (J.EQ.0) GO TO 220 142. R=ALT+6371.0 143. CT=SINLA 144. GO TO 230 145. 220 SINLA2=SINLA**2 146. COSLA2=1.-SINLA2 147. DEN2=A2-A2B2*SINLA2 148. DEN=SQRTCDEN2> 149. FAC=C<<ALT*DEN>+A2)/(CALT*DEN>+B2>>**2 150. CT=SINLA/SQRTCFAC*COSLA2+SINLA2> 151. R=SQRTCALT*<ALT+2.*DEN>+<A4-A4B4*SINLA2)/DEN2> 152. 230 ST=SQRT(l.-CT**2> 153. NMAX=MIN0CNMX,MAXN> 154. c 155. CALL FIELD 156. c 157. Y=BP 158. F=B 159. IF (J) 240,250,240 160. 240 X=-BT 161. Z=-BR 162. RETURN 163. c 164. C TRANSFORMS FIELD TO GEODETIC DIRECTIONS 165. c 166. 250 SIND=SINLA*ST-SQRT<COSLA2>*CT 167. COSD=SQRT(l.0-SIND**2> 168. X=-BT*COSD-BR*SIND 169. Z=BT*SIND-BR*COSD 170. RETURN 171. c 172. 260 FORMAT <2Il,1X,F6.l,10A6,A3> 173. 270 FORMAT <213,5X,6HEPOCH ,F7.l,5Xl0A6,A3> 174. 280 FORMAT C213,6Fll.4) 175. 290 FORMAT C6H0 N M,6X,1HG,10X,1HH,9X,2HGT,9X,2HHT,8X,3HGTT8X,3HHTT// 176. l> 177. 300 FORMAT C213,6Fll.4> 178. 310 FORMAT C213,Fll.4, 11X,Fll.4, 11XF11.4> 179. 320 FORMAT (///)
36
180. c 181. END 182. SUBROUTINE FIELD 183. COMMON /NASA/ GC 18. 18) 184. COMMON /FLDCOM/ ST.CT.SPH,CPH,R,NMAX,BT,BP,BR,B 185. DIMENSION P<18,18>. DP<18,18), CONST<lB.18>, SP<l8>, CP<18), FN<l8 186. 1) , FM< 18) 187. DATA P<l,1)/0,/ 188. IF <P<l,l).EQ.1.0) GO TO 120 189. PC 1, 1) = 1. 190. DP<l,1)=0. 19 1 . SP C 1) = 0. 192. CPCl)=l. 193. DO 110 N=2,18 194. FN<N>=N 195. DO 110 M= 1 , N 196. FM< M> =M-1 197. 110 CONSTCN,M>=FLOAT<<N-2)**2-<M-1)**2)/FLOAT<<2*N-3)*<2*N-5)) 198. 120 SPC2)=SPH 199. CP<2>=CPH 200. DO 130 M=3,NMAX 201. SP<M>=SP<2>*CP<M-l>+CP<2>*SP<M-l) 202. 130 CP<M>=CP<2>*CP<M-1>-SP<2>*SP<M-l) 203. AOR=6371.0/R 204. AR=AOR**2 205. BT=0. 206. BP=0. 207. BR=0. 208. DO 190 N=2,NMAX 209. AR=AOR*AR 210. DO 190 M=l,N 211. IF CN-M> 150.140,150 212. 140 PCN,N>=ST*PCN-1,N-l> 213. DPCN,N>=ST*DP<N-1,N-l>+CT*P<N-1.N-1> 214. GO TO 160 215. 150 PCN,M>=CT*PCN-1,M>-CONSTCN,M>*P<N-2,M> 216. DPCN,M>=CT*DPCN-l,M>-ST*P<N-l,M>-CONST<N.M>*DP<N-2,M> 217. 160 PAR=PCN,M>*AR 218. IF <M.EQ.l) GO TO 170 219. TEI1P=GCN,M>*CP<M>+G<M-l,N>*SP<M> 220. BP=BP-< GC N, M> *SP< M>-G< M-1, N> *CP< M> >*FMC M) *PAR 221. GO TO 180 222. 170 TEI1P=G< N, M> *CP< M> 223. BP=BP-CGCN,M>*SPCM>>*FM<M>*PAR 224. 180 BT=BT+TEMP*DPCN,M>*AR 225. 190 BR=BR-TEMP*FN<N>*PAR 226. BP=BP/ST 227. B=SQRTCBT*BT+BP*BP+BR*BR> 228. RETURN 229. c 230. END
