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I gratefully ecanowledga my indebtedness to Dr. B. T.
Sandofur for his interest, encouragement, and critical
review of the manuscript.

I wish to oXpross my gratitude to Dr. C. u. Frouty
and Dr. J. 1. Fisher for their assistance during this
investigation.

I thank all tue members of use geology staff for
their helpful EJJQOBtIOJS with special tnuuka to Jane 1.
Smith for her interest in the stratigraphy phase.

The cosperution given by the members of the dicnigan
Geological Survey in helping select and furnish well

samples 18 also aggreciated.

11

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lt¥.l~2.~uit Co NLLU

"1'.-.\.l\'_'\ 5.‘ Ago”,
. '- v. , r" ,
’.‘h-U.Llltib‘

Tao tectonics. focios, and p31605005raphy or Bevonian
rocks in the Jichigan basin are not well known. This Itudy
of the sylvunia sandstone affords a good ooyortunity to
ovalaato older concaota roiativo to the additional infor-
mation presented.

Previous work on the Sylvaoia sandstone in flichigan
and Ohio is briefly roviewod, and some or the concepts or
other workers appear in the text.

The analysis of the Sylvania sandstone was partially
onegical uni partially mechanical. The results of the
analysis are presented as contour m pa which snow the dis~
tribition of he constituents in lower :lcnigao.

Tao data from the analysis and the known stratigraphy
and poleogoography were used to modify the goologioal
history on conceived by otmor writors.

The study showed the Sylvania sandstone to to marine
in origin. loo principle source area supplying the sand

was aoutuoeat of xichigan.

iii

It won difficult to name tho a;out roSyonaiblo for
curryiad tna Sylveais sand into the Syquuia sea; but,
noverthcleas, once the sand {on dogosited in the marine
sea, waves and currents woro most important in diatri-

butiug, roworaing, and sorting the anod.

1v

C" >~'~-"-“- - mm.
J4); do»);

13THDDUCTIQfi-ooo-ooooooocooo00000000000000.0000...
Purgoss of Study................................
Kati-WISHES 15353;...so.our"...oucossoooso‘oosooosoooooo
THY.....................................o
SE:ISI§‘~LIJ’PM:Z xii-Erikzii‘jfilgosooosoocoo-ossso-osososocooos
Purposo.........................................
Selection of iells and intorvala................
SyIVuuia Saudatouo..............................
LAAJJfi‘I:-:-.£ :"iiQCEZ-93$.no.eooosooocooounto-9000.000.
Eetaod of SfimplinéooosoooooosoosossosOosooooosso
fiomoval of Acid 3oloblo3........................
Removal of Clay and Silt........................
Separation of Chart and Sund....................
523E: K‘LYSISIOOOOOOOOOO0.0IOOOOOIOIOCOOOIOOIIOOQ.
Bievs Aunlysis..................................
Cumulative CUP?“ Analysis.......................
fihaps Analysis..................................
IRTEfi'fiET T133 0? TfiE DATA...................o..oo

Porcantage maps................................o

Conclusions drawn from,porcsntago maps...........

130p16tn flaps...”nu-on.......................

Conclusions drawn from Iaoylath maps............

TSiTCTQIIIC T315"; fir'ffi‘iz'i‘afifl 3'4" LITE: SIL" 2'iIA33I. . . . . . . . . . . . . . 53
GBDLO-SIC HIST? 5:13 034‘ Tiff» Elli-1131A. . . . . . . . . . . . . . . . o 514.
souftdl 3:333 CJ JECLUW I. 31:30 0 o s o u a o s o o o o s o s c s a o o s o o s 0 S7
BIEIaIJGRfiPinfs-oooocassava-concoosossoso-ocos-s... ()0

Vi

Tabxg

I.
II.
III.
IV.
V.

VI.

¥ in". 7 '3'
iéuuuua

nulls Used in Analysis.....................
Quantitative Analysis...........o..........
Quartile Calculations..........o.........o.
Data from Solve Andlysil...................
Statistical Measures.......................

Average houadnasa and Sphorloity...........

911

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031:4. 1.3-,“de {Il‘z I‘m‘"“;‘r'-L§’ J?
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1:: 24-33; 3mm“ E‘ASIL-‘i

Fuvpose of Study

'lhia study war a caniucted in as atte: ;)t to determine
the origin of the Sylvania sandsLone of the fiichigan haaiu.
1?;3 proclflms to be answered by an uzxaly sis of the SyIVunia
sandstone are: i) the deyositional environment or the aand~
atoua, 2) the type and location of the area aupplying tho
sediment, and 3) the 3&0103ical history as it can Do do—
duced from the crayosition, and pr :33 sic 91 properties of th
Sylvanin rocxa, 33* from the formations position relative
to other bad

Landon (1951) states that:

The 5: aaozal pruc tics of 300103iats in des-

czibin3 t:.a subuarfaco stratL grap.' .ic section

in too nicui3an Lasin botwuex $.10 Eundac for~

matiun aud tug 3333 Island and Selina forma-

tioaa is to refer to the ovaporite sequence

of roc3a wituin the Lutruiz mivur group as

tho "Detroit River" and the underlying car-

bonate rocks as tna "33133313 farmutioa"

will an ovUrlies tna "33133313 sandstone"

vuero present.

30 the reader will ngt become confused, L33 use of the

terms ":"lvaaia sen fiastone" or "33iVu;:.ia formation" in tnia

study is restricted to the sandy phage bounded above and
below by carbonntoa. This sandy phase in the "Syivunin

sandstone" referred to by Landon.

‘3'?! 1“" " " "‘5‘ “"1531"
tutu—no’u‘rJJQ 'ILJ.“‘

Tao origin and age of tho B3lvania smudatono have
been under discussion far many years. newterry (i370),
working in onio, correlated a white, 23 {oat bed of
sandstone. generally lacking in fossils with tho Oriakany
aanfiatono, the lowest mefibor of tho revonian in flow York.
This sanflstone was later namod Svlvagia t3 Eduard Orton
in 1333, State 390103i3t of Jhio. Graham and Sharzor
(1997) presented evidence for an eolinn origin of the
Sylvania sandstone. They 3903a of a new fauna of late
Siluric ago with Devonian affinities in higher beds.
snerzer and Grntuu (iaJG, pp.SAD-SSB) placed the Sylvania
in the Silurian ans abused that the strata contained
upger "Siluric" fauna with proceaaivo "Devonic" fonma,
and that the Sylvania 3&5 not the equivalent or the
Eovonian Driakany sandstone. German {1987, pp.h81~506)
canciuded tfiat the Sylvania was stratigraphiy and fa" -
ally so closely related to the overl3in3 Detroit River
group that wantever age is assigned to the Setroit Rivor
that the Sylvania sandstone ahouio go with it. an faunai
cvifienco. Carman concluded that the base of tho Sylvanin
was the bevonian—Siiurian s3stemic bouudry in Chio.

