MICHIGAN STATE UNIVERSITY

EAST LANSING, :{LILLIL'IAN

NOV 3 1961

 

 

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Hj

lasoic icicrxation can be built up as the sum
simple tensions or compressions along three mutually pa

> "1 .. O O . O I >. '
axes known as one rrirciple axes of strain. »inilerly t»

principle axes of stress.
coincifie. Denote tie principle axis as X; X"; and K:
on the X,exis yroduces one conycnent of nor Fl stress 3:!

o ’ ’ I
components of stra1n£~,£xz and g 13 .

to

no

ion or

L‘.
a.) one
sets of 3"s
4-1 a
omen a t-n31on

”‘1‘ I". W f“ ‘\r L:
,rcsc ”re rallt« if f ! r‘iecions

5'1; 3“ 5’” .- .5: 5.“ 5’”: —_<: 3., ,
J’

.-.4
V y

similarly ?or the ctr r two axes,

E 1/ : ~35": 6”” =_’.. 5}; El}: :- --..9: 5:2.

5';'1='___251J E;;:—-_§__j;1 €xJ=rL§xJ .
r r V

nrre t neions or congres ions,

’ A
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(‘f

51/, Sn; 3nd Y’J,
the strain generately nrofiuced ry each

.
. a.
fi'lr] 8Tb.

“ . m“ ’- 9‘ L: 4". 7* \ " *4
oenSIOn. - c reelluizj com.onenvs of str_

En =.A[.Yw -~ a-(Sn. +513):
V’

£1: 3—; C sz _ 6/51: (51.3))

62.3 =_.4[513 — (7(le 4 .51).),1

.LL ‘ . VJ, , .. a . 3
also bhe shear componenos KC] he extras.ed as

12m +_cZ£_xz_:._;_C_/7«£J.7n

Z ( /¥-a".2, 7x1.
91. Y

61/ 3‘ alng ': 2( 140') 7;: .
47X; (.976 }/

it
+.
t

 

(

'.».”;“:ere 71/ , 7‘12. and 7;: represent the ta“;'ff‘-‘T‘+l$l ‘7‘ "Cf

respective directions.

V" (ta .' ' -.».7 l1; . -' «7..

uOLZOflthMai “ending
' " 'z “ " 'L‘rw

ornation lead to a w.eo-—

reticel GFnroech to the Velec1tv of :lestic waves in lowinnted nedfn

L‘.;.1 v

.. .v. .' , '1, .J. ' 4. t. ' + J.‘ '1'. :~ 1 H ‘ ,t
by as “minfi t-e material to we in static CCHi l riam ane cr'oerfl to

. ‘- \ . 4 ~‘, YT?!” \ - | ‘ ‘ . q , ~ ~~, ’\ J. n. a . h‘ . (-
ccrtein sor'sces. lane stresses will i75.14.1«Marnte streins Slqll;r to

.2: . -. .v- +1. ‘ a o , z +‘—
tnose ganerettd in o»6 yes are oi an Oltft M,V~ t rolmn two would.

L

HI
0

"“E“ 'Jc'-‘“"7(’d “~’ 7 ”of ‘. “- 00’0“ "’1 b new 1'31": "3 f 70v“; "’1'. +‘. O ‘"
..l. I O.u's.l-«.h:... LJJ—LA 4' ...L: a . Av--Os‘t.-‘» CA ...C.4 ~A'] . (.2'1' '_vl \J O .L\oru‘-. L5. VJ" n“

I . f . . ‘ ‘r- ' -. ‘ * fl “ r‘ - V" -r\ q "I‘ "5‘ 1‘» '\ ’ .1"
wuose lflleldhul tlicinrs.us are pmgil COttered to tfie Wavelengt s

o ,’|J~I~-5-'.
1'6 . "two-v \ *an- 1" 1 1‘F‘5‘ Do lr\'r'\"" tvr"? 1 pv‘rvtlrc *‘v‘ r‘ ’. P-‘(\ 7"?- *‘PT‘L' r‘
1.4.0 18 ‘1' 1L" (.rvgkkt4 LCLL. .0: LthI‘ ‘1..>fj r'ILLV 3'.;\ 'C' ." . f1;le I] roll L -‘Ol-‘L- ,lC~)

e wav l nrrln n

, . a
- -~. Vt.) (A

control the projggation. amen t}

s...‘

"\ ‘ ‘\ :v‘ r~‘ ,N. ~-\
:.I%iAC}1 tx.€ (Tl.h:ny710rx:

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p:
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7',‘
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’3"

..A‘.

of the inzomszneitiee the velocity is ccyenflent on t“.

Pr: ++ V Vr-"‘j. .(j ,‘qr‘ 1‘nL{-\ (j I; 4" r '1 C' r,(‘<r~n] v." \1‘ 4".r '1 .— ‘V ‘.'A— 3‘11
CA 1Q. ak.u€I1h¢.'.-On 1»: (“-04. I" m. U 1.1 L O curl. Cw -' .‘iv ' i u --

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elV? n:e 18 stili e mi” tony T61 to the wevelrr) n

 

7.