' 8 8 N M
EPOCH 1980. 0 G H
2 1-29988.0000 2 2 -1957.0~00· 5606.0000 3 1 - 1997·. 0000 3 2 3028.0000 -2129.0000 3 3 1662.0000 -199.0000 4 l 1279.0.000 4 2 -2181 • 0000 -335.80G0 4 3 1251.0000 271.0000 4 4 833.0000 -252.0G00 .. 5 1 938.0000 5 2 783.0009 212.8000 .5 3 398.0000 -257.0000 5 4 . -419.0000 53.0000 5 5 199.G000 -298.0000 6 1 -219.0000 6 2 357.0000 46.0000 6 3 261.0000 149.0000 6 4 -74.0000 -150.00®0 6 5 -162.0000 -78.0000 6 6 -~8.00®0 92.0000 7 1 49.0000 7 2 65.0000 -15.0000 7 3 42.0000 93.0000 7 4 -192.0000 71.0®00 7 5 4.0G00 -43.()000 7 6 14.0®00 -2.0®®0 7 7 -1€>3.0000 17.0000 8 1 70.0®00 8 2 -59.0009 -83.0000 8 3 2.0000 -28.0000 8 4 20.0000 -5.0000 8 5 -13.00®0 16.0000 8 .. ,6 1.0000 18.0000 a· 7 11.0000 -23.0@00 8 8 -2.00®0 -10.0000 9 1 20.0000 9 2 7.GGGG 7.GG00 9 3 1.0000 -18.0000 9 4 -11.0®®0 4.0000 9 5 -7.0000 -22.00®@ 9 6 4.GG00 9.0000 9 7 3.G0~0 16.0®®0 9 8 7.0000 -13.0000 9 9 -1.0000 -15.0000
10 1 6.0000 10 2 11.0000 -21.0000 10 3 2.0000 16.0000 10 4 -12.0@00 9.0000 10 5 9.0009 -5.0©00 rn 6 -3.0G®0 -7.0000 rn 7 -1.0®®0 9.0GG0 10 8 7.0000 rn.0000 10 9 1.000~ -6.0009 10 rn -5.0000 2.0000 11 1 -3.0000 11 2 -4.00®9 1.0000 11 3 2.0()00 1.0000 11 4 -5.0000 2.0000 11 5 -2.0000 5.0~@0 11 6 5.0000 -4.GGGO 11 7 3.G©00 -1.0090 11 8 1. 0000 -2.0@00 11 9 2.®G0® 4.0000 11 lG 3.0~00 -1.0000 11 11 -5.0000 -6.0000
GT
22.4008 11.3008
-18.3000 3.2800 7.0000 0.0
-6.5000 -8.7000
1.0000 : ·. -1.4000
-1.4000 -8.2000 -1.8000 -5.0000 1.50~0 0.4000
-0.8000 -3.3080
1.3000 1.4000 0.4800 0.0 3.-4000 0.8000 8.8060 8.3000
-8. 1000 -1.0000 -0.8000
0.4e00 0.5000 1.6000 e. 1000 8. 1000 0.0 0.8000
-0.2000 -0.3000 0.3000
-0.8000 -0.2000
0.7000 -0.3000
1.2000 e.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.8 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0
19 BT
-15.9008
-12.7808 -25.2000
8.2008 2.7000
-7.9000
4.6808 1.6000 2.9008 8.4000
1.8008 -8.4800 8.0 1.4000 2. 1000
-8.5000 -l.4000 e.e
-1.6000 8.5008 0.0
-0.4000 0.4000 0.2000 l.4000
-0.5000 -0.1000
l.1800
-0.1000 -0.7000 e.0
-8.8000 8.2000 0.2000
-1.1000 9.8000
8.0 0.8 8.0 8.0 e.0 0.e 8.0 0.0 8.0
0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 8.0