Stella w. Alty (1932, pp.239-330) studied the hogvy
mineral content of the Syivuaiu both subsurface and aur-

fuce in gichigan, as well as outcrops in Ohio. filty

h.

pointed out that at Sylvauia Ohio, a more varied suits
or heavy minerals existed, and that they wars slightly '
more plentiful than at the Hockwood and fittinor outcrops
n ;".Eic?'.'iga;1. German (1935;, pp.253-2.;~6) working in north-
western Ohio. felt that tho Sylvania represented tbs basal
member or the Detroit hive» group in a transgressivo ovar-
lap by the Sylvania sea to tho aouthoaat. He gave as
evidence tho fact that the fauna becomes younger to tho
south.

Enyort (1939). on tho basis or the heavy minerals.
concluded that the fiylvsnin was a wind-transported. wutarw
reworked sané, carried cast from the Wisconsin Highlands
into the Sylvaais sea. Landes (1951) bssod his conclusion
of a wind-blown origin for tho Sylvanis sandstone largely
on Fnyort'a study. Londea also propoasd that Sylvanis bs
asaignod to the lower-miodlo vovonisn sad that it should
be considered the basal member tho Amhsraburg formation.
Landon also states that it in the general oonnonnua of
most practicing geologists to consider tho Sylvania ss a
mar no sand having an origin similar to modern beach sad
barrio: aund, with currents selectively transporting the

sand to tan doposition site.

I {"1 LII'AA E'Fi

aha Sylva.aia sax .datonc has a liuoar pattern which
extends {rem tho southwest poz‘tlon o: “1ca33mu wall into
the northern half of tue lower peninsula Where it ends in
Roscommon County. This sandy unit thins quite rapidly
east and west and grades laterally into carboufites. Khare
ever the Sylvania can be identified it lies betweau cur-
bonates. Th Syltar.1a fsrmetion gradas upward with di-
minishing sand Contaat and ulthout a snarp break into tho
Amharstburg dolomita of the Detroit Eivar gang. The
Sylvanla is coasidered coaformaalo with the overlying
3mharatbu 3 farmation (Cm'n an, 1936, Landes et.al. 1945)
The coni‘or1cble rel atianshlp with the overls 133 .etro t
fiiver graup causad Landau (1751) to prepoae that ha
Sylva:;1n be co:1a; dared tha basal manber of tha Estroit
fiivar group. iho Sylvagia aaudstane is overlain by thn
Amherstburg formation, excagt 1n iillsdalo County where
the Lucas formation rests directly on tha Sylvania (Lamdea.
1951).

Thrau3’ bout mast of lower 53cuan‘4 t31a SflV£_1Lie rests
unconformably on the Lois Liane farmnt ion. To the east
and south, it overlaps the Sllu rlan Lass Island formation
(Landau, 1951). fiCCOPflin? t0 3. £- COCpur ot.ai. (19h2),

If this unconfornity is followed to its fartnast
limits or the icnilan i asiu province. the base
of tha "Sylvaaia” baagl sand wl 11 rise in the

column, this tar-out "Sylvnaia" sand is urobubly
to to fauna in t4@ Fangletuu of Indiana, he

5'

6

Rillaboro sandstone of southern Ohio. and the

Springvaio sandstone in the region around

Cayuga, Ontario.

In Ohio. whore the Sylvauia crap: out. it rests un-
conforaably on the Lass Island formation. German (1936)
atstod:

The contact surface has irregularities of only

a few inches with saidntono fitting closely

down over the irregularities. The contact in

sharp, thera is no sand in the dolomite below

tne contact. but above is a pure quartz sand-

atone. Further. the 883113130118 has oozmonly a

basal conglomerate, tho pebbloa of which war.

dorived from the underlying dolomite.

rue unconformaole roiationnhip or base or the Sylvania
is shown (Figure l) as it oxiata in lower micai3an. Ehlara
(l9h3), proposed the names Garden Island (Oriahany ago)
and 5313 Elana for the two formation. identified which
were found to be older than tho Sylvania. The Garden
Island and the 301. Blane have now boon incorporated in
the xichigan Stratigraghio Column. The nomenclaturo or

the michigan formation: appears in Figure 2.

SOUTHERN PENINSULA

OF
MICHIGAN
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0 Well L ocotions

Figure 2. ~ fiomunclature of Lichi;an For:rtiwns

 

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inderdon ls. fm.
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MICHIGAN
DEPARTMENT OF CONSERVATION

GEOLOGICAL SURVEY DIVISION
Figure 3.- Location of Wells used in Analysis

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ngu'lfi‘sb .456; fill! F451;.“ XI; *0.)

Eofore tna origin or a sedimentary unit can to aa-
cortsined, one has to cxyiora and investigate tho sedi-
mentary and litholo3ic characteristics or the unit. Tho
951803003raony at the time of deposition must be explored
in the light of the present stratigraphic knowledge and
the charactoristica of the sedimentary unit. The ra-
construction of the pn1003eogruphy. consistant with the
stratigrayhy, structural, and sedimentary data should
lead to a hi3h doéree of accuracy in intcrprcting tho
over-all conditions present and govorning tho sedimontury
unit at tho time of doyositioa.

it is the goal of the writer to determine too origin
or the Sylvnnia candttono by a quantitative facion and
sedimentary analysis of the unit. From the results or
the analysis and tna prosont gaological information. it
is felt that the sedimentary conditions present during

Sylvnnia time can be interpreted with a fair degree of

 

Eccurflcyu
goioation of Wollqufind Intergall
no wells utilized to obtain the composito samples

for this study were obtained from the tichigan 6001031031

Survey, Lansing. nicnigan. The spacing or wall. from those

10

ll

available wee chosen to give the most representative
coverage of the area (Figcro 3).

The interval selected for study is the candy Sylvanio
aeguenco bounded both above and below by carbonate rocks.
The Sylvania sandstOuo grades upward into carbonato rocks
causing the uppor contact to be oxtroeeiy difficult to
determine accurately. nooert Ives, misdigun Geological
Survey, gave valuable assistance to the author in selecting
the interval for study. Toe top of the unit was picked
with the aid of tin: bi zoo-alm- microscooe at the point

where the sandy unit could be safely difierentiatod from
the overlyir; carbonates of tne Letroit fiivor group. :30
bottom of the unit was selected at the to; of tho under-
lying Loin Llano or the top coco island formation where

the Eois clone is missing. Tue uncouformaoio relation-
ships of these units and tho egproxlmate areal distribution
of tho Sylveaia in michigan is shown in Figure l. A

taouletod list of the wells used in this analysis appear:

as Table I.

Sylvonie Sefifistogg

 

The unit studied has been discussed in the literature
and described as a "very pure" quartz sand. Carmen (1936,
p.26h) stated: I

The SyIVunia is typically a pure quartz sand-

etono but it shows all gradations from send-

etone tnrougn dolomitio sandstone and ereenceoua
dolomite to dolomite.