—

 

 

 

 

 

 

 

 

xl Ta

c Q I. V. a 7"» ‘J- 0 K “1 ‘~, 0 r~ V’o ‘ r, I’i “‘0
rjrwre l. a T@,T‘F(JEEVIVC cno~ in e lwninet.d Ktfiia.

-. ‘_°. '! ,
Lox re: ional .;v S

rn1_ '1} _ l _ _ 4 . ‘ __ _ o _ _. . 1 » A _ _7 r 7 o , l ,
. 1‘ (W3 . in, 3 (~ A.“ ,'i2‘ v ‘ .‘ , _‘ 15‘ Y“ I:- . ‘Y‘ ,
.10 ‘. Lb. i-“ «.3 C(..r’148 (Ar:~..«un- :. n..r1 q (Lam—1.13.”? CID“ ‘ J. 7L: 1 3:18 L]: V(

Ext : 0 6n. :o 860 9,1: ‘0 96””)? "

Toe stress-strnin relationships in noteriel A of the meflium comr “rd
of raterials A ens E are
(x/:_/.[J}/ aa-(S‘u 431:).78 0
.V
{:4 :_4L 5:). -0‘f5'au 4 5:3): :2 0
}’
(1.3,..4 L 51.: -0“‘(5‘u +5339} .
Tenf:ntisl rtrrsres arr zero. llimination of-Y}I 5rd .5}: ‘Jill
give the r L°Flfifi~rlp betvean Stress on" "bf'lfi e)1sLLn* in an" ls r

-. "“.: . ,. T," ‘- “-..—.J ‘ -. ‘3: , ‘L‘ . ‘+ ' f‘ - ‘
A. his may he accom.l35nec og asllng one e’unoions "or £31 an? 6};
I - J

so 51! - ESfl +_.Lu_ ——~ 0.512 _ gG‘Sg :0
Y r y V V

rsgrouping

1; L Sui/(l—a‘) + fuzfl—a") - £02713 :0

._[(Ln +.S‘xz.)C/-a") ... 275x33

V

.S‘u +512. : ZO‘J‘IJ '
/—-6‘

Substitution of this value of' 51/ end ,5}; in the efiur'rtion for 6;;

produces

61:: 37/.[5’3 -C_ iij")]

vflich reduces to the formula

(is =4 .51 .- .S‘u
(1-?) 5J- a--20-' ff;

Whore Cl is the vrloci fr of COIH‘I‘LCiil ioncl 3-: river in A and P is e

 

 

1“ ~_ 0‘ l--. “ ‘fi '1 c :_ ‘rfi
,qn_;e in oF1c2nreo of a inytr is buy e} .e L

1 I 1 N 0

union it is Civided into levers. iriler stern cen be on lied to layer F.

(TY- r‘ r~ o o _-_ if . 1f. 0 _.I_ W v. ‘ . ‘ o 4 ‘ o 1 a 0
ine 3v rifle strrin 1n lie Clue 18 one onenre in tnicxnese oi
W ' fl ,‘ ' ‘ 1w 1* r- -: ‘I : w ‘- ‘ r‘ V r. " . r‘ ’7 3 . . "I“ 7‘
materiel h 3143 tne CL nth in txl?fifl?&w of alteriul L iV1deu by the
o m _o v- TN~ 1. .1 >0 .1. a ’ . L1._ ‘ L o o $— " 1‘ 1 r ’3‘
cube dlmCflSlng. ly chLrnaoint txe ‘OToJOfl 0. one cute comiosan of

material A as Z0? and a corres:ondinj rennin? for‘5&3 the avererg

W

+. ‘ J» o . ‘_ I ~ 0 .' . 1 ’ " --x ‘ -
stress-strain TulfolOflFfilC may :0 :Nr299nteu :v

pth: one cube roves essentially as a unit, ell lay rs undergo tTC
- " 2 * '1“ rx ' ”t ' ‘ 1 \V ‘ . V . i r ’v‘h
same acceleration, and tne efftctlve OCASltj is tve total “use
' \ ~ Lb ~~A i no ° . l ' 4-“ L ,. r.
uiVided by the tOLal voll t. .ne eiiectivc elastic constent and one

L

D . ~ 7‘ . V’ V. \ 1 L2“ ' . \r‘ “-0- . ‘ ' I . r
QLfQCthQ C€L31tv 31613 on? exerSSion for FrOluiaulOfl V£l\CltV

1613.:(6723//?%caf’ 1/.Zép//HQJC:aJ-;>£R,3 = .Y>J' 1p2?z

C:

 

/ _
@3257 + 2%?){27184075Pcy .

v o rp ‘ a~ I“ . ~ ‘.‘ \r"ru.‘ . ‘1“ . VI" ‘
iorieontully -chfillny CCWzltaglOXul “eves
' w . V I“ ~. .~ q ~ rx ". “.-’ r . V“ ”xx." r‘tfi.
A COMUTCCSlOUQl waxe elOJ: X]: causes a :1: 1QC3LL;L an ch

is uniform in anv rlene prrpendiculer to XI: . Tmnce

I
I A

é;%;§£ ;:[l/ .=' :7 n$k§kz ‘éQXE 'r c> .