37 IGR COEF CIEB
GTl' KIT
••• 0.0 0.0 8. 0 8.0 e.e 8.8 e.e e.0 e.e 8.8 8.8 8.0 8.0 8.0 8.0 8.8 8.8 e.e 8.0 ••• 8.8 8.8 ••• 8.8 8.8 8.8 8.8 8.8 ••• 8.0 8.0 8.0 8.8 e.0 0.8 8.0 e.e 8.0 0.0 e. 8 e.e ••• 0.e 8.0 8.0 e.0 8.e e.8 e.e ••• 8.0 e.8 e.e 0.e 8.0 8.e 8.8 8.8 8.0 e.0 e.e 0.e 8.0 t>.0 e.e e.0 8.8 8.8 8.0 8.0 8.0 0.0 e.0 8.0 0.0 8.0 8.0 8.0 e.0 0.0 0.0 0.e 0.0 8.0
••• 8.0 8.8 0.e e.0 0.8 0.0 0.0 0.0 8.0 8.0 0.0 0.0 0.0 0.0 8.0 8.0 0.0 0.0 8.0 0.0 8.0 6.0 e.8 8.0 8.0 8.0 8.0 0.0 8.o 8.0 8.0 8.0 f).0 0.0
38
APPENDIX 3: DATA TABLES
DA
TE
TIM
E l..O
NOIT
UDE
LATI
TUD
E FI
ELD
IC
RF
RF.S
IDU
AL
INC
DEC
AU
GU
ST
21
1
8.8
3
-81
.80
46
4
9.1
98
7
56
26
8.9
5
62
24
. l
SS
.9
69
.82
08
-5
~526
2 A
UG
UST
2
1
19
.99
-8
1. 8
16
5
49
.23
96
5
61
86
.2
56
24
3.9
-5
7.7
6
9. 8
51
5
-5.5
30
2
AU
GU
ST
21
1
9.0
8
-81
.81
53
4
0.2
38
9
56
20
8.2
5
62
47
.4
-39
.2
69
.85
72
-5
.53
41
A
UG
UST
2
1
19
.23
-8
1.8
03
1
40
.23
39
5
62
12
.4
56
24
4.2
. -
31
.8
69
.85
36
-5
.54
35
A
UG
UST
2
1
19
.42
-8
1.7
99
3
40
.23
96
5
62
84
.5
56
24
6.7
3
7.8
6
9.8
58
3
-5.5
49
0
AU
GU
ST
21
1
9.4
8
-81
.80
71
4
0.2
41
3
56
24
6.3
5
62
48
.2
-1.9
6
9.8
59
5
-5.5
42
6
AU
GU
ST
21
1
9.6
2
-81
.81
59
4
0.2
46
3
56
24
1.5
5
62
51
.3
-9.8
6
9.8
63
6
-5.5
37
4
AU
GU
ST
21
1
9.7
5
-81
.81
69
4
0.2
51
3
56
19
7.l
5
62
53
.8
.-5
6. 7
6
9.8
67
6
-5.5
37
5
AU
GU
ST
21
2
0.0
0
-81
.82
99
4
0.2
43
5
56
20
6.7
5
62
51
.2
-44
.5
69
.86
18
-5
.52
30
AU
GU
ST
22
1
4.5
0
-81
.78
55
4
0.1
71
3
56
19
1.4
5
62
13
.3
-21
.9
69
.80
44
.::
0. 5g6~-·
AU
GU
ST
22
1
4.5
7
-81
.78
85
4
0.
16
89
3
62
16
.4
56
21
1. 4
5
.0
69
.80
19
-5
.53
38
A
UG
UST
2
2
1-4
.83
-8
1. 7
98
0
40
. 1
54
7
56
15
7.3
5
62
05
.5
-48
.2
69
.79
10
-5
.52
01
A
UG
UST
2
2
11
5.0
0
-81
.83
91
4
0.1
87
6
56
19
4.4
5
62
24
.7
-30
.3
69
.81
78
-5
.49
54
A
UG
UST
2
2
15
. 1
2
-81
.84
38
4
9.
19
43
5
62
29
.9
66
22
8.1
l.
8
69
.82
32
-5
.49
43
A
UG
UST
2
2
15
.40
-8
1.8
44
1
40
. 1
99
7
56
14
6.8
6
62
30
.9
-84
.1
69
.82
74
-5
.49
54
A
UG
UST
2
2
16
.50
-8
1.8
43
0
40
.20
38
5
61
98
.2
56
23
2.7
-3
4.5
6
9.8
30
5
-5.4
97
8
AU
GU
ST
22
1
5.6
2
-81
.83
10
4
0.2
09
9
56
23
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