12

aaouamuaw

aahq

aofloum
humum

nfiooam
coma

Haonam

naowhpuodm
confide
«Bad
huhanaq
oovmflm
afloocua
donaeuuaw

mmw

m. mod m

mma mm ow
maa up :a

mma 1 mm
H» ma mm
vs mm mm
ma w a“
:m m h

ma mm mm

mm mh aa

”has“ .u CHwamuw HAOHO
-naom sown

no.“ QWUOWM

 

HM .eaao

wade» M.GQDQOpap chsamam com

Aw asna whom .00 ago gamma

«% no .ua naaam
.ou «mm a Ham noumum

Hm xowfiom canaeum
.oo oaaq omfim .m caucanaaa
Aw fihouauau .Cnénmam sandmaddm
«% «a pa anamoc .naaaoo .m .0

am manuummom .a.m

acaaoaaa aadnmacau
«% honaam. .ou .maan aseflhoa»
am hoaaoa .auou aaaohuom ona
aw Mzog.m .hanpdamnam.m
aw homaflhw .oo Ham ahaauom
an wxmom .m .ou Awoanomo you
H% anmam .uam a HAO dawnw¢

Hm akfima .ww.> .finmhu :«uvn.m

 

hwmfififi 0mm wfiauw «HWamfioc

canonsB
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3800mm

“madame

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"3393

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outwaoq

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13

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hm wNN mm m adkvdom anamfioo Ado cum coa§couom
Boa mad «m mm saawuopm .m.m .ou Hag oago «Haeoao
ma mmd mm H% mafiuaq .00 ”an aha; aaaoamuH
mm mma ~ new aaan you .00 Haunamau boa vmuanwm
mm mma a mmw can sun .00 ago gnaw tom sandman
.4 mm” gm Hm ”Hum .09 ”an made man
id‘s“. la .9; 4 .1311‘4‘! i... . g .L ... ~ 0... \HH u .. 1. c a
0! .1“ r. PJWIQ LOH.“ haw/brarpc “at: LIN «.mpH hrufirvfinou “L300
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1h

In subsurfaca sectiona the Sylvania prooubly contain: morn
dolomitic cement than where it is exposed to the leaching
action of surface caters. Tho "sand" or the Sylvania is
relatively fret of impurities but in curtain wall: consid-
erable chart. silt, and shale were found. Under a binocular
microscope the grains appear to be wall-rounded with coarao‘
toriatic frosted and pitted surfaces. fiany of the grains
show secondary enlargement and the doveloomont of sharp
crystal faces.

Cartoon (1336), uftox‘ examining much of the 56:“! with
the aid or the petrograghlc microscooc found hundreds of
quartz grains but only a tea grains of other minerals.
Alty (1932), while atuding the Cylvania. round a docroaco
in the amount or heavy minerals from the aouthoaat to the
northwest. The so bar's study verified Alty'a work.
Several attempts to separate heavy minerals from tho 38nd
produced only a tow heavy miaertl grains. Eecauso of tho
scarcity of heavy mincraln and the limited supply of nam‘
ple. no heavy mineral study was made, Quartz grains from
tho subsurface are not as well rounded as those at the
outcrOpa. Talc cnarcctorictlc we: observed by Houcombo
(1933. 9.162) and Snyort {1339); the work of the author
substantiates this ooservation. Enyort (19%?) found that

tho SyIchln contained a maximum of #3 P93 cont 6°10m1t0-

This ctudy revealed that in places the subsurface Sylvncic

contains a maximum of 53.10 per cent carbonate.

15

Chart 1: round in larger quantities in the subsurfaco
fiylvania than in the outcrops in southeastern flichigan and
Ohio. Each of the cucrt may be attributed to the erosion
of underlying charty £013 Blane (Landon, 1951). This atudy
rcvcalcd that larger amounts of silt and clay size parti-
cles were obtained from subsurface ea plea, than from then.

taken at tho outcrop.

a T 0' t“ . FA Na 11" 7“ -, 1 ft": ”ft-j r '7“ w!
l . . ‘ v- .‘x . ‘2. ‘ . . ,. ‘ ,.‘
Ln.- ‘. luui viii. i m Jul nia’v a. . u

lfctfiod oi‘ 3:319ng

—- —_._-.

The well samples utilized for this study c'mo from tho
Hichigea Geological Survey in trays containing about twenty-
fivo vials or soil moat rcgwresentin' the drilled interval.
‘ncn vial held tixroo to cl; Ext grams of cuttin3c which.repro~
tented a five root drilled interval. The contents or each
vial was put througu a microsplit, the aaLple was halved or
quartered until a little more than a one gram aamglo ro-
mained. This split camyle was treated with an electro-
ma; net to remove iron rra @floutS from the drilling tool.
(wfiich contaminated most aamgles). At this time, a few
large. black shale cavings were removed. The sample was
then put into a previously weighed and numbered too mi.
backer. tech vial of sediment was treated in the above
manner until a composite mangle representing the Sylvaaia
from coo.) well was compiled. lhe cor poo to e oplee were

tlon dried and wei3rood to tile nearest tAousandth of I gram.

ggggyel_o§;;ci d

ifi01dbl9q

ith the weigAt for occlz of tue co.:pocito 83.npieo known.
tr l0 acid so ublea could now be removed. inch couple on.
treated several times Nita 3A hydrochloric acid. than tho
acid was spent it was siphoned from the beaker and fresh

acid applied. When chemical action ceased, the cem;:les

it»

1?

wort warmed on an electric plate for several hours to insure
that all of tun solution were taken into solution. After
all tho carbonate had discolvcd. tho acid was siphoncd from
the beaker, water added, and the sample agitated. inn
sample was allowed to cattle over-night and the water
ciphonao off. The washing was rooaatcd a second time.

Thu sample: were then dried and weighod. Tho ions or

weignt from he original weight of tho samplo was recorded

and tabulated as the acid soluble: (Table 11).
§emovcl of Clay and Silt

Soveral hundred milliters of water was adood to tho
camplcs from which.thc carbonates had been romovod. Th.
samples were then placed on an eloctric hot plate and
allowed to boil. Approximately 50 ml. of ammonium hy-
droxide was added to the water to holp deflocculatc the
clay particles. The samples corc than wot-aicvod through.
the 233 mesh sieve to remove the clay and silt. Excminc-
tion with old or the binocular microscope showed aggratca
of clay particles still remained. The sample was dis-
n33rotod by placing it on a sort tine block and gently
rubbing another plan block over the too. This method
probably caused loos cdvcrao effects than other methods of
disaggregation described in the literature. After the
second cttcnpt to not sieve tnc couples. examination rc~

vealed almost perfect removal of the clays. The aasplec

TABLE II

0 t.TIZ‘.14 13111313
Per Cent Par Cant Per Cent Per Cent Total
ggiég Carjaaznatg Silt '-: 53:11.0; (3110:": 31:11:! Par C611;
1 77.19 .12 .11 26-19 100.21
2 73.69 6.66 6.63 15.26 99.65
3 65.39 .01 .05 33.70 99.15
6 73.22 1.70 5.63 16.60 100.15
5 75.82 2.69 11.92 9‘66 99.89
6 53-36 9.23 3.07 36.11 99.75
7 66.67 11.21 35.07 6.95 99.70
a 66.77 3.87 16.78 12.39 99.31
9 27.05 6.62 3.19 66-60 99.70
10 63.66 1.07 n.1h 65.86 99.51
11 71.07 .71 16.62 13.56 99.93
12 61.66 1.66 5.99 30.66 99.79
13 22.56 .26 3.65 72.97 '99.hh
111 83.10 3.110 5.77 7.58 99.85
15 26.32 .h9 22.25 52.75 99.81
16 33.13 1.70 6.72 55.00 99.63
17 28.38 3.01 18.69 50.02 99.90
13 61.99 2.73 26.77 8.33 99.87
19 59.65 6.55 25.36 11.29 100.63
20 66.61 2.76 20.01 10.53 99.71

 

 

18

 

19

more than driod and wnighod. This loss or woight from

the previous weighing reproaautod the clay and silt

fraction of tho sample.