r‘ ‘ '. ‘1‘ ‘ t u A. . - - L W" J- . . J wv n 1“ ‘fi,
QHCFriu? stresses ere zero, enc cue to cont: nit; Oi nor el

’4

F4

, . ,- 1., ,, fl \ lr‘
streams, $114 .1 Yua = 53.3 . gr: can not be 7';I“O Icr te
above Con3itions. 7be WSPQntiel refuirrr:nt is that tic tbicine"; of

' 1-, ‘ a f: w. w- W ' . : m“
the cube in fine IaulrtCLICH co»: not c_eage. June ry»i;rcnznt 1~

I ' ‘ ' ,i - ' .- 4. ' z -' ,,“I ‘L ‘LL '. .
maintained if tnc thlquflluF in L?o’?‘&1 n ;s accomzunicc .v a bilflwlflg

. -' ~ ‘ . r -' 2“, '3 ’,vv. ' 1 ~1- _. +‘ 7‘:
1n T’Iflt'..3r.l.::.l V as a COHFO ‘ICHCC' Cf Cunt Juglnalt(} YIELHlI‘C. Of J ‘9 .‘f.

The condition for ZfTO avwrryc strain icl

27. a5,“ (W, + 273 Jam: 3/: : 0 .

l.‘

' C L O 0 - -7 _.
“ion? in oecfl, the stroer—etrrln rel: ions in metrrxel

6w :__/_. [51/ —C7:o(5.¢z I513): . 0
’[

6:: =—

512. -- 6'74 [S‘H ¢SJJJJ

em [5m .. C7. ( 5., +3.13)

:._/
)/ 9

Similar efuetione to lv to HStQlel P.

For horizontal trAVel, the stzeirxész is tie care in both
materials, but the normal stresses 5'va €.T1d51&13521‘0 different. Ty
defining an aVcrafe or effective stress as tne total force on the face

of the cube divided by the area of that face, the e??cctive strece in

terns of the two materials is
5'12. .: ”aft/1.4 f 7765.126 .

‘ . J- R ‘ ‘. -: g~ '< ' I" ,
The tnrce strene-strain relebions for met T'clfl a an-

3
J;
"1
L4
73
’2

, _ O 3 L _ A ’ _. i H ,"' : i
the efuetione for the av rere stra1n enc bhfi Lff“CELVQ SCIOE; Give 3

J

I?
:3

. .“‘~ “ 1 ‘ a ‘4? ' ‘I r '1‘: ‘ -r-s -r- 1+.L ,._
total of elqht inccpenccnt e<ugtione fIOfl h” ca sew n r1;xo1oi {

«7r. ‘ 4H .
*2 l . ...
'_‘e C filing

“1
..L

Sun; S‘s/a a 5:2.» .. 5125 J In J (km/47h 45' 96‘”: a]:

were eliminated. The resulting eruation gives a constant of rroror-

be eliminated. tics

tionalitv l6" ’.'»3 Fill 5‘. 217781? 5'8 S,“ {4 T17 5‘. tl7l'.:.i 371% L'l' . ”IT“, 7 ‘7- l : IT‘Q'”

P. A A .3 ‘ fl _.
e: an e°I< VLYC r.nr_lc *o '.‘3 Ur 2'0 lg” estrd "IJ‘TlTl. 7‘0 r?“:c—

 

 

 

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'7,o rewn s 51”? :r 1"‘;A‘ .\ ic 15*icu'}uow ;;1c xnxioc;:{r ragixu‘s

+2.. -‘7 - , w . o ,2 \V+._-.31 '1..-
Lyon one * ' icel :rcgur,:cr oi p.‘ lxer7HlLl *acxi7xis of the lexgnaz—
1 7' cu“ , :w, x - n . ..‘: ° " ‘V, -. \,
cc 'qlcfirirl. «:e v lrw7.t:re rrfi-cifrrece,:.zu: 3 Tfith)Cfl' file lewu'r=tefl
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vu-r- "D 117.1 ‘r‘nl' ‘ 7'1"\ “7“" z 4‘0 «- ~..- 3": ‘11 "V- lr-*-".Y\4 4‘0 J TV'r"]‘l‘ "
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1

r ' . "r '1‘ '. ‘ . ".t"1 p \ ‘\ 7» ~ . 7" o ‘ . -~~ -
Velocity TLVLOS w r: vericu -rom l to 2 end d(n91 : ‘hthS from to
I“
4.

T - y. \rl' .> f‘ (7". VI‘] . 'n ‘(1 ' rwr‘ .1 -: ,\ u- 4 q 12-. 7.: r;,\~r‘+ t 1 :: T‘ .

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L4

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K13 . --_\J x.‘

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u _ 7 .7 ’ -_o f‘?‘ P’.- "{""~\
Vivcn e votfie c, i for totn he’ie \vn“ ‘T, 1; by.

 

 

 

 

 

 

7740

Figure 2

The compressional wave velocity for waves traveling in the vertical
direction is plotted against the fraction of material A.- Also shown
is the effect of changing the density ratio between material A and
- material B while holding the velocity ratio between them constant.