Sgparation 9f Chort and;§snd

W W

With the removal of carbonates. city and silt, from
the sample. only sand and chart romainod. It was noted
tnat in many aanplos chart was a major component. It was
further observed that the chart variod in texturO'and
color. Some or the weathored court fragments could proba«
bly be couoidarod with the quartz :and and may havo.had
the some origin and sedimentary environment as tho quartz.
Some chart could have been primary and should not be con-
sidered as a port of the dotrital road.

It was decided to separate the cmort from.tho quarts
since it was obvious that wits such large quantities of
chart it could very well mask the true onvironmontal charac-
ter of the sand. A search of tho literaturo to find an
acceptable method for ragidly separating such closoly
allied substances was to no avail. Experimenting with
various concentrations or potosaium hydroxide on the
theory that the difference in toxtaro might cause tho
chart to be more aoluablo than tho quartz grains proved,
for all practical purposes, unsatisfactory. It was found
that aolutiona or potassium hydroxide throng enough to take

abort into solution also dissolved the quartz grains.

20

A method similar to that used to separate and con-
centrate era was t'icd. It was hoycd that difforcncca in
tho tcxturo and surface area of the chart might bring about
a separation of the chart from the qucrtz sand in flowing
water. Based on tho assumption that moving tater might
transport tho chart )ot allow the quartz grains to scttlo,
a piece of glass apparatus was designed for this cxpori-
moat. The two aubatanooa voro placed in the center of
tho glaaa olatrictcr which.had tho rotor flowing upward,
out the top, and into a catch basin. Somo degree of
aucccas was cccomylishcd with this rising-water clutriatcr.
but it was still not satisfactory.

The method for separation.utilizod the differences
in optical prepcrtica a: wall as texture or the two lub-
atcncoa. After the temples wore sieved. a rcprcoontativo
sample of each size was mounted on a glass slide in Canada
balsa, 200 grains were counted to determine tho percentcgc
or the quartz sand and chart.' because of the texture.
shape, and amorphous chart. it was easily distinguished
from the quartz and othsr minerals with the aid of tho
pctrograghic microscope. This method, of coarse, did not
physically separate the cacrt from the quartz and some
error in determining the over-all composition of the
Sylvania mcy have boon introduced at this point. the
samples containing much chart generally had 30 to 50 por

coat of it larger than 60 mesh, which could be weighed

21

directly. Tner fore, most or the chart would.nct be

subject to any error induced by tne count method.

r! :7“: h‘f 'w Fifi n
C) 1‘.be 11.3: AL‘X h: I .2)

wlo Audio? 3

rrp- p

After the removal of too silt and clay particles. the
r coining chart and quartz was sieved by hand in a nest of
U.S. Standard sieves, sizes 40, 60, 83 .103, lBG, 1h). and
200. The scdimont from ecci. sieve was wci3L'.cd and placed
in a small labeled vial. From each or the viola containing
the sediment, 3J0 to 500 grains were mounted on e single
glass slide. A frequency count of 239 grains of chart and
quartz was than made. With tau pores: Mta 3c of chart and
quart: known, the amount by weight of each mineral was
determiuod from the total weight of the particular sieve
size. The weights of tho sand fractions computed in this
manner could then be plotted on two stage semi-logarithmic
paper for the our cos of cor structing cumulative curves.
The quartile calculations determined from the data on the

cumulative curves are tabulated on Table III.

C‘i__lotivo Parvquic_i i

M Oe‘bd -M

 

in constructing the cumulative curves, the 3.8. sieve
sizes were converted to Tyler sieve sizes with the aid or
a comparison table (Leroy ot.cl. p.137). The diameters of
the grains in millimeters worc plottod logarith.icclly

along the horizontal axis and the cumulative weight

22

 

.2k0
.275
.th
.230
.173
.230

TRELS III

'QZ

.133

‘ " Mm
’7? Cattle
-73 ’
n 1—ffiriTIda
. I fun
43»:

23

TI'JEIS

21;
percentages plotted urithmeticelly along the vertical
axis (Table V). With the data plotted end cumulative
curves drawn, rive values were obtained: the median,
Ed; the first and third quartiles, Q1 and Q33 and the
tenth and ninetleth percentiles, P10 and 990. The
median size, sorting, skewness, and kurtosis, are widely
used quartile measures for descriolng and comparing
swrples. Sorting was computed using the geometric form
introduced by Tree; (1933). fie called it the sorting

coefficient "So", Which is defined as:

3o ' Ql/Q3

The quartile skewness which expresses the assymmetry
of the curve was computed using the geometric equation
below:

seq 0 Q1 Q3/2352

Kurtoeis. unlike the first two, measures are usually
eXpreseed in the arithmetic form. Krumbein {1938). Thil

measure is eXPreased as:
Kq‘ ' (Q1 ‘ Q3) /2 (P10 -ng)

Kurtosie is a measure or the Central portion or the curve

as compared to the curve as a whole, or more cemmonly

referred to as a measure or the peakedness of the frequency
curve (firumbein, 1935). The statistical measures are

tabulated in Table V.

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30

Th. median size. which in the diameter of the middle-
moat pufticlo, represents an aVorago of the group. Thin
value coerSponds t0 the point diréctly below where the
50 per cont lino crosses the cumulative curve (Krumboin.
1933).

The first quartile (here meaning the value at th.
diamatar which has 75 per cant of the distribution Imaller
than iteelf. and 25 par cent larger than itself, und which
corresyonda to the intersection of the 25 per cent 11a. of
the cumulative curve) is used for comparing the samp1ol.
Krumbein (1933) atatos: “Isopleth map: may be prepar0d with

any variable which shows a continuous gradational value.”

$15106 Ann). 318 1 g

 

Several hundred quartz grains betweon the 0.3. siovo
01:03 50 to 33 usrc m dated on glass slides with.aroclor
(n-i.Gb) for tha purpose of measxring roundnasn and Spheriv
city. The slides were placed on a petrographic microscope
specially adapted for projecting the image on a wall or
other amootn white aurfaco. All measuremunts were and.
directly from the projected grain image. Fifty quart:
grains from ouch safiple were muusurad for roundnezs and
aphoricity. The measuring of fifty grains was luggnsted
by Krumbein (1733, p.61). The roundnesa of anon graLn was
determined by using radell'l roundnesa formula: p s...£é§.