 

 

 

 

 

04 0.5 0.1. 0.7 0.3 0.9 1.0

77»

Figure 3

’The compressional wave velocity for waves traveling in the horizontal
direction is plotted against the fraction of material A. Also shown
is the effect of changing the.density ratio between material A and

material B while holding the velocity ratio between them constant.

'T ‘ f‘l
j. 7\ ”‘n "
. D. t

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raqiifiw «‘i»p==~ or p~+rrwn 4L nv~+ : . .m-s - : +~ -
1-"- ‘9‘ J-~‘; \V ‘-'-¢~‘-‘ -—-L ‘ C~f‘ ’ k.) _‘.. 1.) _,‘, ..‘. V RE. ..I 130.. bf {215. ‘l. ' (I 1 t ,1 5‘ Vr‘p 01 _1f
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.7. '~‘ ‘r: . L~~ 0~ ,, \ *vr _, ai‘. —~ vw - D . ‘r‘ ‘ ' ‘ ‘
Lain OF maximum V61001o , onus b «as 1K? 39;? O; are prrcozrn: hy
4 '. L . 'J ..
p01.1"'Yi"“ '7 r 1‘ ‘P Yvw'r~°v - W f‘r- 7, t-t'np, ‘11» 41w P‘r‘“ r— ‘hr‘fio 1"" * i‘r .0 4*“:
L ‘..l_\)¥‘ J‘- — Q }C-,i U;‘l UL ...- 1.- 4-. ‘7‘ 1K1 ..L *J, “_,- _L ‘ A "JJLO AL‘). .Or'. LO"'~L. (1 4rd. 4‘ C — L . 6.

rock. an in ortcnt fart ir p'0"rd by fractures rcrpcnfiiculcr to .Kc

waAWé pa5fltV'icPLC1picot,133 b3vx;cccd {Hui N‘IJ "aVC‘EJNJuT \rllocitfi<%€ 5“

to th, troV'rsicg of the slowor Lciiuw. “his is cupccial‘y truc of air

filled fractures causcd by jointirg, clcsiag: or hco inc 113cc so arctic”.
-ne factors w;ich must be considcrcd in such a case er“ the vclocit‘

throujh the fluid: fil in: the voids (5:8 or liquid), the vciocity tnronr‘

the solid rock alone, the acoustic coupl'ng kitvccn the {Enid ani the
rock and the rcomctric structure of the rock.
Y'ncral Corposition

Host cryctcls Show prononnced v lfiCitfi ,nisotroyy ”1icn is
Icprnd:nt on toe axis along woich tie weararcficnto arc TL‘C. One of
the more cov:on minrrrlU '9 (J f" t are the Vrlccii" vericc from

11.

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flflCYpd in tQ;3 inver,irntion. fi*is iostrunrnt, whici is
dcsiwned brim rilv for stsllow scisnic studies, is well suited to this
tyre of investigrtion bee use tne entire unit can be easilv trrnssnortd

by t”0 men. It consists of the follow n” comfonents: Ceismonitcrs

wticn Chan 3e the verticr component of earth motion caused by an rxnlo-

sion or o r artificial disturbance into echtrical imrnlses which are

5 unit provides a

p.

transmitted by xepns of a cable to a test unit.

apid means for checking continuity in the vsrious connections and

m

ign nal leelzafe caused by t e groundi n; of non-insila ted connections

This unit also provides a means of eliminating through a QC be 1 nee

ny steady state signals inO‘ oucer 1n nto the geoplones or cabl<s by High

(‘0

tension ;OWcr transnission lines. The si*nal proceeds from *he tcst

unit to an ampliffing unit where it i made stronn enough to cause

In

galvcnonet r deflection. Tiny mirrors are attache d to th 0 meter novrrrnt
in suci a May that li:nt ravs are retlected from the mirrors onto r;oto-
graphic paper. At the same time a tiring motor with an at ached inter—
rupted di 1sc pas ing an independent ligh+ source is also cousin: lfrnt
rays every one bundretn of a second to be rnotocrapned on the sane
paper. ‘be en nd resilt is a pr—mri nent Cont inous record of crlvcn' etnr
deflections spaced by timing line..

The time break or snot instant “p ea.rs on the number six trace, in

a make and break form, that is, there 's a mlf c cle kick \.'hen the

current is app ied to the line or can by tne switch and one of orposita

l8

polarity when Jle on p ruptures. The initiation of the second break

1e seismic wave orisinates and is therefore used
for time calculations when dyna nite was sad. uhcn th e enerrv source
was not dy;%m1tc, the times were measured with reference to a given
timing line as described under the section on errors. “so tyéioal

records are snown in Figure 11 FE? 9l.

Errors Associs ted with Instrumentation

A a . 0 I 1 a I

a micrometer HlCTOSCIPP was uses in msP 1r 15 all moas1rcments
(measuring distances to the enclosing timing lines and trace break)
on the records. The horizontal scale on the microscope is divided
into 0.04 inch divisions. This 0.04 inches is broken down into one
hundred divisions on the associa d drum, nr11n" to ossible the reading
of distances on the records to 0.0004 inches. Cince the time interval
measured (0.01 second) covered, on the average, 0.14 inches a reading
of a given point on the record could be made to 0.000029 seconds
(0.14:0.01::0.COC4:X). In each detw m ination it was necessary to
measure the distance between the two timing lines and the instant of
arrival of energy, as shown in Figure A. nape 21 .

a 'L.

The condition for maximum error in making a pick would be obtained

if all three readints (the two timing lin sand the trace break) were

additive in the same direction, and would therefore be 0.00009 seconds.

In many instances the+ race brca k was not sharp enough to male 8 gizk
to the above soiuracy (Figure 4 trace 5 ), but from re, sated readings

of a large number of records it was concluded that the total error in
picking the instant of arrival and measuring the three necessary intrr—

Vals on any one trace did not exceed 0.0002 seconds.

20

For any one record all piers were mrasured relative to some

timing line. A minimum time of 0.01 seconds before the first break

}.

was 81h W3;'s c: oer.n for the re fch nce timing line. This nrecautione
measure insured an error les tlan O. 02. That is, th. minimum time
measured on any one record was at lCest 0.01 eeconde, so since the

time could be mcesw. (d by use of die ricroccopc of O. OOC2 seco. 63 the

k5
n3
’1
(r)
’73
:5
d
~ 3
...:
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O
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:0

no to he less than (. 0002/0 .Cl) X 130 nerce“t.

mcpooop i

Lg

 

 

 

The problem of d t raining ss isc ric v‘locitv v rietions with
respect to structural orientation cictated tnst v:riou. “(epicse legh
outs be uses. for any one structural orientatitn a l "trCOnrs were
placed in s curaifnc line at a constant spceecl int;rvcl. moucv Ir, this
:1 stacl tape was varied to suit
the ccniitions of the individual areas statics, the shot or enersv

L. (1
source was initiat d and the re or mil devrl pod. In areas where out:rops
wgre invcstifi'tcd tn: encrev source was slefige hem er blows wit

\4'!

foot of the first geonhone. For areas where the refractiné horizon was

buried, the princirle of rec M5} mity of ti.xe was applieC. That is,
the time reruired for a weve to trrvel a given path in one direction

would euual the tiie revuired for the wave to travel tie S'Tc lath in
the opnosite cirection. In order to apply this prinoi 1e tte flvnanie
was burieo at the end of the normal len: tn of s road aft r the first

.L

geopbone had been moved in half the distance t the second geophone.
1

After the record was taken tne same proceflure was aniliec to the enro—

site end of the s; end.

m on“. “-Tm'.'r:~*"i‘ *- fl Tr
f‘ ..l I. .u. ”‘ O

Lk“\JosLJ ‘uAllei I

&

The plot of time vs. distance provided a rapid and convenient

g

method of analyzing the seismograpn records. The slepe of all time-
distance lines was obtained by the method of least squares.

For records taken on outcrops the velocity is the reciprocal of
the slope of the line passing through the origin. For records taken
over buried formations, the reciprocal of tJQ slope of the line through
the origin gave the velocity of the first horizon. V3 and the recipro-

al of the slope of the second line gave the velocity of the second
horizon 90 . Where th‘ slope of the second line was not the same
when shooting from opposite ends of the geophone spread (Tigure 12
graph #1. page :fil), the true velocity of the underlying formation

was obtained from the following formulas which are derived in any tasio

geophysics book such as Dobrin, (1952).

ll: :K/ym L's
£1 :73. K I..." KMJ -5;n'/% m)

‘zmdis the slore of the down d’p seement
ififiais the slope of the up dip segment
These various factors are SJOWD in Figure .2 page lui.
In many instances several duplicate records were made. In each

CC.

U)

e a least sruarcs curve was determined and the values averaged to
enable the presentation of one curve for Eflch locality and shooting
orientation. The tabulated results of calculations can be found in

Table 1 page 26. Time distance curves are presented in the back.

22/,

 

 

 

 

 

 

 

777778
7‘ §Iope= smc ebb/,4,
” Deva—077:3
”rd/P" \ 93>mm@:+4>/v
//C’)"( ' :' / - r \
a; 0::0; / / '/ ~-_ Slam : J ”/J’ \ \47flf8fCP/0f z _
V C», / ‘4’ - ZzuCOS'IE.
0. —_VO
1 0/87?! Dcegx
T \ .\ 7T
/ \ I
/ \ \ /
I \ \ I
/ Dd \ / I
J ' ’2 \ ~L \l
' \L / . . 2“ pa
~fl 22‘ / o l
" ,5, ..I ‘8 I
[c "' a 7’ / I
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' v
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“- r- '— Q
’ v
‘I
Figure .5