I:
(236011. 1935). where;

31

h 8 radius of maximum inscribed circla.
r I radius of curvac1ra of individual corners.

n a number f corners msasured.

£1

ty of

\

9‘ ~. .~. - 8
fine 3y48P&C

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each grain Has daturjinud using
Riley's formula 5 : .é (Liloy. ljhl). Where:
i = radius 01 lerseab insc~i$ed circle.

0 8 radius 0f aunliest circumscrised circle.

The nvarvge rauguncsa and sphericity are COflglled for aucn

c.) -l C‘ U1 #3

NC.

 

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Far prescntatioc 0f the data, the autncr constructed
a series cf pcrccnt*;e ma gs a¢001n3 the aistribctioa of
the constitucnts of tmc scfilmcntcry unit. median grain
size and tsc sucticai measures or tun sazld are 0153 pre-
sentcd as coztour mags. ?1c maps show in a 31:.1916 and

‘

prcciac mcnucr the litholcgic cnfi 8c 01 watary chartctcr-
istics of the uuit

Zhe isocnorc any shows thc variations in the strhti-
graynic thicknema of tha formatioa and the approximate
01001 distribut101.1 of $119 :ylv mlia (fl gurc h). 1313 map
was cangtructcd from tbc thicknesses of the drillcd in-
tuerls gulfiud by measured sections w.01 a the unit crops
cut. it anaws u gradual thinning in all directions tram
a central thick area but tfic rate of tgiuning t0 the
001thmcst is causidcrably 1053 tuaJ in other directions.

The structural map snows, by means of contours, the
configuration of the bottom of the Latroit fiiver sediments
or the to; of the Syivc in Sandstone—where it is prcscnt
( i;u;0 S). The j'uall unticline, in the ccuthwcst portion
of kichigan, is thc moat intcresting structural feature

in tha 0100.

F- - 3' w ~I- . II? ‘fl
{tiffladte hi1” . (3:48

3‘-

pcrccnta;o canton? may 13 3111100 to a ratio map,

\

that t: 16 numLcr used f0? contouring is the percentcge

(?

0X0

('5

"4 .r. -, ' T .~ ~ .- ,
7-9 4‘ .. 11 ‘7‘ . “V,
e‘ .. t 1a ' a - - 1

SOUTHERN PENINSULA
OF

MICHIGAN

’-

CCLt‘Jr IateFVfil fa féet.

*...*...~CI.

 

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0. <3
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O
SCALE
l0 2
L__._____J_____,- J
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H‘ ‘3 I Y: ‘ 9 . O ~ ’ YA “‘ ‘ 'I ‘I', 1‘. I 1 <, ‘ :<‘ l" ‘. I ‘ 'l . .'. _L gr. ‘1 A (‘1 .

SOUTHERN PENINSULA
OF

MICHIGAN

SCALE
0 IO 20

3 ,~ 1, "\ v, _ * - ‘fl-J
Gontdlr Ififvrvu1 :Ln 17~1- 1 I

——_L—_"° -- Miles

000*..0~3..

 

0 Well L ocalions

36

voluo of the lithology of interest (Lefioy et.al. 1951).

rue sand porcont153 may 3L013 cousidorablo parallelism
wits tna isocrore ms 9 (1 igura 6). there tho unit is thicker,
higher porcontogea of 324d are found. Eowover, boyono this
generalization marked departures can be observed. 515hw
porccntages of good than xi5ht be oxooctod are rocorded on
the soutaouat edge of the map and a lossor "higil" is noted
in the area around fiillsdala County. the hi5her percentages
of 11nd in the southeast onion doea not corresoond with
tho thickness map, looéa the author to infer a coats. for
the sediment 1153 to the southeast.

the carbonate and sand percenta5c maps are very
aimilar (Figure 7). If only carbonoto and sand made up
the forxotion, the too maps should coma out exactly
opoosito. The carbonate map shows in ganerul, the tendency
for the carbonate co11tont to decroso a wk1ero the formation
is thickur, it also decreaaen with increase of sand. Lisa
carbonate is found in Inghnm County, which is not rofloctod
by higher sand porcentage. This lack of carbonoto repro-
sent: Eu anon Ht 1y wncn c moored with.the Baud percentage map.

The angle and silt percentage map (Figure 8). bring;
1ut several interesting featurus. The smallest percentage
Value for the fine 51363 was obtained from 1 well in monroe
County. This is consiatant with other workers (Carman, 1936,
and Rnyart, 1919) who found very little shale or silt in
their study at the outcrOps in gonroe County. leero in a

definite tendency for the finer sizes to form an arch around

SOUTHERN PENINSULA
OF

MICHIGAN

SCALE
0 IO 20

L___.._L._--..-J

Miles

 

,1 0 Well Locations

SOUTHERN PENINSULA
OF

MICHIGAN

 

 

 

SCALE

 

IO 20

l 1

Miles

0 Well Locati .

"v ‘1 ‘. ,— . 1 ”‘3 ~~¢. ‘ ‘t
rioxre %.- anale and U1;T 1v701u2abe 1‘0.

SOUTHERN PENINSULA
OF

MICHIGAN

 

 

o
04
06
06
06
SCALE
0 K) 20
l— 1 J
IbOOleth Interval .C?@.
___.—_...____... Miles

1n 0 Well Locations

#0

Yonroe County perhaps indicating that the transoortating
agent was afforded better Opportunity for wiunowing at
of tho ”idea in this region. If the Sylvania somfiatonc
was oopositcd under Karine conditions, tho mourns County
crcc was probably hour shore. ihic chore focturc.mcy be
tad northern nose of the Findlay arch, Just south of the
Chctocm sag. the iorgoat percentc5o of fine sizes occur
in Eugham County waico shows some ovidcnce for a source
of ciactics to tho ucct.

Too chart percentage map. in general, reveal: a reln*
tiveiy low ycrccntcge on tno southwest side (Figure 9).
(are again the lowcst chart value is recorded in Monroe
County. lagoon County has the bignest percentage of chart
followod by the area around Iacbclla and mocosta Counties
an} the Saginaw hay rcgion. Lance: (1951) states that
most of the chart in tho Sylvania was probably derived
from 121 und flying cherty Eoin Elamc formation.

Conciusioos drawn from percentage maps:

1) fine porccntugc-of send becomes less in all
olractions awog from its maximum in the
soctnccst; tais indicates a source fro:
too aouthocst.

ice curconate porcontagc map may show two

to
‘0

tniags: a) it could aupport fiewcomba's
conclusion (1933) that carbonates were do-

poaited by p6PCOl€ ing waters in tho wind

Fiidre 9.- Chart'Percentage Map.

SOUTHERN PENINSULA
OF

MICHIGAN

go

 

 

 

 

SCALE
0 IO 20
L L

J

Isopleth Interval .Ofifi.

fl...‘...

 

 

Miles

211 0 Well Locations

3)

14)

1:3

deposited sandstone, or b) the car-

bouates we; have deposited simultancocsly
once? marine conditions uith the Sylvania

s end-3 .