Refraction along an interface dipping at an angle at. . Respective shots,

are at up'din and downdip ends of profile. ,

R”?ZL“S

A total of seven di ff Ierent localit ie comprising eight different
lithologies were studied. All out crors IJCTG laneller either in the
form of handing, fracturing, bedding or mineral orientroion. They
were snecificallv chosen for these prorerties. Once it had been esfiab-
lishcd that velocity anisotrogy of outcrops was determinable by field
investigations, the study was extended to areas covered by flaci'l
from fifteen to fif ty— fiv ve feet in depth. Areas of good

drill—hole coverage were chosen for these studi

(I)
F).

nee it was neces ary

to have a check on the results. ..e tabulated results of these studies

‘4

Area A

The outcrop is com osed of two different formations; the Goodrich

Quartz ite and the ieCaunee Iron Formation, and is located in the 931,
sec 16, $463, RQQW, RarCuett e Count",, near the town of Reuuhlic. ”he
iron formation grades from vertiéally dinning alternating bands of
specular hematite—magnetite and recrystalized chert with minor amounts
of epidote, chlorite, mag etite and silicates into a silicate iron
format ion comnosed of vertically dipping alternating haids of grunerite
and recrysta lizec chert with minor amounts of magnetite, chlorine,
cumminjtonite and epidotr. fivpical banding throughout the entire
outcrop is shown in Figure 6: page $F7. The chart bands generally rance

from one-tenth of one—ruarter of an inch wh'le those of the iron oxide

exhibit considerable variation (micron size to two iiches).

25

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let mflmuwtwtor mo mama. ecflww.pcwflw 4
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nr‘entini

C‘
L) »

weathered to

1 O

1‘ int

otogra.

In.
L A . l

:: ’)

;

he

Area

{"23 7.1 on .

I?
on -CI‘

Jaewmelr

‘

r‘, H
, T“.

‘._.~

Two lines were run rs rrllel to 'tr e tandins, one in the snecular

$

hematite-mafnetite and one in tne silicate iron formation. these gave
velocities of 13,673 fps and 17,970 fps respectively. An orientation

perpendicular to the banding which extended across the entire iron

formation was then run with a velocity of 13,200 fps in the silicet

(T)

iron formation and a velocity f 9,000 fps in the h ite—manetite.

J. r‘;

The time distance curves for bile area are shown in :igure /

page ILL. Two or tore were ta :n for each ori nta tirn. Ceophone

.'- .1..¢.,° ,. ~-
snaCin s of ten anc tdwn.y-f1ve feet Cave Similar velocc1ties.

A vertically tanned Corn 1 tife erous biotite anyhibclite schist

affroximately srventy feet long and fortv feot w'ide is loczted in the
SEQ, sec 1, TACK, R3 C‘N, Karruette County. This hirhly contorted scnist
whose stre tierC‘ic nosition is eitlor Ufi er Goodrich, Pdchiganne, or
Greenwood (Villar, unpublished), gave no distinct Vrlocity anisotro'V.
ten foot spaced seventy foot long Stread parallel to the scnistosity
resulted in a velocity of 7,330 fps, while a ten foot spaced forty foot
long syrFad perycndicular to the schistosity produced a velocity of

6,900 fgs. Dayli ate records wire taken in both direc ions. The time

distance Crab 5 for this area are snown in Fifnro :: pare Li;.

f‘J

-nis area is locetcc it [@033' longitude and 87923' latitude,

barfluette County, and is locally known as LiChthOIAC e loint. An
a rrorinatrlr v: rtic.s.lly dipping section of the Lona schist wss studied.

{he ana schist at this lOJation is a tasic, well banded, sreenstane

\ ‘ 0 — 'r~ ( "l. O m ‘ _ . . O J _‘ "I _: Y‘ _. ) {‘2
J0 mineral assemhla e is noetlv epicotu, c “lor.t:, hornLlenn,

V ‘ V . \ ‘ I O
plaCioclase and Luarts (Van line, 1911). Geopnone or1en a‘;1on parallel
to the banf in gutilizing a ten foot spacing with a spread length of
fifty feet :roduced a velocit v of 6,7 l f3s, while an orientation

length of twenty-five feet produced a velocity of 3,716 fns. The time

distance c; Awrv;s are shown in Figure 9 3ygxz 3b.

Pres ue Isle is located north of the City of Narquct e at 4<O3E'
longitude and 87 23' latitude. A large fla t oztcrop of peri<Wo i te
altered to serpentinitc lineated by weatherinC character ietic as shown
in Flé :ure (3 is exposed at the north—east side of the isle. A geopnone
orientation parallel to the lane lar orientation witn ten foot snacings
and s,r€ cad length of eighty feet produced a vrloci V of 13, :-C0 fns,

wriile a similar pczgrn31ic1lar orientation produced a v locitv of 9,C©0

fss. The time distw iCe gra , be are snown on page ~f7, Figure 10 .

Extensive outcrops of granite gneiss are expo osed alonC tne ro.ad
in the st, sec 10, T413, H303, “andville aacran nsle i01i§an-Wisconsin.

.ne gneissic banding is ess entia llv vertical, and a sixty foot snread

length with a ten foot spsCing parallel to tn Mk n ng Produced

0.)

Velocity of 10,204 fps,w mile a fiftv foot spread with a ten foot
spacing normal to the banding produced a velocity of t,: 00 fps. The

time distance grarhs are shown in 1 iglre ll.page 33 .

Fr]

Area

The area is located in tne fli- of NF; sec 8, [173, R263, Frrquette

Courty. Rap .1 gives a plan View of the location of the two geophone
orientations, and map .2 is a vertical cross section of the area.

The Grill—hole information rtwv ml fifty—five feet of glacial till
overlying horizontal beds of the Le~a inee Iron Formation. The geornones

were

U)

paced at twenty-five foot intervals with a total sprm ilength of

two hundren and fifty feet in both directions. lime distance sraths

f‘\
[1.168 .1

F1

: ' HM». ' -1. n 1+ 4. r- ,1 1 1
-1s arra 1s locacta s1X ranzzew fezt north 01 aru F as snown

{‘0

on man ;l. 1e combination 01 test nit infor1ation and time distance

curves on page 43 reveals ve-vt fcet of _ mcial till directlv over-
.iamo slace whicn 1s d1nr11q r‘outw r. at 40 . Three different
geophone orientation were used in an attempt to detect the velocity
change with lamellar orienta ticn. The orientations are shown on tsp Kl
with the first orientation parallel to the strike, the second rotated
clockwise thro.gh 450 and the tnird orientation perpcn ndicular to the

trike. The time distance graphs on rays 40 Figure 13 produce velocities

of 10,023 fps, 8,473 fps and 7,056 fps for the respective orientations.

A literature search revealed that velocity anisotropy with respect
to structure orientation has been observed by other aughor s Some of
.ies are presented telow.

}Rite 8: Songbusn, (1954) while working wi th angle and loose sand

ob.erved the t for shale the horizontal connressional velocities ortained

<

were 9,000 fps, the ert iczl corrrcs ,ional velocit1cs were 6, t0 1y3,

31

and in loose sand both vertical and horizontal comyressional velocit
were the same.

lugfies and Cross, (1951) conducting laboratory experiments with
argiliaceoas lixcstoncs from well cores, in which "the cores were cut
one peryendicular and one parallel to the Ledfing from very Closely
neightring yositions. The data shows a definite :nisotrory, with the
higher velocity parallel to the bediing." Perpendicular to the tending

L

1 o 0 j _ o (1 r~< o .
tne veloc1t1es at 27 C anfl 50 bars pressure 1s 1;,/33 fns 1ncreos1ng to

I
\J

2 ,252 fps at 5,000 bars pressure. For the srme concitions, the
velocity parallel to the bed ing starts at 19,776 fps and increases to

20, 892 fpSo

'.T.".1' T) ‘7')" 1“ [TNT “‘1 Ah
n ‘ - n1 r- y{ w u T"
.I .,. ' ..‘ r. t 54'.

AL,

‘T1
3
‘4’)

The results of the field survey provide conclusive evidence that
various forms of lineation cause v “lo i 3 anisotropv. The bendiny in
area A of irratite—r ghetite and recrystal ized chert along with the
banding of grunerite and recrvstalized chert yroduée a distinct velocity
anisotrony. The schistosity of the greenstone
and the slaty cleavage of the buried Siamo slate of area G where the

elocity ratio bet JGGD the orientation at 450 and 909 and the parallel
orientation was 7?f and 65% respectively, give anisotropic velocity
re miings. The gne cissic texture of the granite gnciss in area D and the
fracturing of the serpentinite in area D with the resultant weathering
.aracteristics produce velocity an niso otro.g. For area B whwre the
schist was highly contorted and no gross lamellar orientation observable,
velo citgr anis otroyy'was lacking. The absence of a break in the time
distance curves for area F where the FT :raunee Iron Formation is OVFTle in
by fifty—five feet of glacial till mav indicate tr e energv was not
being refractedu unwa rd or that the formations had similar acoustical
properties.

All of the above information gathered from the use of shallow

seismic refraction etuinnent shows that this method can be used to

detect velocity anisotropy which in turn may be used for delineating

orientation of buried structure.

32

f:at1r€s to try and dutcrxino

C€1t”TGs

fl T ‘ ’0 ‘ "1 " rr~v .0 r*
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le-(1 n,-U\_A_\_,-:1_“T‘J ‘ .L.. 4&11‘

c4-

,1" dipring la Tellar forratlons

ord r to ostnhlirh t“e lih{taLions

litholog‘ 3, degree of lamcllaro

between the comfrisinq hands.

laboratory st1‘ies on field so“

. ‘ a
nay save.

\A)
K.»

a the prevent

. --, 1 .‘L ~r.~. ‘ " "
ln¢fl sLuo1;s on OdoCFOVS to tTy

L‘,";'1j:7‘ f? '1 T'Y VT ‘1'
t 1

‘A L'_.

none for furtoer stufiv.

‘4' ’3- o ‘ v . . l
ELUJy 1n areas wn'r b1T16(

1

have food grill Hole covcr"qe in

\ ‘ t 1r 1
the neLaoo.

and correlate the VQICCitY ratio

’0‘!
L- -1.