The clay and silt were derived from a
western and a southeastern source. inc

low gercectage or clay and silt in flouroe
County caa best be explained by a winuceing
out or the fines due to wave action near

4"

3 bacon, probably on the west .enx of the

The low percentade veiue observed in St.
Clair Lounty ma" also be attributed to
wave action along a beach. This area or
low value corresponds with the northern
nose of the fiindlay arch. The isolated
high in Saginaw County is difficult to
exglain but is more likely the result or
current action then win&. The high veiues
in mecoete County could be contoured to
open out to the vest inferring a source
from that direction.

The caert in the Sylveuia is primurily
cerived frcm the reworked Eoia Llano

formation.

13.3

.9 CL =1; th 3.": .12;ng

IH

The sieve analysis data, computed from the cumulative
curves, is preeentcd in toe form of isopleth maps. An iso-
ploth has been defined by firuutoln (1933, p.231) ”as a line
of equal abundance or magnitude". Isoyleth maps are useful
for depicting the areal variation of sedimentary charactero~
lotion and for comyerotive purposes.

Because the values for sorting and skewness were
expressed in the geometric form es shown on page 2b. the
numbers do not lend themselves directly to n visualization
of what they si3nify in terms of the actual spread of the
curve (Krumbein, 1933). Before the geometric sorting may
to compared directly as on an iaoplcth map, the logs of
the sorting values are used to form an arithmetic eerie:
so that all sorting values may be compared (firumhein, 1933).

The median size isoplcth.meo ehows larger median sizes
to the southeast; nose larger sizes extend into the Saginaw
Bay area (Figure 13). the median sizes ccrease in Osceola
County, revealing perheye a new influx of sediments from
the west. It auould be pointed out that the distribution
of the median sizes Opposes Lendee' idea of a northwest
lource for a wind blown Sylvenia sandstone.

The first quartile iaocleth map, here representing
the largest 25 per cent of the sizes of the sample (Figure
11). follows the median size may quite closely. Hero egeha

a new source of sediment may be interpreted for the well

SOUTHERN PENINSULA
OF

MICHIGAN

 

 

SCALE
0 If) 20

l—_ J

 

Miles

“a 0 Well Locations

i ‘1 “ ' 1 ‘.
r;..'l_"4< .].~ ..‘*- -‘1r-*;ru'm.

SOUTHERN PENINSULA
OF

MlCHlGAN

 

 

 

 

M O
300161.11 Ir'zterval . (1:. g '10 210
*Iooh... ... ,

—-—— Mules

4" 0 Well Locations

5,6

shown in Osceola County. Tue major portion of the largest
grains occur t: tan southeast.

The sorting iaopletrxmap (figurs 12), shows the best
sorting along the edges of the unit and the "poorest"
sorting generally whare the sediment is thickest. Th
sample with the psorest sor ing was from esceola Caunty.

It is possible to contour this well'similar to the map
showing me‘inn sizes and bars again this may be an indi-
cation or sediment being derived tram a westward source.
She better sorting valuoa on the edges of the unit probably

5

are tan reaglt a; wave action, which selected and uinnowod
the andiment. fate too, the high sorting value near tn.
Elnélay arch in Konroe County.

flue sxewneas map is included with but limited inter-
pretation (Figure 13). Krgmbein (1)33) states:

ޢletively few studies have been.mado of the

areal variation of sxewneas within given da-

posits, and the data are perhaps too meager

for generalizations. The almost univoral

presence of skewness in sediments, capacially

in terms of diamoter as the independent varia-

ble, suggests that thare is a genetic relation

between agent and axewmesa, and that fine skew-

mass may vary areally 1a accordance with

definite laws.
There exists some relationship betwoun the positive values
or skewness and the larger sizes.

The kurtasis values do not lend themselves to inter-
pretation in the form of an isoplath map. The values are
presented numerically wits interpretation left to the

reader (Tabla VII). firumbein (1933) states:

SOUTHERN PENINSULA
OF

MICHIGAN

 

 

       

 

‘ 0 SCALE
° 0 IO 20
- L 1 J
Iaoaleth ‘utcr
......____. Miles

‘.".1 . ._ b‘.
147

0 Well L ocations

SOUTHERN PENINSULA
OF

MICHIGAN

 

 

 

 

 

 

lo 20
Iagoletn Interval .CT. ' 4
mic-Mono“... Mi'es

4;} 0 Well Locations

3;?

fiat much is kncun about the significance

of kartasls in aefltmeuts. It apteara to

be related to the selective acting of the

geological agent, but the sum total of the

factors entering into the selective process

are not known.

The areal variation in roundnuas and sphericity are
shown as isoyleth mugs {Figures la and lfi). Thesa two
mugs will be cuualdared together because they represan
tna characteriatlc shape of tha sand. 13% rounduass map
Buowa the send to be aura raundad to the southwest. Ibis
may be a function of tha distance of travel or the result
of chemical activity. ihare seems to be some correlation
betwemn the batter rounaing and the larger sizes. The
question is, would wind tran8port largar. mora rounded
particles further than smaller more angular particles?
$hia woulé have to be true ta supgort Lunfies thsory. The
spaericity map neems to add little to the history. There
seews ta be little er no relationship between roundnaaa
and sphericity values. If tfia sphericity is connected in
any way with the mode of transport it is not apparent.
The Spherioity map has tha tendency to ahow higher values
wharo the saad is thickest.

A westward influence is agparant from tau well sample
in Osceola County.

Conclusions drawn from isopleth maps are:

l) The average size of the sand grains is

greater in the southeast portion of

michigan, indicating a source from that

SOUTHERN PENINSULA
OF

MICHIGAN

   

 

SCALE
__ (2 IO 20
Ianaleth lutLrW-‘zl -C'*»- 4 1
Miles

0 Well L ocations

éiyzre 1w.— Avera;9 bprerifilty neg.

\.

SOUTHERN PENINSULA
OF

MICHIGAN

 

 

 

   

SCALE
9’? \

O I? 20

l J
Isv“leth Intervvl .51.

.00~000“0v0n.. Mi'es

 

0 Well L ocations

2)

3)

5+)

S)

6)

If")
.15.

direction. $33 largo avaraga sizes
shawn in Osceola Caunty may Show tbs
influx of same sand from the test.

The largest 23 per cast or the sangla
(first quartile lsopletn.map) snawa
gsnarally a cancantratiou to thn south¢
east, wli again sfiowa Sedimeat may have
been derived tram the west in Osceola
County.

The better sorting gmmrfl 1y confined

to the edges of the sedimentary unit is
believed to be the result of wave action.
The mora "poorly” sorted material in the
central portion or the Sylvania Sea was
nut greatly affected by mavo actlan.

The skawneaa and kurtoala values are
p~obably a result of the truasparting
agent, amd conclusions 33 to direction-
and mode or tranayort are left t0 the
reader.

Tho best rounding in confined to tha
southeast section of Elohigan.