C

:1;

qLion or d1 fioror L391 veloci-

tfng various laxellar

.4. <mm< to“. 114mm moz<._.w_o m2;

 

 

VA
/

  
 

.oom
0.0 0.0 Ca? 0% ON 0.. .
, \. :oo.
...... 28:5 2 __ - . . .
2: omm§u> 1 , \ imoo
,. \m._ 23:5 3 A. .moofi.
“.... 3:25: 2 : 2: oo~.m_...> .m
2: mhw§u> .voow.
.8
w... 2:95: 2 ... .moo
2: ooo.mu> -ooo.

 

 

m <mm< mom India woz<._.m_o m2;

 

 

 

Eon.
ON om on ow OM ON. 0. o
.. .. _.o o.
- - moo.
- \\+ -moo.
3.2 no... 239 on. . S
.. 2.: oom.mu> «woo a
- -moo.w
D.
. ..ooo.s
I 3:83. Loo.
2: ooo~u>
.. .moo.
.. mtzon. >:oo_m> Eton ux -moo.
. fisoa 3_oo_m> 3.323331 u . L05.

 

_ V=3,7l6 fps,
'00? Perpendicular ’

 
    
  

l
V=6,730 fps.
parallel l

Seconas

 

 

lo ‘ 20 ‘ 3b ‘ 4‘0 ‘ 570'
Feet
TIME DISTANCE GRAPH AREA C.

 

d <mm< mom In_<mo moz<._.m_o m:2_._.
3m...

 

37

 

Om Oh . om om CV on ON 0.

d d d d

 

. .oo.
.80.
189mm.
3:23 .¢oo.m
I D.
me 003:, 3322333 .moo.s
2: owed;
. .80.
.500.

.m <mm< In_<m0 moz<._.m_o m:2_._.

.omm
owl o‘n.o‘¢‘ oml 8‘ 2. o

q

 

.00.

{a
o
0.

3:923
3.: v8.0. u>

IO

0

0.
spuooes

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o

1 3.36532. .moo.
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x L

 

 

 

 

 

 

 

 

1W. Eu
V=6,|68 fps. v=e,402 fps.
.06 .
.05' ‘
“.04l
'2 ._
3-03l v=e,265
$.02
.Ol-
044‘05e‘o‘lz'o leo'zao‘zio
Feet
r . ” N.-
V= 5,745 fps. V =6,440 fps.
05’ +
”.04-
‘O
803- 1
3 - ‘_
(n.02l V-6,692 '
.Ol*
o ‘ 440 ‘ ab ’ Iéo ’ lea ‘ 2‘00‘ 240
Feet

TIME DISTANCE GRAPHS AREA F.

My. 5..
° V=9,2|4 fps. V=l2,460 fps
393'
S
g.02~ _
0) Va '05026
.0:-
0 4b 86 L lie .so A 260 ‘ 24o
V=8,750fps. v=e,I96 fps.
.04.- . , . 1
«8 .
=-°3' ,
302' ‘
55' Va 8,473
.0:-
0 4b 86 I230 C use A 260 ‘ 240
'3. F001 N.
=6,9l3 fps. v-7.200 fps. l
.04 .
.. .
3.03»
302
3' V=zoso
.0:-
0 46 ea :20 I60 ‘ 260 L 240
Feet
TIME DISTANCE GRAPHS AREA 6.

 

 

 

 

 

 

 

 

 

.lul’"llll§llsl|fllnu..ll l. I‘ll

 

 

PEFVrF"C’S CITCC

Dobrin, M.B., 1952, Introduction to geophysical p ospecting: Jew York:
kcGraw-Hill Bowk Company, Inc., 435 p.

Hughes, D.S. and Cross, J.d., 1951, Elastic wave velocities in rocks:
Geophysics, v. 16, p. 591.

Jaeger, J.C., 1956, Elasticity, fracture and Flow: New York: John Wiley
and Sons, Inc., p. 58.

Iaughton, A.S., 1957, Sound propagation in oc an sediments: Geophysics,
v. 22, p. 233-2600

Van Hise, 1911, Geology of the lake Superior region: V.S. Geological
Survey, Monograph 52, p. 254.

Villar, James, Preliminary report of the pe To ranhy and petrology of
the iron formation near Republic, lichi fin: Lichigen State Univ r-
sity, unpublished.

White and Angona, 1955, Elastic wave velocities in lay
Journal of the Acoustical Society of Av~rica v

inated media: The
27, p. 310—317.
ements in near

E.) v
V}
i; .

6.
surface formations: Geophysics, v. 16, n. 591.
“11119: GTCEOIY and Gardner, 1946, Factors affecting VleCity: Geophrsi"s,
v. 23, p. A79.

 

91'

 

 

 

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SW-SE — SEC 5~47-26 M/CH

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lNTER-STPVTE [RON CO,
NEGAUNEE PROPERTIES
SEC. 8- 47- 26 MICH.
CROSSSECTlON 3630-5

LOOKING WEST

 

 

 

 

 

 

 

 

 

5'CALE. l"=50' DATE.

 

 

 

 

 

 

 

 

 

 

 

 

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