The apharlcity distribution 13 erratic
and may be neggtivu cvideuoo for a wind
blown Origin, for wind 13 more selective

nan water as an tgant or transport.

fL“‘o\Y qn:\

Xvi-.‘JIC “.u‘” "Jan 1.3.“ Ln Liz. SIN'JE' ‘21de

The tootonio features, is early Cayuxum (Saiina time)

a
Isiah woro affoctivo in restri"tiu- tho Sioui3an Ensin
pursiatod but were less y.oniuoau o “irxr 9333 Island timo.
iho Cincinnati arch, r Findlay or n, oxtoaiiug from
control ohio to aoutawet t Jut wir o la; to too oust of the
Michigan basin. Prior to Lass Island ougositiga, a sag
dovelopad in tho iindiay arch (“EL otham sag) which por-
sisted during Lass Island time. The doapest portion of
the ”Imtlm'z 3a.:s dqri1. f The xto.) ti as." was noor Chatl‘m-n,
Gntario, ago tho Laxe St. Clair region of nichigan and
Ontario. :.t tlio soitxor 1 end of too fiiohigaa basin another
tectonic fozzturo existofi. most fr-qgon 13 raforrod to as
the Kcnxakoo arcs. Spoon (195?) points out that the
Kankaxeo arch might batter be called tho :;\wan~;uto
platform which oxtouda iron east-ceotrtl this throuw
northern Indiana into Illinois.

To to west. in curt? o1 “iscon in, a poaitivo feature
referred to as the hiaconsin iono prevailed airing late
Silurian and ocoor in3' ta Laruloy (1)31} ampliftod
following too uupositi on of Silurian buds. apparintly,
the regions to the north of fiichignn were flat. low-lying

stable areas.

1..“‘.‘".‘7 ‘vfi" .'-*l n H;

a ‘u ~ Y 3.. _ :‘ “ ,n" f." V .. ~ I .I- I, ‘_'.‘ .ih I f' . . .‘H? '
§ ‘ f . . ‘ ‘ s \. v . _ -. . L,-
d «JAJK-WJXU 4.-.“; VAL vi 4...... Q‘.’.4 I. u ii an. Llama. 4.}.4

,ortincat ListHry of the ;glVLJia oLLLstone be-
slanfi tigc. Lftcr the Loss :aLan dolo-
mite was éuyDSith over an area nLca 3roatcr than the grosont
liChiaJfli Lain, w.tna"'uri oi to .c can cx3oaoc the newly
formed rocks to 81"341» L. out this Vic, 91: Cui‘diilc; to
Ferlej (1,51), the Ticcoz. in Como ans ugliftci. During
he period of excrgcnce, some of he uppiP-IDS' LL35 Island
sc‘imcntc rcro removed. I?o fir ct Lovonioa sco ontorod
lower Lic.i3au umzin3 crisuzr" ti;o ("rM cfo“t. iTSL).
ibis 30a agrczot cstLer from t}:.c illcgaay trou3o into lower
Tichigun. The garden ISlLfld foray; on was degseitad,
probably coveriug a mgch wider area thsn its yreacot extant

cud

.- ‘ "" «x .
(3hiers, 1:42). rvit

..

\

:riaaany 9:33.33 rCflOV£€ nearly all
of the Garden island formation. The Snonéega ace followed
and agreed over ioaer iLLi‘Li c:veri:3 tt.e eroooo 33rden
Island and too twice eroded Les: £31536 sediments and in no
doing dogositeé txc Lois tianc formation. xiuor Goon-
warping took ;iscc at tt.is time with the resolt that the
thicxest Lois ilonc cadimcxts more Cogosited immediately
north of Srginau‘iay urea (Lazdcs, 1051}.

marina uithirgnal followed the deposition of tho fiois
Elana dolomite. Sutseqoent erosion of conoidoroolo mu3z1i-
tudo convicteiy ronovod the 3313 Llalc from t1e liarxs of

'1

W0 Findlay arch am: the Irifiifi.i‘1&~3i1io .olati’orm (Laados. 1951).

t.)

b .

The paleo3ealo3y pPlDP t3 the eucraachment of tho
fiylvauia 365 is shown on Figure 1.

According t9 Lauées (1351):

n downerp along a northwest-southeast

axis from central Lichigan into northern

Gnlo permitted the entrance of marine

waters.

Lfindea continues by saying, that it was into this shallow

traugh that wind transportad BLnd, which had drifted east-
ward tram lisconsin across the intervening emergent land.

was deposited and preserved in the Sylvanla sea.

Landoa' theory presupposes two 00ndltlons, 1) there
was but scant vegetation due to naar desert conditions.
and 2) during the fievonlan the prcVLilln3,wind was from
the west as today.

The writer's data does not support Landea' vlews. The
data obtainoé tram the anulyals indicates a water laid

'lment with.th6 major source area to the aoutheast.

('5.

ae
The writer bellavas, the Sylvualu aoa moved into the

lower peninsula of Uichigan from the east threugh the

Chatham 3&3 w lch existed throthout Eatrolt LIVsr time.

The Findlsy arch Lee a well-definad ridgslika feature inlch

extended north and Baufih away fram the Chutham 3&3. During

Sylvauia tine it Letad £3 a physical barrier allowing the

Sylvania sea to encroacn over lcwar filcul3un only through

a deprusalon within the area since called the Chatnam 3&3.

The Sylvania sea thering Lichl3un was tuua quite restricted

1th it's only opening to baa soutnuast through tun

Chatham sag.

56;

The deposition of the Sylvunia sandstone ended
gradually as the Sea encroachad farther over the land

‘

and the lower Ectroit h1Var sadimants wero depositad.

Spfiafiizlnii.’ MID CDJCLJSIJHS

The origén and ago of the ayIV&nia sandatana have
been discussed for many years. Two radically different
achoola of thought.nave devalOyed. Some writers favor an
colian origin for the following reaaans:

l) The surface characteristics of the sand

grains are like present day winfl~nlown
sands.

2) The npparont isolation of the sand fram
poaaible soarce areas.

3) The saull anount of finer clastica {suds

or clay.) usually associated with current
trausported sauna.

An callus origin vita marine reworxi.“ of tha sand
was recently postulated by several writers.

Still, other geologists stick to a straight marina
origin for the Sylvania saying, that it is a transgresalve
Hard or an accvmulation raaulting from current and wave
action such as modern Leash sud barriur sands.

The uritcr's data incicates the major source area for
tun Sylvania sandstoze was he the southeast of iowar filchigau.
This does not exclude the fact that some aofiimeat ans de-
rived from he was: for this, too. is arparent from the
data. The Sylvauia sagdstone is probably a marine sand
where both wave action and current influenced it's distria
bution in lcwcr Michigan. The parcentago maps could ha in-
torprated as evidence that current action was the most lné
fluentlal force gaveruing tbs deposition of the sand.

While the Sylvania son was restricted with its one Opening

57

53

through the Chatham sag, strong currents could havo do-
velOpcd airilar to those present at the straits of di-
braltar today. the watar, warmed in tha Sylvania 565
may have moved back into the allsguny trough earring away
much of the finer sediment, while caldar dauper currents
moved sand into igmor fiicnigan. Tidal action may havo
played an important role.

A southeast aourca is inferred from the analysis.

The sand was probably of sucond or third generation; per-
haps the grains were modified chemically.

To Speculste on a source area for the Sylvnuia sand-
mtame, in light of the present $391051c Knowledge, is a
diffLCJlt task. It may be that th Syivunia in reworked
Qriaxany said; it is also possible that the upper Boia
Slag Leda, new or dad, were aanéy enough to supply the
iylvuuia sea with sand.

filthough Sharzor and other acclagiats believe that
the Silvauia 503d received its unusaal sarke aad aurfaco
characteristics as a result cf wind activity, this writer
wauid not exclude the gossibility that the surface textural
originnta& tram chemical activity. It in to be remembered
that larga auantitius of emert were degoaitvd during Devonian
time. Sung workers believe that trepical conditions are
necesaery to induca such large giantities of silica into

sclution or the calloidai state. Tropical conditions

59

would alao supyort the idaa postulated here that thermal
currents and tides were generated in the restricted
Sylvauia sea, thus producing strong currents through

the Chatham sag.

The concept of currents as a means or tranSporting
the sand of the sylvania sandstone to its site of dOpOli-
tion may seam objectionable to the reader. A similar
oxylanation for sand: occuring in the Powder River Basin
of {yoming was given by Partridge (1957), who statels

The Band patterns of the lat $311 Creek

and Parkman sands indicate a ”Channel" in

the area f the Casper arch through uniah

currents brought sands from the southwest

and spread them anatward across the ?owdar

Elva? basin.

The 132 flail Creek and rarkman sands compare in 3129 and
thickness to the Sylvauia. The ”channel" referred to 13
aiailar to the Cuutnnm 335 in size.

In conclusion. the author believes the Sylvanla
fiandstona to be marine in origin wi h the major source
to the southeast. that current action wss the most im-

portant factur governing the transportation and depcsition

of the amfi'td o

l.

2.

6.

7.

CD

10.

11.

12.

13.

.v 4'

'_\ '1'” 1“ 33“.". 1" 3‘ w) .-
wLJJLJJ. J “315;... 34.x

Alty, S. 3., i932. 2-port of an Investigation cf
LleaLia Lock: in oil ulis oi the Lichigan
L-asin, E‘cpcrs of the fiicnigan Academy of Lcicnco,
firts, and Letters, Vol. XVIZI.. Pp. 239-330.

German, J. Lrncs t., 192 W’ :30 :onroo divisicn of
roc}iu in Jhio, Sour. 63010: J, val. 35, no. 3,
pp. h, nil-) )éo

, 1935, ylvania sanfistozxe cf nortzlwestcrn
Cgio. LL11. Seal. cc. America, V31. QT, pp. 256-
206.
COOper, G. A.. at.ci., 1952, Ccrrclaticn cf the
{Nev Liar: sedimentary formations of Lortn America,
Lull. Geol. Soc. Amcrica vol. 53. pp. 1729-1799.

iardlcy, A. J., 1951, Structural Geology of Lorth
America, Karpcr and brothers.‘PubiiaLcra, Haw York.

. 1935. Gealogy of the Lackinaw Straits

 

region. Lichigau 6901. Survey Pub. uh, pp. 19-121.

Lflur‘a, U0 4-0, Stfim‘im 2:. Cop find 310311.315, .‘Ko V... 1951’
EcVOLian rocks of southeastern Lichigan and ficrth-
western 3*;10, deurda chtnera, Inc.. Ann Arbcr,
LicnigaL, ho pp.

Zfinyert, U. L., l9h9. viL la Deva .ian saLdatcues or
tr :9 Lichi3an 233i :1, (University of Licuigan un-
pubiiancd doctoral thcais.).

Grabau, A. 3.. 1907, The Sylvania sandstcuc - a, _
study of paiLOzecyraphy. Science, ns.. vol. 20, p.332

, 1933, A revised Classification of tho Horth
American Siluric systemg- Science. n.3.. vol. 27.
pp. 622-623.

. 1909, A revised Classification of tnc Rorth
i 3-3can 1?Lcr yalcozoic, Science, n.a., vol. 29,
. 351-33u.

, and SLch ar h. d., 1913, The Monroe formation

W
a; southern ic.JLcL anu adjoining rcgic;a, ;icn.

$901. and Liol. Lurvcy pub. 2, Gc3l. Lav. i, 243 pp.
Green, 2. fi.. 195?, Trentpn Structure in Ohio, Indiana,

and orthu.1 111i noia, ma. £3330. Ictrcicum Geologists
bull. vol. Ll, 3p. LBY-CLZ.

éo

1?.

13.

19.

25.

25.

61

Krumtein, E. Co, find PCttijOhn. P. J.) 1&33. fiaflual
of Sedimentary yetrugnapny, Apgleton-Cuutury-
Crofts. Inc.. flow York.

, ani 31033. L. L., 1951, St a igraphy and

Mi- .- u ‘ -.-, -. . ‘ .. f' .. . 5 \‘
sou¢muutation, .. a. rreoman and .umpany, gun

Francisco.

Landes, K. H., 19&5. Guslogy and 011 and gas possi-
bilities of Lylvania and bola Blane formations in
the alchigan, U. fi. Gaol. Survey Breiiminary map ho.

, 1951, netrait hivor group in thn Qicnlgan
husIn, U. 3. Seal. Survey Circular L33.

Ledoy, L. a. at.al., 1951, Subsurface Geologic methods.
(A Symposium) Colcrudo School of zines. Salaam,
Colorado.

gartin, H. m., und Straight, 5. T., 1956, An Index _
of alchigun Goolo;y, gicnidan Joel. Survey Pub. 33.

hawcombe, a. h.. 1933, Oil and gas fields of itchigan,
Sichlgan anal. 5urvey Pub. 33.

Partridge, J. F. Jr., 1957, Potential Stratigraphic
oil Accumulation: in Upper Cretaceous sands, Powder
giver basin, fiyoming, hull. Amur. Assoc. Fatrol.
8991., V01. kl. fig. 832-3930

Riley, H A., 19h1, Projaction Sphericity, Jour. Sod.
Futrolcgy, vol. 11. pp. 93-97.

Scnuchert. 0.. 1955, Atlas of Pulaogeographic flaps of
Earth .merica, John Wiley and Sons, Inc., He! York,
Ch&pmaa and Hall Limited, London.

Sherzer. T. 3.. Criteria for nuoognition
or the Various types or sand grains and the Origin
of the bylvumla Sandstone. lull. cool. Soc. America,
V01. 21.. p?0 635-662.

?wenhofel, fi. 5., 1353, Princiglos of Sedlmantatlon.
xcfiruu-iill boom 60.. Inc.. flew York.

fadell, H. 1935, Volume. Shape and houndnasa of
Quhz‘t‘fi FfirtiClES. Jauro 33010. V0].- h3g pp. 2))"
230.

145 00/00
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